ML20027C366
| ML20027C366 | |
| Person / Time | |
|---|---|
| Site: | Vogtle  |
| Issue date: | 10/31/1982 |
| From: | BECHTEL GROUP, INC. |
| To: | |
| Shared Package | |
| ML20027C362 | List: |
| References | |
| NUDOCS 8210150373 | |
| Download: ML20027C366 (809) | |
Text
{{#Wiki_filter:I . I 1' \ l VOGTLE ELECTRIC l l GE\lERATING l l PLANT ) Report Prepared for l Georgia Power Company I i @ OCTOBER 1982 I g VOLUME I l g [8ea88Pa8a8)l:
I !I lI
- I VOGTLE ELECTRIC
!I GENERATING l PLANT !I I STUDIES OF !I POSTULATED i MILLETT FAULT I Report Prepared for il l Georgia Power Company
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l Il , I M l OCTOBER 1982 ,I i g VOLUME I lI I
TABLE OF CONTENTS - VOLUPE I Pago LIST OF TABLES LIST OF FIGUFES LIST OF PLATES TABLE OF CONTENTS - VOLUE II EPORT
SUMMARY
i
1.0 INTRODUCTION
1-1 2.0 SCOPE OF JrUDIES 2-1 3.0
SUMMARY
OF CONCLUSIONS 3-1 4.0 GEOLOGY 4-1 4.1 Physiography and Geomorphology 4-1 4.2 Stratigraphy and Lithology 4-2 4.2.1 Late Precambrian and Paleozoic Era 4-2 4.2.2 Mesozoic Era 4-5 4.2.2.1 Triassic Period 4-5 4.2.2.2 Cretaceous Period 4-8 4.2.3 Cenozoic Era 4-10 4.2.3.1 Tertiary Period 4-10 4.2.3.1.1 Paleocene Epoch 4-10 4.2.3.1.2 Eocene Epoch 4-12 4.2.3.1.3 Oligocene Epoch 4-16 4.2.3.1.4 Miocene Epoch 4-17 4.2.3.2 Quaternary Period 4-18 4.3 Structure 4-18 4.3.1 Tectonic Framework of the Georgia Coastal Plain 4-18 4.3.1.1 General 4-18 4.3.1.2 Triassic Features 4-19 4.3.1.3 Cretaceous and Cenozoic Features 4-20 4.3.1.4 Minor Framework Features 4-21 4.3.2 Folding 4-22 4.3.3 Faulting 4-22 4.3.3.1 Belair Fault Zone 4-23 4.3.3.2 Gulf Trough 4-23
TABLE OF CONTENTS - VOLUE I (Continued) Page !" 5.0 HYDR 0 GEOLOGY 5-1 5.1 Occurrence and Fbvement of Ground Water in the Coastal Plain 5-1 5.1.1 Tertiary System 5-2 5.1.2 Cretaceous System 5-2 5.2 Local Aquifer Conditions 5-3 6.0 FIELD EXPLORATION FETHODS 6-1 6.1 Geologic Mapping and River Meander Analysis 6-1 i 6.1.1 Geologic Mapping l 6.1.2 Savannah River Meander Pattern Analysis 6-3 6.2 Core Drilling 6-8 6.3 Downhole Geophysical Logging 6-11 6.4 Observation Well Installation 6-13 6.5 River Reflection Survey 6-15 6.6 Water Well Survey 6-17 0 .6 .1 Schedule of Field Work 6-19 6.6.2 Well Data Reduction 6-21 6.6.3 Supplemental Data 6-22 7.0 OFFICE STUDIES 7-1 7.1 Literature Search and Review 7-1 l 7.1.1 Searches 7-2 7.1.1.1 Computer Search 7-2 7.1.1.2 Thesis Search 7-2 7.1.1.3 Bibliographic Search 7-3 l 7.1.1.4 Published Reports 7-3 l 7.1.1.5 Unpublished Geologic Data 7-3 7.1.2 Review 7-4 7.2 Acquisition and Review of Existing Field Data 7-4 7.3 Review of Existing Geophysical Data 7-6
- l 7.3.1 Seismic Surveys 7-6 lE 7.3.2 Gravity Surveys 7-9 7.3.3 Magnetic Surveys 7-11 7.4 Remote Sensing 7-12 7.4.1 Imagery and Photography Employed in the Study 7-12 7.4.2 Digital Processing and Image Analysis Techniques 7-15 7.4.3 Results of Remote Sensing Studies 7-16
- l l
7.4.3.1 Lineaments of Cultural Origin 7.4.3.2 Lineaments of Geomorphic Origin 7-16 7-17 I I
TABLE OF CONTENTS - VOLUME I (Continued) Page 7.5 Lithologic Analysis 7-20 7.5.1 Lithologic Analyses of Samples from Water 7-21 Wells AL-66, AL-40 and Core Hole VSC-4 7.5.1.1 Lithology of Water Well Cuttings from AL-66 7-22 and AL-40 7.5.1.2 Lithology of Samples from VSC-4 Core Hole 7-23 7.5.1.3 Comparison of Samples Collected from Similar 7-24 Elevations in AL-66 and VSC-4 7.5.1.4 Comparison of Samples Collected from 7-25 Below the Postulated Pre-Late Cretaceous Unconformity in AL-66, AL-40 and VSC-4 to Triassic Rocks from DRB 10 7.5.2 Lithologic Analyses of Core Samples 7-26 from VSC and VG Core Holes 7.5.2.1 Barnwell Group 7-27 7.5.2.1.1 Grif fins Landing Member 7-27 7.5.2.1.2 Twiggs Clay Member 7-27 7.5.2.1.3 Utley Limestone Member 7-28 7.5.2.2 Lisbon Formation 7-28 7.5.2.2.1 Blue Bluf f Member 7-28 7.5.2.2.2 Unnamed Sand Member 7-29 7.5.2.3 Huber Formation 7-29 7.5.2.4 Ellenton Formation 7-30 7.5.2.5 Tuscaloosa Formation 7-30 7.5.2.6 Discussion of Lithologic Results 7-31 7.6 Seismicity 7-33 7.6.1 Felt Ear thquakes in the Study Area. 7-34 7.6.2 Earthquakes Located with the Regional 7-36 Seismograph Network 7.6.3 Data from the Savannah River Plant Array 7-39 7.7 Surface Water Hydrology 7-42 7.7.1 Analysis by U.S. Geological Survey 7-42 7.7.2 Factors Af fecting Baseflow 7-43 7.7.3 Calculation of Baseflows 7-44 7.7.4 Effects of Possible Streamflow Gauging Errors 7-46 7.8 Ground Water Hydrology 7-48 7.8.1 Reduction of Ground W a ter Data 7-48 7.8.2 Numerical Model 7-51 7.8.2.1 Purpose and Approach 7-51 7.8.2.2 Inpu t Da ta 7-52 7.8.2.3 Numerical Model Results 7-54 7.8.2.3.1 LeGrand's Hypothesis 7-54 7.8.2.3.2 Hypothesis of Barrier Fault 7-55 7.8.2.3.3 Hypothesis of Reduced Transmissivity 7-55 I II l ll
I TABLE OF CONTENTS - VOLUME I , (Continued) i Page ; 8.0 ASSESS $ENT OF POSTULATED MILLETT FAULT 8-1 8.1 Results of Investigations 8-1 8.1.1 Results of Geologic Mapping 8-1 8.1.2 Results of Core Drilling 8-2 8.1.3 Results of Geophysical Logging 8-5 8.1.4 Results of River Reflection Survey 8-6 8.1.5 Results of Existing Geophysical Studies 8-11 8.1.6 Results of Remote Sensing Studies 8-13 8.1.7 Results of River Meander Analysis 8-16 8.1.8 Results of Lithologic Studies 8-17 < 8-18 8.1.9 Results of Seismicity Studier 8.1.10 Results of Surface Water Hydrology Studies 8-18 8.1.11 Results of Ground Water Studies 8-20 8.1.11.1 Water Well Survey 8-20 8.1.11.2 Numerical Modeling 8-23 ; I 8.2 Conclusions 8.3 Consultant Conclusions 8-26 8-29 REFERENCES CITED i I I I I I I
LIST OF TABLES
!Almber Title A
SUMMARY
TABULATION OF RESULTS OF STUDIES TO DE'IERMINE PEfENCE OF CAPABLE FAULT 2-1 SCOPE OF INVESTIGATION 6-1 DRILL HOLE
SUMMARY
7-1 AVAILABLE INFORMATION ON PETROLEUM COMPANIES AND NELL OPERATORS 7-2 GOPHYSICAL AND PETROLEUM COMPANIES CONTACTED , 7-> 7-4 _ c R _ cE , _ S _ c _ ANALYSIS OF IMAERY LINEAMENTS I 7-5 ENERAL ETROGRAPHIC DESCRIPTIONS OF SAMPLES FROM WATER E LLS AL-6 6 AND AL-4 0 I 7-6 ENERAL PETROGRAPHIC DESCRIPTIONS OF SAMPLES FROM VSC COE HOLES 7-7 X-RAY DIFFRACTION ANALYSES OF BULK AND CLAY SIZE FRACTIONS OF SAMPLES FROM VSC CORE HOLES 7-8 HEAVY MINERAL ANALYSES OF SAMPLES FROM VSC COE HOLES 7-9 ENERAL PETROGRAPHIC DESCRIPTION OF SAMPLES FROM VG COE HOLES 7-10 X-RAY DIFFRACTION ANALYSES OF BULK AND CLAY SIZE FRACTIONS OF SAMPLES FROM VG CORE HOLES 7-11 HEAVY MINERAL ANALYSES OF SAMPLES FROM VG COE HOLES 7-12 ESULT OF BASEFLOW ANALYSIS BY USGS 7-13 ESULT OF UNIT BASEFLOW ANALYSIS , mESTx-- mWF-S 7-1. <c,S, 7-15 ESULT OF BASEFmW ANALYSES I I I I
I LIST OF FIGUIES Number Title A COMPARISON OF GEOLOGIC SECTIONS 1-1 SITE LOCATION MAP 4-1 GEtERALIZED REGIONAL PHYSIOGRAPHIC MAP 4-2 BASEFENT FEATURES, GEOICT A COASTAL PLAIN 4-3 STRATIGRAPHIC CORIELATION CHART 4-4 LITHOLOGIC CHART 4-5 TRI ASSIC ROCKS ALONG TIE EASTERN SEABOARD I 4-6
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BOUNDARIES OF THE TRI ASSIC DUNBARTON BASIN 4-7 APPROXIMATE LOCATIONS OF BELAIR FAULT ZOFE AND GULF TROUGH 6-1 GEOLOGIC MAP 6-2 MORPHOLOGY OF TIE SAVANLAH RIVER AND FLOOD PLAIN 6-3 LRILL HOLE LOCATION MAP 6-4 OBSERVATION ELL DESIGN 6-5 EEISMIC IEFLECTION SURVEYS 6-6 WATER ELL SURVEY AREA 6-7 WATER ELL SURVEY 6-8 ' ELL HYDROGRAPHS 7-1 PEGIONAL MAP OF DRILL HOLES AND WATER NELLS 7-2 SEISMOGRAPH SERVIG CORPORATION REFIICTION SURVEY OF THE SAVANNAH RIVER PLANT 7-3 LOCATION MAP OF REMCTTE SENSING IMATRY 7-4 VOGTIT, PROJECT SITE GEORGI A LITE AENT INTERPRETATION FROM LANDSAT IMAE TAKEN FEBRUARY 11, 1974 I
I LIST OF FIGURES (Continued) 7-5 VOGTLE PROJECT SITE GEOICI A LINEAMENT ItEERPIETATION FROM LANDSAT IMAGE TAKEN JUNE 6, 1976 7-6 LITHOLOGIC SAMPLE LOCATIONS AL-66 WATER ELL AND VSC COIE HOLES 7-7 LITHOLOGIC SAMPLE LOCATIONS VG CORE ilOLES 7-8 MINERAI4GY OF SAMPLES FROM AL-66 AND DRB-10 7-9 EELT EARTliQUAKES 1900-1974 7-10 FELT BEPOlWS AUGUST 14, 1972 EARTIIQUAKE 7-11 LOCATIONS OF EISMOGRAPH STATIONS 7-12 ELL-LOCA7ED EARTHQUAKES 1974-1982 7-13 SRP EISMOGRAPH ARRAY 7-14 SEISMIC FREQUENCY VS. DISTANCE FROM SRPN 7-15 LOCATIONS OF STIEAM GAUGING STATIONS 7-16 AVAILABLE STIE AMFLOW RECORDS 7-17 SAVANNAH RIVER UNIT BASEFI4W CONTRIBUTION UPSTFE AM RE ACH 7-18 SAVANNAH RIVER UNIT BASEFIDW CONTRIBUTION DOWSTRE AM RE ACH 7-19 POIENTIOETRIC MAP OF TERTI ARY (UPPER) AQUIFER (MAY-JUTE , 1982) 7-20 POIENTIOtETRIC MAP OF CPE'/ACEOUS (LOhER) AQUIFER (MAY-JUNE, 1982) 7-21 COMPARISON OF COMPUTER AND I!CERPRETIVE PIEZOETRIC CONTOURS-7ERTIARY AQUIFER 7-22 LOCATION OF WATER LEVEL PROFILES 7-23 WATER LEVEI. PROFILE - GEOICIA 7-24 WATER LEVEL PROFILE - SOUT!! CAROLI!*A 7-25 FINITE ELEME!C MESH I
(: LIST OF FIGUES (Continued) 7-26 SCHEMATIC EPESENTATION OF LEGRAND'S () ' s HYP0rHESIS [ 7-27 CAIEULA'IED PorENTIOETRIC SURFACE. ( IEGRAND'S HYPorHESIS (BASE CASE ' 7-28 CAIfULA'IED POTENTIOETRIC SURFACE. (- BARRIER FAULT HYPOTHESIS (KB= 100 FT/YR) 7-23 CALCULA'IED POIEhTIOETRIC SURFACE. BARRIER FAULT HYP0rHESIS (KB= 1 FT/YR) 7-30 FINITE ELEENT ESH USED POR THE EDUGD TRANSMISSIVITY HYP0rHESIS 7-31 CALCULA'IED POIENTIOETRIC SURFACE EDbGD TRANSMISSIVITY HYPorHESIS 8-1 GEOLOGIC SECTIGN A-A" 8-2 GEOLOGIC SECTION B-B" 8-3 GEOLOGIC SECTION C-C' 8-4 NUCLEAR LOGS - SECTION A-A" 8-5 ELECTRIC LOGS - SECTION A-n" 8-6 NUCIEAR LOGS - SECTIOh B-B ' 8-7 ELECTRIC LOGS - SECTION B-B' 8-8 CORELATION OF GEOLOGIC SECTION WITH EISMIC EFLEC'IORS 8-9 RIVER EFLECTION PROFIIE - LINE 4 8-10 PIEZOETRIC SURFACE IN LATE CETACEOUS { AQUIFER (OC'ICER,1954) [ [ l (:. ( ( r ___j
I l l LIST OF PLATES Number Title I 7-1 VOGTLE PROJECT SI'IE GEORGIA AERI AL PHCrrOGRAPHY MAY 8, 19 51 3 7-2 VOGTLE PROJECT SITE GEORGIA AERIAL l PHOTOGRAPHY DECEMIER 16, 1969 7-3 VOGTIE PROJECT SITE GEORGIA FALSE l COLOR OBLIQUE U-2 PHOTOGRAPHY MAY 1, 1 1979 , I 7-4 VOGTLE PRa7ECT SITE GEORGIA ENHANCED l LANDSAT SA'IELLITE IMAGERY FEBRUARY < 11, 1974 l l I 7-5 VOGTLE PRa7ECT SITE GEORGIA ENHANCED LANDSAT SATELLITE IMT.GERY JUNE 6,1976 lI i i l l l l
I ' TABLE OF CON'IENTS - VOLUFE II l Appendix No. Title A ANNCTTATED BIBLIOGRAPHY I B C OBSERVATION ELLS CONSTRUCTION REPORTS EXISTING DRILL HOLE AND WATER ELL DATA D CORE LOGS E GEOPHYSICAL LOGS F !EISMIC EFLECTION STUDY (HARDING LAWSON) G PETROGRAPHIC DESCRIPTIONS H HEAVY MINERAL ANALYSES I CLAY MINERALOGY STUDIES I I I I l I l l
I REPORT SUMPARY United States Geological Survey Open-File Report 82-156 raised the possibility of faulting of Coastal Plain sediments near the Vogtle Electric Generating Plant, under construction approximately 26 miles southeast of Augusta, Gecrgia. The Open-File Report suggested that a fault, named the Millett fault, exists approximately seven miles
- I southeast of the plant site at its closest approach. The report cited then-existing stratigraphic, ground water, and surface water hydrology data as supportive of the existence of the postulated fault. The Open-File Report also briefly mentioned the possible existence of a fault named the Statesboro fault about 32 miles southeast of the Vogtle site. Although the report did not state that these faults were capable, that is, had moved once in the past 35,000 years, or more than once in the last 500,000 years, it did not preclude this possibility.
Nuclear Regulatory Commission regulations require the determinacion of fault capability; therefore, it was necessary to determine if the postulated faults were capable. If the faults were not capable, they could have no ef fect on the existing accepted seismic design bases of the Vogtle plant. I In response to the Open-File Report, a task force comprised of representatives of Georgia Power Company, Southern Company Services, and Bechtel was assembled to evaluate whether the postulated faults were or were not capable. Based on information in the Open-File Report, the postulated Millett fault was of primary interest and the i c
I l postulated Statesboro fault was of secondary interest to this study. A review of the data and evaluations used in the Open-File Report indicated that additional data and evaluations would be needed to adequately determine the capability of the postulated faults. Bechtel was assigned the responsibility of conducting an investigation to determine if faults existed at the locations suggested by the Open-File Report. If a fault or faults were found to be present, the capability of such faults was to be determined. The investigations encompassed several scientific fields which address the question of faulting. These include sur face geology, subsur face geologic and geophysical characteristics, ground water aquifer characteristics, surface water hydrology, and the nature and distribution of historic seismicity in the area. I To provide guidance and review of the studies, a number of eminent consultants were re tained. The following group of consultants was chosen because their fields of expertise were related to the planned studies: Dr. Bruce Bolt, Director of the Seismographic Station at the University of California, Berkeley; Dr. R.D. Hatcher of the University of South Carolina; Dr. V.J. Henry of the University of Georgia; Dr. P.E. LaMoreaux, President of P.E. LaMoreaux and Associates; Mr. H. LeGrand, an independent consultant in geohydrology; Dr. R. Lyon of 11 I
'I l Stanford University; Dr. S. Papadopulos, President of S. Papadopulos and Associates; Mr. Carl Savit, Senior Vice President of Western Geophysical; Dr. Carl Stepp, affiliated with Woodward-Clyde l Consultants, and Mr. L. Wood, ground water geology specialist with G. Papadopulos and Associates. The results of the studies conclusively demonstrate the absence of a capable fault in the vicinity of the postulated Millett fault, and strongly suggest that no capable fault exists near the location of the postulated Statesboro fault. l These conclusions are based on the following:
- 1. Core drilling and geophysical logging clearly demonstrate subsurface continuity of beds 40 to 80 million years Before i Present (m.y .B .P. ) across the trace of the postulated Millett fault (See Figure A).
- 2. Acoustic reflection surveys performed in the Savannah Rh'er l
demonstrate continuity of subsurface strata deposited across the strike of both the postulated Millett and Statesboro faults during the last 80 million years.
- 3. Geologic mapping and remote sensing studies reveal no surface expression of faulting.
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- 4. Examination of recorded and reported seismic events indicate that there is no historic seismicity which can be associated with either of the postulated faults.
I S. Surface and ground water hydrology studies do not support tric presence of faults. Table A summarizes the results of individual studies in terms of 1 whether or not they support the presence of a capable fault. These s j studies are described in detail in the body of the report. )I i' It is concluded that no capable faults exist in the vicinity of the l I postulated Millett and Statesboro faults; there for e , they can have no impact on the existing accepted seismic design bases of the Vogtle Electric Generating Plant. ( 1 i
- I a
!I i iv
I I TABLE A I
SUMMARY
TABULATION OF RESULTS OF STUDIES TO DETERMINE PRESENCE OF CAPABLE FAULT METHOD EVIDENCE FOR FAULT
+ o -
GROUND WATER HYDROLOGY Review of Existing Data X Evaluation of New Data X Ground Water Modeling X
' I SURFACE WATER HYDROLOGY X
I SEISMICITY Earthquake History Microseismic Data X X REMOTE SENSING Satellite Imagery X Low and High Altitude Photography X GEOLOGIC MAPPING Lithologic Units Distribution i X Tectonic Structure Features X CORE DRILLING AND LOGGING I Offset of Formations from Core Offset of Formations from Geophysical Logs X X LITHOLOGIC EVALUATION Petrography X Clay Mineralogy X Heavy Mineral X GEOPHYSICAL EXPLORATION River Seismic Reflection Survey X SRP Survey X SeisData Services X I Legend: + Results support the presence of a capable fault o Results indeterminate as to fault capability
- Results support the absence of a capable fault I !
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1.0 INTRODUCTION
I This report carefully examines a postulated fault discussed in United States Geological Survey Open-File Report 82-156 (Faye and Prowell, 1982). The Open-File Report states: " Geologic and hydrologic investigations by the U.S. Geological Survey have defined stratigraphic and hydraulic anomalies suggestive of faulting within Coactal Plain sediments between the Ogeechee River in east-central Georgia and the Edisto River in west-central South Carolina." The postulated fault, referred to as the Millett fault, was proposed to exist approximately seven miles rooutheast of the Vogtle Electric Generating Plant (presently under construction southeast of Augusta, Georgia) . Figure 1-1 shows the location of the postulated fault in relation to the plant site and other geographic reference points. A second fault, referred to in the Open-File Report as the Statesboro fault, was proposed to exist approxinately 32 miles southeast of the Vogtle site. This feature was given secondary importance in the Open-File Report and was described as having less basis for existing than does the Millett fault. The U.S. Nuclear Regulatory Commission has established criteria for determining whether a fault is " capable" and therefore must be considered in establishing the seismic design bases of a nuclear power plant. A fault is considered capable if it has moved either once in the last 35,000 years, or more than once in the last 500,000 years. The Open-File Report did not attempt to assess the age of last movement i on the postulated Millett fault. No evidence was presented which would 3 !
) preclude the postulated fault being capable. l
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I To evaluate the ef fect, if any, of the postulated fault on the accepted seismic design bases of the Vogtle Plant, a task force was assembled. This task force consists of personnel from Georgia Power Company, Southern Company Services, and Bechtel. Bechtel was given the responsibility of conceiving and conducting a program of investigation designed to determine the presence or absence of a fault at the location suggested by the Open-File Report and, if present, the capability of such a fault. 'I The investigations were directed at several scientific fields which address the question of faultina. These include surface and subsurface geology, geophysics, ground water characteristics, surface water hydrology, and historic seismicity of the area. The scope of the studies performed is discussed in Chapter 2 and subsequent sections of this report. The studies were performed from March through August, 1982. The principal participants included personnel from Georgia Power Companf, Southern Company Services, and Bechtel. Drilling services were provided by Alabama Power Company and Law Engineering and Testing Company (LEKO). Geophysical logging of core holes was performed by the Birdwell Division of Seismograph Service Corporation, and by LEKO. Seismic reflection work was performed by Harding-Lawson Associates in conjunction with Dr. V.J. Henry of the University of .l 'E Georgia Marine Geology Program. Contract numerical modeling services were provided by Geomath, Incorporated, of Denver, Colorado. Clay mineralogy studies were performed by Dr. R.E. Grim of the University of 1-2
E Illinois, 'and heavy mineral analyses were performed by Reservoirs, Incorporated, of Denver , Colorado. To provide guidance and review of the studies, a number of eminerat consultants were retained. The following group of consultants was . l chosen because their fields of expertise were related to the planned [: studies: Dr. V.J. Henry of the University of Georgia; Dr. Bruce Bolt, Director of the Seismographic Station at the University of California, Berkeley; Dr. P. E. LaMoreaux, President of P.E. LaMoreaux and Associates; Dr. Carl Stepp, affiliated with Woodward-Clyde Consultants; - Dr. R.D. Hatcher of the University of South Carolina; Mr. H. LeGrand, an independent consultant in geohydrology; Mr. Carl Savit, Vice President of Western Geophysical Dr. S. Papadopulos and Mr. L. Wood, ground water geology specialists with S. Papadopulos and Associates; and Dr. R. Lyon, remote sensing specialist at Stanford University. [. 1 This report is organized into two volumes; the first contains a discussion of the studies performed along with the results of the [ studies and derived conclusions and the second contains supporting data and more detailed development of certain of the subjects covered in {' volume I. T + In Volume. I, Chapter 2 describes the scope of studies and Chapter 3 presents a summary of the principal conclusions. Chapter 4 discusses
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the geologic features .of the region and study area, while Chapter 5 {. - describes regional and local ground ' water characteristics. Chapter 6 discusses the field investigations, and Chapter 7 describes the office [ c? l-3 u - . _ _ _ _ _ _ _ _ _ _ - _ _ _ _ _ _ - _ .
studies conducted in parallel with those in the field. Chapter 8 concludes the first volume and presents a detailed assessment of the postulated Millett fault. Volume II contains appendices which present the supporting data as well as further details on certain of the studies. The report includes tables and is illustrated by figures and plates.
'Ihe writers gratefully acknowledge the helpful contribution of information and assistance provided by Dr. P. Huddlestun of the Georgia Geologic Survey. In addition, personnel of the USGS, the Georgia and South Carolina Geologic Surveys, and the South Carolina Water Resources Commission, provided data from their files. Mr. M.J. Sites III of DCE, and Dr. I.W. Marine of the Du Pont Company, provided open-file data, geophysical data, and microseismic records from the Savannah River plant, as well as many helpful suggestions during the course of the study. Mr. M. Hawkins and Dr. P. Mayer, representing Allied General Nuclear Services, also generoosly provided data, guidance, and review of the studies. Appreciation is extended to the management of the Savannah River Plant, to the Burke and Allendale County Boards of Commissioners, and to Mr. William Morris III, who gave permission for core holes to be drilled on federal property, county right-of-ways, and private land, respectively. We also wish to thank the raany owners of existing wells who graciously cooperated with the well survey crews by providing access to their wells.
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[ i 2.0 SCOPE OF STUDIES [ The task force decided on a program of thoroughly investigating all [ lines of evidence which could help to resolve the issue of the
. existence and potential effects of faulting. Accordingly, an investigation was developed which encompassed a number of different fields. Care was taken to ensure that different studies would retain a measure of independence from one another and would not be overly
[- influenced by the results of companion studies. Table 2-1 illustrates the tasks conducted. [. The investigations performed can be classified into three general groups: 1) those designed to assemble and evaluate the vast body of existing datar 2) those designed to generate new original data to positively demonstrate the presence or absence of a capable fault; and [- 3) those designed to specifically address issues raised in the Open-File Report and cited as suggestive of faulting. This third category includes studies dealing with both existing and [ newly-generated data. [ The first group of studies involved searches for published and unpublished data and the review and evalnation of these data. University theses were researched. Previous geologic data generated [_ for the Vogtle project were assembled and reviewed. Visits to federal, state, and county agencies were conducted to procure and review [ 2-1 i-
open-file data. Oil and gas exploration companies as well as geophysical prospecting firms were contacted to determine the availability of exploratory well and geophysical information. Discussions with knowledgeable local geologists also provided unpublished background material. All historic earthquake information within a radius of 62.5 miles around the Vogtle site was studied. Geologic and seismologic data collected by staff members of the Savannah River Plant, across the river from the Vogtle site, were reviewed and evaluated. This information provideo a framework for understanding the re gional and local geology, ground and surface water hydrology, and seismicity. Renote sensing studies using air photos and satellite imagery provided the background for geologic mapping and lineament locations. 1 . The second group of studies involved the collection of new data pertaining to the question of faulting. Tasks included surface geologic mapping of an area including the postulated Millett fault. This mapping was tied to previous mapping of a five-mile-radius area l around the Vogtle site, and to previous published mapping of the Savannah River Plant (Siple, 1967). Subsurface information was obtained by drilling and logging of two lines of core holes across the trace of the postulated fault for correlation purposes. These lines of holes generally parallel the Savannah River with one line on the Georgia side and the other on the South Carolina side. The holes were I 2-2
- I e
drilled to depths of about 600 feet, but one hole reached to a depth of 1024 feet. All holes were continuously cored and suites of geophysical logs were recorded. Soil sampling techniques were used in selected zones with poor core recovery. Petrographic studies and clay and heavy mineral analyses were p erformed on selected core samples to assist in correlating between holes. Upon completion of drilling, the holes were converted into ground water observation wells. I In addition to core drilling , several continuous seismic reflection profiles were run along the savannah River across the traces of the postulated Millett and Statesboro faults. These surveys generally parallel the two lines of core holes and provide information on the subsurface geology as delineated by seismic reflectors. A uniboom and two airgun systems were employed to achieve varying degrees of penetration of the strata underlying the river. I The third category of studies mentioned above included analyses of existing data and gathering of new information designed to address specific criteria cited in the Open-File Report as suggestive of faulting. The Open-File Report addresses ground water evidence, therefore, a study of aquifer characteristics in a broad area around the postulated Millett fault was conducted. Water wells were inventoried and water levels and other pertinent information were collected and recorded to provide a concurrent data base for ground water studies and numerical modelling of aquifer characteristics. I I 2-3
Surface water hydrologic characteristics were evaluated based on historical stream flow records as this had been discussed in the l Open-File Report as being suggestive of faulting. Petrographic descriptions of well-cuttings from key wells cited in the Open-File Report were made to determine whether there was a basis for the existence of upthrown Triassic rocks on the southeast side of the postulated Millett fault. Wells P5R and AL-66, the two wells cited in the Report as straddling the Millett fault, were re-logged geophysically to aid in correlations in the subsurface zone between th em. All of the above studies are described in greater detail in following sections of this report. I I 2-4
F E E E E g g TABLE 2-1 SCOPE OF INVESTIGATIONS Field Studies Office Studies PU RPOSE TASK PURPOSE TASK Core drilling Investigate stratigraphic Literature search Assemble background information correlations across trace of postulated fault Thesis search Assemble background information Acquisition of open- Use for ground water studies; Li thologic
" file data from federal, geologic structure studies sampling state, county agencies Geophysical " Evaluate available Use for geologic structure geophysical data studies logging of core holes Seismicity study Check for association of
" seismicity with postulated fault Savannah River acoustic re-Remote sensing Search for surface expression flection survey of faulting Geologic Mapping Stratigraphic correlation and search for surface Lithologic evaluations Lithologic correlation across expression of faulting Petrography trace of postulated fault Clay Mineralogy Remote sensing Search for surface express- Heavy Minerals field check ion of faulting Ground water evalua- Reduction of field data; tions numerical modelling using Observation well Investigate water levels concurrent base to check for installation in upper and lower aquifers across trace of fault effect postulated fault Surface Water Analyses of base flows using Water well survey Provide concurrent data Hydrology study concurrent data base to check base for ground water fault effects studies k_
3.0
SUMMARY
OF CONCLUSIONS I The results of the studies described in this report conclusively demonstrate that even if the postulated Millett fault referred to in the Open-File Report actually exists, it is not a capable fault. Therefore, it has no effect on the existing accepted seismic design bases of the Vogtle Electric Generating Plant. The evidence suggests that no fault is present within the depth range of this investigation. A second conclusion is that no capable fault exists near the location of the postulated Statesboro fault. These conclusions are supported as follows: I 1. Results of core drilling, lithologic studies, and geophysical logs demonstrate continuity of subsurface horizons across the trace of the postulated Millett fault on both the Georgia and South Carolina sides of the Savannah River. These unfaulted subsurface horizons have ages ranging from approx'.mately 40 million to approximately 80 million years Befere Present. I 2. Results of acoustic reflection studies demonstrate continuity of I subsurface reflecting horizons down to an elevation of approximately -1,100 feet across the trace of the postulated Millett fault. A reflector at elevation -1,100 feet, believed to be the surface of the Triassic rocks in the Dunbarton Basin, may have an apparent offset of approximately 50 feet. This 50-foot I I I >-
I I l of fset is questionable but would agree with small faults or l erosion ef fects interpreted from SRP geophysical records. It disagrees with the 700-foot of fset proposed in the Open-File Report. Reflectors above this feature are not offset. I 3. Results of acoustic reflection studies demonstrate continuity of subsurface reflecting horizons across the trace of the postulated Statesboro fault. I 4. Detailed surface geologic mapping and remote sensing studies reveal no evidence for surface expression of faulting in the area indicated in the Open-File Report.
- 5. Groiand water studies performed using a concurrent data base do not support the existence of a fault.
- 6. Surface water hydrologic studies using a concurrent data base do not support the existence of a fault.
I 7. Historic seismicity, including microearthquake records, reveals no evidence of active faulting in the area. I 8. Petrographic studies of well-cuttings from well AL-66 strongly indicate that this well bottoms in Cretaceous rather than Triassic rocks as suggested by the Open-File Report, thus removing upthrown Triassic rocks as a basis for a fault. I 3-2
1
- Q ^
- 9. Core hole VSC-4, drilled near well AL-66 and approximately 300
[ feet deeper than the Triassic contact proposed in the Open-File Report, bottoms in Cretaceous rather than Triassic rocks, confirming the conclusion in eight, above. The bases for the above findings are discussed in detail in the following sections of this report. I I p t I E ; I E B 3-3
I 4.0 GEOLOGY This chapter discusses the geology of the plant site and surrounding area. Reference can be made to the Preliminary Safety Analysis Report (PSAR) for Vogtle for additional discussion of both the local and regional geology. W Since the PSAR was written, the stratigraphic nomenclature in the study area has undergone a certain amount of reinterpretation and some of the formation names and intraformational boundaries are changing. The ! names of the intraformational units may change, but the formations of which they are a part are distinct, lithologically and geophysicallf, ! and can be correlated. The stratigraphic nomenclature adopted for this report accepts, in general, the current thought of geologists working in the area, most notably, P. Huddlestun, of the Georgia Geologic Survey. The terminology used was selected because, although not yet completely formalized, it is thought to accurately represent the best knowledge of the stratigraphic framework of the study area. A correlation chart (Figure 4-3), and a lithologic chart (Figure 4-4) are provided for reference. I 4.1 Physiography and Geomorphology I The Vogtle site is approximately 26 miles south-southeast of Augusta, Georgia, in the Atlantic Coastal Plain Province. This province I I I '-1
[ adjoins the Piedmont Province to the northwest. Within a 200-mile radius of the site in Georgia are the Blue Ridge and Valley and Ridge Provinces. These provinces and the location of the site are shown on Figure 4-1. I L The Atlantic Coastal Plain Province extends approximately 4,000 miles along the eastern edge of North America and covers approximately 60 Percent of the total surface area of the State of Georgia. Along its inner margin, at the boundary with the Piedmont Province, is the Fall Line, which marks the contact between the crystalline basement rocks and the overlying Cretaceous and Cenozoic sediments. The Vogtle plant site is on the eastern margin of the Tif ton Upland, a sub-maturely dissected area of the Atlantic Coastal Plain Province just seaward of the Fall Line. The Savannah River valley is old, with a broad flood plain trending northwest-southeast across the coastal plain. Adjacent to this flood plain the land surface has been dissected by the tributaries of the Savannah River. Leaching of the soluble Utley Limestone (described in Section 4.2.3.1.2) has caused local subsidence producing small, shallow depressions. 4.2 Stratigraphy and Lithology I~ L 4.2.1 Late Precambrian and Paleozoic Eras I L The crystalline basement complex beneath and north of the plant site L is composed of igneous and metamorphic rocks of late Precambrian - through Paleozoic age (800 to 250 m.y.B.P. ) . 4-2
The southern Appalachians evolved in a series of collisions of fragments of continental or island are material at the easter n edge of Nor th America. Several models have been developed to explain the development of the southern Appalachians (Hatcher, 1972; 1978; Ra nk in , , 1975; 197 6 ; Cook and o ther s , 1980; 1981; Hatcher and Odom, 1980; Ceak and Oliver , 1981). About 750 m.y.B.P. a megacontinental expanse split into at least two li .ge continents and at least two continental fragments, the Piedmont-Blue Ridge fragment and the Carolina Slate Belt f r agment . 16 the period of early rif ting volcanic and the metasedimentary rocks of , the Blue Ridge, were deposited in a basin between proto-North America and the Piedmont-Blue Ridge fragment. Volcanism started in the island arc of the Carolina Slate Belt about
- 650 m.y.B.P., meaning that subduction, which gave rise to the volcanic - acti'Jity, also began at about the same time. As a result of the w
subduction the basin between proto-North America and the Piedmont-Blue
~
Ridge fragment began to close about 500 m.y.B.P. E
- The first period of deformation and metamorphism (500 to 450 m.y.B.P. )
-- can be attributed to closing of this basin and the subsequent collision ~~ of the Piedmont-Blue Ridge fragment and proto-North America. This '~ deformation caused a shift in the source of the sediments that gave W N L 4-3 w - ..
I rise to the Ordovician sandstones and shales of the Valley and Ridge Province, changing their character from poorly sorted grayweckes, siltstones, shales, and conglomerates to better sorted material. I The second period of mountain building, from 400 to 350 m.y.B.P. , was ,l 5 characterized by extensive metamorphism and deformation. It was triggered by the closing of the ocean basi between the Piedmont-Blue Ridge and the Carolina Slate Belt fragment. 'I The last major compressional event was from 300 to 250 m.y.B.P. This mountain building episode can be attributed to the collision of proto-North America and proto-Africa to form the supercontinent of l Radioisotopic age dating indicates that many of the igneous Pangaea. I bodies in the Piedmont were emplaced during this time. Between 250 and l 200 m.y.B.P. extensional tectonism began to break Pangaea into smaller continents. I The crystalline basement rock ranges in age from Precambrian (?) through Paleozoic. The basement rocks exposed northwest of the Vogtle site include the gneisses and granites of the Kiokee Belt and the phyllites and greenstones of the Belair Belt (O 'Connor and Prowell,1978, Snoke and others,1980) . The upper surface of the basement rock has been I eroded, tilted to the southeast, and buried. The general plane of this surface strikes approximately N62*E and dips southeast at 30-40 feet per mile. I I 4-4
I 4.2.2 Mesozoic Era 1 I 4.2.2.1 Triassic Period The tectonic model which best explains the stratigraphic distribution of lower Mesozoic rock now on the eastern coast of North America includes the following cequence: 1) Permian to Late Triassic (280 to 205 m.y.B.P.) uplif t and crustal thinning along the axis of the future Atlantic Ocean; 2) Middle to Late Triassic (215 to 205 m.y.B.P.) strike-slip faulting and volcanism along east-trending fracture zones followed by the advance of the Tethys Sea; 3) Late Triassic (205 to 193 m y.B.P.) rif ting along the axis of the proto-Atlantic Ocean and I shearing along east-west fracture zones. This action had the combined effect of decoupling segments of the African and North American plates causing deposition of clastic sediments in the " Triassic" basins that formed. Late Triassic to Early Jurassic (205 to 188 m.y.B.P.) crustal extension and extrusion of basaltic lavas was followed by collapse of the continental margins and concomitant deposition of marine carbonates I (Manspeizer and others,1978) .
" Triassic" basins occur along the eastern seaboard from Connecticut south to Georgia (Figure 4-5). Basins north of South Carolina are exposed in Piedmont crystalline rocks while those in South Carolina and Georgia are overlain by Cretaceous and Cenozoic sediments. The clastic sediments within these basins have been tentatively correlated to rocks I
4-5
I I of the Newark Supergroup of Late Triassic and Early Jurassic age I (Siple,1967; Olsen and Galton, 1977; Van Houten, 1977; Gohn and others,1978; Manspeizer and others,1978) . It is difficult to obtain an accurate age for the sedimentary rocks within these basins due to their nonfossiliferous, time-transgressive nature (Manspeizer and others, 1978) . Because of these problems, considerable controversy still exists about the age of these basins, and the chrono-stratigraphic relationships of the various Newark depositional , basins (Cornet and others, 1973; Manspeizer and others, .'978). Correlation of these sediments to the Newark Supergroup is based on a similarity in flora and fauna and that in some cases, they are overlain by basalts of Early Jurassic age (Cornet and others, 1973; Manspeizer and others,1978) . l As shown in Figure 4-6, the general area of the Vogtle site, the Savannah River Plant, and the postulated Millett fault are underlain by I l the buried Dunbarton " Triassic" Basin. The sediments within this basin I have been identified as Triassic based on stratigraphic position and lithology. No microfossils (V?rine and Siple, 1974; Marine, 1976; l 1979) or igneous rocks (Popence and Zeitz,1977; Dames and Moore, 1980) of Jurassic age have been found in the Dunbarton Basin, and for this reason the Dunbarton Basin is considered to be Triassic. Marine and Siple (1974) have presented the most complete lithologic description of the Triassic rocks of the Dunbarton Basin based on drill cores. I g 4-e
- I They described the central northwest portion of the basin (DRB 9 on Figure 4-6) as a fanglomerate comysed of red-brown breccias containing pink, weathered gneiss fragments and quartzite in a matrix of claystone and siltstone.
The central part of the Dunbarton Basin (DRB 10 on Figure 4-6) is composed of alternating layers of: 1) a friable and weakly cemented arkosic sandstone, medium- to coarse-grained, pink to buff, with of a matrix of hematitic clay containing sand-size particles of schist, quartz, and eathered pink feldsparg 2) a well consolidated and poorly sorted, fine- to medium-orained, gray-brown, sandstone, including much silt and clay; and 3) a mudstone containing sjlt, clay, and some ~~ ~ fine-grained red to maroon sand (Marine and Siple, 1974). The rocks from this centrol area of the basin were apparently deposited under fluvial conditions, and commonly contain calcareous cement, probably from the evaporation of ground water shortly af ter deposition. I Rocks from what may be the southeastern part of the basin (P5R on
- Figure 4-6) are described as
- 1) maroon siltstones and claystones, containing gray calcareous nodules; and 2) fine- to very fine-grained gray-brown sandstones, alno containing calcareous nodules (Marine and Siple , 197 4 ) . The clastic sediment fraction appears to have been flood i
t deposited but the calcareous nodules apparently have formed in place. I The lithology of the rocks in the Dunbarton Basin is of great importance to the present study because well cuttings reported to be Triassic in ag in the Open-File Report are used as evidence for 4-7
I postulating the Millett fault. This subject is discussed further in I Chapters Seven and Eight. The sedimentary fill in the basin may have reached a maximum thickness of 6,000 to 8,000 feet greater than at present based on estimates made from the conversion of montmorillonite to illite with depth of burial (Marine, 1976b) . Subsequent erosion (Jurassic-Early Cretaceous , aproximately 188 to 100 m.y.B.P.) has not only removed the Triassic highlands, but also up to 8,000 feet of the former basin fill. 4.2.2.2 Cretaceous Period lI l Fcllmzing a period of uplif t and erosion in the Early Cretaceous (140 to 100 m.y.B.P.), there was a transgression of Late Cretaceous (100 to 65 m.y.B.P. years ago) seas (Vail and Mitchum,1978) . The basal clastic formation in the area of the postulated Millett fault is the subaerial Tuscaloosa Formation (Middendorf Formation in the Open-File Report - See Figure 4-3). Deposition of this formation began sometime l between 100 and 94 million years ago (Cramer and Arden,1980) . An unconformity exists in the Upper Cretaceous series of South Carolina between 94 and 82 m.y.B.P. (Gohn and others,1978; Christopher,1982) which may be correlated in part with an erosional surface within the l l= Tuscaloosa downdip of the plant site (Cramer and Arden,1980; Gohn and other s, 198 2) . Following this period of erosion the sea again transgressed onto the continent. Clastic sediments ranging in age from 86 to 79 m.y.B.P.
- were deposited in localized regions in western and central Georgia.
4-8
I I These deposits are overlain by a sequence of marine sediments which, in I the study area, are predominantly sands (Cramer and Arden, 1980). The Tuscaloosa Formation consists of fluvial and estuarine deposits of cross-bedded sands and gravels intercalated with lenses of variegated silt and clay (Siple, 1967; Cramer and Arden, 1980; Gohn and others, 1982). The Tuscaloosa is unconformably overlain by the Ellenton Formation, or where the Ellenton is missing, by sediments of later Tertiary and Quaternary ages. In the drill core, the Tuscaloosa Formation consists of light-gray to white, tan, and buf f quartzitic to arkosic sand and minor gravel intercalated with lenses of white, pink, red, brown and purple silt and clay. Individual beds of coarse and fine sediment are interbedded in no regular sequence, and grade laterally into one another or pinch out in short distances. Abundant kaolin is present along with other clay 4 minerals. No rocks of latest Cretaceous age are present in Georgia or South Carolina (Rankin,1977; Cramer and Arden,1980; Gohn and others, 1982). The Cretaceous-Tertiary boundary is marked by an erosional surface which may be due, in part, to a post-depositional fall in sea level (Vail and Mitchum,1978) . 4-9
[ I 4.2.3 Cenozoic Era l I 4.2.3.1 Tertiary Period I 4.2.3.1.1 Paleocene Epoch Sediments deposited during the lower Paleocene (65 to 60 m.y.B.P. ) are thickest in the southwest indicating that seas transgressed from that direction. "ollowing this period of deposition, uplif t of the region resulted in the erosion and removal of most of these rocks in Georgia (Rainwater,1964; Cramer and Arden,1980) . This uplift was accompanied by faulting in response to the tectonic forces resulting from the northwestward drif t of a passive continental margin (Bott, 1978). Tne lower Paleocene series consists of the Ellenton and the Huber Formations. Ellenton Formation The Ellenton Formation is of a dark-gray to black sandy lignitic micaceous clay interbedded with medium- to coarse-grained quartz sand. Authigenic gypsum crystals are commonly distributed throughout the unit. The upper part of the formation contains a gray silty to sandy micaceous lignitic clay with which the gypsum is commonly associated. In some drill holes the clay zone was overlain by coarse quartz sand. The lower part of the Ellenton is sandy, lignitic clay which, in some areas, becomes very coarse and gravelly. The sand grains are bluish-gray quartz. 4-10
I I l l The Ellenton is unconformable with the underlying Tuscaloosa J Formation. The contact is characterized by a change in color of the clay and a change in composition of the sand. The dark-gray to black l clay of the Ellenton is readily distinguished from the variegated clay of the Tusacloosa. The Ellenton grades into the overlying Huber Formation in two of the holes drilled for this study. The color of the sediments changes from the dark-gray to black sands and clays of the , Ellenton to the red, tan, or mustard-yellow sands and clays of the overlying Huber Formation. Siple (1967) tentatively assigned the Ellenton to the Late Cretaceous based on the similarity of the lithology and stratigraphic position with other formations o.' Late Cretaceous age in other parts of the Coastal Plain. Based on analysis of palynomorphs (U.O. Fredricksen, unpublished data, 1980) and planktonic foraminifera (P. Huddlestun, personal communication, 1982), the Ellenton Formation has been placed in the Paleocene in this study. Huber Formation The Huber Formation lies between the top of the Ellenton Formation and base of the overlying sands and limestone of middle Eocene age. The lithology of the Huber Formation is diverse, ranging from beds of multi-colored clays, high-purity and sandy kaolin, to thick, g , W cross-bedded members of coarse, pebbly sand, and conglomerate composed of boulders of pisolitic kaolin (Buie, 1978). In the drill core the uppermost part of the Huber Formation shows signs of weathering and reduction. 4-11
A second transgtession occurred in the late Paleocene (Rainwater, 1964; Cramer and Arden, 1980). The full landward extent of this transgression is unknown due to later Eocene erosion, but the thickness of the carbonate section in Georgia suggests that it was extensive (Cramer and Arden, 1980). 4.2.3.1.2 Eocene Epoch I Following a period of erosion during the early Eocene, the sea again transgressed over the Georgia Coastal Plain during the middle Eocene. The bulk of the middle Eocene (4 9 to 45 m.y.B.P. ) sediments are carbonates, with up to 10 percent chert and evaporite. Updip, all of the carbonate rocks become coarser and grade into calcareous sands, indicating a higher energy environment. Outcrops of the lower unit of middle Eocene sediments are sparse at the Fall Line because of overlap l l by the calcareous sand and limestone beds of the Lisbon Formation which effectively mask it. Marine overlap onto the Coastal Plain is evident and paleontological data indicate that the transgression was very slow (Cramer and Arden,1980) . Following the transgression of the Lisbon seas, regression again occurred and erosion of the middle Eocene rocks ! began. I I I . l l 4-12
Late Eocene V5 to 38 m.y.D.P) deposition is represented by a relatively thin, uniform blanket of shelf 1imestone and calcareous sands. These rocks unconformably overlie rocks of middle Eocene age, but with only a small hiatus in time. The basal beds are part of the Utley Limestone Member which is sandy limestoner. Northeastward clong the Fall Line the fluctuating strandline of the .Tackson-age sea is apparent in the intertonguing of carbonate and clastic formations. A period of regression is apparent, and rocks of late Eocene age overlain by upper Oligocene deposits. The Eocene series consists of the middle Eocene Lisbon Formation and upper Eocene Barnwell Group. Lisbon Formation The Lisbon Formation occurs between the top of the Hrber Formation and an unconformity at the base of the Barnwell Group. In the study area, the Lisbon Formation is subdivided into three members: an unnamed basal sand and limestone Member, the Blue Bluf f Member, and the McBean Limestone Member. The basa? R. ember was present in the core holes drilled for this study. The lowermost portion consists of quartz sand which grades both up . sectior,and downdip into a calcareous sand. Overlying these sands is a limestone. These deposits were dated as middle Eocene and correlated with part of the Lisbon Formation based on examination of foraminifera from hole VG-8 (Huddlestun, personal communication, 1982). The Blue Bluf f Member is a greenish- to bluish-gray, moderately hard calcareous siltstone or marl. In the core holes the marl is thinly interbedded to laminated, with isolated limestone nodules and shell fregments. Examination of foraminifera by Paul Huddlestun (personal communication, 4-13
!I 1982) from holes VG-6 and VG-8 have verified the marl to be middle Eocene age, Lisbon Formation. Updip, the McBean Limestone Member is composed of sof t, gray limestone and calcareous sand. Downdip the Blue Bluf f Member interfingers with an unnamed gray calcareous sand and f .4iliferous limestone. Barnwell Group In the study area deposits of late Eocene age include the Barnwell Group. This group consists of the Clinchfield Formation which contains the Utley Limestone Member; the Dry Branch Formation which contains the Irwinton Sand, Grif fins Landing, and Twiggs Clay Members; and the Tobacco Road Sand. Downdip the Barnwell Group grades into the
= carbonate facies of the Ocmulgee, Crystal River, and Williston Formations of the Ocala Group.
Clinchfield Formation The Utley Limestone Member of the Clinchfield Formation is typically a sandy, glauconitic, slightly argillaceous, and locally cavernous limestone of varying degrees of induration (Huddlestun and Hetrick, 1979). The Utley Limestone is locally discontinuous in Burke County. Dry Branch Formation Huddlestun and Hetrick (1979) raised the Dry Branch to formational rank and defined three distinct but interfingering lithofacies: a montmorillonite clay (Twiggs Clay); a distinctly bedded sand (Irwinton Sand); and an indistinctly to massively bedded, calcareous, fossiliferous sand (Griffins Landing) . 4-14
The Twiggs Clay is a pale greenish, olive green, bluish-gray, dark gray, or locally, almost black, silty clay with hackly, blocky, subconchoidal to conchoidal fracture. As shown in Figure 4-3, Twiggs Clay interbeds occur in both the Irwinton Sand and Grif fins Landing Members of the Dry Branch Formation (Huddlestun and Hetrick, 1979; Huddlestun, personal communication, 1982). The Irwinton Sand consists of fine- to medium-grained, well sorted, deeply weathered, almost pure quartz sand that shows well developed horizontal and local cross-bedding in outcrop. In core holes, the Irwinton Sand was difficult to recover owing to the lack of silt and clay in the matrix. Downdip, the Irwinton Sand interfingers with the Griffins Landing Member, a fairly well sorted, massive to indistinctly bedded calcareous sand. The unit often contains lenses of Twiggs Clay associated with oyster shell (Crassostrea gigantissima) beds. In the drill ccre, the Griffins Landing generally consists of oyster shell sands and clay overlain by massive calcareous sand. Downdip, the Grif fins Landing i grades into the Williston Formation, a non-fossiliferous, sandy I l I equigranular limestone (Huddlestun, personal communication, 1982). I Tobacco Road Sand The uppermost formation within the Barnwell Group is the Tobacco Road Sand, which is predominately a quartz sand. The sand in the Tobacco Road varies from fine-grained and well-sorted to very coarse-grained, granular, pebbly and poorly sorted. The Tobacco Road is characteristically massively bedded and bioturbated although locally I I 4-15
I the formation may be thinly and distinctly bedded, even laminated (Huddlestun and Hetrick , 1978; 1979). The core and split spoon samples did not show these bedding features, but did show significant evidence of plant and animal life. The Tobacco Road Sand in Screven County grades into the Ocmulgee Formation, which includes: 1) foraminiferal marl; 2) fossiliferous, granular limestone; 3) clay. Further downdip, , the Ocmulgee grades into the Crystal River Formation, a coarse bryozoa-i rich limestone (Huddlestun, personal communication, 1982). 4.2.3.1.3 Oligocene Epoch !I l At least two transgression / regression cycles occurred during the l= Oligocen e. Only the upper Oligocene (32 to 25 m.y.B.P.) transgression deposited material in the study area. The full extent of this overlap (Suwannee) is not known, since an undetermined quantity of updip rocks have been removed by erosion. Facies patterns indicate that the overlap was probably extensive. The remaining Suwannee rocks are shelf lW deposits, with none of the updip clastic facies preserved. Suwannee Limestone
- In the downdip portion of the study area the Suwannee Limestone rests unconformably upon the Ocala Group. The basal part of the Suwannee
.l 5 consists of sandy limestone that is sparingly fossiliferous. Above this is a layer of predominantly cream-colored, relatively sof t, somewhat chalky, fossiliferous limestone. The upper part is a light I 4-16
I l i I gray to cream color, dense, nodular, cherty, and somewhat sandy limestone (Cramer and Arden, 1980). These limestones occur downdip from the core holes drilled for this study. I 4.2.3.1.4 Miocene Epoch I The rocks of Miocene age appear to be a sequence of predominantly clastic rocks deposited during and following the regression of u..e coast line. Considerable post-Miocene erosion took place before the return of the sea during Pleistocene time. In some places (Vogtle site included) erosion continued from the Miocene to the present. The erosion has altered the original sedimentary patterns, making changes in lithofacies dif ficult to interpret particularly since some of these sedimer.ts include terrigenous deposits of deltaic or possibly fluviatile origin. I Hawthorn Formation The Hawthorn (Altamaha) Formation is the yoangest Tertiary formation in the study area. It has been assigned an earliest Miocene (25 to 23 m.y.B.P.) age (Huddlestun, personal communication, 1982). Hawthorn sediments include poorly sorted clayey sands and gravels, containing cross-bedded stringers of limonite-goethite pebbles. These sediments were mapped during this study and are discussed in Section 6.1. The base of the Hawthorn sediments is generally above 200 feet elevation in the area of the core holes. Therefore, few borings penetrated these I -"*~"c-I 4-17
[t 4.2.3.2 ' Quaternary Period Geomorphic evidence indicates that uplif t and subsidence of the Coastal [: Plain of Georgia and surrounding states continued through at 'least the Pleistocene (Winker and Howard, 1977). Sediments have accumulated and related geomorphic features such as erosional scarps and terraces have developed. C; Alluvial deposits consisting of coarse gravel and poorly sorted sand occur. irregularly and discontinously in the tributaries and main channels of the Savannah River. [ 4.3 Structure C 4.3.1 Tectonic Framework of the Georgia Coastal Plain l 4.3.1.1 General The crystalline basement underlying the Georgia Coastal Plain dips toward the southeast at approximately 30-40 feet per mile. This regional dip is interrupted by several local structures. Most of the
- knowledge of the basement rocks comes from geophysical work, as few wells of suf ficient depth to encounter the basement have been drilled ,
C.- in this area. [ 4-18 P .s ... . _. . . ,. _ .. . .. 1
[- 4.3.1.2 Triassic Features [ The Dunbarton Basin is one of several elongated basins filled with Triassic (and in some other cases, Jurassic) sediments, found buried beneath the Cretaceous and Cenozoic age sediments of the Georgia Coastal Plain. [ The most probable origin of the Dunbarton Basin is the formation of a [ graben by normal faulting. Evidence has been presented for a northwest border fault of unknown displacement, and faulting has been hypothesized for the southeastern margin (Ma rine , 1976a , 1976b) . ( Substantial evidence for a southeastern border fault is lacking, however, and the nature and extent of this margin of the Dunbarton Basin is derived from gravity and aeromagnetic surveys (Marine and Siple, 1974; Marine, 1976b). The basin is oriented I northeast-southwest, and is about 31 miles long and six miles wide (Figure 4-6) based on an aeromagnetic survey. { The floor of the basin has been penetrated near the northwest basin margin by one well (DRB 9, Figure 4-6) which encountered an augen gneiss basement. This well penetrated 1,593 feet of Triassic rocks (Marine and Siple,1974) beneath the Cretaceous before encountering { basement rocks. Recent geophysical studies (including aeromagnetic, gravity and seismic reflection) have indicated possible faulting within the Dunbarton Basin
. and in the underlying crystalline basement (Marine, 1976b; Dames and Moore, 1980) . The data obtained in these studies suggests that the 4-19
I basin is composed of a series of blocks separated by steeply dipping (8 0 *-9 0 * ) faults, none of which can be traced into the Cretaceous sediments. An attempt to verify displacement along one of the more prominent of these intrabasinal faults was made and yielded inconclusive results (Marine, 1976b). Two holes, 690 feet apart and on different sides of the geophysically located trace, were drilled. No fault of fset of the Triassic-Cretaceous erosional contact was observed. An attempt to core th rough one of these steeply dipping intrabasinal faults in the Triassic by directional drilling was also inconclusive. Therefore, although minor faulting may have occurred within the Dunbarton Basin, the prominent intrabasinal fault indicated by aeromagnetic and gravity data was not verified by drilling. Available data indicate that from the northwestern border, the bottom of the Dunbarton Basin deepens to approximately 6,500 feet below the ground surface (about two miles southeast of DRB 10) . The basin then decreases in depth to the southeast to approximately 4,203 feet near the southeastern boundary of the Savannah River Plant. 'Ihus the bottom of the basin then appears to vary from 3,000 to 6,000 feet below the land surface southeast of the Savannah River Plant. Because of stratigraphic thickness and the nature of the truncation as shown on the gravity and magnetic data, faulting is a likely explanation for the southeastern boundary of the Dunbarton Basin. I 4.3.1.3 Cretaceous and Cenozoic Features I The dominant structural features of the Georgia Coastal Plain are two J large sedimentary basins separated by a structural high (Figure 4-2). l I 4- o I
I These features may be part of a larger system of southeast-northwest oriented structures in the eastern United States (Murray, 1961; Cramer, 1969). I The Southeast Georgia Embayment (Toulmin , 19 55) includes an area of downwarping and sediment thickening which formed during Cretaceous and Cenozoic time (Cramer,1969; Cramer and Arden,1980) . This feature has also been called the Okefenokee Embayment (Pressler, 1947), the Atlantic Embayment of Georgia (Herrick and Vorhis, 1963). I A second sedimentary basin, the Appalachicola Embayment, is an area of thickened Tertiary sediments extending into the southwest corner of Georgia. This feature has also been called the Soutnwest Georgia Basin (LeGrand,1961; Mur ray,1961) . Between these two embayments is a positive feature called the Central Georgia Uplift (Pressler,1947), which is defined as a southeast-northwest striking upwarped feature between the two flanking ! downwarped areas. The southern extension of the Central Georgia Uplif t l
- is the Peninsular Arch ( Applin , 1951) which also forms the spine of E Florid 4.
,g t i 4.3.1.4 Minor Framework Features I The Yamacraw Ridge is a basement feature trending parallel to the Georgia and South Carolina coastlines. It was first identified seismically and was later substantiated by a drill hole (Cramer and I 4-21
l Arden, 1980). Maps by Herrick and vorhis (1963) show that this feature C may have had some influence on Jpper Cretaceous sedimentation (Cramer, 1969). 4.3.2 Folding [ Several small undulations appear within the confines of the Appalachicola Embayment. Most have been recognized from subsurface data, although a few are expressed as surface features. The folding in southwestern Georgia appears to be of Tertiary age, and some folding may have occurred as late as Miocene (Sever,1966; Cramer,1969) . 4.3.3 Faulting Faults with minor displacement of Cretaceous and Cenozoic deposits are present in the southeastern United States (York and Oliver,1976) . The geology of the southeastern Atlantic Coastal Plain, however, is su<f) that faulting is not easily recognized. Poor exposure and subtle stratigraphic variations require that a detailed search for surface expression of these structures be made (Wentworth and Mergner-Keefer, 1981; 1982a; 1982b). Recent detailed work, for example, has indicated that northeast-trending faults with Late Cretaceous and Cenozoic reverse displacements do exist in the Atlantic Coastal Plain and [ Piedmont (Mixon and Newell,1977; Prowell and O'Connor,1978; Behrendt and other s, 19 81) . Wentworth and Mergner-Keefer (1982b) propose that many of these faults may be reactivated Mesozoic and older high-angle normal faults. [ 4-22 F . l- . . .
l 1 4.3.3.1 Belair Fault Zone 1 I The Belair fault zone is a structural feature extending alonq the inner margin of the Atlantic Coastal Plain (Figure 4-7). This fault is l located a few miles west of Augusta and about 29 miles northwest of the Vogtle site. It is thought to extend at least 15 miles from Fort Gordon Military Reservation on the southwest, to a quarry just west of the Savannah River on the northeast (O'Connor and Prowell, 1976b; Prowell and others, 1976; Prowell and O'Connor, 1978). l The Belair fault zone has been shown to consist of at least eight en i echelon reverse faults trending from N13*E to N50*E and dipping 50* to the southeast (Prowell and O'Connor, 1978). The fault zone juxtaposes t crystalline phyllite of the Little River Series of late Precambrian or Cambrian age against Coastal Plain kaolinitic sands and gravels, which l are formally correlated with the Upper Cretaceous Tuscaloosa Formation (Prowell and others,1976) . Individual fault segments are from one to three miles in length, with gouge zones only a few feet wide at most. I According to Prowell and others (1976) the basal Tuscaloosa unconformity is vertically displaced from 15 to 100 feet. The most recent documentable movement along the Belair fault zone occurred about 40 million years ago (Wentworth and Mergner-Keefer, 1981; 1982b). l 4.3.3.2 Gulf Trough l l Much controversy surrounds the structure and origin of the Gulf Trough l of Georgia (Figure 4-7) . Herrick and Vorhis (1963) identified the Gulf Trough within the Appalachicola Embayment from isopach and structure i 4-23
k_ 1 (;.
. contour maps ' prepared from subsurface data. The structure is linear
]
and more sharply defined than the surrounding folds, and for these reasons Cramer (1969) concludes that the trough was formed by ) [ faulting. In an earlier work, Callahan (1964) interpreted this feature as two parallel, down-to-the-southeast faults. Cramer and Arden (1980) also suggested evidence for faulting within the trough. Bechtel Corporation (1978) studied the Gulf Trough using both field reconnaissance .ind well log data. The studies concluded that well log data are compatible with the propcsed graben structure of Cramer (1969) southwest of coffee County, but the structure could not be projected north-eastward - to the Savannah River. If the Gulf Trough is due to faulting, the available data indicate that this movement would have to have occured prior to the beginning of the Miocene (Bechtel Corporation,1978; Gelbaum and Howell,1982) . The evidence suggests that other geologic phenomena, such as erosion, local variations in regional tilt, local subsidence or warping can also. explain the trough (Becht.1 Corporation, 1978). The origin of the Gulf Trough is not clear. Various authors have [ suggested possible mechanisms for its formation (Herrick and vorhis, 1963; Cramer, 1969; 1978; Patterson and Herrick, 1971). Patterson and-Herrick- (1971) have reviewed the proposals which include 1) normal faulting producing a graben; 2) down-warping forming a syncline; and 3)
-a Tertiary marine strait or valley.. Data from well log analyses by Bechtel Corporation (1978) _ do not favor any one of these proposed origins over the other biat-are compatible with all three.
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~~- SAPLE f t9871 i OPE N -F ILE RE Pon? $2-156 NOTE: ,
SOUNDARIES E9eCLEE THE APPROXIMATE AREAS ) i DeSCUSSE D IN THESE PUBLICATIONS. eLaca miseso ponvava. P A 2 2 EX PL A N A TIO N h UNCONFORMITY
- - - - - - - - AGE OF FORMATIOte IN OUESTON AT TIME OF REPOaT
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fop %3T90h BECHTEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT STRATIGRAPHIC CORRELATION CHART FIGURE 4-3
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$ $ POORLY SORTED CLAYEY SAND AND E g E HAWTHORN (ALTAMAHA! FORMATION PURPLE 1N COLOR. CONT AINS SOME C LIMONITEGOETHETE PEBBLEL i
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- SUWANNLE LIMES *0NE LIGHT 8
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@ MEMBER UNNAMEQQMESTONE: GRAY, FOSSIL b Ab N IN N b bt$
UNNAMED SANDS AND LIMESTONE HUBER FORM ATION HU8ER F4 MULTICOLORED CLA Y,L p KADDMTL COARSE BEDDED SANO. a w k* # E QN EM- DARK-GRAY TO BLAC V, EDIUM-TQ DARKGRAY COAH y ELLENTON FORM ATION a. o W TAN, BUFF. UGHT-GRAY ANO WHI N *w TUSCALOOSA FORMATION
- 5 O.UAR.TZITE Eo. RO.= AND PuRRLEANDCtAYARKOS AND ,
8 0 2 8 U GR AY. DARK 8ROWN AND BRICK RED W NE WARK (?) SUPE RGROUP CLAYSTONE WITH SECTIONS OF CONT
. GLOME RATE.
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!9 22 jo BASEMENT ROCK OF THE KIOKEE BELT AND BE LAIR SELT GRANITE, GNEISS.PHYLLITE AND GRt
($ Si t AFTER SIPLE,1967; BUIE,1978; HATCHE R,1978; HUDDLESTUN AND HETRICK,1978,1979; HUDOLESTUN, PERSI
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- LAY,CLT AND GRAVEL.
RAYEL; TAN.E.ED AND 40SSBEDDED ST24NGE RS OF NOTE: FORMATION AGES ARE GIVEN ON FIGURE 4 3 AND IN TEXT. LIFEROUS Lt"ESTONE. BASAL AND WELL SO3TED TO Rt. AND LIMEETONE. FERCUS LIMESTONE.
-GRJJNED OUAKT2 SAND.
O CALC /4.EOUS SAND. 4 C RJ.Y, SILTV S/ ND. ANDY LIMESTONE. X,0NITIC FOSSILIFEROUS Si+GMY MARL.
- f. SANDY LIMESTONE wlTH tFERCUS LIMESTONE.
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.; L K Upper Cretaceous deposits.
Triassic rocks overloir by Lower Cretaceous deposits. Source : Af ter Marine and Siple,1974 VOGTLE ELECTRIC GENERATING PL ANT L POSTULATED MILLETT FAU'. T SCALE IN MILES .TRI ASSIC ROCKS ALONG THE EASTERN SEABOARD FIGURE 4-5 l l l
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G 33'00* I 82'00' 45' / 30' 81'15' EX PL AN ATION O 2 4 6 8 WF"" Boundary of Triassic basin SCALE IN MILES inferred from aeromagnetic anomalies (Petry and others, 1965). Boundary of Triassic basin REFERENCES _: as interpreted from seismic and aeromagnetic data
- 1. Marine, l.W., and Siple,G E.,1974, Buried (Marine and Siple,1974 ;
Triassic basin in the central Savannah Petty and others,1965; River crea, South Carolina and Georgia- 3;ple,1967 ). GSA Bull.v.85, p. 311 -320.
- 2. Petty, A.J. and others,1965, Aeromagnetic $ Deep reck boring penetrat-ing Triossic rock.
map of Savannah River Plant, South Carolina and Georgia USGS Geophys.Inv. Map GP-489
- 3. Siple,G.E.,1967, Geology and ground water of the Savannah River Plant BECETEL and vicinity, South Carolina USGS Water-Supply Paper 1841,113 p. VOGTLE ELECTRIC GENER ATING PLANT POSTULATED MILLETT FAULT
- 4. Bechtel Corp; 1973, PS AR, v.I, Alvin W.
Vogtle Nuclear Plant : Unpublished report. BOUNDARIES OF THE TRIASSIC DUNBARTON B ASI N FIGURE 4-6
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FLORIDA ~~h l O 20 40 60 80 10 0 SCALE IN MILES BECETEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT SOURCE: Cro mer ,19 69 ; Bechtel Corp '1978 APPROXIMATE LOCATIONS Prowell and O'Connor,1978 :* OF BELAIR FAULT ZONE Cromer and Arden,1980; ANO GULF TROUGH FIGURE 4-7
I I l 5.0 HYDROGEOLOGY L l 5.1 Occurrence and Movement of Ground Water in the Coastal Plain I The alternating beds of sand, clay , marl and limestone that underlie the Coastal Plain of South Carolina and Georgia comprise a complex l sequence of aquifers and confining layers that dip to the southeast only slightly more than the regional ground surface. Water enters the i ! permeable sands and limestones principally by direct infiltration of precipitation in their outcrop areas, and migrates downdip. The interbedded clays and marls, being nearly impermeable, confine the water within the aquifers, leading to artesian conditions. Recharge to ( the aquifers can also occur from small streams crossing their outcrop areas, but most streams, including the Savannah River, receive ground I water discharge in the aquifer outcrop areas. Much of the recharge from water infiltrating the outcrops on the ridges between streams is discharged to the adjacent streams. l f Because of the facies changes and discontinuity of interbeds that characterize the geologic units underlying the region, aquifer l characteristics and interconnection between aquifers vary considerably I from place to place. The sedimentary complex can be grouped into two l aquifer systems that, at least in the area of confinement, are l separated by the relatively impermeable Ellenton and Huber Formations. The systems are most conveniently identified by the geologic age of the l I 1 I i 5-1
- I rocks comprising each system
- the Tertiary and the Cretaceous,.
t equivalent to the A2 and upper part of the Al systems designated in the Open-File Report. They both extend over a much larger area than is discussed in the present report, and are commonly identified by local aquifer names. I 5.1.1 Tertiary System , I Underlying the southeastern United States is a limestone aquifer system of Tertiary age that is referred to as the Floridan aquifer in Florida and as the principal artesian aquifer in Georgia, Alabama and South i Carolina. It is the primary source of municipal, industrial and i agricultural water supply on the coastal plain of Georgia (Krause and Hayes , 19 81) . Within Georgia and South Carolina, the aquifer system includes the sequence of carbonate rocks (and associated interbedded sands) of Eocene and Oligocene age shown on Figures 4-3 and 4-4. From these charts it can be seen that within a single stratigraphic time iW horizon, facies changes downdip can result in a confining layer i becoming an aquifer. For example, in the study area, the Tertiary l aquifer is comprised of unnamed sands and limestone of the Lisbon Formation that underlie the Blue Bluf f marl. However, downdip, the [ Blue Bluff interfingers with a permeable limestone that becomes part of the Tertiary aquifer system, and younger beds form the confining layer. I 5.1.2 Cretaceous System ! l Beneath the Tertiary aquifer system is the equally extensive Cretaceous system. It is a thicker and more transmissive aquifer than the 5-2
l I l Tertiary system, but is only minimally developed for water prodoction. 'g only in and near outcrop areas, where the aquifer is relatively 3 shallow, do many wells penetrate this aquifer. Downdip, the Cretaceous aquifer is too deep and few wells extend below the Tertiary system. E The Cretaceous system is made up primarily of Tuscaloosa Formation (or equivalent) sands and gravels, and is separated from the Tertiary system by extensive Paleocene carbonaceous clays of the Huber and Ellenton Formations. These clays appear to be an effective confining layer, providing hydraulic separation of the two aquifer systems where the clays are present. These clays tend to pinch out updip, toward the outcrop or recharge areas of the aquifers. In those areas water is relatively free to move from one aquifer system to another. As in the Tertiary aquifer, interbedded silts and clays tend to separate the Cretaceous into aquifer zones. However, the Cretaceous j stratigraphy is not as well defined and lithologic members have not l ! been mapped. i 5.2 Local Aquifer Conditions
- The aquifer systems of the coastal plain are present within the study l
area under water table conditions in outcrop areas, and under confined conditions where younger, less permeable beds overlie them. The outcrop areas are principal r,ources of recharge. The high permeability, thickness and extent of the outcrops indicate a high
- I
- 5-3
I I potential for acceptance of recharge, and the average precipitation in the area, in excess of 40 inches per year, is a large source of recharge. However, because the water levels in the aquifers are high, part of the recharge is rejected as discharge to streams that have incised the outcrops. The principal stream of the area, the Savannah River, has incised most deeply into the aquifers, f rom the Fall Line, north of Augusta, to more than 50 miles downstream. The average amount of ground water discharging to the Savannah River in the outcrop area of the' Cretaceous aquifer (rejected recharge) has been estimated to be about 170 mgd (Siple, 1960). From the Tertiary aquifer, similar drainage of rejected recharge is also occurring, but in smaller amounts. Both aquifers also discharge to the tributary streams crossing the octerops. Downdip of the outcrop areas, the Tertiary aquifer system is overlain by younger beds of the Lirbon Formation and the Barnwell Group, and it becomes hydraulically separated from the Cretaceous aquifer by the carbonaceous clay facies of the Ellenton and Huber Formations. These finer grained geologic units act as confining layers of the two aquifer systems throughout the southern portion of the study area. It is dif ficult to assess the hydrologic interrelationships of the ,I several aquifer zones of the Tertiary system found in the study area. Potentiometric levels differ from one zone to another, although the zones are hydraulically interconnected. Domestic wells extract water
~
5-4
I from the thin, but permeable Utley limestone, as well as from overlying sands of the Dry Branch Formation. However, when larger yields are desired, wells are drilled into the more permeable and thick, but unnamed, sands and limestones underlying the Blue Bluf f marl. All of i these units are part of the Tertiary system, and are interconnected, at least indirectly, updip in the recharge area and downdip through the limestone that is the age-equivalent of the Blue Bluf f marl. Because of these hydraulic complexities, investigation of the Tertiary aquifer system has been limited, in the confined area of the aquifer, to studying the hydrologic regime of the unnamed sanos and limestones underlying the Blue Bluf f marl. They are referred to herein as the upper aquifer which is approximately equivalent to the A2 aquifer of tne Open-File Report (Figures 4-3 and 4-4). In the unconfined, or recharge area, it is unnecessary to distinguish between zones. I Vertical dif ferences in potentiometric levels are also present within I the Cretaceous aquifer system. This is well illustra_ad in the data collected by this study and is discussed in Section 7.8.1. Again, in order to minimize the variables in the hydrologic analyses, ground water data of the Cretaceous system, referred to as the lower aquifer, were restricted to wells open only to the uppermost part of the Tuscaloosa Formation in areas where it is confined. This is only partially equivalent to the Al aquifer of the Open-File Report, which includes all of the Tuscaloosa Formation as used in this report. 1 I I I 5-5
[ . 6.0 FIELD EXPLORATION ETHODS This chapter presents discussions of the field exploration methods used in the study. Results of each field task are described in Chapter [. Eight. [ 6.1 Geologic Mapping and River Meander Analysis 6.1.1 Geologic Mapping [ Geologic field mapping was carried out to examine the exposed geologic units in the area of the postulated Millett fault to determine a correlatable stratigraphy, to map geologic structures that might be found, and specifically to search for any surface evidence of the postulated Millett fault. The mapping supplemented previous work for the Vogtle plant, work by Siple (1967) on the Savannah River Project l and a field trip guidebook of Huddlestun and Hetrick (1979). !
)
Reconnaissance mapping for this study covered approximately 500 square miles isee Figure 6-1) in a northeast-southwest trending zone that extends from five to ten miles on either side of the postulated fault. Due to the flat-lying nature of the formations and the lack of topographic relief, relatively few formations are exposed. It was found that roadcuts, ravines and the bluffs along the Savannah River contained the best exposures. The bluf fs adjacent to the postulated [ fault were examined in detail. [ ( 6-1
I The uppermost bedrock unit, the Hawthorn (Altamaha) Formation, is primarily fine-grained sand with lesser medium- to coarse-grained sand and gravel. The underlying Barnwell Group is dominantly loose to very poorly consolio, ted sands which is divided into two subunits, the Tobacco Road Sand and the Dry Branch Formation. The contact between the Hawthorn Formation and the Barnwell Group is exposed at many localities in the field area. Local exposures of the Lisbon Formation (Blue Bluff Member) occur along the bluf fs adjacent to the Savannah River. The field investigation began with an examination of 7-1/2 minute U.S. Geological Survey topographic quadrangles and low altitude photographs to determine the likely locations of exposures. Approximately 170 possible outcrops were located by this method, and this number was supplemented by additional roadcuts discovered enroute to these locations. This examination was aided by the field trip guidebook of Huddlestun and Hetrick (1979); the geologic contacts and terminology used in this report conform closely to their report. The map of the Savannah River Project completed by Siple (1967) and previous geologic mapping of the Vogtle plant and vicinity are also included on the geologic rap that accompanies this report (Figure 6-1). The Vogtle and SRP maps have been modified to conform to the terminology and unit definitions of Huddlestun. In particular, extensive outcrops of the McBean Formation shown on the SRP and Vogtle maps have been reclassified as part of the Barnwell Group. At the time of Siple's mapping, ambiguity existed as to the exact nature of the McBt..n and Barnwell Formations and his division of the units reduces the thickness 9
I of the Barnwell to 60 to 70 feet. This unit, as defined by Huddlestun, is now believed to have a thickness ranging from about 150 to 200 feet, l l The results of the geologic mapping are shown on Figure 6-1. The l mapping found no surface geomorphic or geologic features which could be associated with faulting. The depositional contact between the l Hawthorn and Barnwell units was found across the trace of the postulated fault with no detectable offset. This contact represents a l horizon with an age of about 25 million years. 6.1.2 Savannah River Meander Pattern Analysis According to the Open-File Report the position of the postulated l Millett fault was partially determined by using a change in channel geometry of the Savannah River. The Report (p. 23) positions the fault trace across the Savannah River at the point where the channel changes l from a " straight" to a " meandering" pattern (Figure 6-2). Although not cited as evidence for displacement, such a geomorphic expression of the fault trace may be construed as evidence for Quaternary fault I activity. As part of the Millett fault study, a geomorphic analysis of the Savannah River was conducted to determine possible causes for the change in channel geometry. It is concluded that although the trace of the postulated Millett fault coincides with the abrupt change in channel geometry, there is no geomorphic basis indicating that the r [ change is a result of fault displacement. I L From Augusta, Georgia to the Atlantic Ocean, the Savannah River flows r down a broad, alluviated valley. In the vicinity of the postulated L 6-3
1 i Millett fault, the river floodplain is well developed and averages 1.5 to 2 miles wide. This width is consistent across the postulated fault. Rivers flowing in such broad alluviated valleys adjust to many variables. The principal independent variables (variables over which the river has no control) include base level, discharge, bedrock geology and sediment load. The principal dependent variables (variables wnich a river will change in response to other changes) are channel width and depth, bed roughness, grain size of sediment load, velocity, channel slope and channel geometry. In the vicinity of the postulated lillett fault, most of these variables may be considered constant. Over such a local stretch in a large river, a change in the amount or grain size of sediment load, and hence bed roughness (Leopold, Wolman and Miller, 1964), sufficient to cause an abrupt change in channel geometry is not probable. Gaging station data from Augusta and Burtons Ferry Bridge (Section 7-7, Tables 7-13 and 7-15) indicate that there is no significant change in discharge. Sea level may be considered a constant base level (although alluvial fans constructed by tributary streams on the floodplain of the Savannah River may produce temporary base level changes) . Navigation charts (U.S. Army Corps of Engineers,1980) indicate that the river maintains a consistent average width of 250 to 300 f t and a thalweg (depth of deepest part of channel) depth of 12 to 15 feet. Because l l water velocity is a direct function of discharge, width and depth l (Leopold, Wolman and Miller ,1964) , it too is relatively constant. l l 6-4
A river may also adjust its channel to changes in slope and bedrock geology. The slope of the Savannah River floodplain increases from about 0.5 f t/ mile along the straight stretch of river upstream from the postulated fault trace, to about 0.7 f t/ mile along the meandering stretch downstream from the fault trace and could be interpreted as causing the change in channel pattern. This increase in slope coincident with a change from a straight to a meandering channel, however, is consistent with empirical observations by Leopold and Langbein (1966) and Schumm and Khan (1972) and is not an anomalous or unusual condition. These authors and Ritter (1979) conclude that the change in slope probably did not induce the change in pattern, but more likely is the result of the pattern change. Therefore, the difference in river slope is not the cause of the change in river meander pattern. The change in channel geometry of the Savannah River is therefore probably related to a change in local geology. Empirical observations by numerous investigators (Leopold and Langbein, 1966; Leopold, Wlman I and Miller, 1964; Schumm and Khan, 1972; Humphries and Hughes 1974; Keller, 1972), indicate that meanders develop when rivers carrying a relatively fine-grained bed load flow at low gradients and have cohesive but easily eroded banks. The Savannah River generally meets these requirements and should develop a stable meandering channel. nbservations of the river below Augusta indicate that meandering is common while straight reaches are rare and thus the straight reaches are probably an unstable condition. The thalweg of the river in fact, 6-5
does meander (Figure 6-2) and the straight reach may be in transition e from a straight to a meandering channel (Stage 2 or 3 of Keller, 1972). The important question to be considered, therefore, is not why does the river begin to meander below the trace of the postulated Millett fault but why is the river straight upstream of the fault? Meanders develop and propagate by eroding material from the concave or outer bank of the meander and depositing it downstream on the convex or inner bank of the meander (Leopold and Langbein,1966) . A prerequisite for meander development, there for e , is lateral erosion. In the straight reach of the Savannah River the river is eroding the I southeastern bank of the floodplain consisting of the resistant Blue Bluff marl member of the Lisbon Formation and overlying limestone and semi-consolidated sand and clay of the Barnwell group (Figure 6-1) . Subsurface projection of stratigraphic units also suggests that the base or the river is eroding the resistant marl. Difficulty in eroding this resistant bank probably consumed any preexisting meanders as the river laterally traversed the floodplain towards the southeastern bank. Channel scars on the floodplain adjacent to the straight river section are evident on 1:20,000 and 1:40,000 areal photography (section 7-4; illustrated on Figure 6-2) . Their arcuate shapes demonstrate that meandering has been a dominant fluvial process in this region during Holocene time. As the river crosses die postulated Millett fault, it gradually swings away from the resistant southeastern bank. In this area the 6-6 I .
I I resistant marl and limestone and overlying semi-consolidated sand and clay units have dipped beneath the river banks and channel so that the river is once again free to meander. Within the floodplain, where both banks consist of cohesive but easily eroded fine grained alluvium, the river again develops a meandering pattern. Channel scars in the floodplain cross the postulated fault trace with no evident I displacement. In summary, the local change in channel pattern from a straight to a meandering form appears to be related to local bedrock and not to regional or local changes in discharge, sediment load, base level, channel width or depth, velocity or channel slope. The stable channel pattern below Augusta appears to be meandering, the straight channels are anomalous, unstable features. Channel scars on the floodplain upstream from the postulated Millett fault suggest that although the river presently maintains a straight channel in this reach, it meandered across the floodplain in the IIolocene. The straight channel probably results from the resistance to erosion of the river channel bank and is not a product of Quaternary displacement on the postulated Millett fault. I It can not be definitely determined with the evidence available what caused the river to swing against the southeastern bank. The presence I of channel scars on the floodplain, however, suggests that the lateral migration is a natural evolutionary process of the river and that the present straight reach is a geologically temporary condition. I ~
I I 6.2 Core Drilling I Core drilling was used to define and to correlate the subsurface stratigraphy along two lines across the postulated Millett fault. The first line of holes was drilled along River Road in Georgia southeast of the Vogtle plant site. Eight holes were drilled over a distance of about eight miles. These holes supplement existing holes which had been drilled earlier to the northwest and southeast, as shown on Figure 6-3. The alignment of the holes is roughly perpendicular to the strike of the postulated fault and centered along its projected trace. The second series of holes was drilled to define the subsurface structure and stratigraphy between wells AL-66 and P5R in South Carolina. Wells AL-66 and PSR were used in the Open-File Report as a basis for postulating the Millett fault. Four holes were drilled, as shown on Figure 6-3. These holes are approximately five miles northeast and subparallel to those drilled in Georgia. The core drilling program was designed to determine whether faulting does occur in the area postulated, and if so, to define its location, extent, and capability, as defined by Nuclear Regulatory Commission criteria. The majority of the holes were drilled to a depth which would penetrate the Cretaceous materials defined as the A1 aquifer in the Open-File Report. Holes VG-7 and VG-8 of the Georgia series were drilled to the top of the kaolinitic clays at the base of the A 2 aquifer as defined in the Open-File Report. In South Carolina VSC-4 was drilled adjacent to well AL-66. This hole was drilled to a depth which would retrieve sediment samples from a horizon which the Open-File 6-8
I Report states is of Triassic age, based on cuttings from AL-66. VSC-4 was drilled to a total depth of 1,024 feet which exceeded the depth of AL-66 by over 200 feet. The adjacent holes PSR and AL-66 were geophysically logged to assist in correlation with the holes cored during this program. Section 6.3 discusses this program in more detail. The core drilling was performed by Law Engineering and Testing Company (LETCO) , and Alabama Power Company drill rigs and crews. A total of five drill rigs were used during the majority of the field period. Every effort was made to acquire continuous core samples with minimal core loss. Early in the program it was found that the loose sands of the Barnwell Group in the upper part of the holes were dif ficult to recover even though several coring methods were used. Therefore, the remaining core holes used split spoon sampling to a depth where the samplers could no longer be driven; at this point core drilling was begun. The core drilling used triple-tube NQ wireline equipment which provided core samples 1-7/8 inches in diameter. The drilling fluid consisted of clear water mixed with bentonite or a synthetic polymer mud (EZ mud) with barite and other additives used as required. During drilling it was found that the proper mud type, viscosity and density were critical for good core recovery, to prevent caving and to control artesian flow in the holes. I An experienced geologist was assigned to each drill rig to monitor drilling and log the core as it was retrieved. These personnel were 6-9
I I provided by Georgia Power Company and Bechtel. The geologist on each rig noted changes in drilling rate, character; mud color; loss or gain of fluid; and monitored cuttings in the mud. I The core was placed in strong wooden core boxes, with the run and recoveries noted on the box. Each box was then appropriately labelled and photographed once it was full. The core, which will be retained for permanent storage by Georgia Power Company was made available to the USGS, Georgia Geologic Survey, and Savannah River Project personnel for independent logging and sampling. All samples taken were catalogued and marked with a block in the core boxes. I The core hole locations were surveyed by a licensed land surveyor following the drilling. The holes were positioned horizontally and vertically to an accuracy of greater than 0.1 foot. Table 6-1 gives the Georgia State Grid coordinates and the ground surface elevation at the hole collar for all holes cored in this study. Logs of core holes drilled for this study are reproduced in Appendix D, Volume II. While this study was in progress, the USGS cored a hole near the Savannah River. The USGS kindly allowed G. Grainger of Southern Company Services to log the core. This log is also included I in Appendix D. I The results of the core drilling program are shown on the geologic section on Figures 8-1 through 8-3. Several distinct marker horizons and geologic formations were correlated in the core holes between AL-66
^
and PSR and between core holes and existing borings along a section
~
- I e-1e
I I from the Vogtle plant southeast for 20 miles, across the postulated fault. These sections clearly show no detectable fault offset of the marker horizons or geologic formations. These undisrupted horizons have approximate ages of from 40 through 65 million years. As postulated in the Open-File Report they should show vertical of fset of up to 140 feet. I 6.3 Downhole Geophysical Logging I Each core hole was logged using small diameter downhole geophysical logging equipment. The logs recorded were natural gamma ray, neutron, caliper, resistivity and spontaneous potential information. The downhole geophysical logging was conducted to assist in the correlation of stratigraphic units between drill holes. The logging was found to be very useful in correlation and in accurately defining geologic contacts. Nuclear logs were also run in cased wells PSR and AL-66. These holes are adjacent to those drilled in South Carolina and were presented as evidence for postulating the Millett fault. Geophysical correlation of these existing holes with the newly drilled core holes was significant in determining the existence and capability of the postulated fault. I The downhole geophysical logging was initially performed under contract with the Birdwell Division of Seismograph Service Corporation of Henderson, Kentucky. Drill holes VG-1, VG-2, VG-3 and the upper portion of VG-4 were logged by Birdwell. Due to the lengthy travel time from Kentucky and commitments in the petroleum industry, Birdwell could not continue their services and Law Engineering and Testing 6-11
I I Company, Geophysical Services of Marietta, Georgia, was contracted to continue the downhole geophysical logging. LE'ICO logged VG-4 af ter the hole was complete. The logs for VG-4 from Birdwell and LETCO were then compared to determine if any appreciable dif ferences existed using different types of equiprcent. The logs were found to be almost identical. As a result, LETCO logged the remaining holes in the program. An acoustic-velocity log was run in VSC-1 to determine if the velocities assumed in the seismic reflection survey along the river were correct. Additionally, the velocity log was used to aid in identifying the depth of materials having strong velocity contrasts. The dounhole logs were first compared from hole to hole independent of I the geologic correlations. This allowed an independent verification of the correlations to be made based on the core logs and a re-examination of any apparent conflicting data. I l The geophysical logs for surveys run as part of this study and those acquired from others and used in the sections are shown in Appendix E of Volume II. The correlation of geophysical logs are shown on Figures 8-4 Grough 8-7. These figures show dat logs define unique and diagnostic geophysical signatures which are readily correlatable with adjacent drill holes. Due to the unique signature of the geophysical logs and ease of correlation, the geophysical sections could be used alone to demonstrate the absence of significant vertical offset as proposed in the Open File Report. The geophysical correlations strongly support the stratigraphic correlations shown on Figures 8-1 and 8-2. I 6-12
I l l 6.4 observation Well Installation I I Following core drilling and geophysical logging, a ground water observation well was installed at each of the 12 core hole sites. In the case of VG-2 and VSC-4, caving in the core hole prevented installation of the well casing, and the well was installed in ancther hole drilled immediately adjacent. Six observation wells were constructed in the upper (Tertiary) aquifer and six were placed in the lower (Cretaceous) aquifer. The distribution of the wells is shown on Figure 6-3. i The wells are constructed as shown on Figure 6-4 to isolate the aquifer being monitored. The majority of the wells are constructed with a l 2-inch diameter stainless steel screen at the base of 2-inch diameter l black steel riser pipe. The screens are five feet in length and are continuous-slot, wire wound type (0.0 20-inch) manufactured by U.O.P. Johnson Company. Two wells in the South Carolina series of he s t (VSC-1 and VSC-4A) were constructed using four-inch diameter PVC screen (0.018-inch machine-cut slots) and riser pipe. The well screen on VSC-1 is five feet in length and the screen on VSC-4A is 15 feet in length. 1 I Cement grout was tremied through the drill rods to cement off the lower aquifer in those holes screened in the upper aquifer (Figure 6-4). Ground water in zones above the aquifer monitored was sealed off by placing cement grout in the 6- or 8-inch reamed portion of the hole. The grout was tremied to the base of the reamed portion of the hole 6-13
I I using 1-inch black plastic pipe. A steel ring plate welded to the outside of the riser pipe was used as a seal to prevent migration of the grout into the lower screened portion of the hole. In the holes completed with PVC casing, sand was placed as a seal at the base of the grouted section. Each observation well was purged of at least two well volumes either by hand bailing or by injection of compressed air following installation. The rate of recovery of each well was measured following purging. Rapid and complete recovery indicated that the wells were functional with good interconnection between the aquifer and the well. Four of the twelve wells did not recover rapidly - VG-1, VG-6, VG-7, and VSC-2
- and additional development work was attempted to improve the hydraulic response.
Well VG-1 was purged by air lift for a considerable time, but only slight improvement in the response rate resulted. The well is I apparently open to the aquifer zone, but is either restricted in some way or is screened in a lower permeability zone. Water level measurements in VG-1 indicate that it is functioning properly, but has a slower response time than other wells. It was found that well VSC-2 was plugged with silt. As a result of cleaning, it now responds effectively. Investigation of well VG-7 revealed that grout had entered the casing and filled the screened interval. Although the grout within the well was drilled out, it was necessary to use a small amount of explosive (Nipak) to fracture through the grout outside the well screen. The fracturing was successful, as evidenced by recovery 1 l s-14
I I after bailing. Considerable ef fort was made to clean out grout that had entered VG-6, but without success. I 6.5 River Reflection Survey An acoustical seismic reflection survey was performed in the Savannah River in May, 1982. This survey obtained information on subsurface reflecting horizons in the vicinity of the postulated Millett and Statesboro faults. When correlated with particular geologic interfaces, these reflections allow determination of geologic horizon continuity and charaterization of geologic structure. I The survey was conducted under Bechtel's direction by Harding Lawson Associates, a company with extensive marine geophysical experience. Dr. V. J. Henry, of the University of Georgia served as technical consultant for the survey. Dr. Henry has conducted previous geophysical work on the Savannah River and other rivers in the I southeast, and has also been involved with the of fshore fault study o'f I the Charleston, South Carolina area. The survey used three different energy sources. To obtain the highest resolution and deep penetration along approximately 19 miles of the Savannah River in the area of the postulated Millett fault and along about 10 miles near the postulated Statesboro fault. A precise record I of the depth to river bottom along the surveyed area was obtained using a Raytheon DE719 Fathometer. I I e-1e '
I I For shallow structure (from river bottom to approximately 150 feet below river bottom) an EG&G Uniboom and hydrophone eel (receiving array of eight elements) were used. The Uniboom system gave the highest resolution records (horizons mapped to an accuracy of 5 to 10 feet) but could penetrate to only about 150 feet. A single strong, continuous reflecting horizon was identified on the Uniboom records. I Intermediate depth structure (down to 350 feet below river bottom) was mapped using a 10-cubic-inch Exploration Equipment Research Inc. lEERI) air gun. Several reflecting horizons were identified on the 10-cubic-inch air gun survey. These horizons are mapped with a resolution of 10 to 20 feet. Finally, deep structure was investigated using a 20-cubic-inch EERI air gun. This large air gun survey identified a deep horizon at a depth of approximately 1,170 feet with a resolution of 30 to 50 feet. I Figure 6-5 shows the coverage of these seismic reflection surveys in relation to the postulated Millett and Statesboro faults. The postulated Millett fault coverage included 19-1/2 river miles of Uniboom survey,16-1/2 river miles of 10-cubic-inch air gun survey, and 5-1/4 river miles of 20-cubic-inch air gun survey. All of these I surveys were conducted so that the postulated fault location was bracketed on both the upstream and downstream sides. The equipment and methodology used in the reflection survey are discussed in more detail in Appendix F. I 6-16
( The location of the survey on a shallow, fast-moving river and the rigid time constraints required some special planning, particularly for the large air gun. In order to get both the air gun compressor and { survey vessel up the shallow river without running aground, a raf t containing the several-thousand-pound compressor was tied alongside the survey vessel. This configuration allowed three separate systems to be used (Uniboom,10-cubic-inch air gun, and 20-cubic-inch air gun) tehich enabled the best possible data to be obtained. There are two types of noise in the seismic reflection survey data: 1) that common to all reflection surveys (such as electric fluctuations in (- the recording equipment and multiple reflections), and 2) that arising from the complicated shallow river environment (such as spurious reflections from the irregular river channel margins, ( side reflections at or beyond the river banks, and onboard noise from the boat motors and compressor) . All noise sources have characteristic signatures. They do not prevent identification of several high quality reflection horizons along the survey lines. ( The seismic reflection studies did not identify either of the postulated faults. The results of the seismic reflection studies are discussed further in Section 8.1.5 and in Appendix F, where the Harding Lawson report is reproduced. ( ( 6.6 Water Well Survey During the period from May 3,1982 to June 26, 1982 a water well survey was conducted as part of the field investigations. The purpose of this ( 6-17
I lI survey was to accumulate a comprehensive hydrogeologic data base applicable to the evaluation of the postulated Millett fault, during a short time period. The resulting data base is referred to as a concurrent data base since all wells were measured nearly concurrently. The area selected for the survey consisted of 62 contiguous 7-1/2-minute and three 15-minute USGS tooographic quadrangle maps. These maps encompass a total area of approximately 4,400 square miles (Figure 6-5). Engineering and environmental personnel from Georgia Power Company performed the water well survey under the guidance and supervision of a Bechtel ground water geologist. Bechtel geologists processed and organized all incoming canvass data and performed a preliminary analysis before transmittal to the San Francisco of fice for further !g IE evaluation. The primary tasks assigned to the ground water l investigating team are summarized as fellows: a) Canvass as many wells as possible within the study area, with l particular emphasis on municipal, industrial, and irrigation wells. b) Perform a preliminary evaluation of each well for applicability, coherence of data, etc. lI c) Summarize canvass data on tabulation sheets and assign a discrete modeling code number for each well. lI 6-18
Il d) Plot each well, its modeling code and ground water elevation on control copies of quadrangle maps. e) Transmit data to the office for final evaluation and classification of wells by aquifer systems. I 6.6.1 Schedule of Field Work To minimize the impact of dif ferences in ground water levels related to time, it was considered essential to complete the survey in the shortest period practicable. For this reason, the large area of the survey was covered in three stages, beginning in the immediate vicinity of the postulated fault zone and then progressively expanding to the maximum area possible. The first stage, in the immediate vicinity of the postulated fault, was designated as " priority one". It consisted of 35, 7-1/2-minute quadrangle sheets covering an area of approximately 2,100 square miles. A total of 620 wells were investigated in this area. I Data obtained during stage two of the survey encompassed an area designated as " priority two" which surrounds the priority one area. This section contained 27, 7-1/2-minute and three 15-minute quadrangle sheets covering an area of approximately 2,300 square mi.Les. A total of 93 wells were covered in this area. The priority one and two boundaries are shown in Figure 6-6. I II lg e-1g o
r L Sta.qe three of the survey consisted of a screening and investigation of well information obtained from Georgia and South Carolina state records and USGS well tabulations. During this stage 173 additional wells were L located and recorded. In summation, a total of 886 wells were measured within zu area covering 4,400 square miles. Figure 6-7 shows the locations of all wells included in the field measurement program. t The majority of the wells were located in the field by the canvass crews. Coordinate locations and surface elevations not surveyed or supplied by a reliable outside source were estimated. Low altitude aerial photographs obtained from the U.S. Department of Agriculture were used as a supplemental aid in well location. Field data were obtained from a combination of actual measurements and owner-supplied information, and were recorded on a water well data form. All wells were measured under static conditions whenever possible. If a pump was running, an attempt was made to shut the pump of f and allow the well to recover for one hour before any measurements were taken. I L Wa ter level measurements were made with one of two instruments: 1) a I L battery operated water level indicator, or 2) a steel surveyor's tape dusted with blue chalk to aid in making the water surface mark readily visible. Measurements deemed questionable due to condensation on the f sides of the well or due to possible obstructions within the well were L so noted in the remarks section of the form. I ~ s 6-20 ? l .
l l 1 l l l The total depth of the well was measured whenever possible with the j surveyors tape with an attached weight. Owner-reported depths were recorded when the wells were too deep to measure or were blocked by a pump. 1 Af ter the field well canvass crew had finished surveying a complete i quadrangle sheet, the water well data forms and the quadrangle sheet I showing the well locations were returned to the field office for review f and preliminary evaluation. l 6.6.2 Well Data Reduction I The field evaluation of the survey data began by screening the well f data sheets and deleting those wells which were obviously unusable, e.g., shallow hand-dug wells, wells for which little information was available, and artesian wells that were flowing at the time of the survey. No pressure readings of artesian wells were made during this survey. The data were recorded on a summary sheet prepared for each quadrangle. l I l A preliminary attempt was made to determine which aquifer was penetrated by each well. The geologic section included in the l Open-File Report was the primary source of information for this purpose. It was assumed that the section was representative of aquifer { elevations over a fairly broad area. Each well was spotted at its I L, corresponding location on the section and the depth of penetration into E 6-21
I . the aquifers was estimated. Geophysical and lithologic logs were utilized whenever available. I The wells were plotted on quadrangle sheets, with water level elevations shown for each of the two aquifers penetrated. The quadrangle sheets, summary sheets and water well data sheets were then sent to the San Francisco of fice for final evaluation. lI 6.6.3 Supplemental Data To provide a control data base for fluctuations in water levels during the period of the survey, water levels of selected wells were monitored weekly from May 21 to June 21, 1982, and hydrographs were drawn. These wells were ET-1-1, ET-1-5, IDL-4-3, and Vogtle observation well l no. 32 (VEGP No. 32) . Well locations are shown on Figure 7-1 and hydrographs are on Figure 6-8. The purpose of this monitoring program was to observe weekly fluctuations in order to determine the ef fect on water levels of external conditions such as weather and irrigation during the survey period. These control wells were chosen according to l their depth of penetration into the aquifers and their accessibility. Well IDL-4-3 penetrates the lower aquifer, and the remaining wells l (ET-1-1, ET-1-5 and VEGP No. 3 2) penetrate the upper aquifer. !I Water level fluctuations were extracted from the hydrograph data base and plotted on Figure 6-8. The 4.7 foot maximum fluctuation shown at
- ET-1-1 is attributed to pumping of this well for irrigation purposes.
The 5.0 foot fluctuation at ET-1-5 is also attributed to pumping. The i g 6-22 3
L [ relatively low elevation of ground water at VEGP No. 32 is attributed to the proximity of the well to the Savannah River; in this area, the marl confining layer does not exist and the upper aquifer is discharging to the river. Additional error is possible due to the interpolation of ground surface elevation from topographic maps. Taking these variables into account, the hydrographs indicate that the maximum probable error introduced in the water level readings taken for the duration of the program is about five feet. It pumping of the wells is excluded from consideration, the probable error factor appears to be less than two feet. In addition to the wells measured by the Georgia Power well canvass crews, wells on the Savannah River Plant property were measured by SRP staff members. Water level measurements were also taken from the newly drilled observation holes in Georgia and South Carolina and used in the final analysis of the hydrogeologic data (refer to Section 6.6) . These data were sent to the San Francisco of fice to supplement the data collected by Georgia Power and Bechtel personnel. The concurrent data base { compiled during this intensive effort was used to prepare potentiometric surface maps for both the lower and upper aquifers, and to evaluate the possibility of a ground water barrier through modeling. Evaluation of the well data is discussed in Section 7.8. A discussion of water level contours is presented in Section 7.8.1. Section 7.8.2 F L describes the use of the collected data for computer modeling studies. L 6-23
- uns -
iman - --- umas - - -- Postulated Millett Fault Study TABLE 6-1 Vogtle Electric Generating Station DRILL HOLE
SUMMARY
LOCATION ANGLE DEPTH VERTICAL ELEVATION DRILL BEARING GROUND ELEVATION FROM - ---- DEPTH BOTTOM HOLE ELEVATION NORTH EAST HORIZONTAL LENGTH TOP OF N TOP OF m OF HOLE Georgia Stat.e Grid (Pr. ) (FT.) (FT. ) (FT. ) (FT.) VC-1 1120358.26 660009.14 90 - 156.6 565.0 156.3 0.3 -408.4 VG-2 1122608.99 650596.85 90 - 253.1 618.0 250.0 3.0 -364.9 VG-3 1121183.52 655725.83 90 - 165.7 574.9 163.0 2.0 -409.2 VG-4 1124o29.41 644971.51 90 - 150.3 554.4 129.0 21.3 -404.1 VG-5 1116669.12 665818.68 90 94.5 502.0 112.0 -25.0 -407.5 VG-6 1110896.34 669643.15 90 - 217.1 620.0 237.5 -20.0 -402.9 VG-7 1127245.60 640322.37 90 - 250.6 392.0 225.0 -8.3 -141.4 VG-8 1104446.34 678744.09 90c - 103.7 355.4 143.6 -39.9 -240.8 l VSC-1 1134867.04 679423.71 90 - 219.0 620.0 186.5 34.5 -401.0 VSC-2 1141512.71 673492.62 90 - 201.7 600.0 152.0 49.7 -398.3 VSC-3 1138356.84 676254.55 90 - 170.3 570.0 134.0 36.3 -399.7 VSC-4 1130590.27 683271.46 SD 156.7 1024.0 137.9 18.8 -867.3 Estimated Coordinates P5R 1145300 671700 90 - 208.0 1250.0 --157 51 -1042.1 AL-66 1133400 684250 90 - 202.2 800.0 ~ 186 16 -597.8 AL-317 1128800 672300 90 - 97.1 230.0 89.0 8.1 -132.9
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FIGURE 6-8
I I 7.0 OFFICE STUDIES In conjunction with the field investigations described in Chapter 6, a number of studies and analyses were also performed in the office. The data for these studies were derived from published and unpublished sources, and from the field investigations. This chapter discusses the office studies and the sources of data for each. Chapter 8 discusses the results of the studies. During the office studies a substantial amount of literature and drill hole data were assembled and evaluated. Much of this information did
- I not ultimately contribute directly to the resolution of the Millett fault issue, but did provide an extensive data base for understanding the geology of the Coastal Plain. For this reason it was decided to include as appendices listings of information which could also prove useful to others conducting similar studies in the region. An
.l= annotated bibliography of references procured and reviewed in the literature search is included as Appendix A, and a complete tabulation of collected data pertaining to drill holes and water wells throughout the area is in Appendix C. l l 7.1 Literature Search and Review A literature search was conducted as part of an effort to compile a broad base of background information relative to the geology of the southeastern Atlantic Coastal Plain. This search consisted of four 7-1 I
I parts, each discussed separately below: computer searches; thesis searches; bibliographic searches; and identification of appropriate published reports from agencies and facilities in the area of study. The material obtained through the various searches included not only geologic, seiemologic, and hydrologic articles, reports, and theses, but also geologic maps and geophysical surveys. 7.1.1 Searches 7.1.1.1 Computer Search The computer search involved the use of COMPENDEX and GEOEF. The data base for COMPENDEX is The Engineering Index which covers materials published in the engineering field from 1970 to the present. GEOE F, II the data base of the American Geological Institute, covers technical l literature on geology and geophysics. GEOEF corresponds to the I following printed publications: Bibliography and Index of North American Geology; Bibliography of Theses in Geology; Geophysical Abstracts; and the Bibliography and Index of Geology. This data base 1 l currently covers the time period from 1961 to the present. 7.1.1.2 Thesis Search l In addition to those theses listed in GEOEF, further listings were
- found through University Microfilm (Ann Arbor), and bibliographies and
, reference lists in the published literature. University libraries and I 7-2
I geology departments revealed a number of additional theses not yet listed elsewhere. Theses were obtained from 13 universities, most of which are in the southeastern United States. 7.1.1.3 Bibliographic Search Beginning with the Open-File Report, the bibliographies and reference lists of published reports and articles under review were used to supplement the listings obtained through computer searches. The Bibliography of North American Geology, covering a period from 1900 to 1960, was also reviewed for pertinent literature. 7.1.1.4 Published Reports Numerous reports dealing with the local geology and hydrology were obtained from state and federal geological surveys and from local facilities such as Vogtle Electric Generating Plant, the Savannah River Plant, and Barnwell Nuclear Fuel Plant. ig 3 7.1.1.5 Unpublished Geologic Data Several unpublished geologic reports and maps were made available for this study to augment the existing published information. In addition l to the unpublished data, discussions regarding the general geology of the study area were held with university professors and other experts in the field of southeastern coastal geology. Assistance in compiling the stratigraphic correlation chart shown in Figure 4-3 was provided by lI 7-3 lg
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Dr. Paul Huddlestun of the Georgia Geologic Survey. Dr. Huddlestun also provided guidance in identifying formational boundaries during e coring operations carried out specifically for this study. 7.1.2 Review 'I All material obtained through the various searches was first entered intc a master reference list which was made available to all those involved in the Millett fault studies. Each article, report, or map was then reviewed and its contents discussed in a brief paragraph. The resulting annotated bibliography is included in this report as Appendix A. With the exception of the Open-File Report, none of the reviewed literature suggested any tectonic offset of Tertiary units in the vicinity of the postulated Millett fault. 7.2 Acquisition and Review of Existing Field Data Numerous water wells and exploratory borings have been drilled in the area of study. Information concerning the geology and hydrogeology of the area exists in the form of records produced during and af ter drilling of these wells. Both the quality and quantity of data varies from well to well and may include such items as drill logs, geophysical logs, well construction reports, water level, water quality and pumping 1 test reports. The specific types of information available for each i l l drill hole are indicated on Table C-1 of Appendix C. Drill holes for which adequate location information is available are plotted on Figure .I 7-1, although some fall outside the area covered by the map. The l j 1 I 7-4
I primary sources of drill hole data were state and federal geological surveys, state and county water resources agencies, and local plant sites such as the VEGP, SRP and BNFP. Although very little petroleum exploration has taken place in the study area, a search was made for existing geologic and geophysical data resulting from petroleum exploration activities. Contact with the Georgia Geologic Survey revealed six petroleum exploration wells within 40 miles of the postulated Millett fault (Table 7-1) , but no data on these wells vere found during this study. The drill hole data were used principally to help define the geologic structure and stratigraphy of the area, and to identify aquifer elevations. For details regarding the individual sources of data and the nature of the information provided by each, refer to Table C-1, Appendix C. Several types of geophysical data are available which provide subsurface geologic information for the study area. Types of data r available include both reflection and refraction seismic data, aeromagnetic data, and gravity data. The information consists primarily of USGS and university studies, seismic surveys by geophysical exploration companies, and seismic lines and gravity surveys run at SRP, available through the Oak Ridge, Tennessee repository. Contact with numerous geophysical and petroleum companies produced very little information (Table 7-2). Contact with seismic 1 brokerage firms, which have geophysical data available for sale, did i 1 1 not reveal any previously unknown data (Table 7-3) . l l 7-5
I Review of available geophysical studies performed by others is discussed further in Section 7.3. I In an ef fort to identify any surface expression of the postulated Millett fault, three types of remote sensing data were acquired during the course of this study. These include: Landsat satellite imagery, NASA U-2 high-altitude photography, and U.S. Department of Agriculture low-altitude black-and-white aerial phdtographs. These particular I images and photographs were produced over a broad span of years and were choser. to represent different seasons and sun illumination angles so that any trace of the postulated fault would be more readily apparent. A detailed discussion of the remote sensing study is presented in Section 7.4. 7.3 Review of Existing Geophysical Studies W A comprehensive attempt was made to collect and evaluate available geophysical data relevant to the study of the postulated Millett and Statesboro faults. The specific geophysical data found include seismic, gravity and magnetic surveys. 7.3.1 Seismic Surveys Two reflection seismic surveys pertinent to the postulated Millett I fault study were found. These were a conventional explosive source survey conducted on the Savannah River Plant property (see Figure 7-2) I 7-6
and a proprietary Vibroseis survey crossing the postulated fault near Sardis, Georgia (see Figure 6-5) . The Vibroseis survey was conducted in September 1981 and released through Seisdata Services Inc. The survey data acquisition parameters included: I 96 channel, 24 fold CDP, 220 foot geophone group spacing, 440 foot vibrator point spacing, split spread of 11,000-600-600-11,000 feet, and source sweep of 48-12 Hz. Because the survey was designed to investigate deep basement structure, the shallowest identifiable horizon is the top of the Triassic crystalline basement where a strong continuous reflector crosses the postulated fault trace (shot point 4875) with no indication of fault of fset. The depth of this reflector is approximately 475 milliseconds or -1175 feet elevation (assuming a velocity of 6000 feet per second and an elevation of shot point 4875 as
+250 feet) . The top of Triassic reflector starts to loose coherence at shot point 4885 most probably due to processing problems. If this loss of coherence interpreted as offset, the maximum displacement is on the order of several tens of feet.
The reflection survey of the Savannah River Plant site run by Seismograph Service Corporation (SSC) was conducted in 1971 to determine the structural characteristics of the bedrock surface, map the Triassic basins, and to identify any possible faulting. The study used standard geophone split spreads of 900-75-75-900 feet, buried explosive shot holes spaced 900 feet apart, digital recording of the data, standard numerical postprocessing of the data, and expert interpretation of the final digital replay sections. The final I ,-,
I interpretation was correlated with a number of logged test holes and these results were displayed as structural cross sections. General record quality was labeled fair to poor by SSC. The results interpreted by SSC which are relevant to the postulated Millett f ault include: no identification of faulting of the Cretaceous horizons found by SSC; elevation of the top of Triassic varying frc,sa -770 feet to -1,160 feet; gentle southeastward dip of approximately 50 feet per mile; and minor normal faulting in the Triassic with displacements generally less than ;10 feet. The survey coverage region, shot lines, Also shown and interpreted Triar nic faults are shown in Figure 7-2. in this figure are t'ie interpreted amounts of displacement of each fault and the location of the postulated Millett fault. The replay section record for line 7 has been reanalyzed for this study since it crosses the postulated Millett fault and Is the closest shot line to the Savannah River acoustic reflection survey described in Section 6.5. Because of the shot method and analysis technique used, no useful information on the structure above the Triassic in line 7 is available, although some Cretaceous horizone have been identified on other lines. Line 7 does suggest fault of fset of the top Triassic (depth 1,245 feet .g g or -1,045 elevation) in the vicinity of the postulated Millett fault at
- the SRP site but with only one-half the SSC interpreted of fset l
(approximately 50 feet instead of the slightly greater than 100 feet) . The discrepancy for the interpreted of fset is believed to be the over-emphasis by SSC of the near-fault drag phenomenon. When the of fset is measured af ter eliminating the drag component, about 50 feet of of fset remains. The independently conducted acoustic reflection Savannah River survey, the Savannah River Plant explosion reflection 7-8
survey, and the Seisdata Vibroseis Line 7 all show the Triassic basin reflector to be at a consistent depth. Various interpretations of this I reflector are possible. If the undulations on the river reflection survey and the break-up of the reflector on the Vibroseis line are interpreted in a conservative sense as fault of fset, all three surveys indicate approximately the same amount of offset. 7.3.2 Gravity Surveys Two gravity surveys were found that had coverage of the postulated Millett fault zone. The first is a composite of the simple Bouguer anomaly maps for Georgia and South Carolina (Long and Champion, 1977) and the second is a special study done on the Savannah River Plant site l (Birdwell, 1972). The simple Bouguer anomaly map of Georgia and South Carolina has l l contour intervals of five and ten milligals based on station spacing of 2.5 to 3.7 5 miles (Popenoe and Zietz,1977) . The patterns on gravity , i i maps of this type indicata density variations associated with lI lithologic changes in the crust. The rocks involved in the Appalachian i orogeny including rocks beneath the Atlantic Coastal Plain exhibit anomalies that are elongated in the northeast-southwest direction. This type of anomaly elongation is strongly evident in the simple l Bouguer anomaly map of Georgia and South Carolina. Most of these l anomalies are believed to be produced by deep (greater than 1,000 feet depth), intra-basement crustal sources since these rocks have the greatest density contrast. The wide station spacing used does not I 7-, g
I allow the upper structure to be resolved so that no information on the shallow structure (less than 1,000 feet depth) of the postulated Millett fault zone is available. I The sinple Bouguer anomaly survey of the Savannah River Plant (Bitdwell,1372', witn about a quarter-mile station spacing and 1 mgal contour interval, shows more detailed information on the crustal structure in the vicinity of the postulated Millett fault. The result of this survey is a gravity contour map that is elevation corrected (including average density) and latitude corrected. The occurrence of high density-type rock about three miles northwest of the postulated Millett fault trace is indicative of of fset in the Triassic basin beneath the pre-late Cretaceous unconformity. Some faults located by the gravity survey correlate with those located by the seismic reflection surveys, while some modeled faults only correlate with the , magnetic survey which was run over the same vicinity. As a result of the method used (e.g. quarter-mile station spacing) all the interpreted structures are at depths below the Cretaceous-Triassic boundary. Cored
- holes on the Savannah River Plant site indicate high angle foliation in the metamorphosed sediments forming the basement rocks. This would suggest that some of the gravity inflections could be representative of I
minor changes in rock density instead of faulting. Thus, the eroded l top o e Triassic basin sediments may have a more uniform surface than that inferred by the fault interpretation, and the of fset of the Triassic basin " faults" in the vicinity of the postulated Millett fault would be less or non-existent. I I 7-10
I l 7.3.3 Magnetic Surveys I Magnetic surveys conducted in the vicinity of the postulated Millett fault include a vertical component magnetic survey of the Savannah River Plant (Birdwell, 1972) and various aeromagnetic surveys (Pe t ty , and others,1965; Geodata International,1975a and 1975b; and Zietz and Gilbert, 1980). The vertical component field survey of the Savannah River Plant was conducted to provide data for use in model studies of the metamorphic rocks underlying the Triassic basin. The principal uses of this magnetic survey are to estimate the depth of sedimentary basins and to locate faults. l B The Savannah River Plant survey was conducted using two vertical t I magnetometers which could be read to an accuracy of about 2.5 gammas and a station spacir.3 of one-quarter mile. The magnetic data indicate I a change of rock type in the crystalline basement about three miles northwest of the postulated Millett fault trace. To the south, several i g i 5 other faults in the basement are suggested by the magnetic data. It should be noted that recovered cores from the vicinity show a high angle schistose foliation of the basement rocks. This high angle foliation suggests that metamorphosed sediments have been tilted (Birdwell,1972) so that magnetic inflections could be representative of minor changes in magnetic content of the rocks in the metamorphic section instead of faulting. As a result, the basin may have a much more uniform basement surface than suggested by the fault E 7-11
I interpretations. Because of the lack of magnetic signature of the Cretaceous and younger sediments and the wide station spacing of one-quarter mile, no information on Cretaceous or younger faulting can be obtained from the Savannah River Plant magnetic survey. , The patterns shown on the aeromagnetic maps reflect structure and lithology in the crystalline and metamorphic rocks of the postulated fault region. The magnetic contribution of the Coastal Plain sedimentary rocks is negligible. These sedimentary rocks do increase I l 5 the distance to the magnetic basement rocks. The effect of the l increased distance is to decrease resolution of shallow anomalies, l smooth and merge anomalies from deeper sources, and lower the amplitude and gradient of the shallow anomalies. The nonmagnetic rocks of the Triassic Dunbarton Basin are believed to be related to a deep, smooth, northeast-trending aeromagnetic low indicated on the various aeromagnetic surveys. 7.4 Remote Sensing l 7.4.1 Imagery and Photography Employed in the Study j I Imagery and photography of varying scales were used to search for evidence of faulting in the area of the postulated Millett fault.
'Ihree main types of imagery, collected by different sensor systems, were employed.
I I 7-12
1 I l (1) Iow-altitude aerial photography at scales of 1:20,000 and 1:40,000, (2) High-altitude (approx. 65,000 feet) NASA U-2 oblique false color infrared photography, and (3) Landsat satellite imagery including multispectral scanner (MSS) and I return beam vidicon (RBV) sensor data. The MSS data are at a scale of 1:3,369,000 and the RBV at a scale of 1:500,000. The areas covered by the various types of imagery are shown on Figure 7-3. The area examined includes all of the 47 mile length suggested in the Open-File Report as the location of the postulated Millett fault. Low-altitude panchromatic black-and-white photographs taken in May, 1951 and December,1969 at a scale of 1:20,000 were assembled into mosaics, as shown on Plates 1 and 2. The location of the postulated fault has been indicated on these plates as a zone between the dotted lines. An examination of this imagery revealed no surface evidence of faulting. Similarly, the oblique U-2 false color photography taken on May 1, 1969 was found to show no surface indications of faulting. This oblique photograph, shown on Plate 3, measures energy reflected from the surface of the earth in the visible and photographic infrared portions of the light spectrum. i l Seven Landsat satellite images covering two seasonal conditions and different sun illumination angles were examined. Imagery from different seasons of ten reveal any features temporarily obscured by surface cover at other times of the year. Imagery taken with varying I 7-13
I sun angles, especially low sun angles, was used as shadows are useful in enhancing lineaments and hence aiding in their detection. The six Landsat digital images and an RBV subscene examined for the study area are as follows: I Landsat MSS Imagery I December 1, 1973 Scene #1496-15301 Sun Elevation 29' February 11, 1974 Scene 41568-1528100 Sun Elevation 33' June 17, 1974 Scene 41694-1525200 Sun Elevation 61* January 23, 1976 Scene #2366-1518300 Sun Elevation 27' June 6, 1976 Scene #5414-1448000 Sun Elevation 53' January 17, 1977 Scene 12726-1507200 Sun Elevation 25* I Landsat RBV Imagery
- I November 30, 1980 Scene #83100ll5085XC I
I ; I ; I 7-14
(- ' 7.4.2 Digital Processing and Image Analysis Techniques ( These satellite images, stored as digital data on computer compatible tapes, were examined on Bechtel's image processor, Model-70, built by International Imaging Systems, Sunnyvale, California. { Digital enhancement procedures designed to enhance linear features were employed. Plates 4 and 5 show the satellite images over the area of the postulated Millett fault in Georgia and South Carolina. The two digital images, a summer scene (June 6,1976) and a winter scene (February 11, 1974) were contrast stretched by the image processor to enhance surface features. This operation expands the digital range of the data by converting it from 7-bits to 8-bits utilizing the full f dynamic range of 256 values. When the resultant digital data are displayed on the image processor the visual effect is to increase the contrast between adjacent pixels and her.ce the features of interest. I J [ The enhanced subscenes were then photographed directly from the 9 television monitor using standard 35 mm equipment and assembled into a f mosaic for study. The enhanced subscenes have not been geometrically corrected; hence the overall geometry of the mosaic is not considered a (- standard projection. 1 1 The imagery and photography were examined closely to identify linear features and isolate the lineaments that might represent the surface expression of a geologic structure. The procedure employed was to first identify lineaments on the imagery, then eliminate all of those lineaments having an obviously non-geologic basis, such as roads,
~
7-15 1 _m ____ _ , , _ _ _ _ _ _ , _ _ _ _ _ . . _ . -
I transmission lines, property lines and other cultural features. The remaining lineaments, tPose which could not be immediately attributed to cultural origins, were subjected to further study. I Professor R.J.P. Lyon of Stanford University, Remote Sensing Laboratory provided assistance in designing the study and interpreting the imagery. 7.4.3 Results of Remote Sensing Studies Clear mylar overlays were placed over each mosaic which were then studied individually by geologiste and remote-sensing specialists and the lineaments marked on the mylars. For the summer image taken on June 6, 1976, 168 lineaments were identified; for the winter image taken on February 2, 1974, 136 lineaments were identified. The lineaments are shown on Figures 7-4 and 7-5. Each lineament was then individually assessed and classified according to six criteria, as l shown in Table 7-4. These criteria were further grouped into two major categories representing (1) those lineaments with a cultural origin and l (2) those with a geomorphic origin. These two categories appear in Figures 7-4 and 7-5 where the lineaments colored in olack indicate the l l cultural features, and those in red and blue indicate the geomorphic features. t I 7.4.3.1 Lineaments of Cultural origin The majority of the lineaments were found to be caused by the optical i I alignment of field boundaries and some stream sections and hence were classified as having a cultural origin. The low-altitude 1:20,000 7-16
I aerial photography and selected field observations confirm the origins of these optical lineations on the satellite imagery. A smaller number of the cultural lineaments was attributable to roaoc which of ten parallel agricultural fields. 7.4.3.2 Lineaments of Geomorphic Origin A high percentage of the lineaments not associated with cultural features are predominantly attributable to the alignment of stream and river sections. These lineaments appear in blue on Figures 7-4 and 7-5. Lineaments identified in red on Figures 7-4 and 7-5, and individually identified by letters, are predominantly associated with floodplain features and karst topography. Lineaments Associated with Flood-Plain Margins I Comparison of Figures 7-4 and 7-5 indicates that many of the lineaments l occur along the flood plain margins of streams and rivers the Lanosat image of June 6, 1976 (Figure 7-5), while fewer are seen on the image taken February ll, 1974 (Figure 7-4). These lineaments are labelled A through I and M on Figure 7.5 and B1, C1 and X on Figure 7-4. Using Figure 7-4, it is possible to gain a better understanding of the margins of the river and stream floodplains, and the neighboring agricultural fields than in the image shown in Figure 7-5. Concurrent use of the two mosaics allows the interpreter to accurately identify the river floodplains and the associated depositional features such as meander scars and paleochannels. I 7-17
Lineaments Associated with Drainage Basin Divide Two geomorphic lineaments near the Vogtle plant site (labelled J and K on Figure 7-5) are present on the June 6,1976 image. Field observation of these lineaments, together with an examination of the other mosaic in Figure 7-4 reveal that these linear features represent the drainage divide of the drainage basin in which the Vogtle plant is located. I Lineaments of Geomorphic Origin near Ellison's Landing One lineament close to the postulated Millett fault and intersecting it near Ellison's Landing northeast of Girard was examined in the field. This lineament is labelled V on Figure 7-4 and L and L1 on Figure 7-5. This lineament is also identified by the green dashed line on Plates 4 and 5. It is approximately 13 miles in length. From the satellite imagery a number of stream branches and agricultural fields appear to be aligned. Additionally, Brier Creek deviates from its general northwest-sou*.heast direction to flow north along the linear feature for a distance of 0.3 miles before resuming its southeasterly flow direction. I The results of the field investigation are: (1) No scarps or other evidence of fault activity were found along the I I <2> 8 81 t< e 81 e 111 t ei e it < 1 1 e- ie8 < side of the linear feature, but there are no outcrops. I 7-18
I (3) The deviation in the flow direction of Brier Creek is most likely caused by chert deposits varying in size from 1-inch to 1-1/2-foot diameter boulders found in the stream bank deposits. The areal extent of these deposits is not known. The stream ir less able to erode these hard deposits than the surtounding material and so is diverted in a northerly direction around this obstruction before proceeding to the southeast. I (4 ) The dark tones seen on the summer image east of the linear feature contrast with the distinctive white and red color signatures on the west side. These differences in color due to variations in ground cover contribute to the visual impression of a linear feature. I No evidence for faulting is present along the trace of this linear feature. I Lineaments Associated with Previous Quaternary Sea-Level Locations A number of small geomorphic linear features identified in the southeasterly section of the imagery are possibly old ' strand lines' related to previous Quaternary stands of the Atlantic Ocean and are considered non-structural in origin. These lineaments are labelled R and S on Figure 7-4 and 0, P and Q on Figure 7-5. I Linsaments Associated with Karst Topography. The geomorphic lineaments identified as karst features are caused by I the apparent alignment of circular ponds and agricultural fields in 7-19
I l this area. These lineaments are located mainly in the eastern half of both images on the topographic highs and are labelled T, U, Z, Y, W and Al on Figure 7-4 and N and N1 on Figure 7-5. The karst features were easily identified by enhancing the thermal bands on the image processor to preferentially display water bodies. There is no common orientation direction for these karst associated lineaments. The satellite imagery shows that sections of the Savannah River and other major consequent drainage lines parallel one another and change flow direction from southeasterly to a more southerly direction. This general change may be caused by a change in regional dip as discussed in Herrick and Vorhis (1963). I The conclusion drawn from the remote sensing studies is that the ,I lineations on the satellite imagery are unrelated to faulting. They l ( are confidently explained as alignments of field boundaries, stream sections, karst features and fluvial geomorphic features not l structurally controlled by faulting. None of the satellite imagery and phctography examined showed any evidence of surface expression of the postulated Millett fault. i 7.5 Lithologic Analyses 1 Lithologic analyses were performed on water well cuttings from AL-66 and AL-40 and on core samples from VSC and VC holes to supplement stratigraphic studies on the postulated Millett fault. The main purpose of these studies was to determine if Triassic rocks were I
'~"
I
I ; penetrated by holes in South Carolina and to verify stratigraphic correlations based on field evaluation of core from VSC and VG holes. Lithologic analyses inc,;ded petrographic examination, x-ray diffraction of both bulk and clay size fractions of submitted samples, and heavy mineral analyses. The sample locations used in the analysis are shown on Figures 7-6 and 7-7. Petrographic examinations were performed at Bechtel and splits of the collected samples were sent to Dr. R. C. Reynolds and Dr. R. Parnell of I Dartmouth University, and Dr. Ralph E. Grim of the University of Illinois for x-ray diffraction analyses. Heavy mineral analyses were performed by Dr. J. Thomas of Reservoirs, Inc., Denver, Colorado. 7.5.1 Lithologic Analyses of Samples from Water Wells AL-66, AL-40 and Core Hole VSC-4 The Open File Report states that upthrown Triassic rocks have been encountered in water well AL-66 at about -500 feet elevation. In order to investigate this possibility, samples were analyzed from above and below the postulated contact in AL-66, AL-40 and in nearby VSC-4. These samples were submitted for lithologic analyses in order to; l) compare lateral lithologic variability of samples collected from similar elevations in each hole, and 2) compare samples collected from below the postulated Triassic contact with the known Triassic-Jurassic I rocks from DRB 10 (Marine, 1976b). I Samples collected from AL-66 and AL-40 were taken from the same stratigraphic horizons, but their lithologic characteristics dif fer. This is probably due to the treatment of the samples af ter they were 7-21
I originally collected by the well driller. Samples from AL-40 were washed, while AL-66 samples were not. The washing process probably removed any clayey material that was originally in the samples from AL-40. Because the fine fraction of AL-40 was removed, only the coarse fraction was used for comparison with other samples. 7.5.1.1 Lithology of Water Well Cuttings From AL-66 and AL-40 Samples collected fron AL-66 were submitted for petrographic examination, heavy mineral and x-ray diffraction analyses (Table 7-5 and Figure 7-8). Samples collected from AL-40 were submitted for l petrographic examination only (Table 7-5). Petrographic examination of AL-66-1 (-468 to -478 feet elevation) and AL-66-2 (-558 to -568 feet elevation) , revealed them to be clayey quartz sands, based on the predominance of quartz within a matrix of
= fine-grained quartz, clay, and muscovite / sericite. The matrices of both samples are heavily stained by hematite and probably limonite. A few shale fragments and patches of kaolinite are present in AL-66-2.
Bulk x-ray diffraction studies support the results obtained from petrographic analyses by indicating a predominance of quartz, moderate amounts of clay, and minor to trace amounts of hematite. Because these lg ig water well samples are unwashed, a certain amount of drilling mud may be present as a contaminant. Therefore, discrete clay clasts were carefully extracted from the samples and analyzed. In most cases, these clay clasts consisted almost entirely of kaolinite with minor I 7-22
amounts of smectite, indicating that they were derived from local units and are not contaminants (Appendix I) . The clay matrix was also analyzed for its clay content and was found to consist predominantly of kaolinite. The heavy mineral assemblages in AL-66-2 consist mainly of opaque minerals with trace amounts of rutile, and possible epidote and zircon. I Petrographic examination of washed water well cuttings from AL-40 (-440 to -450 foot and -550 to -560 foot elevations) indicated that they are almost entirely coarse-grained, moderately sorted quartz with some silt. 7.5.1.2 Lithology of Samples From VSC-4 Core Hole Samples from VSC-4 were collected from elevations -448.3, -528.3,
-538.3, -553.3, -641.3, -709.3 and -843.3 feet (Figure 7-6). Results of petrographic, x-ray diffraction, and heavy mineral analyses performed on these samples are presented in Tables 7-6, 7-7 and 7-8.
In general, petrographic examination of these samples showed them to be sandy clay, quartz sand, interbedded shale and sand, sandy micaceous clay, sandy carbonaceous shale, sandy micaceous clay and quartz sand, respectively.
~
X-ray diffraction analysis of the interbedded shale and sand sample from elevation -538.3 feet, shows equal amounts of quartz and clay, with kaolinite predominant over illite. As determined from heavy mineral analysis, opaque minerals, garnet, unidentified minerals, I 7-23
I l zircon and other accessory minerals are present in decreasing abundance. The sandy, micaceous clay from elevation -553.3 feet contains predominant quartz with moderate amounts of illite and smectite clay. Muscovite was not noted, but may have been identified as illite since x-ray diffraction peaks for the two minerals overlap. I Heavy mineral analysis of the quartz sand from elevation -528.3 feet inoicates that opaque minerals are predominant with lesser amounts of z ircon , tourmalinc, garnet, epidote and other accessory minerals. The quartz sand from -843.3 feet elevation contain opaque minerals, zircon, tourmaline, and other accessory minerals. 7.5.1.3 Comparison of Samples Collected from Similar Elevations in AL-6 6 and VSC-4 The sandy clay sample collected from VSC-4 at elevation -448.3 feet is very similar in lithology to that of the clayey, quartz sand from fj elevation -468.0 feet in AL-66. Both samples consist of quartz grains within an iron-rich clay matrix. The clayey quartz sand of the sample collected from an elevation of about -558 feet in AL-66 (Al-66-2) is very similar to the sandy, micaceous clay from -553.3 feet elevation in VSC-4. Both samples contain quartz, clay, muscovite and a trace of feldspar. These, in addition to the sample from about -550 feet in AL-40, contain trace amounts of dolomite (Appendix G). I ' i 1 I 7-24 I 1
I Minor shaly material found in AL-66-2 was not found in the sample closest in elevation to VSC-4 (-553.3 feet) . Similar shaly material was found in VK'-4 at elevation -538.3 feet. Since AL-66-2 consists of water well cuttings, it is probable that the shaly material in AL-66 is the result of contamination from above. I 7.5.1.4 Comparison of Samples Collected from Below the Postulated Pre-Late Cretaceous Unconformity in E -66, AL-40 and VSC-4 to Triassic Rocks from DRB 10 g Samples were collected from approximately 50 feet below the postulated pre-Late Cretaceous unconformity in AL-66, AL-40 and VSC-4. Their lithologies were compared with those of Triassic rocks approximately 50 feet below the known Cretaceous-Triansic contact in core hole DRB 10 on the Savannah River Plhnt. Figure 7-8 shows the lithologies of samples I AL-6 6-1 AL-66-2 and core from DRB 10 (Marine, 1976). There cre several significant differences between the lowermost samples from VSC-4, AL-66 and AL-40, and the Triassic rocks. First, a significant amount of plagioclase and minor amounts of potassium feldspar are present in Triassic rocks, but only minor amounts of potassium feldspar, and no plagioclase were detected in VSC-4, Al-66 or AL-40. Second, illite, followed by chlorite and mixed-layer clays, are the predominant clay minerals in Triassic rocks. Kaolinite is occasionally present but always in lesser amounts than illite. By contrast, kaolinite is the predominant clay in AL-66. Kaolinite is also the predeminant clay type in VSC-4 at -538.3 feet elevation although equal amounts of illite and rmectite were reported in VSC-4 at
-553.3 feet elevation. Illite may have been mistaken for muscovite 7-25 I
since x-ray diffraction patterns of the two minerals overlap. Because samples from AL-40 had been washed, clay minerals are lacking in these samples they were not used for comparison. I The lithology of samples collected from AL-66, AL-40 and VSC-4 at elevations below the postulated pre-Late Cretaceous unconformity proposed in the Open-File Report are inconsistent with known Triassic-Jurassic lithology based on mineralogical analyses of core samples from DRB 10. Further, samples taken from AL-66 and AL-40, both abova and below the proposed contact (-500 feet elevation), are not significantly different from each other suggesting that there is no lithologic contact at this elevation. I It is therefore, concluded that lithologic evidence does not support the existence of Triassic rocks in VSC-4, Al-66 or Al-40. I 7.5.2 Lithologic Analyses of Core Samples from VSC and VG Core Holes The lithology of selected core samples from VSC and VG holes was studied to supplement the stratigraphic correlations interpreted from the core drilling program described in Section 6.2. The intent of these studies was to delineate mineralogical and textural criteria which could aid in correlating and differentiating stratigraphic units. The samplet c.11ected are considered representative of selected stratigraphic units encountered in the core holes. Sample selection { was based on visual timilarities of portions of core from each of the I holes that appeared to represent stratigraphically wuivalent units. i 'I 7-26
I Figures 7-6 and 7-7 show sample locations in the VSC and VG core holes. The samples submitted for various studies were taken from the Barnwell Group; and Lisbon, Huter, Ellenton and Tuscaloosa Formations as determined from field study. Tables 7-6 through 7-11 summarizes the results from analytical testing. 7.5.2.1 Barnwell Group 7.5.2.1.1 Griffins Landing Member The samples collected from the Griffins Landing Member of the Barnwell Group were determined petrographically to be quartzose, calcareous sand consisting of moderately to well scrted, angular to sub-angular quartz grains poorly cemented by microcrystalline calcite (micrite) and clay. Minor to trace amounts of feldspar, microfossils, muscovite, opaque minerals and epidote are often present. Bulk x-ray diffraction analyses of selected samples indicate that they usually contain predominant quartz with lesser amounts of calcite and clay. Clay generally makes up about 10 percent of these samples and usually consists primarily of smectite with some kaolinite and illite. Heavy mineral analyses show that these samples contain mainly opaque minerals with lesser amounts of garnet, zircon, tourmaline, kyanite, sillimanite, epidote and hornblende. 7.5.2.1.2 Twiggs Clay Member Samples VSC-2-1 and VSC-3-2 were collected from the Twiggs Clay Member of the Barnwell Group. These samples were determined petrographically 1 7-27 ; 1 1
to be clayey glauconitic sand, and sandy glauconitic claystone, respectively. X-ray diffraction studies verify the high amount of clay, mainly smectite. The high clay content, a relatively higher amount of unidentified minerals and the presence of collophane differentiates these from samples of the Griffins Landing Member.
- I 7.5.2.1.3 Utley Limestone Member I
l Samples collected from the Utley Limestone Member of the Barnwell Group are determined petrographically to be fossiliferous, sandy limestone which contains abundant shell fragments and some moderately sorted quartz grains cemented by micrite. Minor to trace amounts of glauconite, feldspar, opaque minerals and epidote are also present. X-ray diffraction analyses indicate that these rocks are predominantly calcite with minor to moderate amount of quartz and usually only a few l percent clay. Smeetite is usually the predominant clay mineral with l l traces of kaolinite and illite also present. Although glauconite was reported in the petrographic examinations of these samples, it pas not noted by x-ray diffraction techniques. This may be caused by either overlapping glauconite and illite peaks on the x-ray diffractogram or low concentrations of glauconite in the sample. 7.5.2.2 Lisbon Formation 7.5.2.2.1 Blue Bluff Member Petrographic examination of samples collected from the Blue Bluf f Member of the Lisbon Formation show them to be sandy to silty marl, and 7-28
I shale, often glauconitic and usually laminated. Minor to trace amounts of microfossils, feldspar, opaque minerals, epidote and zircon may also be present. X-ray dif fraction analyses of these samples indicate that they generally consist of 30 to 70 percent clay with quartz and sometimes calcite. , ectite is usually the predominant clay mineral with secondary amounts ot kaolinite and illite. I 7.5.2.2.2 Unnamed Sand Member Samples collected from the unnamed sand member of the Lisbon Formation consist almost entirely of unconsolidated quartz sand. Petrographic I analyses show the sand to be medium-grained and moderately to well sorted. Trace amounts of clay, opaque minerals, epidote and staurolite are often present. The heavy mineral assemblage consists mainly of opaque minerals with lesser amounts of garnet, zircon, tourmaline, hornblende and epidote. I 7.5.2.3 Huber Formation X-ray diffraction analyses of samples ccl.lected from the Huber Formation indicate they consist mainly of c sy, predominantly kaolinite, with minor amounts of smectite and illite. Moderate amounts of quartz and amorphous material are present in some VSC and VG core holes. I 7-29 I
lI 7.5.2.4 Ellenton Formation I The carbonaceous silt and clay of the Ellenton Formation were analyzed by x-ray dif fraction techniques. These samples are generally found to contain about 30 to 65 percent quartz, with the remainder consisting of clay and/or carbonaceous material. The predominant clay mineral is i either kaolinite or smeetite with lesser amounts of illite. 7.5.2.5 Tuscaloosa Formation Samples collected from the Tuscaloosa Formation were determined petrographically to be clayey sand and sandy clay. In thin section, the matrix appears to consist of iron stained kaolinite. These samples contain, in addition to kaolinite clay, poorly sorted quartz with moderate to minor amounts of muscovite, gypsum and potassium feldspar. X-ray dif fraction analyses indicate these samples contain 50 to 80 percent quartz with lesser amounts of clay and occasional feldspar. I The clay content ranges from 15 to 45 percent, with kaolinite usually the predominant clay mineral. Illite, not muscovite was reported by x-ray diffraction; however, these minerals are virtually indistinguishable on an x-ray diffractogram. Heavy mineral analyses indicate that opaque minerals are predominant with lesser amounts of zircon, tourmaline, garnet, hornblende, epidote, and rutile. I I 7-30
I 7.5.2.6 Discussion of Lutelc-;;"c Results I The samples collected from the fortnations described above are classified based on mineralogical and textural characteristics determined from petrographic examinations. X-ray dif fraction results support the petrographic study. Although clay mineral percentages (relative to each other) are very similar in the Griffins Landing Member, the Utley Limestone Member of the Barnwell Group, and the Blue Bluf f Member of the Lisbon Formation, total clay amounts varied greatly. The total clay content for each formation in about 10, 3 and 50 percent, respectively. I The dominance of kaolinite in the Huber Formation samples is quite distinc tive. The Ellenton and Tuscaloosa Formations are differentiated by the relatively higher quartz content and predominance of kaolinite in the Tuscaloosa Formation. In general, heavy mineral analyses indicate that samples from various stratigraphic units contain similar heavy mineral assemblages. Two depth related trends in the VSC and VG core were noted though: 1) opaque mineral content increases with depth 2) sillimanite and kyanite content decreases with depth. As determined from petrographic, x-ray diffraction, and to a lesser extent, heavy mineral analyses, the lithologic charateristics of the stratigraphic units sampled are quite distinctive. As is shown in Figures 7-6 and 7-7 , samples from the same stratigraphic unit occur at 7-31 w
1 I
- the proper elevations. Also, samples were taken from near the lower contact of the Barnwell Group and the upper contact of the Lisbon
.IE Formation in order to verify formation contacts identified during core logging. The lithology of the samples confirms the stratigraphic correlations.
I The lithology of the stratigraphic units described above are consistent with published descriptions of each formation. The lithologies of the Griffins Landing Member and Utley Limestone Member of the Barnwell Group as described by Huddlestun are consistent with the lithologies of samples thought to be from those units. The samples collected from what is considered to be the Blue Bluf f Member and unnamed quartz sand member of the Lisbon Formation are lithologically consistent with Siple's description of the McBean Formation (1967) and Sever 's I description of the Lisbon Formation (1965). Buie's description of the kaolinite-rich Huber Formation (1980) is consistent with the " pure clay" (kaolinite) unit described in the present study. The lithology of samples taken from the unit below the Huber Formation is consistent with Siple's description of the Ellenton and Tuscaloosa Formations (1967). I Two conclusions can be made based on the lithologic studies. First, samples collected from AL-66, AL-40 and VSC-4 at depths below the Triassic contact shown in the Open-File Report are not consistent with the mineralogy of the Triassic rocks in DRB 10. They are consistent with the mineralogy of the Tuscaloosa Formation. The second conclusion i is that mineralogy of the paleocene and Eocene marker beds is similar I 7-32
within each formation, thus verifying the stratigraphic correlations made between the core holes. Samples considered to be represtative of stratigraphic units encountered by the VSC and VG core holes were found to be lithologically distinctive. The lithology of the samples confirms the stratigraphic correlations interpreted. 7.6 Seismicity All available seismicity information within 62.5 miles (100 km) of the Vogtle site was reexamined to test for any association of earthquakes 1 i= with the postulated Millett and Statesboro faults. This was done because, even should the Millett or Statesboro faults exist, they would l be of interest for seismic design at Vogtle only if they should prove to be capable within the context of Appendix A to 10 CFR 100 (U.S. Nuclear Regulatory Commission,1973) . One test of fault capability g lW provided in Appendix A above is exhibition by the fault of
" macro-seismicity instrumentally determined with records of suf ficient precision to demonstrate a direct relationship with the fault".
Earthquake detection and location have been greatly improved in the Vogtle area in recent years by the installation of many regional high gain seismograph stations. A permanent seismographic network was installed in 1974 in South Carolina between Charleston on the Atlantic Coast and Columbia in the central part of the state. Other stations have been installed permanently or temporarily at sites of particular I g >->>
I I interest, especially at nearby reservoirs and at the Savannah River Plant (SRP) just across the Savannah River from Vogtle. Earthquakes located by a sufficient number of these high gain static.ns provide the main data set of accurately located events in the Vogtle site area. Two other catalogs of site area seismicity are also considered in this section. Felt events through 1974 within 62.5 miles of the site are I listed for completeness, although most of these earthquakes are not well-located. In addition, all earthquakes found in a search of the SRP array records are discussed. I Felt Earthquakes in the Study Area 7.6.1 A brief review of several recent studies (Stover and others, 1979; Reagor and others,1980) was performed to compile a list of all known felt earthquakes through 1974 that have occurred within the 62.5 mile radius study area of this section. All earthquakes found as a result of this review are shown on Figure 7-9. I Although evaluation of instrumental data for some of the earthquakes shown on Figure 7-9, was performed in the references used by Stover and other s (1979) and Reagor and others (1980) , the epicenters of these 4 g events are not as precisely located as epicenters of earthquakes W occurring after 1974. A rough estimate of epicenter location accuracy for these felt events indicates a range of error of one-tenth to several tenths of a degree (about six miles or more) . Even within 7-34
L, I L these broad location limits, only the earthquake of August 14, 1972 L (magnituae 2.5 to 3.0) can be considered near one of the faults postulated in the Open-File Report. An attempt was made to more precisely locate the August 14, 1972 earthquake by performing an independent evaluation or' all available data. Both felt reports and instrumental data were considered. c L Shortly af ter the earthquake in 1972, G.A. Bollinger of Virginia Polytechnic Institute and State University (VPISU) mailed postcards to individuals in about 60 towns around the Bowman, South Carolina area requesting felt or damage information (Bollinger, personal communication, 1982). Responses from seven towns indicated that the L earthquake had been felt by at least a few people. These towns (Barnwell, Bowman, Cordova, Iforatio, North, Springfield, and Summerton, South Carolina) are shown as solid circles on Figure 7-10. The event was reported as " felt by many" and as a "small rumble" at Bowman. Otherwise it was felt only by a few as a slight shaking. Forty-seven other towns reported that the earthquake was not felt. These towns are shown as open circles on Figure 7-10. Although the felt information is dif fuse, it is clear that an epicenter in the Barnwell area is not well supported by the data. The nearest seismograph stations operating at the time of the August 14, 1972 earthquake (Poppe,1979) were also contacted. These were ATL L F l L, 7-35
lI (Atlanta, Ceorgia) , CSC (Columbia, South Carolina) , BLA (Blacksburg,
- Virginia) , !!BV (Harrisonburg, Virginia) , LEX (Lexington, Virginia) , ORT l
(Oak Ridge, Tennessee) , and CPO (McMinnville, Tennessee). Emergent P-and S-wave arrival times were found for several stations. However, 1 initial analysis indicated that the readings were not mutually i consistent for any epicenter location, and that differenceo between i l observed and calculated P-wave arrival times of 15 seconds or more occurred. Thus, available instrumental data do not significantly constrain the location of this earthquake. It is concluded from the above discussion that no felt earthquakes l occurring before 1974 are located near enough or with sufficient precision to suggest association with either the postulated Millett or l Statesboro faults. W5 7.6.2 Earthquakes Incated with the Regior.al Seismograph Network l ! The installation of additional seismograph stations near the Vogtle site since 1974 has allowed much improved detection and location of more recent study area earthquakes. A summary of station distributicn for the period 1978 through 'he beginning of 1982 is presented in Bcllinger and Mathena (1982). Over 30 stations are currently operating within South Carolina and the northeast corner of Georgia (see Figure 7-11). Most are maintained by the U.S. Geological Survey, the Georgia Institute of Technology, and the Savannah River Plant. The detection I I 7-36
I and location capabilities of this network are summarized by Tarr (1982). Tarr estimates that earthquakes within the study area with I magnitudes between about 1.3 and 2.0 should be detected by five or more stations, and that earthquakes with magnitudes between about 2.1 and 2.5 should be detected by 15 or more stations, both at the 90 percent confidence level. Semi-major axes lengths for 90 percent confidence ellipses are on the order of three miles for most study area earthquakes of magnitude 2.0 or above (Tarr,1982, Figures 3 and 4) . All published well-located earthquake epicenters within the study area (1974-May 1982) are shown on Figure 7-12. Sources of earthquake 1 information for this figure are the various bulletins of the j Southeastern U.S. Seismic Network (E USSN) compiled and edited at Blacksburg, Virginia (Bollinger and Murphy, 1978; Bollinger and Ma thena , 1978-1982), and compilations of U.S. Geological Survey data (Rhea,1981; Tar r, and others,19 81) . In addition to published information, an independent study was I conducted to locate the recent earthquake of January 28, 1982. This is discussed further below. I All earthquakes shown on Figure 7-12 are small. The average magnitude is about 2.1 and none is greater than 2.8. Focal depths are shallow, the average being about four miles. The great majority of the I earthquakes shown are located in the extreme northwest part of the I I I '-"
study area. These events are generally in the Piedmont Province, near and around Clark Hill Reservoir. A number of earthquakes in this part of the study area have been identified as explosions associated either with quarry operation or road construction (Long , 19 81) . It is not known which, if any, epicenters shown on Figure 7-12 are actually explosions. However, past experience in the area and the clustering of origin times during the af ternoon indicates that many of the Piedmont epicenters shown in this figure are not tectonic earthquakes (Long, personal communication,1982) . None of these events are near the postulated Millett or Statesboro faults. I The three earthquakes nearest the postulated faults occurred on September 15,19 76, June 5,1977, and January 28, 1982. Parametric studies were performed on these earthquakes to investigate the effect on location of crustal model variation, stations used in the solution, trial location, and azimuthal weighting. In no case was the final location changed by more than about three miles by these variations. The ll-station hypocenter solution for the September 15, 1976 earthquake is very near 33.13'N, 81.40*W with a focal depth of just less than 2.5 miles. The smallest distances between this epicenter and the postulated Millett and Statesboro faults are about six miles and 18 miles, respectively. I Sixteen seismograph stations recorded the June 5,1977 earthquake. This event is located near 33.02'N, 81.43'W at a depth of less than one mile. The closest approach of this epicenter to the postulated Millett 7-38
and Statesboro faults is about 11 miles and 14 miles, respectively. A focal mechanism solution has also been published for this earthquake (Guinn, 1980) . This solution implies high-angle reverse motion on a fault striking northwest-southeast. This strike is inconsistent with the strike of either the postulated Millett or Statesboro faults. However, detailed studies of the first motion data for this event reveal that the Guinn focal mechanism solution is not well-constrained. A 14-station solution of the January 28, 1982 earthquake using unpublished arrival time data (Marine, personal communication, 1982; Rhea, personal communication, 1982) places this event near 33.OO*N, 81.41*W at a depth of about 2.5 miles. The closest approach of this epicenter to the postulated Millett and Statesboro faults is about 13 miles and 12.5 miles, respectively. It is concluded that no earthquakes shown on Figure 7-10 are located near enough to suggest association with either the postulated Millett or Statesboro faults. 7.6.3 Data from the Savannah River Plant Array I Since the beginning of September 1976, three high gain, vertical component seismograph stations have been in operation at the Savannah River Plant (SRP) in South Carolina, just across the Savannah River from the Vogtle site. A summary description of the array configuration, properties, and early operating history may be found in Krapp and Stephenson (1977). The relative geometry of the array, the Vogtle site, and the postulated Millett fault are shown on Figure 7-13. 7-39
I To take advantage of the close proximity of the SRP array to the site and to the postulated Millett fault, all available SRP records were reviewed independently as part of the study area seismicity investigation. A brief summary of this review is presented here. The postulated Millett fault, as shown on Figure 7-13, and as taken from Figure 2 of the Open-File Report, ranges from about four to 38 miles from stations in the SRP array. The distance from station SRPN ranges from 11.5 to 38 miles. SRPN is the highest gain station of the array and generally records all events noted on the array. It has, therefore, been used in the following discussion to summarize array I results. During the period September 1976 through May 1982, a total of about 130 possible earthquakes were noted with readable P- and S-wave arrivals on at least station SRPN. Using the crustal model of Kean and Long (1980) , S-P intervals (ranging from 1.6 to 59 seco .ds) may be converted into epicentral distances of from about 4.4 to 356 miles. A histogram of the number of events versus six mile distance intervals is shown on Figure 7-14. As shown on Figure 7-13 and indicated in Figure 7-14, events in the distance range from 12 to 38 miles are of principal interest. Most earthquakes occur at greater distances (42 to 102 miles) , principally in the northwest (Piedmont) part of the study area or to the southeast in the Bowman and Summerville areas. I 7-40
I As shown on Figure 7-14, eight events were noted within the distance range of interest. These occurred on Septenber 15, 1976, December 30, 1976, June 5, 1977, March 6, 1980, February 21, 1981, April 24, 1981, August 25, 1981, and January 28, 1982. Of these eight events, all but those of December 30, 1976, April 24, 1981, and August 25, 1981 were previously known and located. The five remaining earthquakes appear on Figure 7-12. The earthquakes of September 15,1976, June 5,1977, and Janu::ry 28, 1982 have been discussed in detail above. Published locations for the March 6, 1980 (Rhea , 19 81) and February 21, 1981 (Bollinger and Mathena, 1981) earthquakes place their epicenters approximately 46 miles to the I northwest and 24 miles to the northeast of the nearest point on the postulated Millett fault. A preliminary location for the April 24, 1981 earthquake places it in the Clark Hill Reservoir area (Rhea, I personal communication, 1982) about 45 miles from the nearest point on the postulated Millett fault. No other station readings have been found for the December 30, 1976 and August 25, 1981 events. Therefore, both events are unlocatable (being recorded only at SRPN and SRPW) . Both occurred during local work hours when SRP records are noisy, and both may well be cultural rather than seismic. It is concluded that no earthquakes recorded on the SRP array are located on the postulated Millett fault. Nearby earthquakes, noted on regional arrays, are well recorded and distinct on the SRP stations. No similar time histories, but of smaller amplitude on SRP array records, I 7-41
I were found. Therefore, no evidence exists for the occurrence of earthquakes recorded only on the SRP array near the site or on the postulated Millett fault. 7.7 Surface Water Hydrology 7.7.1 Analysis by U.S. Geological Survey The Open-File Report concludes that anomalously large aquifer discharges to the Savannah River occur between Augusta and Burtons Ferry Bridge and are an indirect manifestation of a fault near Millett. To support this finding, the two-year, 30-day low-flows were computed for various gauging stations on the Savannah River and adjacent watersheds, including the Ogeechee River, Brier Creek, and the south fork of Edisto River. Unit baseflows (baseflow rate per unit of surface-drainage area) were calculated for reaches near Millett. The ; locations of the gauging stations used and the aligniment of the hypothetical fault are shown schematically on Figure 7-15. The Open-File Report unit baseflow estimates for the reaches of interest are presented in Table 7-12. l The Open-File Report study calculated a unit baseflow of 0.74 cfs/mi 2 contributed to the Savannah River between Augusta and Burtons Ferry Bridge, about four times that for the Ogeechee River between Louisville 2 and Scarboro (0.17 cfs/mi ) and 1.6 times that for the south fork of 2 Edisto River between Montmorenci and Denmark (0.46 cfs/mi ) . In addition, the Open-File Report contended that the unit baseflow to the 7-42
( Savannah River between Burtons Ferry Bridge and Clyo (0.23 cfs/mi2) is only about 32 percent of that between Augusta and Burtons Ferry Bridge. The unit baseflow to the Ogeechee River between Scarboro and Eden (0.11 cfs/mi2 ) is about 65 percent of that between Louisville 2 f and Scarboro (0.17 cfs/mi ) . In computing the unit baseflow of the Savannah River between Burton 9 Ferry Bridge and Clyo, flow contribution from Brier Creek (at the Millhaven gauge) was subtracted from that observed at Clyo. Based upon these observations, the Open-File Report concluded that anomalously large aquifer discharges to the Savannah ( River occur generally between Augusta and Burtons Ferry Bridge and are possibly an indication of the existence of a fault near Millett. 7.7.2 Factors Affecting Baseflow ( Low-flow characteristics of a stream as predicted from streamflow-gauging records depend upon many factors other than the underlying geologic configuration of the drainage basin. These include the surface soil conditions, drainage area, land use, incised depth of the stream, ground water conditions, both surface water and ground { water usage, stream length and density, upstream reservoir regulation, and most of all, climate. Extent and type of connection between ( aquifers and stream are also of major importance. Without the full consideration of all these factors, accurate projections of unit baseflows are not possible. The concept of baseflow per unit of surface drainage area is in itself a nebulous quantity, since the ground water drainage area is not necessarily equal to the surface f water drainage area. Although data are not suf ficient to accurately [ 7-43 t t . . . . . . ., . . .. - .. . ..
I I define the ground water drainage area, Fig. 7-19 indicates that for the Savannah River, the drainage area for ground water may be larger than for surface water. Accurate calculation of 30-day low-flows for the unit baseflow estimation is not without problems. Basically, the two-year, 30-day low-flows are derived from frequency analysis of recorded low-flows and are dependent on the length of the period of record as well as the flow characteristics within this period. Direct physical relationship between the two-year, 30-day low-flow values at two successive gauging locations on a river reach, or between two stations on different rivers, is probably impossible to project. Because of the lag-time between precipitation and ground water contribution to a stream, it is vital that concurrent records be used if comparisons are to be made between stations, and especially between streams. Two major dams have been built on the Savannah River since 1950. They are Clark Hill, constructed in 1953, and Hartwell Reservoir, constructed in 1958. The first column in Table 7-13 shows unit base flows at Augusta from 1941 through 1970. The years 1953 and 1958 show distinct changes in low-flow regime due to regulation by these two dams. Low flows prior to 1953 are more variable than af ter 1953. In addition, the low flows are substantially higher af ter 1958. 7.7.3 Calculation of Baseflows Because of variations in climate over time it is quite important to use concurrent streamflow records when comparing baseflows at different 7-44
i locations on different streams. The available streamflow records for the stations utilized are presented on Figure 7-16. This chart shows i that the only concurrent period of record for all stations is that from 1
- 1941 to 1949, a very short period for frequency analysis. The minimum 30-day low-flow period for each year at these gauging stations was 1
identified and the results are shown in Table 7-14 for each year. The low flows were found to occur within a common time span of approximately 15 days during each year indicating that the streams do have some hydrologic homogeneity. In computing the 30-day low-flow for the reach of the Savannah River between Burtons Ferry Bridge and Clyo, the contribution frca Brier l Creek (at the Millhaven gauge), a tributary of the Savannah entering 1 [ just downstream of the Burtons Ferry Bridge gauge, was subtracted from the flow at Clyo. The unit baseflow was then determined as AQ/AA where AQ is the incremental streamflow rate and A A is the incremental surface drainage area between successive gauging stations. The results of these calculations are shown in Table 7-13 where all i records were used, and in Table 7-15 where only concurrent records were l used. Plots of the unit baseflow values for the upper and lower l reaches of the Savannah River for the period 1941 to 1970 are presented in Figures 7-17 and 7-18, respectively; average unit baseflows were 0.69 and 0.47 cfs/mi2 for upstream and downstream reaches respectively, I l 7-45
Baseflows per unit of drainage area should be computed using ground water drainage areas. However, since ground water drainage areas cannot be determined, surface-drainage areas used in the Open-File Report were used here also. 7.7.4 Effects of Possible Streamflow Gauging Errors The USGS classifies the streamflow records at all the gauging stations in question as " good". A " good" streamflow record will have 95 percent of the daily discharges reported w.ithin 10 percent of the true discharge values. The mathematical process of computing unit baseflows involves subtracting two numbers of approximately equal magnitude. The resulting number of such a computation may have the same absolute error as the original numbers but its relative error is greatly increased. In order to assess the utility of the computation of unit baseflow it was important to examine the possible error inherent in the calculation. Two separate approaches were used. A statistical analysis was performed of the unit baseflows estimated for the Savannah River reaches and shown in Table 7-13. Using the 30 years of flow records, assuming that the unit baseflows are normally distributed, and applying the t-distribution test indicates that at 98 percent confidence level, the unit-baseflow contribution to the upstream reach would lie between 0.56 and 0.83 cfs/mi2 . For the same confidence level, that for the downstream reach would lie between 0.28 and 0.66 cfs/mi 2, l 7-46
The previous paragraph estimated probable ranges of unit-baseflow values considering random characteristics of errors. It is also important to estimate the possible maximum error based on magnitude of gauging errors alone. If the possible error in a 30-day low flow value is five percent, the range in unit baseflow would be given by the equation p_q , [(Q2 0.05Q2)-(Qi 0.05Qi)] AA AA Choosing the algebraic signs on the right hand side of this equation to give maximum and minimum values respectively, yields what can be considered an estimate of maximum possible error. It should be noted that for rivers with mo. ring beds, the gauging error during low flows is likely to be in the same direction throughout a sequential period since at least part of the error arises due to changes in bed configuration produced by higher flows. Considering year 1946 on the Savannah river es an example, the previous equation indicates that the calculated unit baseflow of 0.60 cfs/mi2 on the upper reach could have been as large as 0.96 and as small as 0.24 cfs/mi 2
. Similarly for the lower reach the calculated unit baseflow of 0.20 cfs/mi2 could have been as large as 1.12 and as low as -0.57 cfs/mi2. The negative value would indicate a losing-stream condition, a condition which actually appeared present during 19 44, 19 65, 19 67, and 19 69.
It is clear from all the surface water studies that variability of computed unit baseflows is great. Figures 7-17 and 7-18 show this variation graphically for the Savannah River 1941-1970 record. Table 7-14 shows that for the 30-year record of flows, unit baseflow in the 7-47
downstream reach was actually greater than that in the upstream reach for 10 separate years while for four years the downstream reach appeared to be a losing stream. The error analysis performed in Section 7.7.4 further emphasizes that computed unit baseflows are subject to enough variation that they cannot be used with confidence to prove or disprove the presence of a barrier (hypothesized fault) in an aquifer. 7.8 Ground Water Hydrology Well data collected in the field survey were examined in the office to determine which aquifers were penetrated by the wells. Wells determined to be open only to either the Tertiary (upper) or the CretacCous (lower) aquifers were plotted on separate base maps. Water level elevations were read into a computer program designed to construct potentiometric maps of both aquifers. These maps were subsequently examined and corrected manually to add the physical insight which a purely mechanical contouring is lacking. Wells with inadequate data to determine which aquifer was penetrated, or those penetrating multiple aquifers, were not used. 7.8.1 Reduction of Ground Water Data The elevation of the top of each aquifer was determined by construction of a structure contour map of the upper aquifer. Data used to construct this map were obtained from publications, lithologic and 7-48
geophysical logs from public agencies, and the lithologic and geophysical logs of the core holes drilled in this study. The water levels of the selected wells in the well survey were evaluated for accuracy. Wells with " reported" levels that are anomalous and those with measured levels known to have been affected by pumping were deleted. Wells located in areas where the confining layers are not present or have undergone facies changes and are no longer confining, were also deleted. hhen all the valid data from the well survey were assembled, contour maps were produced. The maps were computer drawn by a Calcomp 1055 plotter to produce unbiased craphic representations of the potentiometric surface of each aquifer. In areas of insuf ficient data, however, the computer extrapolated and of ten closed contours where there was no justification. Therefore, hand-modified contours were drawn in such questionable areas. These representations of the potentiometric surfaces of the aquifers are shown on Figures 7-19 for the Tertiary (upper) and 7-20 for the Cretaceous (lower) aquifers. These maps provide a basis for qualitative evaluations of the ground water hydrology at the Vogtle site, as discussed in Section 8.1.11. They were also used to calibrate the numerical model, which is described below. I In response to comments from the ground water consultants, interpretive contouring of the upper aquifer potentiometric data was done as a comparison to. the computer-generated contour map. Additional control b I g 2..,
points used for this interpretation include the water level of an observation well at the Vogtle Plant, and the river level upstream of the Vogtle plant in the outcrop area of the aquifer. It is evident that the aquifer discharges to the river in this area. Although ground water flow may have a significant vertical component at the river , the aquifer is unconfined in the outcrop area and the river elevation is believed to be close to the true potentiometric surface. Figure 7-21 compates the computer-generated with the hand-drawn (interpretive) piezometric contours for the upper aquifer, in the vicinity of the Vogtle plant. The principal dif ferences are the more extended zone of ground water discharge along the river, and the relocated 160 and 180 foot contours in the zone of no data near Williston. The overall configuration of the potentiometric surface is not changed relat.ive to the postulated Millett fault. In order to investigate the possibility of anomalous water level l changes across the postulated Millett fault, water levels were measured in two lines of wells and piezometers crossing this inferred structure as shown on Figure 7-22. Only wells completed in either the upper (Tertiary) or the lower (Cre taceous) aquifer were used for this analysis, and all water levels were collected during the summer of 1982. Data from AL-66 were considered unreliable because this well is completed in more than one aquifer unit. Figures 7-23 and 7-24 show the water level profiles constructed. Anomalous water levels are not present, as discussed in Chapter 8. I 7-50
7.8.2 Numerical Model 7.8.2.1 Purpose and Approach As explained in Section 8.1.11.2, the results of the water well survey l indicate that ground water discharges into the Savannah River south of Augusta in the outcrop area of each aquifer. Both maps show reversal of ground water gradient in the vicinity of the Vogtle site. These reversals of gradients are the only features that could be considered anomalous. There are several possible explanations for the observed reversals of ground water gradients: 1) a barrier caused by faulting,
- 2) a marked change is lithology, and 3) the hypothesis advanced by Siple (1960) , and LeGrand and Pettyjohn (1981). This theory describes l
one common type of hydrogeologic system which is dominated by
- consequent streams flowing down a structural basin. This is i
illustrated schematically on Figure 7-26. These streams capture large l quantities of ground water discharge, which creates a natural cone of depression at the lowest exposed point in the aquifer. According to LeGrand and Pettyjohn (1981) , the cone of depression observed in the Cretaceous aquifer south of Augusta, and the uneven distribution of ground water discharge in this area can be explained by the above theory. It is the purpose of the numerical model developed herein to study the validity of these hypotheses. The model also attempts to demonstrate as it was clearly stated at the beginning of this chapter that the interpretation of these ground water data alone does not I 7-51
k l confirm or deny the existence of the postulated Millett fault. The digital model used for this study is part of Bechtel's library of computer programs. This two-dimensional finite element model, referred to as FLUMPB, has been shown to be well suited for a wide class of problems arising in subsurface hydrology. These problems include confined saturated flow, unconfined or partially confined flow, { axisymmetric flow to a well with storage, and flow in saturated-unsaturated soils (Narasimhan et al., 1978). The program uses a special numerical procedure that eliminates many of the f difficulties encountered in modeling extensive aquifer systems, while providing a high level of accuracy and efficienty. The model solves the time-cependent ground water flow equation and reaches the steady state asymptomatically as a limit to the transient problem. 7.8.2.2 Input Data f 7 The input data necessary to operate the model are essentially of three types: model geometry, physical properties, and initial and boundary conditions. 1 The model geometry, as shown on Figure 7-25, has been designed so that the element shapes and the nodal spacings can accommodate variations in trar.smissivity, recharge rates, and boundary conditions. The grid is [ refined in the region of high gradients, especially along the Savannah
~
River in the outcrop areas. I 7-52
I I The transmissivity was varied throughout the model to account for changes in the aquifer thickness, which ranges from 0 to 1,500 f t in the area of the Vogtle site. In the model, the thickness was assumed
- to decrease from 1,250 f t at the lower end of the study area to 100 f t l
f in the unconfined zone. The different thickness zones specified in the l model are shown on Figure 7-25. The transmissivity values for each I element were specified accordingly. The transmissivity changes in a l stepwise manner in the confined part of the aquifer, and varies linearly with the head in unconfined areas. Constant-head boundary conditions were assigned along the Savannah River where it cuts into the outcrop area. The values specified at the corresponding nodes were the average ground elevation in the immediate vicinity. The northwest limit of the model, where the Cretaceous rocks which comprise the lower aquifer thin and crop out, was also assigned a constant head boundary condition equal to the ground elevation. The lower southeast model boundary was similarly kept at a constant head I equal to 140 ft. ides of the model are no-flow boundaries. Recharge to ti,3 grounc Mater due to infiltration was taken into account by assigning appropriate source terms throughout the unconfined part of the aquifer. Of the average 48 inches per year of precipitation in the study area, 10 inches per year were takea to contribute to deep I percolation. This rate of 10 inches per year is 50 percent of the rainfall during the non-growing season. I 7-53
-^
___m___-______
The storage coefficient was estimated to be 0.0001 in the confined part of the aquifer and 0.25 in the unconfined areas. These values are considered to be representative of the geologic materials prevailing at the site. 7.8.2.3 Numerical Model Results I This section presents the results obtaina ^ by numerical modeling. As explained in the previous section, toe numerical model was developed to test alternative hyptheses that may account for the observed ground water conditions in the Cretaceous aquifer. 7.8.2.3.1 LeGrand's Hypothesis - This test case uses the model and the input data described in Section 7.8.2.2. 'Ite corresponding results are given on Figure 7-27, which shows the piezometric contours calculated under the conditions believed to be generally representative of those prevailing in the Cretaceous aquifer. It is apparent that an area of low ground water contours, (sinks), develops in the unconfined part of the Cretaceous aquifer around the Savannah River. This feature exists without taking any account of it in the model of the postulated Millett fault. The calculated potentiometric map is in general agreement with the observed field data (Figure 7-20), which also exhibit the characteristic sink north of the postulated Millett fault. The numerical simulation I I .
therefore indicates that the ground water conditions observed at the site correspond to those prevailing around streams flowing along dipping strata, as stipulated in LeGrand's hypothesis. I 7.8.2.3.2 Hypothesis of a Barrier Fault The next step was to simulate the effect of a barrier at the location of the postulated Millett fault. This was achieved by assigning a lower permeability to the elements located in the appropriate mesh area. The results are shown on Figures 7-28 and 7-29, which correspond to a fault permeability equal to 100 f t/ year and 1 f t/ year, i respectively. The ground water contours are significantly affected in l l the vicinity of the barrier, as it can be seen by comparing the base l case (i.e. LeGrand's hypothesis, Figure 7-27) with Figures 7-28 and 7-29. However, the sink that characterized the ground water contours around the Savannah River in the base case is still apparent. It is j therefore concluded that the ground water data alone cannot be used to prove or disprove the existence of a barrier fault. I 7.8.2.3.3 Hypothesis of Reduced Transmissivity 1 I Another hypothesis stipulated in the Open-File Report, was that of an abrupt reduction in aquifer thickness south of the postulated Millett l fault. This hypothesis was tested with the model by reducing the i l transmissivity of the elements located in the corresponding area of the I I I '-"
I lI ; { finite element mesh. The new distribution of aquifer thickness assumed on the model is shown on Figure 7-30, and the corresponding simulation l
- I results are presented on Figure 7-31. Comparison of Figure 7-31 with the base case similation (Figure 7-27), indicates that the main ef fect l of using lower transmissivity values south of the postulated fault is to shif t southward the 200-foot potentiometric contour. Further comparison of both Figures 7-27 and 7-31 with the field data (Figure lI l
l 7-20) indicates that assuming a reduced transmissivity south of the I postulated fault yields a less satisfactory agreement with the observed I data than when the transmissivity increases gradually from north to south, as it does in the base case. Consequently, it seems that the assumption of reduced transmissivity south of the postulated fault is not a valid hypothesis. I .I lI lI .I l lI 'I I I 'I >-"
TABLE 7-1 AVAILABLE INFORMATION ON PETROLEUM CDMPANIES AND WELL OPERATORS WELL WELL YEAR OWNER LOCATION COMPLETED REMARKS Beddingfield & Falin 1 well: Emmanuel County 1932 These two men collaborated on this well only. No data. 1 well: Screven County 1963 Drilled by Barnwell Drilling F. W. McCain Co., Shreveport, LA. No Data. I well: Emmanuel County 1932 Company formed for this test Georgia Oil Co. well only. No Data. Georgia Petroleum Co. 1 well: Jefferson County 1907 Only known information is that company was associated with A. F. Lucas of Spindletop fame. Three Creeks oil Co. 2 wells: Burke County 1923 No well location or information concerning this company was discovered.
TABLE 7 GEOPHYSICAL AND PETROLEUM CDMPANIES CONTACTED COMPANY NAME DATA AVAILABLE ( I Allen Geophysical Consulting None Alliance Research Co. None Alpha Geophysical Consultants None American Resource Consultants None
.l None l Anneler, Joy J.
Applied Research Concepts None
.B&H Geophysical, Inc. None Baird Petrophysical Group None Ballard, Jack W. None
. Bell & Murphy & Assoc. None Geosource, Inc. None Western Geophysical None f.l Southeastern Exploration & Production Co. Gravity survey, Burke-Screven Co. line
{- Texaco . Seismic reflection survey of Effingham Co., ( seismic reflection study i
-down Savannah River from-Savannah, GA.,and continuing into Gulf of Mexico.
(. L [ ( _._____._l
I I E TABLE 7-3 SEISMIC BROKERAGE FIRMS CONTACTED I COMPANY NAME REQUEST RESULTS I Austin Exploration, Inc. Data Search No data discovered. Dibler Seismic Service Data Search Uncovered Vibroseis line belonging to SeisData Services. I GDI, Inc. Data Search No data discovered. GTS Corporation Data Search No data discovered. Petroscience Corporation Data Search No data discove u'. Discovered Vibroseis line I SeisData Services Data Search crossing strike of postulated Millett fault. I I I I I I I
TABLE 7-4 ANALYSIS OF IMAGERY LINEAMENIS* CUL'IURAL FEATURES GECNORPRIC FEATURES IANDSAT NUMBER PREDCMINANILY PRHXEINANILY PREDOMINANTLY PREDOTINANTLY PREDCMINANTLY IMAGE OF FIELD FIELD BOUNDARIES ROADS AND STREAM FIDODPIAIN KARST DATE LINEAMERIS BCUNDARIES & STREAM ALIGNENT POWER LINES ALIGNMENT FEA'IURES FEA M 2 3 39 17 2 6/6/76 168 55 52 2/11/74 136 47 54 3 21 5 6
*Dcminant feature resulting in observed lineament.
F TABLE 7-5'
, GENERAL PETROGRAPHIC DESCRIPTION OF.
SAMPLES FROM WATER WELLS AL-66* AND AL-40* F: AL-6 6-1 (-4 6 8 to -A7 8 f t) *
- AL-40 (-440 to -450 f t)
Clayey, quartz sand Quartz sand q Coarse-grained, well sorted Coarse-grained, moderately quartz within a matrix of sorted quartz r fine-grained quartz, L- muscovite : and clay AL-6 6-2 (-558 to -568 f t) AL-40 (-550 to -560 f t) Clayey, quartz sand Silty' quartz sand w - Poorly sorted quartz within a muscovite / sericite Coarse-grained, moderately sorted quartz with minor silty and clay matrix, with minor shale material and a trace of d material and a trace of dolomite [ dolomite.
' Heavy mineral fraction consists fj mainly of opaque minerals with minor amounts of rutile, epidote (7) and zircon (?) (See Appendix H) . ***
r L F r. [
- Examination made from grain mounts of water well cuttings.
** Sample locations are designated by elevations from sea level.
***Results provided by heavy mineral analysis.
~ l (- , P L I L p. L I L-F.. ' e J L' a.-
--, , .,. . , _ _ _ - _ _ _ . - _ . _ _ , _ . -- - - . - . , - _ _ _ . . ~ , _ . - . . -. - , _ ..__,__. .
I TABLE 7-6 CENERAL PETROGRAPHIC DF.SCRIPTION OF $AMPLES FROM VSC CORE HOLES Core hole VT-2 Core Scie V9C-3 Core hole VSC-1 Core hole VsC-4 Barnwell Croup VSC-2-I tS 4.7 f t ) ** VSC-3-2 (40.3 f t) VSC-1-It33.5 ft) VSC-4-1(58.7 ft) Twaggs Clay Cla"ey, glauconatte sand Sandy, glauconatic Quartuose. calcareous sand Quattrose, calcareous sand and Griffins Moderately sorted quarts claystoae well sorted quarts Moderately sorted quar ta Landing Members poorly consolidated by a Fane-grained quarts and cemented by mierite poorly cemented by mictite clayey, glauconstic matris glauconste wathin a clay ma tria I Utley Member VSC-4-2(20.7 ft) Poss11tferous sandy timestone Large shell f ragments, moderately sorted quarts with some g1 caco-nite within a micrite cement Lisbon Formation VSC-2-2(30.7 ft) VF-3-3 (3 3.3 f t) VSC-1-2(31.0 ft) VSC-4-St11.7 ft) Blue Bluff $sity earl Sa ndy ear l sandy mari sandy shale Member named clay, micrite and leternedded sandy and Interbedded sandy and very fine-grained quarta very fine-grained qaarts: shaly material, both shaly material, both with within a clay matrix coetaining I Onnamed Sand Member massive VSC-2-3t-70.3 ft) cuar ta sanct with sierofessils, mierite and glaucoe.ite VSC-3-4( '.01.7 ft) Quartr sand mierite and microfossils VSC-1-3 t-111.0 f t) Reartr sand relatively abundant garnet / aircon VSC-4-o f-155.3 f t) Osarta sand I well sorted, Moderately sorted. Macerately sor ted, well sorted, mediuMr a ined, mod 1 & graineJ, Ped i u~g r a i n ed , mediuwgr a ined, unconsolidated unco .solida ted uncon s olida t ed unconsolidated Tuscaloosa Formation VSC-3-6f-296.7 ft) VSC-1-6(-301.0 ft) VSC-4-7 (-3 21. 3 f t ) Oaarts sand I Sane clay Sa ads elay Poord sor ted quarta Poore sorted quarta hell sorted, moderately consolidated within a clay matria fane-grained, by a clay matrix unecesoltdated V9C-4-6 (-4 4 8.3 f t ) Sandy elay Poorly sorted quarts within a clay matrix VSC-4-9f-529.3 ft) Quattr sand teell acrted, medii.m-gr a ir ed unconsolidated I VSC-4-10 (-53 9.3 f t ) Interbedded shale and sand Fane-grained quar ts, carbonaceous with some muscoviter bedded I VsC-4-11t-553.3 ft) Sandy, eteaceous clay Poorly sorted quarts and muscovite within I a clayey matrix VSC-4-12 (-6 41.3 f *) Sandy, carboeaceous absle Fane-granned quarts and some muscovite within a carbonaceous, shaly matrix VSC-4-13 f-709.3 f t) Sardy, macaceous clay I Fine-grained quar ta and muscovite poorly consolidated by a clay matrix VSC-4-14 '-6 4 3.3 f t) Quar ts sand - Weal sorted, medium-grained, unconsolidated
' Core holes ate arranged from left to right as they are located in the field from Nw to St.
a* Sample locations are designated by elevations free sea level. I
I i TABLE 7-7 l l X-RAY DIFFRACTION ANALYSES OF BULK l AND CIAY SIZE FRACTIONS OF SAMPLES I FR04 VSC CORE HOLES Core Hole VSC-2 Core hole VSC-3 Core bole VSC-1 Core Role VSC-4 j'"enwell Croup V!C-2-1 (54.7 f t) vsc=3-1 (61.3 ft) v5C-1-1 (33.5 f t) VSC-4-1 (58.7 ft) Twaggs Clay gujk - 604 quarts, Bule - 904 clay Bult - 654 calcite Bult - 604 quar ts. and Criffins dos clay lot quarts 154 quarts, 104 clay, 304 calcite, 104 clay Landing Members 54 cristobalite(7), 54 doloeite _CJ1ay - 1000 smeetite Clay - est 6meetite. Clay - 1004 smeetite h - 1004 smectite lot kaolinite, 56 1111te I Utity Limestone VSC-4-2 (20.7 f t) Mester Bult - 904 calcate, E quarts, trace clay i~ Clay - trace smectite,1111te Lisbon Formatson v5C-2-2 (30.7 ft) VSC-3-3 (33.3 f t) vsc-1-2 (31.0 f t) V9C-4-3 (11.7 ft) Blue Bluff BuJ1k - 704 clay, M - SC t amos pous M - 504 quar ts, Bult - 704 clay, Mesmer 1st calcite, material, 30t clay, 40s clay, 306 quarts I 156 quartz Q_ay a - 904 smet, tite, 54 1111te, 54 kaolinite
?On quarts Clay - 704 smeetite,
_304 1111t e 104 feldspar Clay - 604 saectite, 40s 1111te Clay - 704 smectite 154 kaolinite, 151 1111te Nub r Formation VSC-2-4 (-119.3 f t) v9C-3-4 (-15 2.7 f t) VSC-1-4 (-14 4.0 f t ) vsc-4-5 (-180.3 tt) gu)Q - 906 clay, Bu_Q - 600 clay, Buj k - 604 clay Bult - 100% clay lot quarts 404 quarts 404 amorphous m.terial I C_ lay - 700 kaolinite Clay - 904 kaolinite, C_ lag - 504 kac1& nite, gjay - 904 kaolinite, _10% amectite 304 smeetite, 154 chlorite, 154 smectite lot smectite i 204 1111te E)1 riton Formation VSC-2-5 (-201.3 ft) vfC-3-5 (-148.7 ft) vsc-1-5 (-205.0 ft) vsc-4-6 (-231.3 ft) Bu]Q - 604 quarts, M - 504 clay Bult - 704 amorphous Bu Q - 404 quarts, 404 clay 304 quarts, 2C4 material, 304 clay 30t cristeballte(7), 3(4 clay amorphous material C_ lay - 754 saectite, Clay - 604 smectite, Clay - 504 kaolinite, Clay - 704 smeetite, , 254 1111te 406 kaalinite, 354 chlorite, _154 kaolinite, 15 4 1111* e 204 1111te 154 spectite Tuse*loosa Formation VSC-3-6 (-298.7 ft) v5C-1-6 (-301.0 f t) VSC-4-7 (-321.3 ft) 1y31 - $54 quarts Bult - 504 quarta, Bu]Q - 754 quarts,
~ 456 clay 25t clay, 25% amorphous 254 clay material - Clay - 70t kaolinite. CJay - 804 kaolinite gley - 40t kaolinite,
_204 smeetite, 104 11aste 20t 1111te 80s illite, 204 smectite I VSC-4-10 (-53 8.3 f t) Bu]Q - 506 quarts 500 clay h - 604 haolinite, 406 1111te VSC-4-11 (-553.3 ft) gy Q - 604 quarts 404 clay Clay - 506 1111te,
' Core holes are arrar.ged from left to right as they are located in the field from NW to SE. 50% saectite
** sample locations are der 2gnated by elevations from sen level.
I
I Table 7-8 I HE AVY MINERAL ANALYSES OF SAMPLES l FROM VSC CORE HOLES 1 Core hole VSC-2 Core hole VSC-4, Barnwell Group VSC-2-1 (54.7 f t) 2 VSC-4-1 (58.7 f t) Twiggs Clay opaque minerals opaque minerals (predominant H/M3)-46%, (predominant H/M)-41%, I and Griffins Landing Members unidentified minerals, garnet, collophane, zircon, garnet, zircon, tourmaline, monazite, others tourmaline, kyanite, others Lisbon Formation VSC-2-3 (-7 0. 3 f t) VSC-4-4 (-155.3 f t) Unnamed Sand opaque minerals opaque minerals Member (predominant H/M)-63% (predominant H/M)-55%, garnet, zircon, hornblende, garnet, zircon, tourmaline, tourmaline, epidote, others unidentified minerals, others Tuscaloosa Formation VSC-4-7 (-321. 3 f t) opaque minerals (predominant (I/L 4)-65% zircon, hornblende, epidote, unidentified minerals, others VSC-4-9 (-528.3 f t) opaque minerals (predominant H/M)-61%, I zircon, tourmaline, garnet, epidote, unidentified minerals, kyanite VSC-4-10 (-538.3 ft) opaque minerals (predominant H/M)-72%, I garnet, unidentified minerals, zircon, others I VSC-4-14 (-843.3 f t) opaque minerals (predominant H/M and I/L)-67%, zircon, I tourmaline, unidentified minerals, garnet, others I Note: Heavy minerals are listed in order of abundance; minerals present in less than 3 percent are classified as others.
- 1. Core holes are arranged from left to right as they are located in the field from NW to SE.
- 2. Sample locations are designated by elevations from sea level.
- 3. H/M= Hematite and magnetite; hematite sometimes coats magnetite grains.
- 4. I/L
- Ilmenite coated with leucoxene.
I
bv TABLE CENERAL PETROGRAPN OF SAMFLES FROM % Core hole VC-7 Core hole VG-4 Core hole VC-2 Core hole VG-3 marnwell Group vG-2-1 (23.6 f t) VG-3-1 (21.2 f t) Griffins Landing Quattrose. calcareous sand Quattrose, calcareous Member well sorted quarts poorly Moderately sorted quar cemented by micrite and poorly cemented by some clay. micrite and some clay. , Utley Limestone VG-7-1 (4 4.6 f t) ** VG-2-2 (9.7 f t) VG-3-2 (6.3 f t) Member Fossitiferous sandy timestone Fossiltf erous sandy timestone Fossiliferous sandy 11 l j Large snell f ragments and Large shell fragments and Large shell fragments moderately sorted quarts moderately sorted quarts moderately sorted quar within a micrite cemen within a micrite cement within a micrite cement. l I,isbon Formation VG-7-2 (2 4.6 f t) VG-4-1 (-3.7 ft) VG-2-3 (-1.9 ft) VG-3-3 (-4.3 f t) 11ue Bluf f sandy marl Clay and fossiliferous sandy shale Sandy glauconitic marl Silty earl 1sber very fine-grained Interbedded clay and sandy shale Well sorted quarts, Fine-grained quarts in quarts and micro- with microfossils and shell microfossils and glauconite micrite, clay, muscovi fossils within a fragments. in a clayey matris; sericite matris; stron clayey matriz bedded. bedded. Unnamed Sand VG-7-3 (-114.4 f t) VG-2-4a (-131.9 ft) VC-3-4 (-134.3 ft) Member Quarts sand Quarts send Quarts sand n>derately sorted, we11 sorted, well sorted, medium-grained medium-grained medium grained unconsolidated. uncorsolidated. unconsolidated. Tuscaloosa vC-4-4 (-294.1 ft) VC-2-7 (-296.9 ft) VG-3-7 (-307.1 ft) Formation Clayey sand Claver sand Sandy clay poorly sorted quarts Poorly sorted quarts, Poorly sorted quarts and some muscovite microcline, and muscovite and some microcline an in a clay matriz. in a clay matriz. muscovite in a clay na
, 4
[d
- Coreholes are arranged from lef t to right as they are located in the fleid from NW to SE.
** Sample locations are designated by elevations from sea level.
VV
P-9 IC DESCRIPTICII F. @RE It0LES Core hole VG-1 Core hole VG-5 Cbre hole VG-4 Core hole VG-8 VG-1 -1 (2 3.1 f t ) WG-5-2 (34.5 f t) VG-4-1 ($0.1 f t) VG-#-1 (1.7 ft) ta,nd. Quartrose, calcareous sand Quartrose, calcareous sand Quartsose, calcareous mand Quartrose, calcareous sand La nell sorted quarta poorly Well sorted quarts and shale puderately sorted qJarts cemented by micrite and moderately cemented by Well sorted quarts poorly moderately cemented by some clay. mictite and some clay. cemented by micrite and calcareous to early possibly some clay, in contact mater ial. with micritic, shaly material. 9C-1-2 (8.2 ft) VG-$-3 (-14.5 f t) vG-4-2 (1.1 ft) 9G-8-2 (-10.3 ft) Fossilif erous sandy timestone Poss111 ferous sandy timestone rossilif erous sandy limestone Foss tilf erous sandy timestone nestone and Large shell fragments and Large shell fragments and Large shell fragments and Large shell fragments and ts moderstely sorted quarts well sorted quarts grains moderately sorted quarts moderately sorted quarts
- t. rithin a micrite cement. within a micrite cement. within a aterite cement. within a micrite cement.
vG-1-3 (-2,4 f t) VG-$ -4 (-10.0 ft) 9G-4-3 (-4 2.9 f t) VG-9-3 (-52.3 ft) Glauconstic, sandy shale Marl and sandy earl Sandy mart Sandy shale very fine-grained quarts Sandy material in contact with Interbedded sandy and shaly very fine-grained quarts 2 with scot sericite and material both with micro- within a matrix of clay te/ shaly material both with clay ply glsucanite in a clayey and micrite. fossils, clay and micrite. with some micrite. matrist bedded. vG-1-4a (-129.4 ft) VG-5-$ (-138.9 f t) VC-4 -4 (-17 2.9 f t ) Quartz sand Quarts sand Quarts sand Well sor ted, medium-grained, Well sorted quarts, Well sor ted, medium-grained, anconsolidated. medium-grained, unconsolidated. unconsolidated. vC-1-7 (-104.2 ft) VG-5-4 (-310.S ft) vG-4-7 (-343.9 ft) Clevey sand Clayey mand Clayey, feldspathiC sand Poorly sorted quarts poorly sorted quarts and Poorly sorted quar tz and 5 cnd some muscovite some muscovite within a feldspar with some muscovite t r i m. within a clay matris. clay matriz. in a clay matrim. w
. p
#O
(> t, 1 l 4 j' k ( i s I h L Core Hole VG-7 Core Hole VG-4 Core Hole VG-2 Core Role Barmeell Group VC-2-1 (23.6 f t) W 3-1 (2 Gr a f fins Landing Approximately lot clay, Approm Member other constituents not other determined detern C - mostly saectite A CA - trace 1111te, kaolinite trace Utley Limestone VG-7-1 (4 4.6 f t)
- VG-2-2 (8.7 ft) VG-3-2 (6 Member g - 854 calcite, Approximately 30 clay, Approm 154 quarts Other constituents not other determined deters a C A - mostly ssectite M-C trace kaolinite, illite trace kaolin r-Lisbon Formation W7-2 (24.6 f t) VG-4-1 (-3.7 ft) VG-2-3 (-1.9 ft) VG-3-3 (-
Blue sluff M - 50% clay, M - 704 clay, Approntmately 504 clay Approx Member 304 quarts, 304 quarts with amorghous material other . 204 calcite and cristoballte (7), other deters constituents not determined CA - 804 saectite. C A - 714 smectite, glag - 1004 saectite, A-C 20t 1111te 296 kaolinite trace soo11te 404 sa 1111te Huber Formation VG-7-4 (-126.4 ft) VC-4-2 (-161.7 ft) VC-2-5 (-19 5.9 f t) VG-3-5 (- g - 804 clay, M - 100t clay M - 1004 clay M-204 quarts 204 qua gig - 75% kaolinite, CA - 954 kaolinite, glag - 954 kaolinite, glag - 254 saectite St 1111te $4 saectite 108 ses i Ellenton Formation VG-4-3 (-2 41.5 f t) VG-2-4 (-265.4 ft) VG-3-4 (-: M - 504 quarts, g - 604 clay, sulk - 354 clay, 154 tot quarts 30% amu
! amorphous material 20% c14 C A - 806 saectite, C A - Set kaolinite, A-C 104 kaolinite, 254 1111te, 254 saectite 304 ill 104 illite Tuscaloosa VG-4-4 (-294.1 f t) VG-2-7 (-296.9 ft) rormation VG-3-7 (-J M - 804 quarts M - 754 quarts, M-
, 204 clay 254 clay 159 cla
)
{ fl.a.r - 504 kaolinite, A - 604 1111te, C M-C 254 1111te, 400 kaolinite 30s ill 254 saectite
- Core holes are arranged from lef t to right as they are located is the field from N4 to SE.
** sample locations are designated by elevations from sea level.
t V%
w TAB 12 7-10 2-RAY CIFFRACTION AMALYSES OF BtfLK AND C(AY SIZE FRACTIONS OF SAprLES FROM VG CORE BOLES .VG-3 core sole + 1 Core note VG-5 core nole vG-6 core note vo-e t k.2 f t) m 1-1 (23.1 ft) VG-5-1 (60.5 ft1 VG-8-1 (1.7 ft) hastely 104 clay, M - 67% quarts, gogg . 606 quarts, b l". - Sol quarts, ponstitueIts not 154 calcite, lit clay E calcite, est calcite, St clay ined St neolite, 34 plagioclas* lot clay mostly smeetite .c3 - mostly saectite g g . 1004 sanctite plag - 1004 1111te teo11:ite, 1111te trace 1111te, soolite l L3ft) vc-1-2 (s.2 f t) v0-5-3 t-14.5 ft1 vG-e-2 (-10.3 f t) Lantely 36 city, approntmately 36 clay, g . 600 calcite, sulk - 504 calcite, 304 quarts, ponstituelt3 not other constitueets not 30% quarts,104 clay Eamorphous material, 56 clay Lned determined glay,- 100t smeetite, glay - 604 1111te, 404 saectite mostly smectite clag - mostly smeetite trace kaolinite illite, seolite, trace kaolonite, 1111te Lte I l.3 ft) + 1-3 (-2.4 ft) w S-4 t-10.0 ft) VG-6-3 t-4 2.9 f t) VG-8-3 (-52.3 ft) Lantely 50t clay, su Q - 54% clay, 326 quarts, DJQ - 504 quarts, M - 690 quarts, su Q - 554 clay, ponstitueits not 6t geolite, 34 plagioclase, 500 clay 404 clay 304 quarts, 155 calcite Lned 20 calcite, 24 hematite, 14 potassium feldspar 1 6 kao1111ta glag - 608 smectite, gg - 604 saectite, Clag - 506 1111te, play - 00% smectite, wtite, trace 300 taolinite, 5t 1111te, 40s 1111te 504 smeetite 20t 1111te 59 soollte ,03.5 ft) + 1-5 (-190.4 ft) v0-5-4 t-los.5 fel w 6-4 t-111.9 ft) vc-a-4 t-251.3 fen l800 (l'y, g }Q - 1004 clay M - 1004 clay EQ - 504 quarts, M - 804 clay L ts 50% clay 154 amorntous material St quarts l904kaoliniti,
- gjal - tot kaolinite, stite St 1111te, 54 saectite g,1,a_g - 704 kaolinite, glaz - 604 kaolinite, gg - 604 kaolinite, 304 smeetite 404 smectite 404 enectite -
l59.3 ft) VG-1-4 (-264.4 f t) vG-5-7 t-242.5 ft) vG-6 -6 (-304.9 ft1 Set quarts, M - 65% quarts, 356 clay au)g - 706 clay, E Q - 554 clay, ryhous material 304 quarts 454 quarts Y t 404 kaolixit:3, glag - 40t kaolinite, gJlg - 804 kaolinite, gla,g - 754 saectite, ,ite, 304 saectite 3061111te, 300 smectite 154 1111te, 56 smeetite 154 1111te, 104 kaolinite
.1 f t) . E -l (-306.2 ft) W 5-8 t-310.5 ft) VG-4-7 t-343.9 ft)
- t quarts, g }Q - 70t quarts, g)Q - 604 quarts, E Q - 604 quarts,
.., let fildspar 306 clay 404 clay 40t clay 700 kaolititt, glar - 706 kaolinite, glal - 754 kaolinite, gaz - Tot saectite, ite . 300 1111te 254 smectite, trace 154 kaolinite, 154 1111te l& lite i
-W%
l t. l 1 i Core hole VG-7 Core hole VG-4 Core h( l Barewell Group VG-2-l ' Griffins Landing opaq Mest er (pr# silli kyanj min $ tisbon Formation VG-7-4 (-114.4 f t) VG-2-44 Unnamed Sand opaque minerals opaq Meneer (predominant N/M)-584, (pro ( garnet, hornblende, kyagarnet, gar # a11anite (7), other e hor # glad mind Tuscaloosa Formation vc-4-4 (-294.1 ft) VG-24 opaque manerals opad (predominant 5/MI-454, 5/M) < garnet, strean uni $ othet ? ep1C Mote Beavy minerals are listed in order of abundances minerale present in less than 3 % as others. i
- 1. Core holes are arranged from lef t to ri@t as they are located in the field from NW t@
- 2. Sample locations are desipated by elevations from sea level. l
- 3. M/M = tematite and magnetite hematite sometimes coats magnetite grains. .
- 4. I/L = 11menite coated with leucomene. I l
l l l
\
l
es TABLE 7-11 HEA*tY MINFRAl. AMAl.75ES OF MAMPLEh FROM VG CORE HOLES le VG-2 Core hole VG-3 Core hole VG-1 Core hole VG-4 Core hole VG-8 123.6 ft) VG-3-1 (21.2 ft) W-1-1 (2).1 f t( vG-8-1 (1.7 ft) e t_aner 12 opaque minerals opaque minerals opaque manerals (predominant n/M)-634, ominant r/r)-444, (predominant N/M)-274, (predominant N/M)-514, manitS garnet, tournaline, kyanite, garnet, sillimanite, kyanite, streon, garnet, sillimanite, sitcon, garnet, strcon, rutile, tourmaline, hornblende, t ;, epidoti, unidentified at:t, siccon, others unidentified s inerals, unidentified, minerals, epidote, sillimanite, epidote, others tournaline, hornblende, others epidote, others t-132,9 ft) vc-3-4 (-134.3 ft) VG-1-4b t-130.4 ft) eLaner:1s opaque manerals opaque minerals ominant 1/L4 )-584, (predominant (H/M) 4 34, (predominant 1/L)-574, t, sitcon, tourmaline, epidote, garnet, garnet, hornblende, tende, epidote, tournaline, others epidote, unidentified onits, anideitified minerals, aircon, et, 6 thers glaucanate, others (-296.9 ft) vC-3-7 t-307.1 ft) VG-1-7 t-306.J ft) VG-6-7 t-343.9 f t) es (predominant opaque manerals opaque manerals opaque minerals 744, tournaline, (predominant n/M)-4 34, (predominant M/M)-424 (predominant N/M)-414 ntified Linerals, unidentified einerals, staurolite, 31roon, epidote, hornblende, te., Ether 3 rattle, tournaline, epidote, rutile, unidentified sinerals, sitcon, hornblende, unidentified ninerals, sitcon, tournaline, epidote, others tournaline, andalusite, pyrite, others other s cent crs classified St. 1 m .
TABLE 7-12 RESULT OF BASEFLOW ANLAYSIS BY USGS w ~~ Drainage 30-Day Unit River Station Area Q2 Baseflow (Mi2) (cfs) AQ/AA l i Augusta 7508 6300 0.74 Savannah Burtons 8650 7150 i River Ferry Br. 0.23* Clyo 9850 7540 Louisville 800 170 Ogeechee ^ River
- 0.17 Scarboro 1940 360
~~ 0.11 ~' Eden 2650 440 F l Montmorenci 198 117 S.F. ~' Edisto i River 0.46
- Denmark 720 358
- The flow contribution from Brier Creek (at the Millhaven Gauge a drainage area of 646 sq. mi2) was subtracted from the flow at Clyo before the computation.
a w W w
[: TABLE 7-13 IESULT OF UNIT BASEFLOW ANALYSIS Savannah River l Ogeechee River S.F. Edisto R. Augusta- Burtons Burtons Ferry Br. Louisville Scarboro Montmorenci
-Denmark Y ar Fer ry Br. -Clyo R -Scarboro -Eden R 1941 0.72 0.83 1.16 0.13 0.03 0.23 0.39
[- 1942 0.54 0.54 0.99 0.12 0.09 0.75 0.35 1943 0.73 0.46 0.63 0.21 -0.05 -0.24 0.63 1944 0.85 -0.16 -0.19 0.16 0.02 0.13 0.44 [- 1945 0.56 0.52 0.93 0.17 0.13 0.76 0.48 1946 0.60 0.28 0.47 0.15 0.08 0.53 0.36 1947 0.58 0.34 0.59 0.20 0.11 0.55 0.47 0.81 0.20 0.29 1.45 0.49 ( 1948
'1949 1.04 1.48 0.84 1.64 1.11 0.32 0.25 0.78 0.78 1950 1.27 0.62 0.49 NA 0.18 - 0.64 1951 0.80 0.98 1.23 NA 0.23 -
0.47 1952 0.41 0.75 1.81 NA 0.17 - 0.41 1953 0.60 0.39 0.65 NA 0.15 - 0.42 1954 0.56 0.04 0.08 NA 0.26 - 0.46 1955 0.80 0.77 0.97 NA 0.05 - 0.30 1956 0.57 1.00 1.75 NA 0.11 - 0.43 1957 0.18 0.68 3.71 NA 0.06 - 0.28 1958 0.25 0.07 0.28 NA 0.18 - 0.28 {- 1959 0.06 0.20 3.21 NA 0.04 - 0.36 1960 0.38 0.56 1.50 NA 0.29 - 0.46 ) 1961 0.50 0.43 0.86 NA 0.04 - 0.71 [- 1962 0.68 0.23 0.34 NA -0.01 - 0.53 1963 0.71 0.79 1.12 NA 0.02 - 0.61 1964 0.74 0.89 1.21 NA 0.13 - 0.41 1.14 0.18 0.88 { 1965 -0.02 NA -
-0.03 1966 0.81 0.62 0.76 NA 0.13 -
0.92 1967 0.90 -0.38 -0.42 NA 0.16 - NA ( 1968 0.82 0.34 0.41 NA 0.01 - NA l [- 1969 0.81 -0.30 -C.36 NA -0.01 - NA 1970 0.69 0.13 0.19 NA 0.31 - NA Remark s: [ (1) (2) Flow contribution from Brier Creek was subtracted Tabulated values are unit baseflows in cfs/mi2 R is the ratio of downstream unit baseflow to upstream unit baseflow (3) (4) NA indicates not available due to lack of corresponding streamflow data [ E [ [
~
w r~m . v 2-m m. m r~m ; . r-m v m m r~ r~m m_ m r-m 'em TABLE 7-14 LOEST 30-DAY LOW FLOWS (CFS) River Station Year 1941 1942 1943 1944 1945 1946 1947 1948 1949 Augusta 2670 2300 3730 3560 3560 3770 3630 3190 4650 Savannah Burtons 3490 2920 4560 4530 4200 4450 4290 4380 6340 River Fer ry Br. Clyo 4180 3370 5060 4650 4750 4750 4730 5110 7670 Brier Millhaven 228 153 247 209 261 146 252 '264 421 Creek Louisville 288 143 200 155 218 118 157 224 424 Ogeechee Scarboro 436 274 439 338 141 294 389 456 794 River Eden 460 341 403 349 507 354 469 662 970 Mont- 96 77 145 116 106 106 118 124 185 S.F. morenci
- Edisto River Denmark 297 258 472 347 359 295 361 380 591
Q _ m 9 5 3 4 8 6 7 9 8 t o i i 3 3 6 4 4 3 4 4 7 c n s ir d e n ek2 m 0 0 0 0 0 0 0 0 0 Evi r r5 oa5
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- n. R 3
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~ A e aE 4 7 6 - v c A 0 2 6 3 1 9 6 8 0 7 f E i S - A - 2 1 T R S
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)
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+ ESTR.L GRID IS 10.000 METERS UNIVERSAL TRANSVERSE MERCATOR LATITUDE / LONGITUDE SHowN SY
; TIC K MARKS.
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""' d " Ie __ REGIONAL MAP OF DRILL HOLES "y.N-8 I AND WATER WELLS o-o O ,
g FIGURE 7-l t , x"? _. s ,, ,f'5 $'$ _ _. _ _ _ _ _ _ . _ _ _ . _ . _ _ _ _ _ _ _ _ _ _ _ _ _ . _m _ . _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _
g-NOTE
- From: Report on Seismograph Surveys
/.// i *
/,/ Conducted in Bornwell, Aiken, and i
Allendole Counties, South Carolino
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by Seismograph' Service Corporction (1972) . g *
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.J O I 2 3 4 5 EXPLANATION -
SCALE IN MILES Numbers indicate reflection lines Letters indicate interpreted faults BEttTEL of the top Triassic VOGTLE ELECTRIC GENERATING PLANT Foult direction indicated by U(up) POSTULATED MILLETT FAULT and D(down) SEISMOGRAPH SERVICE CORPORATION REFLECTION SURVEY OF THE Of fset indicated is for the top Triossic , SAVANNAH RIVER PL ANT in feet; SG=Slightly greater thani FIGURE 7-2 P= Possibly 1
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@ Landsat satellite image b 2 / 11 / 7 4
~/ @ Landsat satellite image ORANGEBURG
%.\ @ Low ottitude block and white Y oerial photographs 12 /16 /69
@ Low oerialoltitude block and photographs 5 / 8white
/ 5:
l pg7p g \, MILLETT FAULT @ False color obilgue U-2 i K.% oerial photograph 5/1/79
#* N # I N , Barn:cIl 1 h ,.
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SCALE IN MILES HAMPTON
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BECNTEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT LOCATION MAP OF REMOTE t SENSING IMAGERY w FIGURE 7-3
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NORTHWEST P5R VSC-2 VSC-3 VSC-1 EL.207.9' EL.201.7' E L.170.3' EL. 219.( 300-200 - ' % \ 100 - I 2
,1 i f2 --
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- 3 - -._
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l o 2000 4000 6000 I HORIZONTAL SCALE i VERTICAL TO HORl; l j EX AGGER ATION 21 v% l d -- - _ _ _ _ _ _ _ - - _ _ _ _ _ - _ - _ - - _ _ _ _ _ _ _ _ _ _ _ _
SOUTHEAST AL-66 VSC-4 i EL.156.7' _300 (cff section)/
-200
~3 BARNWELL -10 0
/I " GROUP
/
2 , SEA BLUE BLUFF -LEVEL MEMBER LISBON
- UNNAMED FM. -100
-_ _ , , _ /,4 [ MEMBER 5 HUBER FM. -200 w
/6 q w L
ELLENTON FM. f7 -300 TUSCALOOSA F M. 2
--400 z fl
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2 , 11
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- --600 w f 12
/ 13 --700
--800 f 14
.. s
--900
--1000
--IlOO poo BECETEL
'IN FEET vocTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT ONTAL LITHOLOGIC S AMPLE LOCATIONS o TO I AL - 66 AND VSC HOLES FIGURE 7-6
- m. n NO RTHWEST VG-7 VG-4 VG-2 VGl E L. 2 5 0.6' E L .150. 3' E L . 253. l
- EL . I' POSTULe MILLE' 300- FAUL' 200- ,
BARNWELL \ 100- GROUP
'l '
SEA ,2 -- % ~~~ 'i<2----- LEVEL- /I LISBON - W FO RM ATION ' ~' -- -- ~ ' ' ' ~ ~ ~ E - 100- ~ ~ - --~ ~ ~
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2 z .. 200_ HUBER _
/----__
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b_ _ _ _ _ FORMATION _ _ _ _ _ _ _ _ z / 3-. ELLENTON AND
- ' ' 'O-----
o - 300_ f4 ' F TUSCALCOSA
<t > FORMATIONS ==
j w - 400- ,, W
-500 -
-600 -
-700 -
-800-0 2000 4000 soc HORIZONTAL SCAL VERTICAL TO HO)
EXAGGERATION t
I P i l SOUTHEAST l VG - 1 VG-5 VG-6 VG-8 EL.156.6 E L . 94. 5' E L. 217. I' EL.lO3.7'
-300
-200 r
/1 /\
-10 0 2
-- Ie2l - - _ __ __
I3 _ __ _ _ --_ _ 42________________ /[
, SEA 3 4 /3-----__________ ,3 -LEVEL h -- - - - - - _ _ _ _ _ _ w l______ g4_a __ __ __ ~ ~ ,3
- - - - - - _ _ _ _ _ . _ _ _ __iOO l 4b
' 5- - - - - - - <6
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2
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-- 600 l
-- 700
-800 20 10,000 LFEET
$TAL BECETEL TO I VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT LITHOLOGIC SAMPLE LOCATIONS-VG CORE HOLES FIGUR E 7-7
{ se S AMPLE AL-66-1 SAMPLE ( EL.-468TO-478') ( EL - 558 IOO-Nx 90-
@ W O
l b 80- Z a O 70- N s z GO- 4 O 50 - 8 5 E o- a. 40- - 30 - o w b s 20- $ W z 10 - O I-g MINERALOGY OF CUTTINGS FROM W 5 5 o sO- N 8 W >. x -
< h I J kJ 40 - J O e d w a s x z 30-- $ N 0 g 5 5 20 -
e x s 10- l 0- _ MINERALOGY OF CORE SAMPLES F
.; y
=
. 1 s-
; ^
!, c . ' z. _ e
' ' ~
A / , i. . f0 L-66
-368 ,)2 ,.
-10 0 ~.'4 . -
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- q. -
b # z - so +., 2 J , o
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x -- 80 .' . +
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- a. z , ' .- _ . +?
- g w -+ ,.
p 4 - 50 o . , 4 g 1 ; i .- d W z $ ;. . s j _ 40 NOTES: . 1. 2 W I . The mineralogy of water well .<' ; _ .' t - z W F b samples AL-66-1 and ~
< H - 30 s.
.v. -
< AL-66 -2 were determined - ~ ; .[ ~
2 by Dr. Parnell, see App. I g D W
- 20
- T. V* f m I 4
^y. ,- . ' .
+
- 2. The mineralogy of core I
' samples from DRB 10 were h_
- #3'.' -
_ io determined by Marine , I .W. .' , , '
- _
1976; percentages based on ~ . , .. * ,- samples collected between I . .. .~)~
-0 25 to 150 feet below the '; -
upper Triassic contact. # TER WELL AL-66 l.- f .<,TS,
,,.4 . *
~ ~
- so
?.h '.,' y% ; . .-
p p , g.'
'g '
4 4 - 40 ~ y g . .. ' J
.3 O O e ? ; . A W W H
- 30 $w 'i. ~'
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t z i- g ..- '.: ,: ; . ~ g g O o W - 20 W ' *- '. o 2 a. W < M .'i, N M j -
-e
~
BECRTEL 4'
....r. . .
l g N JGTLE ELECTRIC GENERATING PLANT ,.
, ']] 1 POSTULATED MILLETT F AULT '~ t
- ,~ '* t '-
90M DRB 10 MIN E R A LO GY OF SAMPLES T'l.- 1 FROM AL -66 AND D R B 10 4 5 7'
; cc t- .
FIGURE 7-8
-]. -
.~. j
, , m t
_ . ,w *.'.- a , m..
I
%w
, 8/2/74 11/2/1875 -
mr G
, II/5/74 IK .
7/29/43 2E O . VC PL i en v% -Q : _ _ - - _ - - . _ _ _ _ - . _._.__L.-..._.._ _ __ _. - - - - - -- - - - - . _ . - . _ . _ _ _ _ _
s4' EXP L AN ATlON Dates of occurrence and 4/2 /64 modified Mercalli intensites gj j73 7/2 /45 g Q are shown by each epicenter SOURCES Reagor, B.G. Stover, C W. , Algermissen , S.T. (1980) Stover,C.W.,Reagor, B.G., Algermissen, S.T.Long ,L.T. (1979).
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GTLE
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M* SCALE IN MILES
/ O SCALE IN KILONETERS O
,/
/ BECHTEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT FELT EARTHQUAKES LuftEs ooo xtt
- 190 0 -1974 FIGURE 7-9 T t a " V StZt
./
83* 82* 81* 80' 3 5 k
/ l
\$ SOUTH C AROLI NA O
34o- hHoratio U'" O O OO O O OO O gNorth eSi mmerton O O O O AugustaC Springfield 8 O ekordoaOo C>o ( O Oe o eBarnwell O BCE O VOGTLEg & 33a _ PLANT O l O g O 1 O Charlestoni 1 GEORG IA 0 N g Mo b s .' O 32'
?
O O EXPL ANATION SCALE IN MILES 9 Felt Report BECETEL O Not Felt v0GTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT
% Epicenter taken f rom Reagor et al. (1980) FELT REPORTS AUGUST 14,1972- EARTHQUAKE FIGURE 7-10
84* 83* 82* 81* 80* 79* 36* 6 A
.. s -- -- - . .
g A 3s'-- 34' \ ' SOUTH C AROLIN A A l VOGTLE PLANT dA [ 33- A 4- / GEORGI A ka , A- g: f y/
\,
2- <
/ N 2 ,. /
32' ( W
^
n} o
} <
r '
- i o 25 50 75 10 0 NOTE: SCALE IN MILES Principal regional seismograph stations in operation during the interval 1974 to the present.
Most stations were not in operation during that entire interval but the pottern shown is representative of coverage of ter the early port BECETEL of 1977, VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT SOURCES: Bollinger and Matheno (1981,1982) LOCATIONS OF SEISMOGRAPH Rhea ( 1981 ) STATIONS FIGURE 7 - 11
A .#,. t at
. O O
O O 9
- 8 4
# 4 e
9 k i i l
\
l l t
O 34' E X PL AN ATION e Recent earthquakes near the site. All events are small (overage magnitude about 2.1 and none larger than 2 Blond G shallow (overage depth about S 4 miles or 7 kilometers). SOURCES B ollinger,G . A.ond Murphy ,C.A. 8 (1978) Bollinger,G. A. and Matheno
# E .(1978- 198 2 )
Rhea, S. (1981) Torr, A., Tolwani,P. Rhea, S. ge Corver,D. and Amick,0.(1981)
- N
/
+# \
VOGTLE PLANT y j
%w-f
,p' *% .
p ssa e 2 / im /
/
2 / A/
$.I#' O s
./
SCALE IN MILES O 10 20 30 40
;f, SCALE IN KILOM ETERS 8 l'
' BECHTEL j
+*
VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT WE LL- LOC ATED EARTHQU A KES u E"' 1974-1982 . J2.s FILES tioo x1 FIGURE 7-12
c% 82*
\
2 e
? '
SRPN y n. I
?
SRPW 38 [ SRPD V0GTLEh, 6 o #' A3 ,, 9,], 33" '#,
# %h esd' I
G EORGl A 9*
/
82' wm, _ . _ . _ _m_ . . _ _ ____ - - - - - - --
m 81' EX PLAN ATION
\
,- = Distance range shown implies Sg- Pg times of about 3 to 8 seconds using
/ the Kean and Long (1980) crustal model.
/
SOUTH C AROLIN A
# 33 N
#~
b 52 4 4) s os
#' o 5 to is ao SC ALE IN MILES f s
\
81 BECHTEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT SRP SEISMOGRAPH ARRAY FIGURE 7-13 I
26 - - 24-22 - 20 - - 18 - m - l-Z 16 - p 0 14 - E o - e 12 - d - 5 - g - - !z iO - g m sa. 8- - z 6- g 4- l 1 - _ i _ i __ a-O , .. O 20 40 60 80 100 12 0 14 0 16 0 180 200 220 240 260 DISTANCE FROM SRPN(KM.) SCALE BECETEL l KILOMETERS 1 VOGTLE ELECTRIC GENERATING PLANT I O O POSTULATED MILLETT FAULT l MILES SEISMIC FREQUENCY vs. I DISTANCE FROM SRPN l FIGURE 7-14
P ' e, o
*1 Montmorenci l
9" 8 t>enmark Thomson 8'
#+/e , VOGTLE c#, PLANT ,,,,#
Burtons Ferry Bridge 9, illhaven s' Louisville O v +9' s 9 84 v Scarboro 9 ' O 1 0 9, Clyo 2
#e m c+ep
- 1
& Goging Station
#+ Eden BECETEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT LOCATIONS OF STREAM GAUGING STATIONS FIGURE 7-15
._.--.=
l
.-------s RECORD 1930 1940 1950 1960 1970 1980 SAVANN AH RIVER sAUGUSTA 'f -
I BURTONS FE R RY : ilR ID G E 8 CLYO : BRIER CREEK THOkSON : I MILL H AVEN OGEECHEE RIVER
- LOUISVILL E : :
ISCARBORO : IEDEN : : S.F. EDISTO RIVE R IMONTMORENCI : ! I DENMARK : l l ! 1 l l ! l i
- BECETEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT AVAILABLE STREAMFLOW RECORDS FIGURE 7-16
MEAN OF COMPUTED UNIT BASEFLOW(0.69) YEARS n _1970 m - m _1968 e _ m _1966 m _ i a _I964 i a _ o _1962 i a _ e _1960 , a _ l e _1958 > e _ a _1956 m - s _1954 , s - e _1952 m - a _1950 m _ m _1948 s - e _1946 a _ s _1944 m _ m _1942 s _ 1940 o o o o o o o o o o 9 O. 9 9 9 m - o - y UNIT BASEFLOW (cf s /sq.mi) BECETEL EXPLANATION VOGTLE ELECTRIC GENERATING PLANT Mean computed unit boseflow POSTULATED MILLETT FAULT E Computed unit baseflow SAVANNAH RIVER UNIT BASEFLOW CONTRIBUTION UPSTRE AM RE ACH FIGURE 7- 17
. - 2 yMEAN OF COMPUTED l' NIT BAS EFLOW(0.47 ) YEARS e _1970 m -
, _1968 a -
e _1966 m - m 1964 a _ e _1962 m _ e _19 6 O a - a _1958 m _ m _1956 s - a _1954 e _ a _1952 m _ a _1950 m _ m _1948 s - e _1946 m _ m _l944 il _ y _1942 e _ i i i , 1940 0 O O O o o o o g 9 Q O O-9 n - o N I I UNIT B ASEFLOW (c f s /sq.mi) BECETEL VOGTLE ELECTRIC GENERATING PLANT Mean computed unit baseflow POSTULATED MILLETT FAULT f SAVANNAH RIVER i E Computed unit boseflow UNIT BASEFLOW CONTRIBUTION ! DOWNSTREAM REACH FIGURE 7-18 I
o
=e
/s , AUGUSTA
/
- ~
b, ' O RT GORDON O N. gy8 4 k
,,4 e
213 15 8 4 188 9.' ho 4 4 126 206
/ Ell ,94 ,
14 6 ,151 % I 4 Ok e gWAYNESBORO #l96 bfS 197 19 4 Ii
%I o *g
\ 202
'210 ## 18
#s 161
+#
203, 20: j y 217 r .c, . -
/
- !4 III
, i72 177 ,
I,./, ' "'s 0
,- ,,, *!72 i5y58 MtLLEN e
16 8, / g0
\'N./) ,
161e 159 *l46 gg 0
.is7 seo \ l
,s <( ,$ rxx
,s.q/
,,/
, x ,
, ( /
/ -
/
y *T
/
/
A .s I
+ '
EXPL AN ATION sca eLtenTow (og \ p h@# dW'LLISTON f # N contours showing r N ' 16O hetacx Ltc kFg water level elevation (feet) 15 5 '
/ '
c, dDENMARK
$ 4g
- Control point with 5 # - 2 elevation of water 176 '
#' E level (feet )
/I,17 0 ,# . ann,gte SRP g-{'# 16 l f5GTLE ,, 60 ,! 'lANT f,, \ ' %h3 *f' ' N g g gstg - - N p-a.,y ,_. .,,, i33gatttuotte f 162 135 # 13 6 <
/
(./ i# -
'48 c \
%,kv I/
y. g -7 i k, /\ O j g J'
/
/
gmvm. f. Oismo / g.- p j' / _ BECHTEL m/ [ x VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT E POTENTl0 METRIC MAP OF TERTIARY (UPPER) AQUlFER
. ( MAY- JUN E, 1982)
FIGURE 7-19
w~ / \
/ T
/{. A""""^
4be, ,.7' FORT GOROON
,y
'e')
220 iso
,1 %s> ,
25
/43
/ Sy , J23
$*' '(, [b \.
/ ~ /' % c- .
I 240 1 Trs I 8 0 V0GTLE PLANT
$'$ W AY NESBORO g= 195 [93 19 6 e
).
am.<,- sf - l - -
/ '
/
/
N (-./.4 5
~ . ,. p g aN ,i
's..r' /
l
\
\ l
(#Y~gg:Pt s l g,,-Q~., ey t i 1 .-
) /
( s
, /
/ '\_n l
~
b/ g6 336 ^- l
** / 0 NEW ELLENTON ~
f a r evel e vation ( M gy,tt, b 210 . o ( ( feet ) N ,% 2ir doca =^= l / 19 5 g 4g
- Control point with J70 n4 SRP '
'!m elevation of water y *l76 ,.* 20,5 level (feet )
/ 173 p. . BARNWELL
/ #
t'
,,,. #' 800
[(*%e(g s 15 6 16 # e'/* 15 7 16 4 '%---- '__h
'\ '
1710 14l g.
. *e s\ o
, 1 23 \* 157 AttENoALc f ,
. 4 13 8 'p s \ f N\
%,% g,?*o
/\
e* o QSYLVANIA
%:Oh5
, STlLL p [' / 3 o s o
, sc u e m mees 8*
.~
/
8, j' / 5- # BECHTEL
/
4%
/ '
VOGTLE ELECTRIC GENERATING PLANT
/ .
POSTULATED MILLETT FAULT POTENTIOMETR;C MAP OF CRETACEOUS (LOWER) AQUlFER
. (MAY-JUNE,1982)
FIGURE 7-20 s
W 0 D" 144 g l 1 r , [ 60 ll 9 uS D
% EY ~' '~'$. s
?.
/ ,"
,J 1% i ; ,,. I SRP tt
'" ~ .,,\:e:w 9 e o..~s. .
% . c ,. $g ,'g 47,, pa
,,;'.e(,,4,. 'e N
,.Y \,,,,' ; ,... :
5 *iss i36 issg j g ALLEPOALE
,, / '*
t o 200 / ,,.*, j
'OS O / $CALE sh WLES 0 tithe,fy COMPUTER CONTOURS 0 c.,tLisroN 0
.... \ \U I
/ .14 8 \
{
'E .Oc
' 8M
\s /
** BARNWELL
#8e p
,80 .f ,4 ** '
,7[MO
,. s . . u ,. ,
- u. d . *,u e
'*; .y, , . RP 2 61 46s.As's
' N----so
.o " SNM>c% . ,,',3, heAYNEsBORO 6196 .\ 3,4 d" .,u .
# iyR
.202 161.g ,.
.f61 1s4
' 25* *.
.,p ' ,,,, i3s isig j 13 6 ARE N
/' "o
'ho /
is,
'\ m
.... ' Aso entC,
,7,*o
% h
( $ca's a u INTERPRETIVE CONTOURS BECHTEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT COMPARISON OF COMPUTER AND INTERPRETIVE PIEZOMETRIC , CO NTOURS -TERTI ARY AQUIFER ; FIGURE 7-21
+
A N
- P SA *b VOGTLEg (4 Y,+
o'# h PLANT VSC-2 ,,o' $
's VSC-3 B%p ,ys'[_g- O AL- 40 I s o#' VSC-4 A' VG-7 VG-4 . #+'
VG-2 VG-3 5 MILLETT G-1
'# VG-5
/ -
O VG-6
,,O E GlRARD gl Og
,,,o vG-8
- e sO y EXPLANATION $j h y{ $ Drilled for this study-screened in upper aquifer Y mQ am ,)y
<g r-
, Q Drilled for this study-screened in lower aquifer 5 r0 mz m l g 5
- O ,, Other drilled boring or well screeneo in lower aquif Z
y m mo i: m A
-4 0' m b d Location of water level profile n p p
to ro rh m --i >nz3 O i 2 3 4 5 N mm
?O m q , *f SCALE IN MILES , i 5 h t
f
. DOCUMENT ~
s PAGE . PU _ LED
. ANO.wus- l ND. OF PAGES / ,
l REASON l DPAG!LifG32, ! O MA4D COPY Fu.ED A1. PDR CF OTHER D SDTER COP (REQUESTED ON - 3 1
'A3,1100 LAlot to Ftu Jitpecoa<msbm. poR OTHER hLWD ON APER 10RENDGODD4% CARD NO 8 i
~<~.....~..,,,_
J es.m - 1 I A POSTULATED , MILLETT FAULT
~
P 5A VSC-2 VSC-3 VSC-1
~
~ -
200 - le3 G ,
~ .u27- < - -
nne7 .\_ mag 10 0 - 1
; Sea Leve/ - BLUE CLUFF MEMBER ) - --
UPPER AQUlFER
-100 -
m N.
N mum N HUBER - ELLENTON FMS.
-200 -
F % % d u - *------.% % E LOWER AQUlFER z 9 - 300 - U W Y -
-400 -
b/
/
L o 2000 4000 sooo
, HORIZONTAL SCALE IN s
VERTICAL TO HORIZOP EXAGGERATION IS 40
-750 -
M
L I 1 AL-40 $ 6230's 4or)
- VSC-4
- 200
^
s _ jV EXPLANATION l I VSC-3: Well number
- !OO _
s
*02 --
~
Water level June-July,1982(where level is above top of well, measured with pressure gouge).
- Sea Level
- ~
~
- -80 0 E Monitored interval
-- 200 w
W
~
~ l- ~ z 2 _- 300 9 m D Z t
-- 400
~
='
-- 650 ET RECETEL VOGTLE ELECTRIC GENERATING PLANT POSTULATED MILLETT FAULT
--750 WATER LEVEL PROFILE SOUTH CAROLINA
f
, .D ; UNCONFINED
. ;, .. . . n CONFINED ,
e 3
^
*/
f % g : { }E .- - . .
' n .
1 3,.- .
- - .Ap# )( w :
,y N q ^'$s-- f MM r m '
, _____ Q
._ - . -,- 3 -
=
- g. .
"7
>n?y,~ t s
L-~ L - s 1 g gg G- 3 - w%p [1.+ r _. __ _.-
-] 4
. y_ p 2-w -
-g -
_ _~ .Laweg,. . 4' CONFINED: pn# _] ' x}
; ._,. ;-j,[Rhi-Q,
.. .j k'- Iy k h-,
-[ [ -i > -
N _.- 3 4- i' %. a_ ,
! _ . L r'~ z . t , q.a -[r w .-..:F j d j [ . i L i 4. b j; h. - -
.-t ' #, - . . a -- - 'g - - ,}. .,f
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_a.- j . - j. p)+ _j 'I ....+4.- t x.
..,'l;
~~~ r
[...- -Q;
~}.L 1};[; ]~ i ; , ;
, ! g 11: ,i;.;
l l;
- l l j Q ~' K'M' x;
' 'x
- _- f.- 125d.,-r I b.. J ",*t " t ' I U. ~ ~ . .
- w
~ .
-+--
i;. t _.. x ;!
- i, Ij , 1
.; ~~
r - . _ ... -
, - - ; ~_ . _ _ . _. .--;- - -
- - - t 1
N, - I
, i *
, , . _ l Y l
;-- i ! . 4 _.. , : ~
- 1
(_ - - " i .._ _. _ _ J! _ . . t t : T 7 . -s' s-
.~j -
i [
! i 4,_ m ..i
. __ i . _ e . .
i ' '~_ ~
'I
/
I EX PL A N ATIO_N i The aquifer thickness increases f rom f North to South as indicated by the l dif f erent colors. BECHTEL VOGTLE ELECTRIC GENER ATING PLANT POSTUL ATED MILLE TT F AULT FINITE ELEMENT MESH FIGURE 7 25
== a 1
i 1 '.i l l 1 a i I
.i a
W %d
- - - - __ - - ^ - - ' " - - - _ _ _ _ _ _ _
+w 15 0 14 0 130 12 0 l10 10 0 90 80 70 F!,'UNG BED I
.\ s Nd
"'" '.,, h m . ...... QM ,
S TRE AM/ - - ' A' I
/
\
- f 15 0 14 0 13 0 N 12 0 11 0 10 0 90 80 70 3TE:
ititude of water level in feet. EFERENCE: BECNTEL sGrand and Pettyjohn (1981) VOGTLE ELECTRIC GENER ATING PLANT POSTULATED MILLETT FAULT SCH E M ATIC REPRESENTATION OF LEGRAND'S HYPOTHESIS FIGU RE 7 - 26 i i [
I M
/' i q
v
"" N
\ o
# o' p /y2
/
220 18 0
-2 0 VOGTLEr,- - Q#s' p PLANT L_ A Y,p*
o seo
]l 4p,Y e ,g.:##'
,s eo j$
N ft,? / #o e O 9?#
/
- i O 10 20 30 2""
SCALE IN MILES BECETEL EXPLA N ATION 200 Potentiometric Contour VOGTLE ELECTRIC GENERATING PLANT (Contour Interval = 20 f t.) POSTULATED MILLETT FAULT S ACE LE R A DS H HSS (BASE CASE) . FIGURE 7- 27 o
22o N
)
J*f # 200 " VOGTLE _ PLANT g,)0 22o [ 220 \ g L__ ,
/
f i ,0
~*' </
7 ,,o FY# 0 , so .~
@0 g$'
a.
/
+ N y# n
/ o i
0 30 SCALE IN MILES EXPL AN ATION K= Hydraulic Conductivity of the VOGTLE ELECTRIC GENERATING PLANT B POSTULATED MILLETT FAULT Postulated Milleit Fault as a Barrier.
~200 Potentiometric Contour (Contour Intervol= 20 ft.)
CggD POTgt TigT}lC HYPOTHESIS ( Ks =100 f t./yr.) i, FIGURE 7 - 28 u
;1 i r'
if j ' ~ ,_
#20 f'
1
% '# 200 ~
j j p
~go %@ VOGTLE (c 480 /
F 1 PLANT L_a 4
/
l # 58 4
/
/
160 s[ # 4<'/
@ c,S -
<d'r$*'
0 l
/ /
i1 l 0 10 20 3o I SCALE IN MILES EXPL AN ATIO N BECETEL K= Hydraulic Conductivity of the VOGTLE ELECTRIC GENERATING PLANT B Postulated Millett Fault as a Barrier. POSTULATED MILLETT FAULT 200-- Potentiometric Contour C g g EDBAR lEb U (Contour Interval = 20 f t.) HYPOTHESIS (KB = 1 f t./yr.) FIGURE 7-29
l ( _ _._ .. ..l i
,D_. 7 4 i
_.2
; UNCONFlNED ,
. ..- , _ I_ _ . +i _ -. i
_ __ - .. .! -.300 -
.e .e . ,i .i ;, i, ; ;
) 1 /- tv ' N l CONFINED l' .g 4 .'..
i al
~4. -l - t._ ,r
///l /.-._ m N~
! i :-1'.i___r +11--.& P1- 1 +fx j ,
< p y --Q g-, g mp-- g w, i
- 2 . 11-v ~
4 3lMth]~[L'p ^ QE
, 1 y' ;"'
v =, c-qp,' /a 3
. son, -
-M -
w;~~'a - G' w/ w-- -)Q .
#7 A* .p.
y ; ' . ,
=,c Q, , #M CCNFINED 1 : L .- - t - i tl l !%
+ _- .-t N. M
- ' ii"g . - p . -- r 4 ~ j_&+; T -*~ _'m %,_,
- r. , .
J
' y(s- ~, },, . +p
-r- (L, J[ /
p - p a ( jjilogoD ! _,;L t : CONFINED p, ! ( _.__L - gg :ji . - L +g *-- -: r: 2.gt 3 - +7 + j7,iL;Pt--[ [] x;w', 4 i i
- n - . . . - . 9c :* p y. . ..;.
zu- 3;; g t qqx -__7N y gpg4 ~*'T 009W N 3 1<.:s. - QQ
. .. '4
, 7 ].q wl..1 -l-'j ,, . ._,: T;., %fN y . A 1 A ; ,.-L- . - . . ,
~N
,. 7n y ;;
~!
71 _
~tEl ; p .3
--t
-p-a-.-. N -
- 4
- 7 -C.y y _
- m. ; ';_
p- .. -flocot-- Ty; l j
./ _ f,/ky{ \ --
; ~-. ,
7 L_ -
~
.~ ~ ~ w; p/j /' / - -- w 1250' N. ]
/
/ / l ! ~
N j w ._ w N',NN
/ - - ..
- I ;
'/ /- ! :
f - m- i 1-+i~ xj
's
._d __
t __{_ ,,T-.1. }. g L.. L._I _ .p l .__1 . h
. . N h'
/
! J
/
E XPL AN ATION The aquifer thickness changes as indicated by the dif ferent colors. BE0HTEL VOGTLE ELECTRIC GENER ATING PLANT POSTULATED MILLETT FAULT FINITE ELEMENT MESH FOR THE REDUCED TRANSMISSIVITY HYPOTHESIS FIGURE 7-30 ____ _ _ _ _ _ . _ )
o h 3 i
% '!eo A
9t$'/ st 21 r VOGTLE ,#' L__' PLAN ,# 1 4U 200
'~
$~ ~ ,,$
,Y '
se h
/* ~
h,-{ i
/ 6N f -
0 10 20 30 SCALE IN MILES EXPL AN ATION BEC TEL 200 Potentiometric Contour VOGTLE ELECTRIC GENERATING PLANT (Contour Intervol = 20 f t.) POSTULATED MILLETT FAULT C ALCUL ATE D P01 CNTIO METRIC SURFACE. REDUCE D TRANSMISSIVITY HYPOTHTSIS FIGURE 7-31
W s
., VOGTLE PROJECT SITE 5 $ lid , GEORGIA ett .. AERIAL PHOTOGRAPHY l MAY 8,1951
- SCALE I" = 1 MILE 4~ U*
THEORETICAL M!LLETT
$r ,- FAULT ZONE 4
't.-
4
,n'
{ 7 *
," , l
-' / - ,/ /'Jr# s J ,& m-u r .a / , , ' ' y 7
p / p.f l.. -
/
, /
A f
~. ...
s ?;'2 f;, . _g . , s -- 906 @ # 9st
<> ->\ W? et
\
,4 * -
~,
~ f-g> N g,
stS]*#' ps *' e69
.p.
T 3
~ _
N T s
\
9 f 3
. ~t \
s \ h ,A. 3 J ' s g' i fp3 ' 7 - \ 2 s'
m m - - - - - ~ m m ~ t VOGTLE PROJECT SITE GEORGIA FALSE COLOR OBLIQUE U-2 PHOTOGRAPHY MAY 1,1979
/ .-
l/ I 1 NASA PHOTOGRAPH
# 579002748024100 E PHOTOGRAPH CENTER N 33' 5' D W 81* 31' m " THEORETICAL MILLETT FAULT ZONE
r
~ , e,,s g has amms VOGTLE PROJECT SITE i
GEORGIA ENHANCED LANDSAT SATELLITE IMAGERY FEBRUARY ll,1974 LANDSAT SCENE
" 1568-15281 ., _
SCALE I"= 2.5 MILES ..
-------- LINEAMENT -
@,o
- THEORETICAL
- MILLETT FAULT N 33" BE 1.
a
" ?
9 Y N 32*42 F l 4 1
, ,,. e
. . , - +
ma p _
~ - -
I VOGTLE PROJECT SITE GEORGIA ENHANCED LANDSAT SATELLITE IMAGERY LANDSAT . 'ENE JUNE 6,1976 "5414-14480 SCALEI"= 5 MILES _
%o
?.
EARTHQUAKE EPICENTER LINEAsc.n'
------ THEORETICAL MILLETT FAULT N 33' IS' 1
c. J .
~ ,.
~
R:. y .
. m 1 e-A
}
- 4kN yys g ,, N 32' 45' 7 -
s - " h j i m w as* 30' w 82* d
+
i ^ -- _ . _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ . _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _ _
I 8.0 ASSESSMENT OF POSTULATED MILLETT FAULT I All of the field and of fice studies described in Chapters Six and seven were directed at resolving the issue of whether the postulated Millett fault could be a capable fault by N11C criteria, and therefore of
. concern to the Vogtle Plant. In this chapter the results of those studies and the conclusions derived from them are discussed. Section 8.1 describes the results of each of the investigations discussed in Giapters Six and Seven which were designed to specifically address the issue of faulting. Section 8.2 discusses conclusions.
8.1 Results of Investigations I 8.1.1 Results of Geologic Mapping The geologic map produced during the field mapping, combined with the SRP and Vogtle get, logic maps is shown on Figure 6-1. This map is a detailed study and is the best possible for the terrain and cover in the area. The conclusions that are pertinent to the postulated Millett I fault can be quickly stated. First, there is no detectable offset of the Barnwell-Hawthorn (Altamaha) contact across the trace of the postulated fault. Second, there is no variation in mappable units across the suggested fault that cannot be more logically attributed to facies changes. Third, no surface geologic features were observed that are typically associated with shearing in or near fault zones. Finally, no geomorphic features were observed that would indicate the presence of a fault in the area mapped. I 8-1
8.1.2 Results of Core Drilling I Key Contacts and Marker Horizons The core drilling program resulted in a clear definition of the
~
subsurface stratigraphy along both the Georgia and South Carolina section lines crossing the postulated fault. Contacts between geologic I units were found to be distinctive, making them useful for hole to hole correlation. These contacts were one of the criteria used in determining whether or not fault of fset had occurred between holes. The lithologic correlations of units and their contacts are shown on Figures 8-1 through 8-3. Analysis of these geologic sections has not au shown any of fset which could be attributed to faulting as suggested in the Open-File Report. The lowermost units cored consist of multicolored clays with interbedded sands belonging to the Late Cretaceous Tuscaloosa lI Formation. Correlation of the individual beds within this formation is I very difficult. These materials were deposited in an envi onment characterized by rapid lithologic changes which resulted in few laterally extensive beds. Significant intraformational periods of erosion and redeposition also occurred, further complicating the I section. Overlying the Tuscaloosa is the lower Paleocene carbonaceous silt and clay unit known as the Ellenton Formation. The upper contact of the I 8-2
unit is the deepest marker useful for correlation in the section penetrated by drilling. The age of this unconformable contact is about 60 million years. I Above the Ellenton are sediments of the Huber Formation. These include a micaceous quartz sand which was found to be a laterally extensive unit in the Georgia core holes (Figure 8-2). However, in South Carolina kaolinitic clay of the Huber Formation extends down to the top of the carbonaceous clay of the underlying Ellenton in most holes (Figure 8-1) . The multicolored clays of the Huber Formation represent another distinct unit useful for correlation. The upper contact of the Huber Formation is an unconformity which exhibits several feet of weathering discoloration. This contact with the overlying non-calcareous sands is a distinctive marker for correlation. The sands overlying the Huber Formation belong to a unit which is unnamed in this report. They consist of upper calcareous and lower non-calcareous sands with gradational contact between. The contact can be determined using acid to detect a change in carbonate content, and in some core samples is represented by a color change. The geophysical logs clearly define this contact, and the contact has therefore been employed as a marker for correlation. I The calcareous sand unit generally increases in fossil content upward into a fossiliferous limestone. The thickness of the limestone and the I i iI 8-3
I I gradational nature of the change from calcareous sand to limestone does not allow use of the sand-limestone contact as a marker horizon. The top of the limestone where it is in contact with the base of the overlying marl does, however, define a good marker. This contact is characteristically abrupt and sharp with an age of approximately 50 million years and is not of fset. I The marl overlying the unnamed sands is middle Eocene in age and is known as the Blue Bluf f Member of the Lisbon Formation. As can be seen on Figures 8-1 through 8-3, the marl is the most distinctive and useful marker horizon for correlating purposes. This unit generally becomes finer upward with local thin bedding. Intermittent thin beds of limestone occur throughout the marl. I The material overlying the marl varies among the core holes. In the northwestern portion of the Georgia section (refer to Figure 8-2), the marl is capped by fossiliferous limestone. This limestone, known as the Utley Limestone is variable in thickness. The basal contact of the I limestone represents an unconformable contact with the marl. Downdip to the southeast, the marl is overlain by calcareous sand which thickens downdip. The calcareous sand is overlain by limestone of similar lithologically to the Utley Limestone overlying the marl to the nor thwes t. The drill holes in the South Carolina section (Figure 8-1) did not encounter the equivalent upper limestone. These holes generally penetrated a deeply weathered, thin bed of sandy clay above I
F. L I W. g the marl. For correlation purposes the top of the limestone was used for the marker horizon in the Georgia section (Figure 8-2). The age of I this contact is estimated at 45 million years. In the South Carolina L section (Figure 8-1),- the top of the marl was used as the marker F L because of the absence of the limestone. The uppermost geologic units penetrated by core drilling are the sands of the Barnwell and Hawthorn (Altamaha) Formations. These formations have late Eocene and early Miocene ages, respectively. Distinct marker [ horizons were not found in these materials. [ As can be seen in Figures 8-1 through 8-3, the stratigraphic markers described above can be correlated across the postulated Millett fault without evidence of offset. This correlation is found in sections using drill hole data from both sides of the Savannah River. { It is therefore concluded from the core drilling that there is no evidence of fault displacement between the core holes within the depth of investigations. { 8.1.3 Results of Geophysical Logging The downhole geophysical logs were interpreted for similiar overall trace character and specific contacts. Correlations were drawn between characteristic points from hole to hole. These correlations were made independent of the lithologic marker horizons described in Section { E . [ 8-5
~
1 l
O'
.5 -
8.1.2 which were cor related from the core logs. The electrical and nuclear log correlations are shown on Figures 8-4 through 8-7. Several discrepancies between the lithologic and geophysical correlation points are readily apparent. These are due to the nature of the physical properties measured by each type of log. The lithologic log has contacts designated at bedding discontinuities observed in the core samples. The geophysical logs, however, measure specific physical characteristics such as porosity, natural gamma radiation, pore water chemistry, etc. As a result the correlative contacts picked in these different logging methods do not always coincide. However, the significant aspect of the geophysical correlation is that physical properties of the formations, as measured by the geophysical logs, can be correlated from hole to hole without apparent of fset. These correlations agree with the lithologic correlations in that neither shows any evidence of faulting. 8.1.4 Results of River Reflection Survey
.I The acoustical marine reflection profile records of the Savannah River (obtained from the three profiling systems described in Section 6.5) were examined for: key reflecting horizons, lateral continuity and variation of the horizons, seismic reflecting characteristics that indicate structural features, and displacements that could be an indication of faulting.
I I I "-'
The original records and reflect ing horizons for the Millett fault portion of the survey are shown in Plates 3, 4, and 5 of Appendix F. Reflecting horizons for the Statesboro portion of the survey are shown in Plate 7 of Appendix F. In interpreting the time and depth scales of these plates it is important to note that the time scale on the figures is as recorded, while the depth scale incorporates a correction for a 20 foot travel path through the water. The depth scale is arbitrarily set to zero at river bottom. Because of the water correction, the assumed velocity of 6,000 feet per second cannot be multiplied by one-half the two way travel time to obtain the corresponding depth. I The general results of the refl.tction surveys are: 1) identification of several key, continuous, southeast dipping reflectors at dif ferent depths ranging from elevation +70 to -1150 feet (see Plate 2 of Appendix F); 2) an indication of localized features, including a depressional feature between river mile marker 143 and 144, and, most important, 3) the absence of the faulting as postulated in the Open-File Report. I The reflectors observed on the river survey were correlated with the adjacent VG core holes about one mile to the southwest. Figure 8-8 illustrates these correlations in the area adjacent to the postulated Millett fault. The reflectors A through C are interpreted to be from beds of clay and shell bioherm layers in the Barnwell Group. Reflector I E correlates with the top of the Utley Limestone, the lowermost unit in I I I "-'
'I the Barnwell Group. Due to the large velocity contrast between the overlying unconsolidated sands, clay, and shells; this reflector can be identified over most of the area. Reflector F represents the base of the Blue Bluf f marl at the contact with the lower unnamed limestone. Reflector G correlates with the unconformable contact between the upper unnamed sands of the Lisbon Formation and the top of the kaolinitic clays of the Huber Formation. The reflector H is interpreted to be the top of the thick sand aquifer within the Tuscaloosa Formation. Finally the deep reflector designated I is correlated with the top pre-Late Cretaceous erosion surface (the top of the Triassic sedimentary rock s) . This correlation is verified by the drill hole P5R, less than 5 miles to the northeast, penetrating the Triassic rock at about the same elevation. Reflection lines on the SRP and the Seisdata line near Sardis, Georgia also show this same strong reflector at that elevation. The lack of bedding offset, along with the overall continuity of the identified reflecting horizons, indicates that no faulting of the kind and magnitude postulated in the Open-File Report has occurred. A similar conclusion holds for the postulated Statesboro fault (see Plate 7 of Appendix F) . I Several shallow reflectors with small, less than 10 feet, displacements I are found adjacent to Fix 13 on the Uniboom and 10 cubic-inch air gun l l l re cords. The features could be the result of interference due to multiple reflections. If the features are interpreted to be displaced I I l l I l 8-8 l
I beds several origins are possible, these include fault of fset, slumping and collapse. Fault of fset would result in displacement of lower reflectors, with increasing of fset with depth and age of the formations. A review of the records show several reflectors below the displaced reflector which do not show of fset. These include reflector C at a depth of about 60 feet, reflector E at a depth of 100 feet, reflector G at 280 feet, reflector H at about 500 feet, and rr fl ector I I at about 1170 feet. Additivnally, the undisturbed reflectors are shown to not be of fset in the adjacent core hole section. The records show several features which are analogous to collapse and buried karstic surfaces. The limestone and upper portion of the marl display solutioning and resultant collapse in both outcrop along the river bluf fs and in the reflection profiles. The overlying sediments collapse into the depression causing offset with the adjacent sedimentary beds. Two examples of the Fix 13 type of features are shown in Plates 3 and 4 of Appendix F. The first is shown on Plate 3, Appendix F, approximately 550 feet northwest of Fix 13 at a time between 11 and 14 milliseconds while the second is shown on Plate 4, Appendix F, approximately 500 feet southwest of Fix 13 in the upper 0.05 seconds of the record. These features are found in reflector A materials which show a blocky, irregular nature in adjacent areas on Uniboom records (Plate 3). The blocks shoe slight rotation of the bedding, which is consistent with slumping into a depression. The areas between the blocks do not show dif fraction patterns, which are associated with vertical faulting. e.g g
I I During the river survey, several passes were made of this portion of the river. The records from the additional passes were reviewed to aid in the interpretation of the features.
-I The record shown on Plate 4 is from Line 6.
Another 10 cu. in. airgun pass is shown on Figure 8-9 from Line 4. The differences between the lines include a change in the filter setting from 170-800 Hz band to 700-1000 Hz band, as well as a different position of the boat in the river channel. Figure 8-9 I clearly shows far less offset of the reflector than is shown on Plate 4. This is most likely the result of posit!.on shift in the river channel. If the feature were a fault of fset, the amount of offset would be consistent regardless of position in the channel. If the feature were the result of block sliding into a depression, different amounts of offset would be expected within a short lateral distance, as was found. Figure 8-9 does not have the same strong ' bubble pulse' interference at 0.06 milliseconds due to the different filter setting. As a result, several good reflectors are evident between 0.04 and 0.08 milliseconds on Figure 8-9, which were masked by the bubble pclse on Plate 4. These reflectors do not show offset as do those above. Reflector G at 0.12 milliseconds does not show offset. 'Itus, the small of fsets shown on Plate 4 can most logically be attributed to collapse and block sliding and clearly not to capable faulting. I 1 I I 8-10
I I A possible of fset is shown in the I horizon (Triassic rocks) on the 20 cubic inch Air Gun record (Plate 5, Appendix F) at the approximate location of the postulated Millett fault. The apparent offset is 40 feet (+10 f t) down to the south. The horizon I feature correlates quite well with the small step-like faults interpreted at the Triassic contact on the Savannah River Plant geophysical records discussed in Section 7.3. This feature, if it is faulting, has the opposite sense I of movement and at least an order of magnitude less offset than the postulated Millett fault. 8.1.5 Results of Existing Geophysical Studies The gravity and magnetic surveys reviewed for this report all contain anomalies which indicate the possibility of faulting. The survey me thods (e.g. station spacing) and the physical characteristics of the local rocks (e.g. nonmagnetic sedimentary rocks to great depth) limit the interpretation to depths greater than 1000 feet (ages greater than 80 m.y.B.P.). Since no information on the shallow Cretaceous structure is obtainable from the gravity and magnetic surveys no conclusions as to the capability of the postulated faults can be made. l I The reviewed reflection survey of the Savannah River Plant was designed to map the Triassic basins. This required survey techniques that gave little information on the Cretaceous structure. Some Cretaceous i I reflecting horizons to the northwest of the postulated Millett fault I I 8-11
were identified as not faulted. Several top-of-Triassic reflecting horizons were identified with displacements generally less than 100 i feet. In the vicinity of the pos ulated Millett fault, of fset of about 50 feet up to the northwest was found on Line 7 (Figure 7-2). This 50 foot displacement is much less than the several hundred feet postulated for the Millett fault. I The purchase of part of Seisdata Vibroseis Line 6 resulted in the identification of a strong continuous top-of-Triassic reflector (elevation -1175 feet) across the postulated Millett fault trace. The top-of-Triassic reflector loses coherence about 1/2 mile southeast of the postulated fault. If the break up is interpreted as displacement, the maximum of fset of the top of Triassic is on the order of tens of feet. An important consistency to note between all the seismic reflection surveys and the cored hole PSR (Marine and Siple, 1974) is the elevation of the top of Triassic. I Source Elevation (feet) Top of Triassic Cored hole P5R (Figure 7-2) -1100 I Savannah River Plant Line 7 - southernmost part (Figure 7-2)
-1100 Savannah River Survey - at postulated fault -1130 (Figure 6-5)
Savannah River Plant Line lE - southernmost par t -1150 (Figure 7-2) Vibroseis Line 6 - at postulated fault -1175 I (Figure 6-5) 8-12
These data indicate that the top of Triassic (age approximately 80 m.y.B.P.) in the vicinity of the postulated Millett Fault, if offsc.' at all, has been displaced less than 100 feet. I Finally, no geophysical data lead to the conclusion that there is a capable fault in the vicinity of the postulated Millett fault. I 8.1.6 Results of Remote Sensing Studies I As explained in Section 7.4.1, imagery and photography of varying scales were used to search for evidence of faulting in the area of the postulated Millett fault. Three main types of imagery, collected by different sensor systems were employed; including low-altitude aerial photography, high-altitude NASA U-2 oblique false color photography, and Landsat satellite imagery. Seven Landsat satellite images covering two seasonal conditions and different sun illumination angles were examined. These satellite images, stored as digital data on computer compatible tapes, were examined on Bechtel's image processor using digital enhancement procedures designed to enhance linear features. The imagery and photography were examined closely to identify linear features and isolate the lineaments that might represent the surface I expression of a geologic structure. The procedure employed was to I I 8-13
I first identify lineaments on the imagery, then eliminate all of those lineaments having an obviously non-geologic basis, such as roads, transmission lines, property lines and other cultural features. The remaining lineaments, those which could not be immediately attributed to cultural origins, were subjected to further study. Only one significant lineament was identified as possibly fault-related and was field examined. This lineament is shown as the green dashed lined on Plates 4 and 5. I Professor R.J.P. Lyon of Stanford University, Remote Sensing Laboratory provided assistance in designing the study and interpreting the imagery. The main conclusion from the majority of the lineaments was that thev were caused by optical alignment of field boundaries and some stream sections and hence were classified as having a ' cultural' origin. The low-altitude 1:20,000 aerial photography and selected field observations confirm the origins of these optical lineations on the satellite imagery. A smaller number of the ' cultural' lineaments were attributable to roads which of ten parallel agricultural fields. Lineaments identified in red on Figures 7-4 and 7-5, and individually identified by letters, are predominantly associated with floodplain features and karst topography. These lineaments colored blue are predominantly associated with the alignment of stream and river sections. I 8-14 j
[- Comparison of Figures 7-4 and 7-5 indicates that many of the
. lineaments occur along the flood plain margins of streams and
~ rivers. These lineaments are labelled A through I and M cn Figure 7-5,.and B1, Cl, and X on Figure 7-4.
[ Wo geomorphic lineaments near the Vogtle plant site (labelled J and K on, Figure 7-5) are present on the June 6,1976 image. Field observatilon of these lineaments, together with an examination of the other mosaic in Figure 7-4, reveals that these linear features represent the drainage divide of the drainage basin in which the {- plant site is located. One lineament close to the postulated Millett fault and intersecting it near Ellison's Landing northeast of Girard was examined in the field. This lineament is labelled V on Figure 7.4 { and L and L1 on Figure 7-5 and is also shown as a green dashed line
~
(' on Plates 4 and 5. The results, of the field investigation indicate no evidence of faulting along the trace of this linear feature.
- A number of saall geomorphic linear features identified in the southeasterly section of the imagery are possibly old ' strand
( lines' related to previous Quaternary stands of the Atlantic Ocean and are considered non-structural in origin. These lineaments are labelled R and.S on Figure 7.4.and 0, P and Q on Figure 7.5. g; [L ' . [ 8-15 3.. < (. . ......f. .*... .
,c
_ _ _ _ _ _ ______1____._____.__.__.____ _ _ _ _ _ _ _ . _ _
I t I
- The 'geomorphic' lineaments identified as karst features are caused by the apparent alignment of circular ponds and agricultural fields in this area. These lineaments are labelled T, U, Z, Y, W and Al on Figure 7-4 and N and N1 on Figure 7-5.
In summary, the remote sensing studies indicate that the lineations on the satellite imagey are unrelated to faulting. They are confidently explained as alignments of field boundaries, stream sections and karst features and fluvial geomorphic features not structurally controlled by faulting. None of the satellite imagery and photography examined showed any evidence of surface expression of the postulated Millett l fault. l l 8.1.7 Results of River Meander Analysis l l An analycis of the Savannah River meander pattern was conducted, since the Open-File Report states that the location of the postulated fault is based, in part, on a change in the meander pattern. The analysis I has shown that the change from a straight to r,inuous p- is a temporary condition in time and is most probably caused by a change in l the erosional resistance of the bank and channel bottom materials. The i 1 flood plain shows meander scars adjacent to the straight channel area, , l demanstrating that the change is temporary. The strata along the ! l \ l straight section consist of hard, well cemented limestone and marl and some semi-consolidated sand and clay beds, i l l I I -"
[ 8.1.8 _nesults of Lithologic Studies { Lithologic studies conducted on samples from AL-66, AL-40 and VSC and VG core holes supplement field studies performed to invostigate the stratigraphy in the vicinity of the postulated Millett fault. These studies include petrographic examination, x-ray diffraction and heavy mineral analyses. The main purpose of the studies on samples from AL-66, AL-40 and VSC-4 was to determine whether Triassic rocks were penetrated near the base of these holes. For the VG and VSC holes, the lithologic studies were used to verify the stratigraphic sections. [ '- The Open-File Report postulated the Millett fault on the determination that the lower 100 feet of AL-66 were in Triassic rocks. Results of , the lithologic studies indicate that: 1) the lithology of samples (': collected from AL-66, AL-40 and VSC-4 at elevations below the postulated pre-Late Cretaceous unconformity in the Open-File Report are inconsistent with Triassic-Jurassic lithology based on a comparison with the mineralogical analyses of core samples from DRB 10, 2) samples collected from similar elevations in each hole are { lithologically similar to each other. These data indicate that the lithologic unit they were collected from has not been offset. [- Samples considered to be representative of some stratigraphic units encountered by the VSC and VG core holes were found to be lithologically distinctive. The lithology of the samples confirms the { stratigraphic correlations. [ g 8 c ' '- rr- --
8.1.9 Results of Seismicity Studies I All available seismicity information within 62.5 milen (100 kilometers) of the Vogtle site was reexamined to test for any possible association with the postulated 11111ett or Statesboro faults. All historic felt earthquakes, all earthquakes located by the regional array of stations in operation since about 1974, and all earthquakes noted on the three station Savannah River Plant array were considered. These data show that earthquakes of Intensity VI (modified Mercalli) have occurred in the Piedmont part of the 62.5-mile-radius study area defined above, and that smaller, scattered activity appeat s throughout the Coastal Plain part of the study area. Small recent earthquakes are also concentrated in the Piedmont (although some of these may be quarry or road construction explosions) with a few scattered Coastal Plain events. No clustering of small earthquakes is occurring near either the postulated Millett or Statesboro faults. It is concluded that there is no evidence of association of any known earthquake with either of the postulated faults. 8.1.10 Results of Surface Water Hydrology Studles I Unit baseflows, computed from concurrent records and shown in Table 7-15, show some agreement with those published in the Open-File Report. I I 8-18
The following listing compares USGS obtained values with average values of unit baseflow obtained in this analysis of concurrent records and longer term records: U.S.G.S. Values from this report Savannah River (Concur rent (1941-1970) record) Augusta-Burtons Ferry 0.74 0.79 0.69 . Burtone Ferry-Clyo 0.23 0.59 0.47 I Ogeechee River Louisville-Scarboro 0.17 0.18 Scarboro-Eden 0.11 0.10 S.F. Edisto River l Montmorenci-Denmark 0.46 0.49 All average values agree reasonably well except for the Burtons Ferry-Clyo reach. Here the Open-File Report analysis indicates a much greater difference between reaches. Analysis of the 1941-1970 record for the Savannah River yields different values of baseflow also closer in magnitude than those quoted in the Open-File Report. In all cases, unit baseflows in the upstream reaches are greater than those for downstream reaches. As pointed out in the section on ground water, the unit baseflow contribution above Burtons Ferry is expected to be greater than that below Burtons Ferry since the ground water aquifer slopes more steeply than the stream bed. I variability of computed unit baseflows is great. Figures 7-17 and 7-18 show this variation graphically for the Savannah River 1941-1970 I 8-19
record. Table 7-14 shows that for the 30-year record of flows. unit baseflow in the downstream reach was actually greater than that in the upstream reach for 10 separate years while for four years the { downstream reach appeared to be a losing stream. The error at. 'ysis performed in Section 7.7.4 further emphasizes that computed unit baseflows are subject to enough variation that they cannot be used with confidence to prove or disprove the presence of a barrier (hypothesized fault) in an aquifer. 8.1.11 Results of Ground Water Studies [ 8.1.11.1 Water Well Survey ( The potentiometric maps of the Tertiary (upper) and Cretaceous (lower ) ( aquifers, Figures 7-19 and 7-20, respectively, indicate that the water in both aquifers moves from the outcrop areas downdip beneath the Coastal Plain. The data indicate that ground water near the Savannah River moves toward the river. Away from the river, the direction of flow shif ts to the southeast, downdip. There is a closed " low" (ground { water sink) shown on each map at the Savannah River just south of Augusta in the outcrop areas of each aquifer, indicating discharge to the river. Both maps show reversals of ground water gradient on the river downstream of the ground water sinks, in the vicinity of the [ Vogtle site. There is no evidence of anomalously different water level { elevations between wells in either aquifer. The reversals in gradient downdip of the ground water sinks in each aquifer are the only fes.tures that could be considered anomalous. [ 8-20
I I Possible explanations for the observed reversals in ground water gradient are: 1) a barriec caused by faulting, 2) a marked change in transmissivity, or 3) the hypothesis first suggested by Siple (1960), and expanded upon by LeGrand and Pettyjohn (1981), that the reversal, or " saddle" configuration in the potentiometric surface, is a natural consequence of ground water flow to a stream breaching a confined ^ aquifer. Examination of the geologic cross sections (Figures 8-1 and 8-2) along the line of core holes drilled during this investigation show that there has not been any displacement of sediments within either aquifer. In addition, one hole, VSC-4, was drilled to a depth of 1024 feet and was completed in sands of the Cretaceous aquifer, rather than in the Triassic rocks postulated to be present at that depth by the authors of Open-File Report 82-156. Since there is no geologic evidence for faulting, it is not likely that the reversals in ground water gradient are a result of fault movement. These same Figures (8-1 and 8-2) show that the sediments are uniform in thickness and rock type along the sections, indicating that there are probably no marked changes in transmissivity. Also, both aquifers exhibit ground water flow reversals in the same region. It is unlikely that both aquifers would have such marked transmissivity changes (from high to low) at exactly the same place. The most probable explanation of the localized reversal of the ground water flow paths is the I I 8-21
I I hypothesis of saddle configuration (Siple,1960; LeGrand and Pettyjohn, l 1981) . The reversal in gradient of both aquifers occurs in areas of reversal in flow due to discharge to the Savannah River as shown on the Cretaceous aquifer potentiometric map (Figure 8-10) of Siple (1954) and on Figures 7-19 through 7-21. I In addition to evaluating regional ground water flow patterns, water levels across the postulated f.ault were examined for anomalous differences which could be suggestive of a ground water barrier. A barrier is usually detected as a result of relatively large water level differences in wells a short distance apart and may or may not be a result of faulting. Anomalies can be produced by local changes in lithology, changes in transmissivity, or more importantly by comparing water levels from wells screened in different aquifers (or in multiple aquifers) . If one well is pumped more heavily than an adjacent well, a semipermancnt pumping depression at the more heavily used well can also produce a difference in water levels. If a ground water barrier is determined to be present, the interpretation of whether or not it is fault-related must be consistent with the geologic structure and stratigraphy. The reverse situation is also true. The absence of water level anomalies does not preclude the presence of a fault. Fault offsets would be more likely to produce anomalous water levels when an impermeable gouge zone is present along the fault plane, or when permeable aquifer materials are offset against less permeable clays or silts. 8-22
I Water level profiles across the postulated fault were prepared from reliable data. Only wells screened in the same unit were used, and all water levels were measured in the field during the same time period. Water wells suspected of having failed seals, or having poor communication with the aquifer, were not included. As noted in Chapter 6, observation wells usee .3r analysis of water levels across the postulated fault were thoroughly developed to ensure reliable measurements. The water level profiles a.*e shown on Figures 7-23 and 7-24 (see Figure 7-22 for location of sections), and show no evidence of a ground water barrier. Anomalous water levels presented in the Open-File Report are believed to be a result of using non-concurrent data (water levels not measured at the same time) and data from wells not completed in equivalent aquifers. 8.1.11.2 Numerical Modeling I As described in Section 7.8.2, a numerical model was developed to test alternative hypotheses that can explain the ground water conditions observed at the study site. . I The first case analyzed considers the hypothesis of Siple (1960) and LeGrand and Pettyjohn (1981). This theory describes one common type of hydrogeologic system dominated by consequent streams flowing down a structural basin. The input data to the model for this simulation I I 8-23
I consist of me.terial properties representative of the Cretaceous aquifer
- nd do not assume any discontinuity at the location of the postulated Millett fault. The corresponding piezometric contours are shown on Figure 7-27.
The second hypothesis analyzed was that of a barrier at the location of the postulated Millett fault. This was achieved by assigning a lower j I permeability to the elements located in the appropriate area of the l l finite element mesh. The results are shown on Figures 7-28 and 7-29, which correspond to fault permeabilities equal to 100 ft/yr and 1 l ft/yr, respectively. l The last hypothesis was that of an abrupt reduction in aquifer thickness south of the postulated Millett fault. This hypothesis was tested in the model by reducing the transmissivity of the elements l located in the corresponding area of the finite element mesh. The piezometric surface calculated in this case is shown on Figure 7-31. I The main conclusions derived from the numerical simulation are as I follows: I 1. An area of low ground water contours (sinks) can exist in the unconfined part of the Cretaceous aquifer, without any consideration of discontinuities around the postulated Millett fault. These ground water conditions, similar to those observed at I I g . -u
(- the site, correspond to those ptevailing around streams flowing k along dipping strata, as stipulated in the hypothesis of Siple (1960) and LeGrand and pettyjohn (1981) .
- 2. . Introducing a barrier fault at the location of the postulated fault does not preclude the development of ground water sinks. Hence, the observed potentiometric contours cannot be used to imply the existence of a fault.
( 3. A reduction in transmissivity south of the postulated Millett fault alters the calculated potentiometric contours in a manner that is contrary to field observations. Hence, the hypothesis of reduced aquifer transmissivity seems invalid. [
^
[ - l [ C L . [ [ [ . [ [ 8 - - - - - - - - - - - - - - - -
I 8.2 conclusions As described in this report, extensive investigations have been undertaken to address the postulated Millett fault described in the Open-File Report 82-156. The results of these studies demonstrate the absence of a capable fault anywhere in the vicinity of the postulated Millett fault. Further, the studies strongly suggest that no capable .I fault exists near the location of the postulated Statesboro fault. I It is therefore concluded that the postulated Millett and Statesboro faults have no impact on the seismic safety of the Vogtle Electric Generating Plant. The contributing reasons for these conclusions are as follows: E g ,
- 1. Results of core drilling, lithologic studiec, and geophysical logs demonstrate continuity of subsurface horizons across the trace of the postulated Millett fault on both the Georgia and South Carolina sides of the Savannah River. These subsurface horizons have ages ranging from approximately 40 million to approximately 80 million years before present.
- 2. Results of acoustic reflection studies in the Savannah River demonstrate continuity of subsurface reflecting horizons down to an elevation of approximately -1,100 feet across the strike of the I
I -'
I postulated Millett fault. A reflector at elevation -1,100 feet, believed to be the Triassic surface, may.have an apparent offset up I of 50 feet. Even this 50-foot of fset is questionable but does agree with small faults interpreted from SRP geophysical records and disagrees with the 700-foot of fset proposed in the Open-File Report. I 3. Results of acoustic reflection studies across the trace of the l l postulated Statesboro fault also demonstrate continuity of j subsurface reflecting horizons. I 4. Detailed surface geologic mapping and remote sensing studies reveal no evidence for surface expression of faulting in the area of the I postulated Millett fault. 1
- 5. Analysis of ground water information, including collection and use of a concurrent data base, indicates there is no basis to support or preclude the existence of a fault. Water levels measured in two lines of piezometers crossing the postulated Millett fault do not show marked changes from one side to the other.
I 6. Surface water hydrologic studies using a concurrent data base neither prove nor disprove the existence of a fault. I 7. Historic seismicity, including microearthquake records, reveals no evidence of active faulting in the area. I 8-27
I
- I
- 8. Petrographic studies of well-cuttings from well AL-66 indicates that this well bottoms in Cretaceous rather than Triassic rocks as suggested in the Open-File Report, thus removing upthrown Triassic rocks as a basis for a fault.
- 9. Core hole VSC-4, drilled near well AL-66 and approximately 300 j feet deeper than the proposed Triassic contact of the Open-File Report, bottoms in Cretaceous rocks rather than Triassic, confirming conclusion eight, above.
- I
!I !I I
'I I
I 8-28
\ y
- 1
[.'l -. y ._ W.. . 6.3 Consultant conclusions i4- _ - .y g a g ' A group of consultants, with expertise in the geology of the region and . in specialized fields, were retained to provide guidance and review of -- this study. Following completion of the study they reviewed the report 9. I and prepared the attached letter. This outline lists their affiliation 1,
,y-and area of expertise /}
Dr. Bruce Bolt Univ. of California Seismologist ,' s e ; Dr. Robert Hatcher Univ. of bouth Carolina Structural Geologist ' 'q ,, Dr. Vernon Henry Skidaway Institute Geologist - e f x. Dr. Philip LaMoreaux LaMoreaux Assoc. Hydrogeologist -
', 4 3 ..I. '
Mr. Harry LeGrand Consultant Hydrogeologist Dr. Stavros Papadopulos Papadopulos Assoc. Hydrogeoloqist i'..I.
..-p Mr. Carl Savit Senior Vice President Geophysicist , ,
Western Geophysical - Dr. Carl Stepp Woodward-Clyde Consultants Geophysicist - -
..' . 4 . 2 Mr. Leonard Wood Papadopulos Assoc. Hydrologist ; , i #'
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September 29, 1982 ft. C. R. McClure Manager-Eng ineer ing/ Geology Bechtel Civil & Minerals, Inc. San Francisco, California 94119 l We, the undersigned, have reviewed the conclusions of U.S.G.S. Open-File Report 82-156, which postulates the existence of the Millett fault near the Vogtle Plant Site southeast of Augusta, Georgia. The Open-File Report also suggests the possible existence of another fault, the Statesboro fault, farther southeast from the plant site. We reviewed the draf t report entitled " Studies of Postulated Millett Fault", prepared by Bechtel for the Georgia Power Company and Southern i Company Services to evaluate these postulated faults, and we provided comments and suggestions on the format and content of the report. Where appropriate, we visited the field during the exploration phase to examine the drill cores and review the hydrologic studies. We also I participated in meetings and discussions with members of Bechtel, Southern Company Services, and Georgia Power Company regarding specific data and analyses related to our individual areas of expertise. Based on the data and interpretations in the draf t report by Bechtel and the Open-File Report, we independently evaluated this information as specifically related to areas of our expertise and experience in the region. The studies performed by Bechtel have focused on the issue of fault capability, as this is of primary importance in establishing the seismic design basis of a nuclear power plant. According to criteria of 10 CFR 100 Appendix A, a fault is considered capable if it has moved at or near the earth surface once in the last 35,000 years, or more than once in the last 500,000 years. A fault shown to be not capsble need not be considered in the seismic design bases of the plant. The studies have therefore concentrated on the capability question rather than the existence of faulting per se. We have primarily reviewed those portions of the studies which fall under our individual areas of expertise, and reviewed the remaining portions in less detail. The results of our individual reviews may be collectively stated as follows:
- Extensive stratigraphic and geophysical studies did not provide credible evidence of faulting within subsurface strata having ages of up to approximately 80 million years.
I I ' I I
- Hydrologic data do not support the presence of a ground water barrier, which could be a fault, within these same strata.
Neither the data nor its evaluation support the presence of a capable fault at or near the postulated Millett fault. The evidence does not support a capable fault at or near the I postulated Statesboro fault. In summary, the existing data and reports together with data and evaluations developed during this study and reviewed by us do not support the existence of a capable fault at or near the Vogtle Plant site.
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~Le'onard Wood M H.tw ry LeGrand kdiafp Ca VWW V V
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Buie, B.F. ,1980, Kaolin deposits and the Cretaceous-Tertiary boundary I in east-central Georgia: Geological Society of America, Field Trip No. 15, p. 311-3 22. Callahan, J.T., 1964, The yield of sedimentary aquifers of the Coastal Plain southeast river basins: U.S. Geological Survey Water-Supply Paper 1669-W, 56 p. Christopher , R.A. ,1982, Palynostratigraphy of the basal Cretaceous units of the eastern Gulf and southern Atlantic Coastal Plain: M Arden, D.D. , Beck , B.F. , and Morrow E. , ed. , Second Symposium on the Geology of the Southeastern Coastal Plain, p.10-23. Cook , F. A. , and Oliver , J.E. ,1981, The late Precambrian-early I Paleozoic continental edge in the Appalachian orogen: American Journal of Science, v. 281, no. 8, p. 993-1008. I
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~
in,Gohn, G.S., ed., Studies
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tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File : Report 82-134, p. 7-8. (f 9
I ' I Gohn, G.S. , Gottfried, D. , Lanphere, M.A. , and !!iggins, B.B. , 1978c, Regional implications of Triassic or Jurassic age for basalt and I sedimentary red beds in the South Carolina Coastal Plain: Science, v. 202, no. 4370, p. 887-890. Guinn, S.A. ,1980, Earthquake focal mechanisms in the southeastern I United States: U.S. Nuclear Regulatory Commission, NUIEG/CR-1503, 150 p. Hatcher , R.D. , Jr. ,1972, Development model for the southern Appalachians: Geological Society of America Bulletin v. 83, no. 9, p. 2735-2760. Hatcher , R.D. , Jr. ,1978, Tectonics of the western Piedmont and Blue Ridge, southern Appalachians: Review and speculation: American Journal of Science, v. 278, no. 3, p. 276-304. Hatcher, R.D. , Jr. , and Odom, A.L. ,1980, Timing of thrusting in the southern Appalachians, U.S.A.: Model for orogeny: Journal of Geological Society of London, v.137, part 3, 3 21-327. Ilazel, J.E. , Bybell, L.M. , Christopher , R.A. , Fredrick sen, N.O. , May, F.E., McLean, D.M., Poort, R.Z., Smith, C.C., Sohl, N.F., Valentine, I P.C. , and Witmer, R.J. ,1977, Biostratigraphy of the deep corehole (Clubhouse Crossroads corehole 1) near Charleston, South Carolina, in Rankin, D. W., ed. , Studies related to the Charleston, South Carolina, earthquake of 1886 - A preliminary report: U.S. Geological Survey Professional Paper 1028, p. 71-89. I Ilerrick, S.M. ,1961, Well logs of the Coastal Plain of Georgia: Georgia Geologic Survey Bulletin 70, 462 p. 11er rick, S.M. , and Vorhis, R.C. ,1963, Subsur face geology of the l I Georgia Coastal Plaint Georgia Geologic Survey Information Circular 25, 80 p. liuddlestun, P.F. ,1981, Correlation chart, Georgia Coastal Plain:
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W 4
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+
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~
f:
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~
southwestern Georgia, fact or fiction: Geological Survey of Georgia, Department of Mines, Mining and Geology, Information Circular 41,16 p. Petty, A.J. , Pe trafeso, F.A. , and Moore , F.C. , Jr. ,1965, Aeromagnetic-map of the Savannah River Plant area. South Carolina and Georgia ~( U.S. Geological Survey Geophysical Investigations Map GP-489. 1 sheet, scale: 1:250,000. Popenoe, P. , and Zietz, I. ,1977, The nature of the geophysical basement beneath the Coastal Plain of South Carolina and northeastern Geor gia, ,i_n_ n Rankin, D.W. , . ed. , Studies related to the Charleston, South
. Carolina, earthquake'of 1886 - A preliminary report: U.S. Geological-Survey Professional Paper 1028, p 119-137.
u ..
I E Poppe, B., 1979, Historical survey of U.S. seismograph stations: U.S. Geological Survey Professional Paper 1096, 389 p. I Pressler, E.D., 1947, Geology and occurrence of oil in Florida- l Bulletin of the American Association of Petroleum Geologists, v. 31, no. 10, p. 1851-1862. Prowell, D.C. and O'Connor , B.J. ,19 78, Belair f ault zones: Evidence of Tertiary fault displacement in eastern Georgia. Geology, v. 6, no. 11, p. 6 81-6 84. Prowell, D.C. , O'Connor , B.J. , and Rubin, M. ,1975, Preliminary evidence for Holocene movement along 'I.e Belair fault zone near Augusta, Georgia: U.S. Geological Survey Open-File Report 75-680, 8 p. Rainwate:., E.H.,1964, Transgressions and regressions in the Gulf Cocst I. Ter tiary: Transactions of the Gulf Coast Association and Geologic Society, v. 14, p. 217-230. Rankin, D.W.,1975, The continental margin of eastern North American in the southern Appalachians: The opening and closing of the proto-Atlantic Ocean: American Journal of Science, v. 275-A, no. 3, p. 298-336. I Rankin, D.W.,1976, Appalachian salients and recesses: Late Precambrian continental breakup and the opening of the Iapetus Ocean: Journal of Geophysical Research, v. 81, no. 2, p. 5605-5619. Rankin, D.F. , ed. ,1977, Studies related to the Charleston, South I Carolina Earthquake of 1886 - A preliminary report: U.S. Geological Survey ;cofessional Paper 1028, 204 p. Reagor , B.G. , Stover , C.W. , and Algermissen, S.T. , 1980, Seismicity map I of the State of South Carolina: U.S. Geological Survey Miscellaneous Investigations Map MF-1225, 1 sheet, scale 1:1,000,000. I Rhea, S., 1981, South Carolina seismic program, seismological data report: U.S. Geological Survey Open-File Report 81-362, 79 p. Ritter, D.F., 1979, Process Geomorphology: Dubuque, Wm. C. Brown Company Publishers, 603 p. Schumm, S.A. and Khan, H.R.,1972, Experimental study of channel pa tt erns Geological Society of America Bulletin, v. 83, no. 6, p. 1755-1770. Sever, C.W., 1965, Ground water rescurces and geology of Seminole, i Decatur, and Grady Counties, Georgia: U.S. Geological Survey [ Water-Supply Paper 1809-Q, 30 p. l l I
Sever, C.W., 1966, Miocene structural movement in Thomas County, l Georg ia: U.S. Geological Survey Professional Paper 550-C, p. C12-C16. Siple, G.E., 1960, Piezometric levels in the Cretaceous sand aquifer of l the Savannah River basin: Georgia Mineral Newsletter, v. 13, no. 4, p. I 163-166. Siple, G.E. ,1967, Geology and ground water of the Savannah River Plant and vicinity, South Carolina: U.S. Geological Survey Water-Supply Paper 1841, 113 p. j Snoke, A.W., Kish, S.A., and Secor, D.T., Jr., 1980, Deformed Hercynian granitic rocks from the Piedmont of South Carolina: American Journal of Science, v. 280, no.10, p.1018-1034. Stover , C.W. , Reagor , D .G. , Algermissen , S .T. , and Iong , L.T. , 197 9, I Seismicity map of the State of Georgia: U.S. Geological Survey Miscellaneous Field Studies Map MF-1060. 1 sheet, scale 1:1,000,000. Tarr, A. ,1982, Detection and location capability of the southeastern United States seismic network: Southeastern U.S. Seismic Network Bullatin No. 9, p. 36-4 2. Tarr , A. , Talwani, P. , Rhea, S. , Carver , D. , and Amick , D. , 19 81, Results of recent South Carolina: seismological studies: Bulletin of l the Seismological Society of Amer ica, v. 71, p.1883-1902. Toulmin, L.D., 1955, Cenozoic geology of southeastern Alabama, Florida, and Georgia: Bulletin of the American Association of Petroleum Geologists, v. 39, no. 2, p. 207-235. U.S. Army Corps of Engineers, Savannah District,1980, Navigation charts, Savannah River, Georgia and South Carolina, Savannah to Augusta: Corps of engineers, U.S. Army, Savannah, Georgia, 57 p. l U.S. Nuclear Regulatory Commission,1973, Seismic and geologic siting I criteria for nuclear power plants, Appendix A to 10 CFR 100: Federal Registar, 28 FR 31279. l Vail, P.R. , and Mitchum, R.M. Jr. ,1978, Global cycles of relative I changes of sea level from seismic stratigraphy: American Association of Petroleum Geologists Memoir 29, p. 469-472. Van Houten, F.B. , 1977, Triassic-Liassic deposits of Morocco and I eastern North America: Comparison: Bulletin of the American Association of Petroleum Geologists, v. 61, no.1, p. 79-99. Wentworth , C.M. , and Mergner-Keefer , M. , 1981, Reverse faulting along the eastern seaboard and the potential for large earthquakes: in Beavers, J.E. , ed. , Earthquakes and Earthquake-Engineering, Eastern U.S., v. 1, p. 109-128. l l ,
1 Wentworth, C.M. , and Mergner-Keefer, M. ,198 2a Regenerate faults of l ) small Cenozoic offset - probable earthquake sources in the southeastern i United States: in Gohn, G.S. , ed. , Studies related to the Charleston, , South Carolina, earthquake of 1886 - tectonics and seismicity J (collected abstracts): U.S. Geological Survey Open-File Report 82-134, j
- p. 34-35.
I Wentworth, C.M. , and Mergner-Keefer, M.,1982b Regenerate faults of small Cenozoic of fset as probable earthquake sources in the southeastern United States: U.S. Geological Survey professional Paper
- 1313, in press.
Winker, C.D., and Howard, J.D., 1977, Correlation of tectonically deformed shorelines on the southern Atlantic Coastal Plain: Geology,
- v. 5, no. 2, p. 12 3-127.
York, J.E. , and Oliver , J.E. ,1976, Cretaceous and Cenozoic faulting in I eastern North America: Geological Society of America ' no. 8, p. 1105-1114. letin, v. 87, Zietz, I. , and Gilbert, F.P. ,1980, Aeromagnetic map of part of the southeastern United States: In color: U.S. Geological Survey Geophysical Investigations Map GP-936,1 sheet, scale 1:2,000,000. I I I I I I
u I e l VOGTLE ELECTRIC l GENERATING g PLAl\T l
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MILLETT FAULT .- <, I Report Prepared for l l Georgia Power Company l I g /@ l ! OCTOBER 1982 I ' g VOLUME 11 APPENDICES I
I I ,I VOGTLE ELECTRIC 'I GENERATING I PLANT I I STUDIES OF l I POSTULATED I MILLETT FAULT I Report Prepared for I Georgia Power Company I I @ OCTOBER 1982 t 'I g VOLUME 11 APPENDICES I I
l TABLE OF CONTENTS - VCT.UbE II l 1 Appendix No. Title A ANNOTATED BIBLIOGRAPHY B OBSERVATION HELLS CONSTRUCTION REPORTS , C EXISTING DRILL HOLE AND WATER WELL DATA l ! D CORE LOGS E GEOPHYSICAL LOGS F S3ISMIC HSFLECTION STUDY (HARDING LAWSON) l G PETROGRAPHIC DESCRIPTIONS H HE AVY MINERAL ANALYSES I CLAY MINERALOGY STUDIES d 1 1 f f 5 il , ll 1 I ll I
h !I 1 1 I 4 l lI APPENDIX A i, f j ANNOTATED BIBLIOGRAPilY !I j 1 6 l 1 l l ir 1 i e a 1 4 k i i 4 3 l i 4 I L 4 1 4 I t d i J, l 4 e I i s ? 4
APPENDIX A Appendix A presents an annotated bibliography of referer.ces which were either cited in the report or used to provide background information. This appendix summarizes 1) journal articles, 2) theses, 3) State and Federal reports, maps and atlases, and 4) unpublished reports. The summaries in this appendix focus on the geology, ground water, seismology and geophysics of the southeastern Atlantic Coastal Plain. Each citation discusses the major points presented in its respective publication. I I I
I Ackermann, H.D. ,1982, Seismic-refraction study in the area of the Charleston, South Carolina,1886 earthquake: in,Gohn, G.S., ed., Studies Related to the Charleston, South Caro)ina, earthquake of I 1886-tectonics and seismicity (collected abstracts): Geological Survey Open-File Report 82-134, p. 11-12. U.S. Seismic refraction spreads in the area near Summerville, South I Carolina, show that the surface of the pre-Mesozoic crystalline basement complex consists of a northeast-trending ridge-like feature. The ridge is bounded on the northwest by I an abrupt 3,000 foot drop in altitude of the basement surface, inferred to represent a Triassic border fault. Fault-plane determinations indicate high-angle faults both parallel and perpendicular to the ridge-boundary fault. Ackermann, H.D., Bain, G.L., and Zohdy, A.A.R., 1976, Deep exploration of an east-coast Triassic basin using electrical resistivity: Geology, v. 4, no. 3, p. 137-140. Thirty-two Schlumberger soundings were made in the I Durham-Wadesboro Triassic Basin of North Carolina. The sounding measurements indicate a large resistivity contrast between the Triassic and the surrounding Piedmont rocks. I Depth interpretations indicate that the thickness of the Triassic sedimentary rocks is as much as 7,500 feet, while further interpretations show to shape of the basin to be consistent with the known geology. Advisory Committee on Reactor Safeguards, Subcommittee on Extreme External Phenomena, 1982, Nuclear Regulatory Commission, 704 p. Transcript of the January 28 and 29,1982 meeting of the Subconmittee on Extreme External Phenomena. Included are references to the 1886 Charleston, South Carolina earthquake and the Grand Gulf Nuclear Generating Station. Allied-General Nuclear Services,1980, Geological investigation at the Chem-Nuclear Waste Storage Site - Barnwell, South Carolina,17 p. This report represents a chronological journal of recent I studies related to reported faults in the burial trenches at the Chem-Nuclear storage site which is adjacent to the eastern site boundary of Allied-General Nuclear Services' Barnwell Nuclear Fuel Plant (BNFP). The observations made during this study do not conclusively indicate the origin of the faults and clastic dikes. They I could be related to regional tectonic deformations or to local movements caused by solution, subsidence, and weathering. The fact that the orientations of clastic dikes reported here are I : A-1 I
I different from the orientations reported by others suggests the control of local factors. In any event, the geologic work indicates that the processes responsible for the faults and clastic dikes in this area have not been active during the considerable period of time required for the development of the present soil profile. Allison, J.D. ,1980, Seismicity of the Central Georgia Seismic Zone: Georgia Institute of Technology, M.S. thesis, 204 p. The Central Georgia Seismic Zone is an area of east-central Georgia where thirteen historical earthquakes have occurred. l F Roughly defined as the area within a 47 mile radius of Milledgeville, Georgia, the Central Georgia Seismic Zone includes the Lake Sinclair and Lake Oconee areas where almost two hundred microearthquakes have been recorded from 1977 through June 19 80. Documentation of the historical events has resulted in a re-assignment of intensity based on the effects mentioned in the original newspaper accounts. The largest historical l earthquake occurred on March 5,1914 and had a maximum W intensity of VII. An isoseismal map constructed from newspaper intensity data gives a magnitude (MbLg) of 4.9 10.1 based on the area of the intensity IV isoseism. Antoine, J.W. , and Henry, V.J. , Jr. ,1965, Seismic refraction study of shallow part o,f continental shelf off Georgia: Bulletin of the American Association of Petroleum Geologists, v. 49, no. 5,
- p. 601-609.
Seismic refraction profiles over the shallow part of the continental shelf of f the Georgia coast showed: 1) a layer a few feet beneath the sea bottom, probably Miocene in age; 2) g the Oligocene; 3) the Early Exene; and 4) the pre-Cretaceous g basement surface. Structural contours on the Oligocene and Eocene refractors indicate the eastern boundary of the Atlantic Embaymer.t of Georgia. Applin, P.L., 1951, Preliminary report on buried pre-Mesozoic rocks in Florida and adjacent states: U.S. Geological Survey Circular 91, 28 p. The report proposes a threefold classification for the buried pre-Mesozoic rocks in Florida, the Coastal Plain of Georgia, and southeastern Alabama. These rocks are classified as: dominantly marine sedimentary Paleozoic rocks, which on the basis of faunal evidence, range in age from Late Cambrian or Early Ordovician to Silurian; rhyolitic lavas and pyroclastic l W rocks that are tentatively classified as early Paleozoic or I A-2 I I
I Precambrian; and granite, diorite, and metamorphic rocks, I I which are probably in part Precambrian and in part of Paleozoic age. Penetration has not been sufficient to show I definitely the vertical sequence of the different rock types that are encountered in different wells. The report discusses tentative conclusions on the sequence of the types of rocks in the foregoing classification. Applin, E.R. , and Applin, P.L. ,1964, Logs of selected wells in the Coastal Plain of Georgia: Georgia Geologic Survey Bulletin 74, 229 l p. This report contains lithologic and paleontologic dr ' criptions I of cuttings and cores from 31 selected wells in the Joastal Plain of Georgia. These descriptive logs are based on microscopic studies made periodically from 1937 to .1962. Bar tholomew, M.J. , Gathright , T.M. II, and Henica, W.S., 1981, A tectonic model for the Blue Ridge in central Virginia: American Journal of Science, v. 281, no. 9, p. 1164-1183. The two principal goals of this paper are to: 1) define and describe the major tectonic features formed in Paleozoic time in the central Blue Ridge and 2) provide a preliminary tectonic model for evolution of crystalline rocks of this region from middle Precambrian (Grenville-age) to middle Paleozoic time. Baum, G.R. , Collins, J.S. , Jones, R.M. , Madlinger , B.A. and Powell, R.J., 1980, Correlation of the Eocene strata of the Carolinas: South Carolina Geology, v. 24, no.1, p.19-27. The Santee Limestone is divided into two faunal zones. The Cross Member of the Santee Limed one is raised to the Cross Formation and is equivalent to the New Bern Formation in North Caro'. ina . I Bechtel Corporation,1969, Preliminary Safety Analysis Report, Appendix C - Barnwell Nuclear Fuel Plant: Unpublished report. General discussion of the geology and ground water of the Barnwell Nuclear Fuel Plant and Savannah River Plant. Bechtel Corporation, 1970, Safety Analysis Report, volume I, Barnwell Nuclear Fuel Plant: Unpublished report. The soils under the site area are capable of supporting the plant and related facilities without undue settlement under the conditions of static load, dynamic load and seismic load postulated in this report. A zone of silty and clayey sand I l A-3 l I l
I (Barnwell Formation) about 40 to 70 feet below the ground surface was investigated for susceptibility to liquefaction " under Design Base Earthquake conditions. To provide and adequate safety factor against soils liquefaction, a 15-foot berm of earth will be placed around the perimeter of the main a process building. No other potential geologic problems are know to exist. A conservative value of 0.12g should be , adequate for the Operating Basis Earthquake and 0.20g surface acceleration is recommended for the Design Basis Earthquake, based of historical seismic activity. Bechtel Corporation,1972, Applicants Environmental Report, volumes I and II - Alvin W. Vogtle Nuclear Plant: Unpublished report for Georgia Power Company, Atlanta, Georgia: Report on file at U.S. Geological Survey, Doraville, Georgia 30360. Brief sections on the geology, seismology, and geohydrology of the Vogtle Plant site. Drilling at the site and across the i river on the Atomic Energy Commission's Savannah River Project property established correlation of the Georgia-South Carolina geologic formations. The correlation was established by means of Oligocene, Eocene, and Cretaceous formations with excellent agreement found in several lithologic units. This interstate correlation of formations refutes the possibility of a g post-Cretaceous " Savannah River" fault. The site area has not g been subject to high seismic activity since deposition of Upper Cretaceous sediments. Shocks may be felt at the site from distance sources, but the intensity is expected to be no more that VI (MM). Bechtel Corporat' ion,1973, Preliminary Safety Analysis Report, volumes , II and III - Alvin W. Vogtle Nuclear Plant: Unpublished report for Georgia Power Company, Atlanta, Georgia: Report on file at U.S. Geological Survey, Doraville, Georgia 30360. Includes discussions of regional and site geology. The results are based both on a literature seatch and field exploration program. The stratigraphy presented in this report is in the process of being updated. Bechtel Corporation,1978, Gulf Trough structure study: Unpublished report, 8 p. Evaluation of the Gulf Trough in Georgia as a possible graben g structure using data furnished by Southern Company Services, g Inc. An appendix by George 0. Gates is included. Based on subsurface information, remote sensing analysis, and field studies the report concludes that the " horst and grcben" faulting theory attached to the Gulf Trough continues to be l B only hypothetical. The evidence suggests that other geologic phenomena, such as erosion, regional tilt, local subsidence or warping are the likely causes of the geologic feature. A-4 I
Mr. Gates concludes that the origin of the Gulf Trough is not clear. Data from well logs do not support any of the proposed origins and are compatible with all three. Behrendt, J.C. , Hamilton, R.M. , Ackermann, H.D. , and Henry, V.J. ,19 81, Cenozoic faulting in the vicinity of the Charleston, South Carolina, 1886 earthquake: Geology, v. 9, no. 3, p. 117-12 2. It is likely that the ancient thrust faults that exist in the I Charleston area and the current stress field are oriented in about the same direction as when the faults developed. Movement on these thrust faults is the primary cause of modern seismicity. Zones of Mesozoic rifting would now be I experiencing reverse fault movement on faults such as the Cooke and Helena Banks. Association of Charleston seismicity with Triassic structures raises the possibility that a I Charleston-type earthquake may not be limited to that immediate region. Behrendt, J.C. , Hamilton, R.M. , Ackermann, H.D. , Henry, V.J. , and Bayer, K.C., 1982, Marine multichannel seismic reflection evidence for Cenozoic faulting and deep crustal structure near Charleston, South Carolina: in Gohn, G.S., ed., Studies related to the Charleston, South Carolina, earthquake of 1836-tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Repor t 82-13 4, p.19-20. Suggests that the seismicity in the Charleston area is caused primarily by movement along the Appalachian decollement and that movement on the high-angle reverse faults in the area, although it is a second-order ef fect, also may cause earthquakes. Benson, P.H. ,1969, Evidence against a large scale disconformity between the Upper Cretaceous Black Creek and Peedee Formations in South Carolina: South Carolina Geologic Notes, v.13, no. 2,
- p. 47-50.
The stratigraphic and paleontologic evidence indicates an interfingering contact between Peedee and Black Creek lithologies. The presence of a large unconformity between the l= two formations in South Carolina is doubtful. ll lW Birdwell Division, Seismograph Service Corporation, 1972, Gravity-magnetic survey Savannah River Plant, Sou th Carolina, 34 p. jg A combined gravity-magnetic survey was run on the Savannah 'g River Plant. Six models were developed in an attempt to define the configuration of the basement rocks surrounding the Dunbarton Triassic Basin, underlying the Savannah River A-5 .I I
I Plant. The density contrasts used in the development of the models were based primarily upon information obtained from DRB 9 and theoretical conditions which could satisfy the observed gravity profiles. The results are such that several conclusions may be drawn. Black, W.W., 1979, Chemical characteristics of metavolcanics in the Carolina slate belt: i_r1 Wones, D.R. ed. , Proceedings on "the Caledonides in the USA" (I .G.C.P. project 27: Caledonide orogen): Virginia Polytechnic Institute and State University, Department of g Geological Sciences, Memoir no. 2. , Blacksburg, Virginia, 24061, g
- p. 271-278.
Rocks of the Carolina Slate Belt were formed in a volcanic arc (island arc) environment and have since been metamorphosed to the greenschist facies. The structure of the Carolina Slate Belt, on a gross scale, is a series of alternating anticlines , and synclines. On a fine scale, it is sometimes " layer-cake" while in other places it is intensely deformed into tight - folds which are nearly vertical. Seismic data in several places suggest that the slate belt extends to a depth of six i to seven miles. Bland, A.E. , and Blackburn, W.H. ,1979, Geochemical studies on the greenstones of the Atlantic Seaboard Volcanic Province, south-central Appalachians: in Wones, D.R. ed. , Proceedings on the "Caledonides in the USA" (I.G.C.P. project 27: Caledonide orogen): Virginia Polytechnic Institute and State University, l W Department of Ceological Sciences Memoir no. 2, Blacksburg, Virginia, 24061, p. 263-270. The tracc element data and its tectonic implications have placed constraints on the interpretation of the tectonic evolution of the south-central Appalachians. The chemical c data has defined the majority of the Atlantic Seaboard Volcanic Province as related to island arc development. Bollinger, G.A., 1972, Historical and recent seismic activity in South Carolina: Bulletin of the Seismological Society of America, v. 62, no. 3, p. 8 51-86 4. The great Charleston earthquake of August 31, 1886 dominates the seismic history of South Carolina and is often cited as an example that no regior is completely safe from earthquake l, up hazard. This paper presents a review and summary of what has been published on the 1886 shock and the subsequent seismic activity in South Carolina; a report on a three-month g microearthauake recording program conducted during the summer gI of 1971 in the Charleston area; and the results of seismic studies of the four earthquakes that occurred in the state during 1971. A-6 I!
I Bollinger, G.A., and Murphy, C.A., 1978, Seismicity of the southeastern United States: Southeastern U.S. Seismic Network Bulletin No.1. A compilation of seismic events recorded ir. the southeastern United States. This report also contains information on ! seismic stations in operation in the area under study, j I Bollinger , G. A. , and Ma thena, E. , 1978-1982, Seismicity of the southeastern United States: Southeastern U.S. Seismic Network Bulletins No. 2-9. l A compilation of seismic events recorded in the southeastern United States. Bonini, W.E. , and Woollard, G.P. ,1960, Subsurface geology of North Carolina - South Carolina Coastal Plain from sei aic data: I Bulletin of the American Association of Petroleum Geologists,
- v. 44, no. 3, p. 298-315.
I This article provides an analysis of 60 seismic-refraction measurements on the Coastal Plain of North Carolina and South Carolina and 39 measurements in the Piedmont Province. The following conclusions were made: 1) the Piedmont complex I extends under the Coastal Plain sedivents as far east as the present coast, 2) the Carolina Slate Belt extends under the Coastal Plain, and reaches a maximum of 80 miles in North Carolina, 3) the buried Florence Triassic Basin is 40 by 13 miles and strikes east-northeast, 4) the Cape Fear Arch has moved twice since Cretaceous time, 5) the Pre-Cretaceous basement is an erosional surface with topographic relief on the order of 200 feet, 6) the break in basement slope in eastern North Carolina must be projected seaward of Cape Fear and the South Carolina coast, 7) there is the suggestion of an I east-west syncline superimposed on the steeper basement slope in eastern North Carolina. Bott, M.H. ,1978, Subsidence mechanisms at passive continental I. margins: American Association of Petroleum Geologists Memoir 29,
- p. 3-9.
I There are four main stages in the tectonic development of a rif ted passive margin: 1) the rift valley stage involving early graben formation, 2) the youthful stage, lasting about I 50 million years af ter the onset of spreading, 3) the mature stage during which more subdued regional subsidence may continue (present stage in the development of most of the Atlantic margins) , and 4) .he fracture, when subduction I starts. This paper discusses recently proposed mechanisms for subsidence at passive margins: 1) gravity loading mechanisms based on local or flextural isostacy, 2) thermal hypotheses,
- 3) crustal creep hypotheses, and 4) necking of the crust at I- incipient margins (not favored); a mechanism for early graben formation prior to splitting provided by applying the Vening Meinesz wedge subsidence hypothesis to the upper brittle part of the crust.
A-7
s Bramlett, K.W., Secor, D.T., and Prowell, D.C., 1980, Displacement on the Belair fault zone in South Carolina: Geological Society of America (abs. ) , v. 12, no. 4, p. 171-17 2. - This article discusses two important fault systems in the crystalline piedmont rocks along the Atlantic Coastal Plain in Georgia and South Carolina. The eastern Piedmont fault system of unknown displacement, trends N70*E along the Fall Line and is late Paleozoic and perhaps early Mesozoic in age. The g Belair fault trends N25'E to N30*E and has undergone Tertiary g displacement. Cretaceous displacement has been 98 feet vertical and 14 miles left-lateral strike-slip displacement. Brooks, H.K., Gremillion, L.R., Olson, N.K., Puri, H.S., 1966, Geology of the Miocene and Pliocene series in the north Florida - south Georgia area: Atlantic Coastal Plain Geological Association and Southeastern Geological Society, 94 p. The Miocene and Pliocene series of the extreme north Florida - South Georgia area have one overall characteristic in common. Terrestrial and near shore marine conditions prevailed throughout this sub-region as evidenced by land vertebrate and marine invertebrate fossils, character of sediments, l composition of the clay minerals, and associated factors, u Brown, P.M., 1974, Subsurface correlation of Mesozoic rocks in Georgia, g in Stafford, L.P., Symposium on the Petroleum Geology of the g Georgia Coastal Plain: Georgia Geologic Survey Bulletin 87,
- p. 45-59.
Mesozoic rocks present in the Georgia Coastal Plain are considered to be Comanchean and Gulfian in age. Comanchean rocks attain a maximum thickness in excess of 2,500 feet in the extreme southwest part of Georgia, have a variable thickness of 100 to 300 feet in the tier of counties that border the Atlantic Ocean and are proportionately thinner or absent in most other segments of the state. Gulfian rocks are proportionately thickest in the central part of the state. Brown, P.M., Brown, D.L., Reid, M.S., and Lloyd, O.B., Jr., 1979, Evaluation of the geologic and hydrologic factors related to the ' waste-storage potential of Mesozoic aquifers in the southern part of the Atlantic Coastal Plain, South Carolina and Georgia: U.S. Geological Survey Professional Paper 1088, 37 p. This report describes the subsurface distribution of rocks of Cretaceous to Late Jurassic (?) age in the Atlantic Coastal Plain, South Carolina, and Georgia, and examines their potential for deep-well waste storage. Subsurface data, A-8
n derived from study of well cuttings, cores, and geophysical logs from about 400 wells, 88 of which make up a key-well network, were used to develop the concept and definition of a waste-storage " operational unit." This data was used to construct 32 regional maps and eight stratigraphic cross sections. Buf fler , R.T. , Watkins, J.S. and Dillion, W.P. ,1979, Geology of the of fshore Southeast Georgia Embayment, United States. Atlantic continental margin based on multichannel seismic reflection profiles: American Association of Petroleum Geologists Memoir 29, p . 11-2 5 . Discusses a geologic interpretation of the offshore Southeast Georgia Embayment based on a 680 mile multichannel seismic reflection survey. The Southeast Georgia Embayment consists of a wedge of Cretaceous and Cenozoic sedimentary rocks that thins from three to five miles beneath the Blake Plateau to about 0.6 miles over the Cape Fear Arch. This sedimentary section is divided into three major seismic intervals. Buie, B.F.,1978, The Huber Formation of eastern central Georgia: Georgia Geologic Survey Bulletin 93, p. 1-7. The term "Huber Formation" is proposed for all of the post-Cretaceous pre-late Eocene strata in the kaolin mining districts of Georgia, northeast of the Ocmulgee River. The lithology of the Huber Formation as a whole is very diverse, ranging from beds of high-purity and sandy kaolin to thick, cross-bedded members of coarse, pebbly sand, and even conglomerate composed of boulders of pisolitic kaolin. Buie, B.F. ,1980, Kaolin deposits and the Cretaceous-Tertiary boundary in east-central Georgia: Geological Society of America, Field Trip No. 15, p. 311-322. I The Cretaceous-Tertiary boundary in east-central Georgia, formerly placed at the top of the highest kaolin bed in local stratigraphic sections, is now known to be lower; invertebrate fossils of Tertiary age demonstrably underlie some kaolins. The fossils and their stratigraphic relationships also help distinguish between Claitarnian (middle Eocene) and Jacksonian (upper Eocene) strata, which are separated by an unconformity. These Coastal Plain deposits are characterized structurally by gentle dips and lack of significant folds or faults, although joints are common locally. Butts, C., and Gildersleeve, B., 1948, Geology and mineral resources of the Paleozoic area in northwest Georgia: Georgia Geologic Survey Bulletin 54, p. 3-8. The Paleozoic rocks of Georgia are in that part of the eastern United States known as the Appalachian valley. This area is I A-9
I bounded on the east and south by the outcrop or trace of a great overthrust fault plane on which more ancient rocks are thrust over the Paleozoic rocks. The fault is located easily by the abrupt change from the stratified Paleozoic rocks to the flaky, greenish schist of the overthrust mass. Callahan, J.T. ,1964, The yield of sedimentary aquifers of the Coastal g Plain southeast river basins: U.S. Geological Survey Water-Supply E Paper 1669-W, 56 p. The aquifer systems of the study area, from lowermost to uppermost, include: the sand aquifers of Cretaceous age; the limestone and sand aquifers of early Tertiary age; the principal artesian aquifer of Eocene, Oligocene, and Miocene age; the sand and gravel aquifers of Miocene and post-Miocene l W age of the southwestern area; and the sand aquifers of Miocene and Pliocene to Recent age of the Atlantic coast. The safe yield of the aquifer systems was estimated from known geologic and hydrologic data and by making broad assumptions regarding the extent, thickness, and permeability of the aquifers and the continuity of physical conditions that control the occurrence and movement of ground water. Carter, R.F. , and Putnam, S.A. ,1978, Low-flow frequency of Georgia streams: U.S. Geological Survey Water-Resources Investigations 77-127, 104 p. This report contains analyses of low-flow data and tabulations of computed low-flow frequency for all stream sites in Georgia where suitable flow records have been collected. These l include 134 continuous-record gaging stations and 102 m partial-record gaging stations. Frequency records for gaging stations with short records have been adjusted where possible to more closely represent results that would have been obtained from longer records. Carver , R.E . , 1966, Stratigraphy of the Jackson Group (Eocene) in central Georgia: Southeastern Geology, v. 7, no. 2, p. 83-91. In central Georgia two distinct facies of the Jackson Group are present. The dominantly calcareous Ocala facies lies to the south and southeast and the dominantly clastic Barnwell facies to the north and east. The Barnwell facies, composed of the Twiggs Clay, Irwinton Sand, and Upper Sand Members of j the Barnwell Formation, is a regressive sequence entirely i equivalent to the Ocala Limestone of the coastal area. The Ocala facies consists of the Ocala Limestone and Cooper Marl. The Cooper Marl is equivalent to upper parts of the Ocala l Limestone. I A-10 l l l l
I Carver, R.E. ,1972, Stratigraphy of the Jackson Group in eastern Georgia: Southeastern Geology, v.14, no. 3, p.153-181. The Jackson Group in eastern Georgia is predominantly upper Eocene in age. It is a transgressive-regrecsive sequence with a thin, extensively developed transgressive sand and a much thicker, more complex fine- to coarse-clastic regressive phas e. In downdip areas the group is represented by the Ocala Limestone; in updip areas, by fluviatile sediments indistinguishable from the Late Cretaceous to possibly middle Eocene Middendorf Formation. Between the downdip marine limestone facies and the updip fluviatile facies occurs a I lithologically complex nearshore facies, the Barnwell Formation. While general patterns of lithologic distribution can be recognized and the formation roughly divided into members, individual lithologic units are lenticular or deeply channeled and can not be traced over distances of more than a very few miles. Carver, R.E. , and Scott, R.M. ,1978, Stratigraphic significance of heavy minerals in Atlantic Coastal Plain sediments of Georgia: Georgia Geologic Survey Bulletin 93, p.11-14. Composition of the heavy mineral suite of Atlantic Coastal Plain sediments is largely determined by the degree of intrastratal solution of the unstable heavy mineral suite: hornblende, epidote, and garnet. Piedmont rivers carry sediment rich in hornblende and epidote to the coast, but hornblende and epidote in this sediment are diluted by mixing of river sediment with more mature coastal plain sediment, and in addition, are depleted by post-depositional intrastratal solution. Cederstrom, D.J. , Boswell, E.H. , and Tarver , G.R. ,1979, Summary appraisals of the nation's ground water resources, South Atlantic-Gulf region: U.S. Geological Survey Professional Paper 813-0, 35 p. Enormous quantities of ground water are available in the South I Atlantic-Gulf states in the extensive aquifers that underlie the Coastal Plain Province. The principal coastal plain aquifers consist largely of deltaic sand and gravel deposits of Cretaceous to Quaternary age; however, a notable exception is the highly permeable Tertiary limestone aquifer, which underlies parts of four states. Most of the major coastal plain aquifers are recharged where they are exposed and water moves downdip to the south. The general direction of ground water movement in the coastal plain aquifers is seaward. There is, however, movement of water vertically and laterally that affects pressure and quality in every aquifer. A-ll I
r Champion, J.W. , Jr. ,1975, A detailed gravity study of the Charleston, South Carolina, epicentral zone, Georgia Institute of Technology, M.S. thesis, 97 p. Approximately 2,000 new gravity measurements were made near Charleston, South Carolina, in the suspected epicentral zone of the 1886 earthquake. These data were used to construct a simple Bouguer gravity map. In the central western quadrangle, a large positive anomaly exhibits a steep gravity gradient of two to three milligals per kilometer on both its northern and southern sides. This anomaly is considered to result from basic flows intermixed with coastal plain sediments. Surrounding this anomaly there are large negative anomalies which are interpreted to be representative of deep sedimentary basins. Three-dimensional modeling of the simple Bouguer gravity data shows that the linear alignment of anomalies can be interpreted to result from basic flows which are down-faulted to the southeast. The throw on the interpreted fault would be on the order of one mile. In general, it is not unreasonable to expect that such a fault exists under the Atlantic Coastal Plain because many such buried grabens have been found. If a graben is present, isostatic readjustments within such a down-faulted block may explain the earthquake activity in this area. Cheetham, A.,1959, Late Eocene zoogeography of the eastern Gulf Coast region: Columbia University, Ph.D. disertation, 212 p. Calcareous upper Eocene (Jacksonia n) sediments in southeastern Alabama, southwestern Georgia, and Florida contrast markedly with stratigraphically equivalent terrigenous deposits from central Alabama westward. The enclosed fossils, chiefly marine invertebrates, permit subdivision of the Jacksonian Stage into stratigraphic (zones) and geographic (biofacies) units. This study is concerned primarily with the abundance and distribution of invertebrate fossils, particularly chellostome bryozoans, in the four major biofacies of the eastern Gulf Coast Jacksonian. Chowns, T.M., 1976, Paleogeology of the pre-Cretaceous surface beneath the Georgia Coastal Plain: A reassessment: Bulletin of the Georgia Academy of Science, v. 34, no. 2, p. 82. Pre-Cretaceous rocks of the Georgia Coastal Plain include: 1) a medium-high grade metamorphic suite, restricted to an area 30-90 miles south of the fall line, 2) a Cambrian or Precambrian (?) volcanic terrane, 3) fossiliferous, marine and A-12
nonmarine Paleozoic sandstones which extend into Florida; and
- 4) a continental red bed association, probably of Triassic age, frequently intruded by diabase, which forms a large graben in the south-central and southwestern part of the state. This graben forms the structural framework of the northern part of the Appalachicola Embayment.
Chowns, T.M. ,1978, Pre-Cretaceous geology beneath Georgia Coastal Plain: Bulletin of the American Association of Petroleum Geologists, v. 62, no. 3, p. 504. The pre-Cretaceous surface beneath the Georgia Coastal Plain is composed of four distinct tetranes. These are 1) a medium-to high-grade metamorphic terrance continuous with the Piedmont, 2) a Cambrian (?) felsic volcanic terrane with associated granite plutons underlying the Sout least Georgia Embayment and Swannee Saddle, and 3) a sequence of fossiliferous marine Paleozoic sandstones and shales (Lower Ordovician-Middle Devonian), which subcrop in the, extreme southeast and soutevest of the state, and extend southward to form the nucleus of the Peninsular Arch in Florida, and 4) a continental red-bed association, probably of Triassic age, occupying a large graben which forms the structural framework for the Appalachicola Embayment. Chowna, T.M. , and Williams, C.T. ,1982, Pre-Cretaceous rocks beneath the Georgia Coastal Plain--Regional implications: M Gohn, G.S., ed. , Studies related to the Charleston, South Carolina, earthquake of 1886-tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Report 82-134, p. 23-24. Four major " basement" terrances are recognized in the southern Atlantic and Gulf Coastal Plains. The first consists of medium- to high-grade metamorphic rocks and granitic plutons immediately south of the Fall Line and represents the subsurface continuation of the Piedmont province. In south Georgia, the " basement" is quite different and comprises a terrane of mildly deformed Paleozoic sedimentary rocks underlain by a terrane of felsic volcanic rocks. These two anomalous terranes are separated from the buried Piedmont by a fourth terrane of lower Mesozoic continental red beds correlated with the Newark Group. The red beds are known to , be at least 11,500 feet thick and occupy a complex graben, the South Georgia Basin. The red beds contain dikes and sills of tholeitic diabase belonging to the lower Mesozoic eastern North American suite. Christl, R.J. ,1964, Storage of radioactive wastes in basement rock beneath the Savannah River Plant: U.S. Atomic Energy Commission, DP-844, 105 p. The ground beneath the Savannah River Plant ras explored to 1 determine the feasibility of storing radioactive wastes in the underlying crystalline basement rocks. The hydrology of the basement rock and overburden was reviewed. A-13
I Christopher R.A. , 1982, Palynostratigraphy of the basal Cretaceous units of the eastern Gulf and southern Atlantic Coastal Plains in Arden, D.D. , Beck , B.F. , and Morrow, E. , ed. , Second Symposium on the Geology of the Southeastern Coastal Plain, p.10-23. Palynologic examination of samples from the Tuscaloosa Formation of Alabama and western Georgia placed them in pollen zone IV of late Cenomanian age. Pollen in eastern Georgia is placed into pollen zone V of latest Coniacian or Santonian. The two are separated by a hiatus representing Turonian and almost all of the Coniacian age. Colquhoun, D.J. ,1965, Terrace sediment complexes in central South Carolina: Atlantic Coastal Plain Geological Association, Field I W Conference, 62 p. Coastal Plain terraces-formations are sediment complexes bounded above by terrestrial and marine landforms and below by terrestrial and marine unconformities. Between these surficial and basal surfaces are lithologic facies, biologic facies and paleoecologic zones representative of Recent coastal plain and shelf environments. Eleven terraces are to be noted. Seven terrace-formations have been proven to exist. Colquhoun , D.J. , Heron , D.S. , Jr. , Johnson, H.S. , Jr. , Pooser , W.K. , and Siple, G.E., 1969, Updip Paleocene-Eocene stratigraphy of Soath g Carolina reviewed: South Carolina Geologic Notes, v.13, no. 3
- p. 1-26. g!
l Detailed information on the establishment of the type section, variations in lithology, mineralogy, common sedimentary l-a structures, paleontology, depositional environments, contacts, age, and correlation of formations of Cretaceous, Paleocene and Eocene age. Two major marine transgressions with respect to tha continent are apparent within the strata studied. The first occurred in Late Cretaceous time and continued into early Eocene time. The second began in the middle Eocene and continued until at least late Eocene or Oligocene. Conn, W.V., 1954, Soil and geologic features of Buford Projec'. Project of the American Society of Civil Engineers, v. 80, no. 425, l W 10 p. This report discusses the geology and soils of the Buford Dam site on the Chattahoochee river in Gwinnett and Forsyth Counties. Connell, J.F.L. ,1955, Stratigraphy and paleontology of the Jackson Group of Georgia, University of Oklahoma, M.S. thesis, 348 p. This report entails a study of the stratigraphic position, facies relationship, and fauna of beds of Jackson age in the A-14
I l Coastal Plain of Georgia. The Jackson Group of Georgia is l composed of two formations, the Ocala Limestone and the j Barnwell sands and clays. The Ocala Limestone has at its base < in central Georgia a tongue of soft, cream to white bryozoan i limestone, and a bed of uncemented, tan, calcareous sand, thus constituting a unit known as the Tivola tongue of the Ocala. The Barnwell Formation consists of several members differentiated by many authors because of distinctive lithologies. In the writer's opinion, the argillaceous red sands composing the typical Barnwell, i.e., outside the area of outcrop of the Irwinton and Upper Sand members, should be termed the Uppermost Red Sand Member of the Barnwell Formation. The Barnwell and Ocala Formations are stratigraphic equivalents, intergrading in central Georgia, and thus indicating a change from littoral facies of predominantly red argillaceous sand and gray to green fuller 's earth type clay to the north and northeast, to deeper water off-shore deposits of relatively pure, extremely fossiliferous limestone to the south and southwest. Cook, F. A. , and Oliver , J.E . ,1981, The late Precambrian-early Paleozoic continental edge in the Appalachian orogen: American Journal of Science, v. 281, no. 8, p. 993-1008. This report presents an interpretation which integrates data from gravity, seismic reflection, seismic refraction, I magnetics, and surface geology studies and suggests that the major crustal change from thick continental crust to thin oceanic or attenuated continental crust is present beneath the crystalline rocks of the southern Appalachians. This interpretation favors the notion that the Blue Ridge and Inner Piedmont constitute an allochthonous sheet overlying sedimentary strata of the late Precambrian-early Paleozoic shelf, at least as far east as the east edge of the Inner Piedmont. Cook , P. A. , Brown, L.D. , and Oliver , J .E . , 1980, The southern Appalachians and the growth of continents: Scientific American,
- v. 2 43, no. 4, p. 156-16 8.
Due to the petroleum industry's exploration technique of seismic-reflection profiles much is being learned about the formation and structure of the continents. By using the technique, new details of the geological structure of the continental basement have been mapped. Application of the technique in the southern Appalachians reveals how the margins of continents change as ocean basins close and continents collide at subduction zones. Profiles made in the southern Appalachians revealed that the mountains are underlain to a depth of at least 11 miles by horizontal layers of material A-15
t that is sedimentary or once was. Furthermore, these horizontal sedimentary strata are younger than or contemporaneous with the highly deformed, metamorphic rocks which overlie them. ; - Cook F. A. , Brown, L.D. , Kaufman, S. , Oliver , J .E . , and Peter sen, T. A. , I 1981, CCOORP seismic profiling of the Appalachian orogen beneath
- the Coastal Plain of Georgia: Geological Society of America Bulletin, part I, v. 92, no.10, p. 738-743.
f A southeastward extension onto the coastal plain of an earlier COCORP has provided some spectacular reflections most of which can be interpreted as either fault surfaces or as metamorphosed strata of late Precambrian-early Paleozoic age. The reflections are consistent with the hypothesis that a major detachment extends eastward beneath this part of the orogen. Deep reflections indicate that the structural g configuration of the rocks is complex and that the remains of g a collision zone are being observed. In conjunction with surface geologic information, these new data demonstrate that , late Paleozoic compressive deformation was pervasive and l resulted in lateral movements in the upper crust, extending from the valley and ridge to the crystalline rocks beneath.the coastal plain. Cook , F.A. , Albaugh , D.S. , Brown , L.D. , Kaufman , S. , Oliver , J .E . , and Hatcher, R., 1979a, the Brevard fault: A subsidiary thrust fault to g the southern Appalachian sole thrust: in_ Wones, D.R. ed., g Proceedings on the "Caledonides in the USA" (I .G.C.P. project 27: Caledonide orogen): Virginia Polytechnic Institute and State
=
University, Departmer' of Geological Sciences, Memoir no. 2, l Blacksburg, Virginia, 24061, p. 205-213.
- Seismic reflection profiling by COCORP has resulted in the g discovery of a thin, layered sequence of Paleozoic sedimentary 3 rocks underlying a four to nine mile thick layer of the crystalline rocks of the Blue Ridge, Inner Piedmont, and possibly the Charlotte Belt and Carolina Slate Belt in the (
southern Appalachians. These sediments appear remarkably undisturbed, and their configuration implied that the overlying thin crystalline sheet has overthrust the Paleoisic continental margin of the southeastern United States for a distance of perhaps 160 miles or more. Cook, F.A., Albaugh, D.3., Brown, L.D., Kaufman, S., Oliver, J.E., and t Hatcher , R.D. , Jr . ,1979b, Thin-skinned tectonics in the crys *.alline southern Appalachians, COCORP seismic-reflection profiling of the Blue Ridge and Piedmont: Geology, v. 7, no. 12,
- p. 563-567.
COCORP seismic-reflection profiling in Georgia, North Carolina, and Tennessee and related geological data indicate that the crystalline Precambrian and Paleozoic rocks of the II A-16 I
I ,
~
l I Blue Ridge, Inner Piedmont, Charlotte Belt, and Carolina Slate Belt constitute an allochthonous sheet, generally four to nine miles thick, which overlies relatively flat-lying authochthonous lower Paleozoic sedimentary rocks, 0.6 to three miles thick, of the proto-Atlantic continental margin. Thus, the crystalline rocks of the southern Appalachians appear to I have been thrust at least 161 miles to the west, and they overlie sedimentary rocks that cover an extensive area of the central and southern Appalachians. Cooke, C.U.,1931, Seven coastal terranes' in the southeastern states: Journal of the Washington Academy of Science, v. 21, no. 21,
- p. 503-513.
This paper discusses the development, elevation, and locations of seven Pleistocene coastal terraces. These terraces are I attribu*ed to sea level fluctuations due to variations in the volume of water in continental ice sheets. Cooke, C.W.,1936, Geology of the Coastal Plain of South Carolina: U.S. Geological Geological Survey Bulletin 867, 196 p. This bulletin discusses physical geography, stratigraphy, structure, geologic history, mineral resources, and ground water. The geologic history of South Carolina records many advances and retreats of the sea during which sediments were deposited and planed off time and again. Many of the formations that were once continuous now persist only as small remanants. The shif tings of the shore lir,e during Pleistocene time are regarded by the writer as due partly to glacial control of sea level. Cooke, C.W.,1943, Geology of the Coastal Plain of Georgia: U.S. Geological Survey Bulletin 941, 121 p. The major portion of this bulletin is a detailed discussion of the sediments found in the Coastal Plain of Georgia. A significant feature is the much more complete outcrop of the formations in the west than elsewhere. Near the Chattahoochee River,11 formations are exposed between the Tuscaloosa and the Hawthorn Formations. Near the Ocmulgee River there are only four, and along the Savannah River there are only three. This difference is the result of progressive overlap. It I appears to indicate either an intermittent downwarp in the central and eastern parts of the s, tate, which permitted the ocean to advance farther and farther inland, or an uplift in the west, which hastened the erosion of the littoral facies of the younger formations and exposed more and more of the underlying beds. I A-17 I
7 1 Cooke, C.W., and MacNeil, P.S.,1952, Tertiary stratigraphy of South Carolina: U.S. Geological Survey Professional Paper 243-B,
- p. 19-29.
The following changes in the current classification of the Tertiary formations of South Carolina are proposed: 1) the Black Mingo Formation, mainly of Wilcox age, may include some Paleocene deposits, 2) the McBean Formation, heretofore including all the deposits of known Claiborne age in South Carolina, is restricted to the Ostrea sellaeformis Zone, of late middle C1'aiborne age, and the names Congaree Formation (equivalent to the Tallahatta Formation) and Warley Hill Marl (equivalent to the Winona Formation) are revived for deposits of early Claiborne and early middle Claiborne age, 3) a large part of the deposits mapped as Barnwell Format. ion (of Jackson age) proves to be Congaree, 4) the Santee Limestone, heretofore supposed to be of early Jackson age, represents the g Ostrea sellaeformis Zone and seems to be an offshore facies of the restricted McBean Formation, 5) the Cooper Marl currently E referred to the late Eocene (Jack son) , is reassigned to the early Oligocene (?) , 6) grave,lly facies of the Mioc,ene Hawthorn Formation similar to that in Georgia is recognized for the first time in South Carolina, where the formation had previously been recognized only by its offshore facies. Cooke, C.W., and Shearer, H.K. ,1918, Deposits of Claiborne and Jackson age in Georgia: U.S. Geological Survey Professional Paper 120,
- p. 41-81.
An early summary of Eocene deposits in Georgia which places the Barnwell " sand" in the Jackson and changes the name to Barnwell Formation. The "Congaree" clay member of the McBean Fortuation is placed in the Barnwell formation and renamed the Twiggs Clay. Cornet, B. , Traverse, A. , and Mcdonald, N.G. ,1973, Fossil spores, pollen and fishes from Connecticut indicate Early Jurassic age for, part of the Newark Group: Science, v.182, no. 4118, p.1243-1247 Palynologically productive localities have been found throughout the Newark Group basins. Palynological data g indicate that the Newark Group has considerable g time-stratigraphic range: Upper Triassic for the Cumnock Formation (North Carolina) , the Vinita Beds (Virginia), and the upper New Oxford Formation (Pennsylvania) , Raeto-Liassic for the Brunswick Formation (New Jersey), Portland Formation (Connecticut and Massachusetts) , and the Shuttle Meadow Formation (Connecticut) . Cramer, H.R.,1969, Structural features of the Coastal Plain of Georgia: Southeastern Geology, v. 10, no. 2, p. 111-123. The structural features of the Coastal Plain of Georgia appears to be both Cretaceous and Cenozoic in age. There is a g '. A-18 i
.1
southwest-northeast alignment of the features and specific geophysical trends such as gravity and magnetic anomaly alignments. Tension appears to have been a predominant source of energy for the faulting. Cramer, H.R.,1974, Isopach and lithofacies analyses of the Cretaceous and Cenozoic rocks of the Coastal Plain of Georgia, in Stafford,_ L.P., Symposium on the Petroleum Geology of the Georgia Coastal Plain: Georgia Geological Survey Bulletin 87, p. 21-44. Volumes of sedimentary rocks are computed from isopach-contour maps. Periods of greatest sedimentation are the Upper Cretaceous and Eocene. Det.ttiled lithofacies maps are included. Cramer, H.R. , and Arden, D.D. , 1978, Faults in Oligocene rocks of Georgia Coastal Plain: Geological Society of America (abs . ) ,
^
V '9. 4, p.156. taulting dominates the interpretation of isopach and ' structure-contour maps of Oligocene rocks from the Georgia Coastal Plain. Faults include: one which is a pronounced graben,'up to ten miles wide, trending northeastward from Decatur and Grady Counties throvoh northern Coffee County to at least the Savannah River. The. throw is several hundred feet. Oligocene and Miocene rocks in the graben are thicker, with Oligocene rocks thin to absent on the upthrown sides. Cramer , H.R. , and Arden, D.D. ,'1980 Subsurface Cretaceous and Paleogene geclogy of the Coastal Plain of Georgia: Georgia Geologic Survey Opea-File 'Repor tf80-8,184 p. , t . The report provides a detailed stratigraphic framework of the Coastal Plain of Georgia and serves to update work published over the previous 15 yc'ars. _DJsement includes paleontologically dated Paleozoic rocks and radiometrically detected Triassic rocks. Granitic, volcanic and metamorphic
, crystalline rocks ase also present. Cretaceous rocks are Comanchean and Gulfiar,in age. Rocks of all Tertiary ages
~
exist in the Coastal $ lain. The Gulf Trough fault theory is
- g. , supported. -
L ' l - 7tamar, H.R., and Grant, W.H. ,< 1965, Some highlights of the Cretaceous
- and crystalline terranes of Georgia, in Southeastern Geological Society, lith Field Trip
- Emory 'Un iver sity, p. 2-11.
Cretaceous rocks in Georhia are exposed in a thin Ifand along the Fall Line in Georgia. Downdip, in the subsurface, the
. Cretaceous system is generally identified only as Tuscaloosa Formation and " post-Tuscaloosa undif ferentiated". Marinu and '
r A-19 w m f p
- j. -h #
.g' 4
4 6
. L - ,
}, .
.;^,. -g, .f .Y , .
I nonmarine (or at least deltaic) sediments exhibit striking alternation. It seems evident that Cretaceous exposures in Georgia represent the deposits of a fluctuating strand line during the Upper Cretaceous and this area is critical for correlation purposes. These rocks are tLe easternmost exposures of the Gulf Coast Cretaceous. Crawford, M.L. , and Crawford, W. A. , 1980, Metamorphic and tectonic history of the Pennsylvania Piedmont: Journal of the Geological Society of London, v. 137, part 3, p. 311-320. The Piedmont Province of southeastern Pennsylvania consists of moderately to highly metamorphosed rocks ranging in age from Precambrian to Ordovician. Three episodes of metamorphism have occurred and include: a one billion years B.P. regional granulite facies episode, a second younger end lower pressure granulite facies episode, and a greenschist to upper amphibolite facies episode. The proposed tectonic model includes a rif ting of continental basement forming a basin with a lower Paleozoic carbonate bank on the northwestern margin and an island arc to the southeast. Crickmay, G.W., 1952, Geology of the crystalline rocks of Georgia: Georgia Geologic Survey Bulletin 58, 54 p. The crystalline rocks of Georgia occupy the piedmont, upland, and highland provinces, and underlie about one third of the state. This paper offers general descriptions of mineral resources, stratigraphy and a historical summary, but is necessari1.y brief. E 4 Dallmeyer, R.D., 1975, The Palisades Sill: A Jurassic intrusion? W Estidence from 40 Ar/39 Ar incremental release ages: Geology,
- v. 3, no. 5, p. 243-245.
Available K-Ar dates from the Palisades Sill (14 2 to 202 m.y.B.P.) are generally younger than the ages of post-Triassic intrusiv? rocks in other areas. 40Ar/ 39A r release spectra of chiAl-zone samples record of ages of 192 and 186 m.y.B.P. and furnish no evidence of posterystallization argon loss. These ages are s?.milar to published K-Ar biotite ages and probably refer te the time of crystallization of the sill. Recent palynologic studies in the Hartford Basin have shown that rocks stratigraphically equivalent to those intruded by the Palisades are, in part, of Early Jurassic age. Dames and Moore, Inc., 1980, Review of potential host rocks for radioactive waste disposal in the southeast United State-Triassic basin subregion: E.I. duPont de Nemours and Company, Savannah l
=
River Laboratory, DP-1569. An evaluation of the exposed and buried Triassic basins from Maryland to Georgia. The purpose of the evaluation was to determine the feasibility of these basins as repositories for g radioactive wastes. g A-20
Daniels, D.L., 1974, Geologic interpretation of geophysical maps, central Savannah River area, South Carolina and Georgia: U.S. Geological Survey Geophysical Investigations Map GP-893, 3 sheets, scale-sheets 1 and 2 - 1:250,000, sheet 3 - 1:500,000. Interpretive geologic , map showing Carolina Slate Belt, I Charlotte Belt, Kiokee Belt, and Belair Belt rocks. Aeromagnetic map and aeroradioactivity level map. Region covered is northwest of Millett fault study area (Sheet 1 of 3). Aeromagnetic map of Piedmont part of Savannah River Plant (af ter Petty and others,1965) (Sheet 2 of 3). Aeromagnetic map with interpretive bedrock geology of coastal plain (after Petty and others,1965) (Sheet 3 of 3). Daniels, D.L., and Zietz, I., 1978, Geologic interpretation of aeromagnetic maps of the Coastal Plain region of South Carolina and parts of North Carolina and Georgia: U.S. Geological Survey, Open-File Series 78-261, 61 p. The U.S. Coastal Plains Regional Commission has joined with the U.S. Geological Survey in a cooperative program to complete the airborne radiometric and magnetic surveying in the Coastal Plain regions of North Carolina, South Carolina, Georgia, and recently, Virgina and Florida. This report covers the aeromagnetic data, and consists of a compilation of the data collected in the first two years of the program and the previous aeromagnetic surveys, with an interpretation of the geology of the basement rocks. The interpretation utilizes the aeromagnetic maps, samples from wells penetrating I the basement, previous interpretations of the basement geology, and other geophysical data. Daniels, D.L. Zietz, I., and Popenoe, P., 1982, Distribution of subsurface lower Mesozoic rocks in the southeastern United States, as interpreted from regional aeromagnetic and gravity maps: in Gohn, G.S. , ed. , Studies related to the Charleston, South Carolina, earthquake of 1886-tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Report 82-134, p. 21-22. Aeromagnetic data reveal some of the complexity of the broad early Mesozoic rif t basin, which appears to extend at least from the Gulf of Mexico to the Atlantic Ocean. Along the northern edge of this rift, in the Savannah River region, depth-to-magnetic-source calculations delineate two interconnected basins, which are ceparated from the main rift by a broad horst of crystalline basement. The Riddleville Q (Georgia) Basin appears to contain at least 7,220 feet of g basin fill; it is deeper than the Dunbarton (South Carolina) Basin, which has at least 3,300 feet of fill. A maximum thickness of 11,500 feet near Statesboro, Georgia is indicated I for the main basin, called here tre South Georgia Rif t. A-21 I
r- - I Davis, L.B., Jr. ,1974, Petrology of the Claiborne Group and part of l E the Wilcox Group, southwest Georgia and southeast Alabama: University of Texas at Austin, M.A. thesis, 215 p. Sediments of the Claiborne Group cropping out in southwest Georgia and southeast Alabama were probably deposited in a complex of fluvial and marine environments. The sediments of the upper part of the Tuscahoma Formation and the Hatchetigbee Formation, both of the Wilcox Group, are probably marine to marginal marine deposits. The boundary between these two groups is difficult to define, for there is locally a layer of sediment with intermediate characteristics. De Boer, J. ,1967, Palecmagnetic-tectonic study of Mesozoic dike swarms in the Appalachians: Journal of Geophysical Research, v. 72, no. 8,
- p. 2237-2250.
Paleomagnetic evidence indicates that most of the extensive dike swarms cutting Triassic and older formations probably intruded in a time of regional tectonic and magmatic activity distinct from the Late Triassic tectogenesis. The fossil g magnetic directions of the dikes suggest a Jurassic age for 5 the intrusions. These dikes were emplaced along tensional fractures that were the surficial expressions of deep-seated movements. Denman, H.E. , Jr. ,1974, Implications of seismic activity at the Clark Hill Reservoir: Georgia Institute of Technology, M.S. thesis, 103 p. Examination of seismograph records revealed a localized sone of seismic activity at Clark Hill. Bouguer anomalies computed for the area reveal a breached, linear northeast-southwest trending ridge of anomalies which corresponds to the area of microearthquake locations. A right lateral strike-slip displacement of approximately 2,000 feet is indicated by - offset of these anomalies along a possible northwest-southeast striking fault. Dillon, W.P., and Paull, C.K., 1982, Summary of development of the continental margin of Georgia based on multichannel and g single-channel seismic-reflection profiling and stratigraphic well g data: in Arden, D.D., Beck, B.F., and Morrow, E., ed., Second Symposium on the Geology of the Southeastern Coastal Plain,
- p. 197-200.
The continental margin off Georgia probably began to form with rifting, mafic intrusive and extrusive activity, and rapid sediment depositiota which led to development of a transitional l basement. Early subsidence was rapid for the basement beneath l A-22 I
the present Blake Plateau Basin, and the Upper Jurassic deposits form the thickest unit. Reefs acted as sediment dams at the seaward side of the basin. The Gulf Stream became I significant on the Blake Plateau near the Paleocene-Eocene boundary, and since then has prevented the shelf sediments from prograding across the plateau. Dillion, W.P. , Paull, C.K. , Buf fler , R.T. , and Fail, J. , 1978, Structur: and development of the Southeast Georgia Embayment and northern Blake Plateau Preliminary analysis: American Association of Petroleum Geologists Memoir 29, p. 27-41. Multichannel seismic reflection profiles from the Southeast Georgia Embayment and northern Blake Plateau show reflectors that have been correJated tentatively with horizons of known age. Doering, J.A.,1960, Quaternary surface formations of the southern part of the Atlantic Coastal Plaint Journal of Geology, v. 68, no.1, p . 18 2-20 2. The Citronelle Formation of the eastern Gulf Coast extends northward across the Coastal Plains of Georgia, South Carolina, North Carolina, and Virginia as a gravelly sand formation 100 feet thick. Deposition of the formation in the Atlantic Coast region occurred on a peneplain developed during a tectonically quiet time in the late Miocene and Pliocene and was caused by the first of a series of uplif ting and warping movements. I Drennen, C.W.,1950, Geology of the Piedmont-Coastal Plain contact in eastern Alabama and western Georgia, University of Alabama, M.S. thesis, 42 p. The chief purpose of this work was to map the contact of the Iiedmont and Coastal Plain rocks in east Alabama and west Georgia, a contact difficult to identify at some places I because the rocks have been intensely weathered. Locally, faulting has involved both the Piedmont and Coastal Plain rocks, and in places the Coastal Plain strata have been disturbed by slumping and soil creep. Eardley, A.J., 1951, Structural geology of North America: New York, Harper and Row, 743 p. A detailed, dated (pre-plate tectonics) discussion of the United States, Canada, and Mexico. Separate sections on the Atlantic Coastal Plain and exposed Triassic basins. Ellwood, B.B. , Whitney, J. A. , Wenner , D;B. , mse, D. , and Amerigian, I C. ,1980, Age, paleomagnetism, and tectonic significance of the Elberton granite, northeast Georgia Piedmont: Journal of Geophysical Research, v. 85, no. Bil, p. 6521-6533. I A-23 I
I The Elberton granite is a large, fine-grained pluton intruded into orthogneisces and paragneisses of the Inner Piedmont of eastern Georgia. Within this paper, two partially conflicting estimates of tectonic rotation are developed and evaluated. The first requires a post emplacement rotation of 30*-35' down to the southeast about a north-northeast axis. The second, indicates a postemplacement rotation for the body of approximately 15' down to the northwest along an east-northeast axis. The Rb/Sr whole rock age of 350+ 11 m.y.B.P., the remnant magnetism, and petrology of samples from 21 sites within the granitic Elberton pluton have been determined. Faye, R.E. and Prowell, D.C. ,1982, Ef fects of Late Cretaceous and Cenozoic faulting on the geology and hydrology of the Coastal Plain near the Savannah River, Georgia and South Carolina: U.S. Geological Survey Open-File Report 82-156, 73 p. Geologic ar.d hydrologic investigations by the U.S. Geological Survey have defined stratigraphic and hydraulic anomalies suggestive of faulting witnin coastal plain sediments between the Ogeechee River in east-central Georgia and the Edisto River in west-central South Carolina. Examination of borehole cuttings, cores, and geophysical logs from test wells indicate that Triassic rocks, and Upper Cretaceous and lower Tertiary coastal plain sediments near the Barnwell-Allendale County line near Millett, South Carolina, are offset by a northeast-trending fault downthrown to the northwest. The location of this suspected coastal plain fault generally coincides with the location of an inferred fault in basement rocks as interpreted from aeromagnetic surveys. Apparent vertical of fsets range from about 700 feet at the base of < Upper Cretaceous sediments to about 20 feet in strata of late g Eocene age. As a result, the Upper Cretaceous Middendorf g_ Formation which directly overlies crystalline and Triassic rocks updip (northwest) of this fault, is absent immediately downdip of the fault. The thickness of Upper Cretaceous sediments is also sharply reduced from about 700 feet to about 180 feet across the fault. Sediments of the basal coastal plain aquifer are largely truncated by uplif ted Triassic rocks at the fault near Millett, South Carolina. Lateral ground water flow near the g Savannah River is consequently disrupted updip of the fault g and ground water is transferred vertically into overlying sediments and possibly into the Savannah River. At several locations, abrupt changes in potentiometric head occur across this fault. Computed transmissivity of the basal coastal plain aquifer is also radically reduced downdip of the fault, sharply reversing a downdip trend of rapidly increasing aquifer transmissivity. E 3 A-24 I I
l Other anomalous stentiometric data along a northeast-trending W line between Statesboro, Georgia, and Fairfax, South Carolina, suggest the possibility of similar faulting in correlative I geologic units. The location of the suspected fault neas Statesboro, Georgia, generally coincides with the eastward extension of the Gulf Trough, a regional potentiometric anomaly in central Georgia. Flint, R.F., 1940, Pleistocene features of the Atlantic Coastal Plain: American Journal of Science, v. 230, no. 11, p. 757-787. This paper reviews the literature of the Pleistocene sediments and surface features of the Atlantic Coastal Plain, and gives the results of reconnaissance study of a part of this region. It discusses three hypotheses concerning the environment in which these sediments were accumulated, and in which the related, scarps, terraces, and other morphologic features were fashioned: 1) marine origin, 2) fluvial origin, 3) a combination of both environments. Forgotson, J.M. , 1963, Depositional h. story and paleotectonic framework of Comanchean Cretaceous Trinity stage, Gulf Coast areat Bulletin of the American Association of Petroleum Geologists, v. 47, no.1,
- p. 69-103.
The Early Cretaceous Trinity Stage is a broad regional wedge of rocks thickening basinward from the zero edge to more than 4,000 feet. The tectonic framework and regional paleogeography were uniform during deposition. I Frazier, W.J., 1982, Sedimentology and paleoenvironmental analysis of the Upper Cretaceous Tuscaloosa and Eutaw Formations in western Georgia: irl Arcen, D.D. , Beck , B.F. , and Morrow, E. , ed. , Second Symposium on the Geology of the Southeastern Coastal Plain,
- p. 39-52.
The Tuscaloosa Formation lies nonconformably on Piedmont crystalline rocks on top of which is developed a thin, lateritic paleosoil, present now primarily on the higher portions of the erosional surface. The Tuscaloosa consists of two major lithologies, a crossbedded, conglomeratic, arkosic arenite and a mottled, silty mudstone, which occur stratigraphically in a series of fining-upward sequences separated by disconformities. Gelbaum, C., 1978, The geology and ground water of the Gulf Trough: Georgia Geologic Survey Bulletia 93, p. 38-48. There is a steep increase in the potentiometric surface in the direction of flow across the axis of the Gulf Trough in the central Coastal Plain of Georgia. This steep gradient I A-25 I
I inticates that the transmissivity of the principal artesian aqui er has been inhibited. Low yields may be due to: 1) the principal aquifer being located much deeper than elsewhere,
') multi-aquifer wells that tap the entire Miocene and only a g small portion of the main aquifer, 3) principal aquifer being g thinner due to erosion, non-deposition or slow deposition,
- 4) faulting parallel tp the Trough resulting in a low permeability barrier, 5) carbonate facies changes.
Gelbaum, C., and Howell, Jr., 1982, The geohydrology of the Gulf Trought in,Arden, D.D., Beck, B.F., and Morrow, E., ed., Second E Symposium on the Geology of the Southeastern Coastal Plain, g
- p. 140-153.
The Gulf Trough is a long, narrow geologic feature that was produced by a combination of depositional and structural conditions. The Trough is approximately 235 miles long about 10 miles wide, and trends N53*E from Decatur through Bulloch Counties. Development of the Gulf Trough began, at least as = early as Oligocene time, with subsidence of several elongate basins and infilling of these basins with a thick sequence of Swannee Limestone. Faulting occurred in limited areas, forming parts of two basins. The Gulf Trough is coincident with a steep potentic:aetric gradient anomaly on the potentiometric map of the principal artesian aquifer. Both the trough and the anomaly extend from Decatur County in southwest Georgia northeastward to Bulloch and Ef fingham Counties, where they disappear. The Gulf Trough creates the potentiometric anomaly and, by acting essentially as a vertical boundary to ground water flow, is responsible for reduced ground water availability. Geodata International, Inc. ,1975a, Aerial radiometric and magnetic survey, Augusta National Topographic Map, Georgia and South Carolina areas, volumes 1 and 2: U.S. Energy and Development Administration, GJO-1663-1, 55 p. = This report includes a general geologic description of the g area, including descriptions of the various geologic units and 3 correlates the airborne data to the geologic units as provided by the geologic maps. Also included is a frequency g distribution study of the data as a function of the geologic g units encountered over the area including tie line data. Geodata International, Inc.,1975b, Aerial radiometric and magnetic survey Savannah National Topographic Map, Georgia and South Carolina areas, volumes 1 and 2: U.S. Energy Research and Development Administration, GJO-1663-1, 50 p. This report includes a general geologic description of the area, including descriptions of the variot.: geologic units and correlates the airborne data to the geologic units as provided A-26 I I
I by the geologic maps. Also included is a frequency distribution study of the data as a function of the geologic units encountered over the area including tie line data. Georgia Department of Natural Resources,1976, Geologic map of Georgia, scale - 1:500,000. Detailed geologic map of the entire State of Georgia. Formations shown in the study area include: Lower Tertiary-Cretaceous undifferentiated, Twiggs Clay, McBean Formation, ! Irwinton Sand, Neogene undifferentiated, and alluvium. Gohn, G.S.,1982a, Studies related to the Charleston, South Carolina, earthquake of 1886 - tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Report 82-134, 38 p. Recent investigations in the Charleston, South Carolina area have been multidisciplinary studies of the materials recovered from the Clubhouse Crossroads test holes; seismic reflection and refraction surveys in the Charleston area and offshore; regional studies of aeromagnetic, gravity, and deep-well data; and continued monitoring and analysis of the seismicity near Charleston. This report presents, as abstracts, principal .g conclusions and working hypotheses of some of the ongoing lg inver,tigations. Gohn, G.S.,1982b, Geology of the basement rocks near Charleston, Fouth l Carolina - Data from detrital rock fragments in lower Mesozoic (?) rocks, Clubhouse Crossroads test hole #3: M Gohn, G.S., ed. Studies related to the Charleston, South Carolina, earthquake of 1886-tectonics and seismicity (collected abstracts). U.S. Geological Survey Open-File Report 82-134, p. 9-10. Four types of basement rocks occur as detrital clasts; granodiorite, microbreccia, basalt, and mylonite. The mylonite and microbreccia may represent relatively ductile and
- relatively brittle deformation, within a single fault zone, or l they may represeat contrasting styles of deformation in i different fault zones of different age. Based on the probable i age of the sedimentary section, the minimum age of faulting is established as early Mesozoic.
Gohn, G.S. , Houser, B.B. , and Schnider, R.R. ,1982a, Geology of the lower Mesozoic (?) sedimentary rocks in Clubhouse Crossroads test
- I hole #3 near Charleston, South Carolina
- M Gohn, G.S., ed.,
Studies related to the Charleston, South Carolina, earthquake of 1886-- tectonics and seismicity (collected abstracts): U.S. , Geological Survey Open-File Report 82-134, p. 7-8. ' In the Clubhouse Crossroads well #3, red beds of probable Late .g Triassic or Early Jurassic age were found to underlie l W l A-27 I l
subaerial basalt flows. The red beds arc similar to those found elsewhere in the eastern United States. Gohn, G.S., Bybell, L.M., Smith, C.C. , and Owens, J .P. , 1978a, g Preliminary cross sections of Cretaceous sediments along South g Carolina coastal margin: U.S. Geological Survey Miscellaneous Field Studies Map MF-1015A, 2 sheets. This report describes the distribution of Cretaceous sediments along the South Carolina coastal margin. Cross sections employing in-hole geophysical logs have been used to illustrate the distribution of the major stratigraphic units. The units delineated on the cross sections are informal rock-stratigraphic units of approximately formational rank. E Formational names were not used, however, to avoid discussions g of stratigraphic nomenclature and to avoid the necessarily tenuous correlation of subsurface and outcrop units. Ages of the units shown on the cross sections are given where they are known in specific boreholes. Cohn, G.S., Bybell, L.M., Smith, C.C., and Owens, J.P., 1978b, Cenozoic sediments, South Carolina coastal margin: U.S. Geological Survey Miscellaneous Field Studies Map MF-1015B, 2 sheets. This report describes the distribution of Cretaceous sediments along the South Carolina coastal margin. Cross sections employing in-hole geophysical logs have been used to illustrate the distribution of the major stratigraphic units. The units delineated on the cross sections are informal = rock-stratigraphic units of approximately formational rank. Formational names were not been used, however, to avoid discussions of stratigraphic nomenclature and to avoid the necessarily tenuous correlation of subsurface and outcrop units. Ages of the units shown on the cross sections are given where they are known in specific boreholes. Gohn, G.S. , Gottfried, D. , Lanphere, M. A. , and Higgins, B.B. , 1978c, Regional implications of Triassic or Jurassic age for basalt and sedimentary red beds in the South Carolina Coastal Plain: Science,
- v. 202, no. 4370, p. 887-890, Clubhouse Crossroads basalt and underlying red beds have been assigned an age of Late Triassic ta Early Jurassic based on whole rock potassium-argon studies. The red beds below the g Clubhouse Crossroads basalt are lithologically similar to g exposed rocks of the Newark Group. The presence of a large early Mesozoic basin (graben?) extended across the southeastern United States is suggested.
I A-28 I
ll ' l Gohn , G.S. , Bybell, L.M. , Ch ristopher , R. A. , owc ns , J.P. , Smith , C.C . , 1982b, A stratigraphic framework for Cretaceous and Paleogene margins along the South Carolina and Georgia coastal sediments: in Arden, D.D. , Beck , B.F. , and Morrow, E. , ed. , Second Symposium on I the Geology of the Southeastern Coastal Plain, p. 64-74. Viewing the coastal Georgia-South Carolina cross section as a whole, virtually all the units are thicker in Georgia than in South Carolina and are thicker on the peninsular arch than on the Cape Fear Arch, thereby giving a considerable asymmetry to the embayment. In the area of thickest sedimentation in Glynn and Camden Counties, Georgia. The section consists of roughly 50 to 60 percent Tertiary sediments, well over half of which are Eocene carbonate rocks. The post-Eocene section consists primarily of upper Oligocer e beds in the Charleston, South Carolina area and primarily of Miocene sediments in southern South Carolina and Georgia. Gray, M.G. ,1978, Pre-Gulfian rocks of the southwestern Georgia Coastal Plain, Emory University, M.S. thesis, 72 p. Differential rates of crustal subsidence had a marked influence on the thickness and distribution of pre-Gulfian I coastal plain sedimentary rocks in southwestern Georgia and southeastern Alabama. Pre-Gulfian coastal plain rocks are subdivided into formats in southwestern Georgia and southeastern Alabama. Both formats consist of predominantly arenaceous clastic rocks, but the lowermost Early Format contains a higher concentration of argillaceous material than does the uppermost Worth Format. This change in the stratigraphic sequence is the result of a relatively abrupt change in the regional depositional environment, and is interpreted to be the result of: 1) an increase in basin-deepening tectonics, 2) a raising of the topography in the source area, 3) an increase in stream activity, or 4) some combination of these. Pre-Gulfian rocks of the Georgia Coastal Plain could be Upper Jurassic and/or Lower Cretaceous (Comanchean and/or Coahuilan) in age. Griffin, J.S. Jr. ,1974, Analysis of the Piedmont in northwest South Carolina: Geological Society of America Bulletin, v. 85, no. 7, p. 1123-1138. Two major autochthonous nappes and a deep synformal structural occur in the Piedmont of northwest South Carolina. The cataclastic Brevard zone, a non-migmatitic belt, is associated . 1 1 l A-29
I with the synformal belt of partially cataclastic and retrograded a rocks. The autochthonous nappe complex probably formed in a continental rise assemblage subjected to intense thermal effects in the early Paleozoic. Guinn, S. A. ,1980, Earthquake focal mechanisms in the southeastern United States: U.S. Nuclear Regulatory Commission, NUREG/CR-1503, l 150 p. 3 Focal mechanism solutions indicate that southeastern intraplate seismic activity does not appear to be the result of a single dominant stress direction. Many of the solutions support nearly vertical fault planes suggesting a low level compressional to tensional environment for the southeast. Hadley, J.B. , and Devine, J.F. , 1979, Seismotectonic map of the eastern United States: U.S. Geological Survey Miscellaneous Field Investigations Map MF-620. 3 sheets, scale - 1:5,000,000. The map describes the distribution of historic seismic activity in relation to geologic structures and tectonic provinces and to identify structures or regions that are characterized by consistent relations between seismic activity and structural features. It is clear from existing structural data, as well as from the distribution of earthquakes, that historic earthquake activity bears no consistent relation to the tectonic provinces of the southeastern United States. Hamilton, R.M. , Behrendt, J.C. , and Ackermann, H.D. , 1982, Land , multichannel seismic-reflection evidence for tectonic features near Charleston, South Carolina: in Gohn, G.S., ed., Studies related to the Charleston, South Carolina, earthquake of 1886-tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Repor t 8 2-13 4, p. 17-18. Reflection studies in the vicinity of the 1886 Charleston earthquake shows a smooth pre-Late Cretaceous unconformity dipping to the southeast. The smoothness shows that vertical faulting within a mile of the surface has not been substantial since at least the Late Cretaceous. There are a few places where the deformation appears to have tectonic significance. One such deformation, the Cooke fault, shows about 164 feet of vertical displacement on a Jurassic age basalt layer at 2,500 feet depth. Two other zones of unknown strike that indicate Cenozoic faulting are seen. In the northern part of the study area, layered reflections are interpreted as Triassic red beds bounded on the southeast by a Triassic (?) normal fault. The shallow minor deformation seen on the profiles is interpreted as a second-order manifestation of deep faulting, possibly caused by reactivation of ancient thrust faults, fE A-30 e I
Harms, J.C., and Tackenberg, P., 1972, Seismic signatures of sedimentation models: Geophysics, v. 37, no.1, p. 45-58. Sedimentation models summarize much geologic information which can be applied to exploration problems, especially in sparsely drilled areas. If lithologic variations, summarized by sedimentation models, control velocities, different stratigraphic sequences should yield recognizable and systematically different reflection seismic cross-sections. Harrington, J .W. , 1951, Structural analysis of the west border of the Durham Triassic Basin: Geological Society of America Bulletin,
- v. 62, no. 2, p. 14 9-15 8.
Normal faulting in Triassic time is responsible for basinal formation. Deposition accompanied and followed the faulting I and erosion of the original fault surfaces. Post-sedimentation normal faulting allowed the deposition of finer clastic rocks against the crystalline rocks, and of ten depressed the conglomerate facies below erosional level. Harris, L.D. , and Bayer, K.C. ,1979, Sequential development of the Appalachian orogen above a master decollement-a hypothesis: Geology, v. 7, no. 12, p. 568-572. Surface geology and seismic-reflection data suggest that rather than having a massive rooted central core the southern part of the Appalachian orogen from the Appalachian Plateau to the Atlantic continental shelf is underlain by an eastward-dipping decollement zone. This decollement zone was a long lived structural element, intermittently growing from east to west during late Proterozoic to late Paleozoic time. Onshore displacement along the detachment surface was episodic through this long period of time, so that reliable estimates of total shortening for the entire orogen are not possible. Harris, L.D., and Milici, R.C., 1977, Characteristics of thin-skinned style of deformation in the southern Appalachians and potential hydrocarbon traps: U.S. Geological Survey Profecsional Paper 1018, 40 p. Roctless folds and gently to steeply dipping thrust faults, which, at depth join a master decollement (low angle thrust) near the sedimentary rock - basement contact, are the key tectonic features of the southern Valley and Ridge and Appalachian Plateaus Provinces. This paper is an attempt to focus attention on the more important characteristics of the thin-skinned style of deformation in the southern Appalachians by presenting a model to illustrate the regional anatomy of a decollement and to identify likely structures that need additional investigation as possible prospects for hydrocarbon accumulation. A-31 I
Hatcher, R.D., 1977, Regional structural relationships of the Chauga belt-western mobilized Inner Piedmont of the crystalline southern Appalachians of northeast Georgia and South Carolina: Geological Society of American (abs. ) , v. 9, no. 2, p. 781. Although the synclinal Chauga belt and articlinal mobilized Inner Piedmont are generally thought to be lithologically and structurally distinct, certain rock units are traceable continuously across a previously mapped " tectonic" boundary separating the two. The boundary in this area is one of minimal tectonic offset, more likely involving a metamorphic gradient. A further complication is a large allochthon of sillimanite grade gneissec, schists and amphibolites which extends from the Georgia-South Carolina border to just east of Gainesville, Georgia. Hatcher , R.D. , Jr. ,1972, Development model for the southern Appalachians: Geological Society of America Bulletin, v. 83, no. 9, p. 2735-2760. A four-phase developmental model for the southern Appalachians is proposed. This scheme includes: 1) an early (late Precambrian to Middle Ordovician) phase of continental margin sedimentation, igneous activity, and initial compression,
- 2) an intermediate (late Precambrian to Late Devonian) phase of compression producing isoclinal folding, regional metamorphism, and intrusive activity with deposits from a rising tectonic source land, 3) next a later (mid-late Paleozoic) phase of compression and igneous activity accompanied by continued deposition from the rising mountain system occurred, 4) finally, there was a tensional phase (Triassic-Jurassic) accompanied by normal faulting, and deposition related to the decoupling of Africa and North America.
Hatcher , R.D. Jr. ,1977, Macroscopic polyphase folding illustrated by the Toxaway Dome, eastern Blue Ridge, South Carolina - North Carolina: Geological Society of America Bulletin, v. 88, no. 11,
- p. 1678-1688.
The Toxaway Dome is located in the Blue Ridge of North and l South Carolina immediately north-west of the Brevard zone. 5 This study is principally a delineation of the structure the southwestern part of the Toxaway Dome. A structural synthesis is presented here based on detailed geologic mape n .g and analysis of mesoscopic structures, with a consideration of its implications to the regional structural history of the Blue Ridge. A-32 I
Hatcher, R. D. Jr.,1978, Tectonics of the western Piedmont and Blue Ridge, southern Appalachians: Review and speculation: American Journal of Science, v. 278, no. 3, p. 276-304. This paper is concerned with the tectonics of the crystalline southern Appalachians from the Inner Piedmont westward and with the relationship of this portion of the Appalachians to the remainder. Its purpose is to review the recent work done in the Blue Ridge, Chauga belt, and Inner Piedmont and add recent ideas relating these belts to a common but complex history of the opening and closing of small ocean basins along the ancient continental margin of southeastern North America. Hatcher, R. D. Jr., and Odom, A. L. ,1930, Timing of thrusting in the sou thern Appalachians, U.S. A. : Model for orogeny: JoLrnal of Geological Society of London, v. 137, part 3, ,. 321-327. Field and geochronological studies in the southern Appalachians reveal a space-time relationship of thrust and other large faults to their relative positions in the orogen, and their ties of formation in relation to thermal-metamorphic peaks. This transgression of thrusting begins with early pre , syn , and late-metamorphic (taconic) thrusting in the metamorphic core. The core was also affected by Devonian (Acadian) thrusting and high angle faulting. Late (Hercynian-Alleghanian) faults are restricted to the flanks of the orogen. Hatcher , R.D. , Jr. , Howell, D.E . and Talwani, P. ,1917, Eastern Piedmont fault system Speculation on its extent: Geology, v. 5, no. 10, p. 6 36-6 40. Geologic mapping, interpretation, and field checking of recent aeromagnetic data suggest the existence of a closely associated series of faults and splays extending from Alabama to Virginia, termed the Eastern Piedmont fault system. Characteristic magnetic anomalies were found to be associated with known faults and were used to trace them through covered intervals. The fault system extends northeastward from the Goat Rock fault of Alabama and west-central Georgia, crossing the lower Piedmont of South Carolina, passes beneath a segment of the Coastal Plains in the Carolinas, and then flanks the Raleigh Belt in North Carolina and continues into Virginia. From east-central Georgia to Virginia, cataclastic rocks along the faults of the system are bounded to the northwest and southeast by rocks of the Carolina Slate Belt, forming perhaps the most extensive fault system in eastern North America. I A-33
ll Hatcher, R.D. Jr., Butler, J.R., Fullagar , P .D. , Secor , D.T. , and Snoke, A.W. ,1979, Geologic synthesis of the Tennessee-Carolinas-northeast Georgia southern Appalachians: in Wones, D.R., ed., Proceedings on the "Caledonides in the USA" (I.G.C.P. project 27: Caledonide orogen): Virginia Polytechnic Institute and State University, Department of Geologic Sciences, Memoir no. 2, Blacksburg, Virginia, 24061, p. 83-90. The Tennessee-Carolinas-northeast Georgia (TCG) sou ther n Appalachians have been divided into several geologic provinces based on the aspects of structure, stratigraphy, metamorphic or plutonic history. These provinces include the Cumberland Plateau and Valley and Ridge, the Blue Ridge which is divisible into three distinctive belts, and the Piedmont which l is divisible into six belts. This paper discusses the W stratigraphy, igneous activity, faulting, metamorphism and plate tectonic models for the provinces. Hazel, J.E. , Bybell, L.M. , Christopher, R. A. , Fredricksen, N.O. , May, F.E . , McLean , D.M. , Poore , R. Z . , Smith , C.C. . Sohl, N.F. , Valentine, P.C. , and Witmer, R.J. ,1977, Biostratigraphy of the deep corehole (Clubhouse Crossroads corehole 1) near Charleston, South Carolina, in Rankin, D.W., ed. , Studies related to the Charleston, South Carolina, earthquake of 1886 - A preliminary repor t: U.S. Geological Survey Professional Paper 1028, p. 71-89. Microfossils (calcareous nannoplankton, dinoflagellates, E forminifers, ostracodes, and sporomorphs) and mollusks have g been used to date the sedimentary part of a 2,599 foot core from a test hole (Clubhouse Crossroads corehole 1) drilled 25 miles west-northwest of Charleston, south Carolina. The sedimentary section is 2,462 feet thick and is of Late Cretaceous and (except for a few meters of probable Pleistocene) early Tertiary age. The drillhole bottomed in amygdaloidal basalt of Cretaceous (?) age. Heller , P.L. , Wentwor th , C.M. , and Poag , C.W. , 1982, Episodic post- g rif t subsidence of the United States Atlantic continental margin: g Geological Society of America Bulletin, v. 93, no. 5, p. 379-390. The Atlantic margin of North America is generally thought to have subsided regularly as a result of cooling and sediment loading. However, sediment thickness, paleobathymetry, and chronostratigraphy from COST wells of fshore from Georgia and g New Jersey indicate periods of rapid subsidence in the 3 Cretaceous and Tertiary. Because no global sea level change can account for all residual movements, it is proposed that a tectonism, variously amplified by loading, is responsible for g the observed episodes of rapid subsidence. A-34
I I Heron;, S.D., 1959, A small basement cored anticlinal warp in the basal Cretaceous sediments near Cheraw, South Carolina: South Cr.colina Division of Geology, Geology Notes, v. 3, no. 4, p.1-4. The origin of the warping is not clear, and se,eral hypotheses have been considered: 1) a tectonic origin for the structure is unlikely as there is no evidence of Cretaceous or post-Cr e tar ous tectonic activity in the region, 2) a sedimentary ligin is not possible, 3) differential compaction is possible, 4) the most logical hypothesis is that the structure is due to solution of the calceum carbonate 3 component of the argillite. Heron, S.D. , Jr. ,1962, Limestone resources of the Coastal Plain of South Carolina: Division of Geology Bulletin 28, 128 p. There are five Coastal Plain geologic formations in South Carolina that contain appreciable quantities of calcium carbonate. Of these, the Santee Limestone of Eocene age has I the highest potential as a source of high grade calcium carbonate suitable for industrial and chemical uses. Herrick, S.M., 1961, Well logs of the Coastal Plain of Georgia: Georgia Geologic Survey Bulletin 70, 462 p. Detailed listing of the geologic well logs from the Georgia Coastal Plain. Her rick , S.M. , 1964, Upper Eocene smaller foraminifera from Shell Bluff and Griffin Landings, Burke County, Georgia: U.S. Geological Survey Professional Paper 501-C, p. C64-C65. Identification of microfossils from equivalent zones at Shell I Bluff Landing and Griffin Landings Georgia reveals lithologic and microfaunal differences that are explained through normal facies change. The foraminifera are of late Eocene age and indicate that the fossil-bearing stratum correlates with the Moodys Branch Formation of Mississippi and Alabama and the lower Barrwell Formation of Georgia. Her rick , S.M. and Counts, H.T . ,1968, Late Ter tiary stratigraphy of eastern Georgia: Guidebvok for Third Annual Field Trip: Georgia Geological Society, 88 p. Formational overlap and interformational facies change are considered to be chiefly responsible for rather profound stratigraphic and lithologic changes in Tertiary deposits in updip areas of eastern Georgia. The principal stratigraphic changes resulting from overlap include: 1) overlap of Paleocene and early Eocene deposits by the McBean Formation of A-35 I
i Ii l middle Eocene age, 2) overlap of the McBean Formation by the Barnwell Formation of late Eocene age, 3) overlap of the i Barnwell Formation and Ocala Limestone by geologically younger deposits of Oligocene age. One striking result of such overlap is that geologically younger deposits are found resting upon progressively older strata. The McBean Formation rests upon the Tuscaloosa Formation of Late Cretaceous age. The Barnwell Formation, as well as beds of Oligocene age, rests upon the Tuscaloosa Formation and, in places, upon the much older basement complex. Her rick, S.M. , and Vorhis, R.C. ,1963, Subsurface geology of the Georgia Coastal Plain: Georgia Geological Survey Information l Circular 25, 78 p. E Data from 354 lithologic-paleontologic logs was used to restudy the subsurface geology of the Georgia Coastal Plain. Two contrasting areas of deposition are described: An updip area of clastics and a downdip area of limestones. Several reinterpretations of stratigraphy were made. The Cooper Marl and the Barnwell Formation are the updip equivalents of the Ocala Limestone. The Lisbon and Tallahata Formations are updip equivalents of the Avon Park Limestone and Lake City Limestone, respectively, of Florida. Howell, D.E . , and Zupan, A.W. , 1974, Evidence for post-Cretaceous tectonic activity in the Westfield Creek area north of Cheraw, South Carolina: South Carolina Geologic Notes, v.18, no. 4, p. 98-105. Post-Cretaceous faulting and folding of Carolina Slate Belt argillites and Late Cretaceous sediments of the Middendorf Formation are well exposed in two roadcuts along Westfiela Creek, northwest of Cheraw, South Carolina. The only known tectonic activity during post-Cretaceous time in the region is that of the uplif ting Cape Fear arch. These faults and folds located on the southern limb of the Cape Fear Arch, could, therefore, be related to the crustal shortening creating the arch during the Tertiary period. Huddlestun, P.F., 1981, Correlation chart, Georgia Coastal Plaint Georgia Geologic Survey Open-File Report 82-1. Stratigraphic column for Burke, Richmond, and northern Screven Counties does not show the Tuscaloosa Formation. The only Cretaceous rock found in the stratigraphic column is an undifferentiated member of the Oconee Group. The Barnwell Group is divided into a number of formations and members. The stratigraphic columns in the correlation chart are based on approximately 110 cores logged and examined by the author, in addition to cuttings from selected oil and water wells and numerous geophysical logs. A-36
I 'I Huddlestun, P.F. , and Hetrick, J.H. ,1978, Stratigraphy of the Tobacco Road Sand - A new fortration: Georgia Geologic Survey Bulletin 93, I
- p. 5 6-7 7.
1 I The Tobacco Road Sand is a belt of coastal marine sands of late Eocene age. This, belt of coastal sands of probable sound or lagoon origin lies parallel to the Fall Line in eastern Georgia. It grades downdip to the south into carbonate facies. 'J Huddlestun, P.F. , and He trick , J.H. , 1979, The stratigraphy of the Barnwell Group of Georgia: Georgia Geologic Survey Open-File Report 80-1, 89 p. [ This redefinition of the upper Eocene deposits of central and eastern Georgia raises the Barnwell to group ranking and recognizes three formations within the Barnwell Group. In ascending order these are, the Clinchfield Formation, the Dry Branch Formation (new) , and the Tobacco Road Sand. The Clinchfield Formation has four members, the Dry Branch Formation has three memberc, and the Tobacco Road Sand has one. Hum @reys, B. , and Hughes, D.J. ,1974, Development of alluvial stream channels: A five-stage model: Discussion: Geological Society of America Bulletin, v. 85, no.1, p.149. A short discussion of Keller 's five-stage model for the 4 development of alluvial stream channels. Uses an open-system point of view rather than a closed-system point of view as Keller used in his model. This removes the need to trace the system back to a starting point and also the need to adjust the conceptualized processes tt. rough the sequential stages. I Hurst, V.J. , and Sandy, J. ,1964, Marl in Burke County, Georgia: Interim Report No.1, Geology Department, University of Georgia, 42 p. The Burke County marl varies in thickness, but is a persistent layer underlying most of the county except the extreme northwestern portion. A thickness of more than 50 feet is common. The marl consists of alternating layers of calcareous sand, marl, and coarse-fossil oyster shells embedded in calcareous sand. Inden, R.F., and Zupan, A.W., 1975, Normal faulting of upper coastal plain sediments, Ideal Kaolin Mine, Langley, South Carolina: South I Carolina Division of Geology Geologic Notes v.19, no. 4,
- p. 159-165.
Normal faulting created a small graben at the Ideal kaolin mine in Langley, South Carolina. Orientation of the west-bounding fault is N30*W, 68'E and of the east-bounding fault is N40*W, 75'W. A-37
'I
I Jacobeen, F.H., 1972, Seismic evidence for high angle reverse faulting in the Coastal Plain of Prince George and Charles Counties, Maryland: Maryland Geological Survey Information Circular No. 13, 21 p. The Brandywine fault system is divided into two en echelon faults. Both extend beyond and are increasing in throw toward the limits of the study area. Maximum throw seen on the southern fault, the Danville fault, is over 250 feet at the top of the granite and top of the Lower Cretaceous Arundel Formation. Throw on the northern fault, the Cheltenham fault, is about 100 feet. Although stream anomalies and lineaments are clues to the location of buried faults, recent drilling has shown that no l W rupture reaches the surface; rather, the fault displacement i t, absorbed upward and only folding occurs in the Tertiary sediments. Johnston, R.H. , Healy, H.G. , and Hayes, L.R. , 1981, Potenticmetric a surface of the Tertiary limestone aquifer system, southeastern United States, May 1980: U.S. Geological Survey Open-File Report g 81-486. Map covers Florida, the southern two-thirds of Georgia and South Carolina, and the southern half of Alabama. The aquifer system includes units of Paleocene to early Miocene age that g combine to form a continuous carbonate sequence that is g hydraulically connected in varying degrees. The contours do not cross the Millett fault study area. Johnston, R.H. , Krause, R.E . , Meyer , F.W. , Ryder , P.D. , Tibbals, C.H. , and Hunn, J .D. , 1980, Estimated potentiometric surface for the Tertiary limestone aquifer system, southeastern United States, g prior to development: U.S. Geological Survey Open-File Report 3 80-406. Map covers Georgia, Florida, South Carolina, and the southern half of Alabama. The upper water-bearing units occur in limestones and dolomites within several formations principally the Tampa, Suwannee, Ocala, and Avon Park Limestones. In l coastal Georgia and adjacent South Carolina the configuration W of the potentiometric surface is essentially unchanged from Warren's generalized map. Kay, M. 1958, North American geosynclines: Geological Society of America Memoir 48, 143 p. Early Paleozoic North America had a rather stable center (craton) margined by deeper sinking belts (miogeosynclines) that initally received carbonate rocks, and quartz sands from the interior; neither crea had appreciable volcanism. The l W A-38 I
0 l l I l continental borders have distinctive volcanic flows and fragmentals, which with associated sediments show deep subsidence (eugeosynclines) and development of associated I tectonic welts. Lands raised in the eugeosynclinal belts yielded sediments to the adjoining miogeosynclines; with deformation of the latter, terrigenous detritus spread into subsiding areas in the margin of the craton. The craton periodically gained basin or trough-shaped depressions isolated from highland source areas or receiving debris from associated intracratonal elevations. Kean, A.E., and Long, L.T., 1980, A seismic refraction line along the axis of the southern Piedmont and crustal thicknesses in the southeastern United States: Earthquake Notes, v. 51, no. 4,
- p. 3-13.
In order to evaluate Moho depths, a detailed refraction line and crustal model were developed along the axis of the southern Piedmont Province from central Georgia across South Carolina. No evidence for an intermediate layer in the crust I was observed. In the coastal plain, Moho depths of 25 miles shallow toward the southeast to 18 miles near the coast. Moho depths of 32 to 34 miles were measured for the mountains of north Georgia, eastern Tennessee and western North Carolina. Keller, E.A., 1972, Development of alluvial stream channels: A I five-stage model: Geological Society of American Bulletin, v. 83, no. 5, p. 1531-1536. A five-stage model is proposed to explain the development of alluvial channels. The mode is based upon channel morphology, channel morphoms ,, and qualitative conclusions based on numerous field obse m pons. Kesler, T.L., 1957, Environment and rrigin of the Cretaceous kaolin deposits of Georgia and South Q ,olina: Georgia Mineralogical Newsletter, v. 10, no. 1, p. 541-545. Unsorted sands containing little gravel and much diseminated kaolin constitute the Upper Cretaceous section from central Georgia at least to central South Carolina. Lenses of relatively pure kaolin occur largely in two areas. A gentle unconformity separates the Cretaceous beds from overlying I Tertiary beds. Kaolinite was formed by decomposition of the detrital feldspar in exposed parts of the deltas. King, P,B., 1977, The Evolution of North America: Princeton, Princeton I Univeceity Press, 197 p. A detailed discussion of the geologic history of North I America, including plate tectonics. Very short section on the Atlant.'c Coastal Plain. A-39
Klein, G. De V., 1969, Deposition of Triassic sedimentary rocks in separate basins, eastern North America: Geological Society of America, Bulletin v. 80, no. 9, p. 1825-1832. The Triassic basins of the Atlantic Coastal Plain were originally assumed to be fault-bounded troughs similar to those found in the recent troughs in the Basin-and-Range l Province. This model assumes the coincidence of physiographic 5 boundaries with structural boundaries. In the Dead Sea graben the basin boundary faults coincide with both the deepest. g portion of the Dead Sea on the west and a fault scarp on the g right. A similar facies model may explain the regional facies distribution of each isolated Triassie basin. Krapp, C.W. , and Stephenson, D.E. , 1978, SRP seismograph network operations August 6, 1976 to August 31, 1977: M Crawford, T.V., I ed. , Savannah River Laboratory Environmental Transport and Effects Research Annual Report-1977, E.I. duPont de Nemours and Company, Report DP-1489, p. 73-79. Three stations (SRFD, SRPN, SRPW) make up the seismographic network at the Savannah River Plant. In one year of nearly continuous operation 25 local earthquakes and more than 100 teleseisms have been recorded. Krause, R.E. , and Hayes, L.R. ,1981, Potentiometric surface of the principal artesian aquifer in Georgia, May 1980: Georgia Geologic Survey Hydrologic Atlas 6. Map covers the coastal plain of Georgia and shows roughly the a same trends in potentiometric surface as U.S. Geological Survey Open-File Report 81-486. The axis of the Gulf Trough g is indicated. Potentiometric contours do not cross the Millett fault study area. La Moreaux, P.E. ,1946a, Geology of the Coastal Plain of east-central Georgia: Georgia Geologic Survey Bulletin 50, p. 1-25. The oldest rocks exposed in east-central Georgia are the metamorphic and igneous rocks of probable Precambrian age, which are present in the Piedmont. The Tuscaloosa Formation of Upper Cretaceous age lies unconformably on the peneplaned cryscalline rocks and crops out in a discontinuous belt from two to eight miles wide along the northern margin of the g coastal plain. Throughout most of east-central Georgia the 5 Tuscaloosa Formation is overlapped by deposits of upper Eocene age because rocks of Paleocene and early and middle Eocene age g are not present in much of the area. During late Eocene time, g approximately 150 to 200 feet of sand, clay, marl, and limestone were deposited in a shallow marine sea. These upper I A-40 I
o T j. c-w ,. Eocene deposits which lie uncomformably on the Tuscaloosa *l.- Formation are represented by the Barnwell Formation, which Jd contains the Twiggs Clay Member, Irwinton Sand Member, and a , y *l / possible thin coarse sand bed with flat polished beach Y. pebbles, tentatively included as the Upper Sand Member, 3M although the latter may prove to be of Oligocene age. . y ., I Undifferentiated depoaits of Miocene and oligocene age lie unconformably on the Eocene deposits. g
, j,,
I La Moreaux, P.E., 1946b, Geology and ground water resources of the Coastal Plain of east central Georgia: Geologic Geologic Survey Bulletin 52,173 p.
.4 2.~
I The area covered includes a major part of the kaolin mining y. . district in Georgia. The oldest rocks in the area are 5 g, ^ metamorphic and igneous rocks of Precambrian age. Rocks of - I Paleocene, and lower and middle Eocene are not present in the /i* area. The Tuscaloosa Formation is the best source of ground ., water. f.,.'
;, 1
- LeGrand, H.E., 1961, Summary of geology of Atlantic Coastal Plain: ., Bulletin of the Fr.ori.can Association of Petroleum Geologists, ' i%
- v. 4 5, no. 9, p. 15 57-1571. [*, ,.
I
,.+
Some noteworthy features of the Atlantic Coastal Plain include: $
.A '[ p
- 1. In comparison with the Gulf Coast, the volume of sediments .I ; . i beneath the emerged part of the Atlantic Coastal Plain is not s ' .'
large. The volume of Cretaceous sediments is several times '!.*^ that of Cenozoic sediments. i ."
- 2. Almost all sediments north of North Carolina are sand and clay b.k . ' .; -
and are unconsolidated; southward, Tertiary limestone beds ?1 I represent the only significant quantity of consolidated beds shallower than 2,000 feet. Permeability of artesian aquifers decreases at great depth.
'[
I
- 3. Fresh water extends to a depth of several hundred feet in the 1.[gh ~~
mid-section of the coastal plain, but extends to shallower * . - depths in coastal areas. The bulk of sediments contain salt f.- K water. 1
- 4. Some sedimentary features includes a) basal Cretaceous fed ; .
I clastics that make correlations difficult, b) calcareous material north of North Carolina, c) the scarcity of the large amount of glauconite deposited from the Late Cretaceous
. ': ~.
'y I through the middle of the Eocene, north of Cape Fear Arch, d) the tendency toward downdip thickening, resulting in subsurface occurrence of beds having no surface equivalents, Q~.
>6-r
( y'. I . ; .* - il :
' '. f sr I A-41 ',,
r, s
.. L 9 ! J,3 I , .- .-
w _.__ _ _ _ _ _ _ _ _ _ _ _ _ . . _ _ _ _ _ _ _ . _ . _ _ .
I I LeGrand, H.E. , and Furcron, A.S. ,1956, Geology and ground water resources of central-east Georgia: Georgia Geologic Survey Bulletin 64, 174 p. This report covers an area along the Savannah River which includes both the Piedmont and Coastal Plain Provinces. Includes Burke, Jefferson and Richmond Counties. The g ' Tuscaloosa Formation y*ields as truch as 1,000 gallons per g minute. LeGrand, H.E. , and Pettyjohn, W.A. ,1981, Regional hydrogeologic concepts of homoclinal flanks: Ground water, v. 19, no. 3,
- p. 303-310.
The Savannah River incraases in discharge as it crosses a number of aquifers that are sandwiched between confining beds. Detailed hydrogeologic work would surely indicate that g several aquifers are crossed by the river, but two major g water-bearing zones are known. The upper one, consisting of limestone of Tertiary age that represents the principal artesian aquifer in Georgia, is crossed by the Savannah River along most of the river's course through Screven County. The
- other major aquifer system is the Cretaceous sand aquifer.
The potentiometric mep of the Cretaceous sand aquifer shows three contours that point downstreart, indicating a water-losing stretch. Using a transmissivity of 200,000 gallons pet day per foot it has been estimated that about 2.8 million gallons per day discharges through each 1-mile-long strip of the aquifer at the 160-foot contour line. LeGrand, H.E., and Stringfield, V.T., 1971, Differential erosion of carbonate-rock terranes: Southeastern Geology, v.13, no.1,
- p. 1-17.
Relief in carbonate-rock terranes may be local and small as expressed by many shallow sinkholes, or large as expressed by escarpments. In addition to relief within the karst terrane, there is commonly significant relief between a belt of carbonate rocks and an adjacent belt of noncarbonate rocks. Differential erosion results from a combination of physical g and chemical processes. Erosion in carbonate terranes is W favorable under moderate rather than under extreme conditions of cover, purity ef the carbonate rock, topographic relief, and precipitation. Leopold, L.B. , and Langbein, W.B. ,19 66, River meanders: Scientific American, v. 214, no. 6, p. 60-70. This paper discusses the formation of river meanders, which appear to be the form in which the river does the least work in turning. , A-42 1 I I
I I Leopold , L.B. , Wolman, M.G. , and Miller , J .P. , 1964, Fluvial processes in geomorphology: San Franciso, N.H. Freeman and Company, 522 p. General geomorphology text containing a detailed discussion of fluvial landforms. I Lewin, J., 1976, Initiation of bed forms and meanders in coarse-grained sediment: Geological Society of America Bulletin, v. 87, no. 2, p. 281-285. In a straight plane-bed channel in coarse sediment under natural flow conditions, primary transverse bars were rapidly formed during infrequent high flows,and the accompanyir.g flow modifications led to bank erosion. Primary bars were subsequently incorporated as the cores of point-car complexes, I with additional lateral and trail accretion, chute formation, and lesser erosional and sedimentary modifications. A three-stage model of meander development is found to be adequate for describing this process. Lewis, S.R., 1974, Significance of the vertical and lateral changes in the clay mineralogy of the Dunbarton Triassic Basin: University of I North Carolina, M.S. thesis, 34 p. Because of the differences in depth at which comparable reactions occurred in the two wells studied, a major fault is postulated as having occurred between the two wells with a theoretical displacement of 4,000 feet. Uplift and subsequent erosion of from 6,000 to 10,000 feet of sediment has occurred after Triassic but before Upper Cretaceous time in order for the sections in DRB 10 and DRB 11 to be present at the top of the basin. Liddicoat, J.C., and Opdyke, N.D., 1979, Paleomagnetic dating of late Neogene deposits in the Atlantic Coastal Plain with application to I dating tectonic deformation in the southeastern United States: Final Technical Report to the U.S. Geological Survey, Contract No. USGS-14-08-0001-17721, 18 p. Upper Tertiary and Quaternary marine deposits in the Atlantic Coastal Plain of Virginia, North Carolina, and South Carolina were studied and correlated by using magnetostratigraphy and 'I biostratigraphy. The geochronology resulting from these integrated paleomagnetic and biostratigraphic investigations has application to a wide variety of geological studies in the <g Atlantic Coastal Plain, including interpretation of tectonic Ig activity, dating of sea level fluctuations, and correlation of the onshore record with the deep sea record and a global time scale. A-43 l l
- I
I l Lindholm, R.C., 1979, Geologic history and etratigraphy of the Triassic-Jurassic Culpeper Basin, Virgina: Summary: Geological Society of America Bulletin, Part I, v. 90, no. 11, p. 995-997. < The Culpeper Basin, in northern Virginia, is but one of many such basins in North America where sedimentat'on extended from Late Triassic to Early Jurassic time. Red beds deposited on broed alluvial plains dominate in most of these basins. The sequence in the Culpeper Basin begins with coarse clastic rocks at the base, passing upward into fine-grained clastic rocks. Long, L.T., 1979, The Carolina Slate Belt - evidence of a continental rift zone: Geology, v. 7, no. 4, p. 180-184. The Carolina Slate Belt in Georgia and South Carolina may delineate the axis of a continental rif t or rif t system and may represent remnants of rif t-derived volcanic and sedimentary rocks. The proposed rift zone is interpreted mainly from crystal thicknesses and velocities obtained from gravity and seismic data. The rift developed from late Precambrian through Cambrian time (650 to 520 m.y. B.P.) , as determined from radiometric age dates. Long , L. ,1981, Microearthquake instrumentation and analysis between Hartwell and Clark Hill Reservoir Areas, Annual Report No. 1: I Project No. G-35-661, School of Geophysical Sciences, Georgia Institute of Technology. The objective of the microcarthquake instrumentation and the g analysis of data on events occurring between the Hartwell and g Clark Hill Reservoir Areas is to document the seismicity prior to, during, and af ter impoundment of the Richard B. Russell Lake. This first report covers the installation of the seismic monitoring system and the analysis of the data l W obtained by the seismic monitoring system through January 31, 1981. Long , L.T. ,1982, Seismicity in Georgia: in Arden, D.D., Beck, B.F., and Morrow, E., ed. , Second Symposium on the Geology of the Southeastern Coastal Plain, p. 202-210. Earthquakes in Georgia occur in the Coastal Plain, central Piedmont and folded Appalachian provinces. Six earthquakes l are known to have occurred in the Georgia Coastal Plain. The W seismic activity in the central piedmont occurs in a zone which extends northeast from central Georgia into South Carolina. Eight events have been felt in central Georgia and two near the South Carolina border in the central piedmont. The folded Appalachians of northwest Georgia have experienced I A-44 I
[ three events from within Georgia and others from adjacent [ areas of Alabama and Tennessee. No geologic fault in Georgia has been found to be associated with seismic activity. Large geologic faults can be found throughout Georgia, but they are considered inactive. Long, L.T. , and Champion, J.W. ,1977, Bouguer gravity map of the Summerville-Charleston, South Carolina, epicentral zone and ( tectonic implications: in Rankin, D.W., ed., Studies related to the Charleston, South Carolina earthquake of 1886-A preliminary report: U.S. Geological Survey Professional Paper 1028, p. 151-166. A new Bouguer anomaly map of the Summerville-Charleston, South Carolina, epicentral zone is interpreted to reveal a mafic intrusive body and associated flows, and a northeast-trending ( Triassic (?) basin. Two shallow structures interpreted from the gravity data and associated with the '*riassic(?) basin may be significant in determining the mechanis.; for the 1886 ( Charleston earthquake. The first is a border fault on the northwest side of the basin striking N45'E, and the second is a linear positive anornaly striking east. The first structure suggests the more conventional earthquake mechanism of [ reactivation of a basement fault. The second structure suggests a newly proposed mechanism of stress amplification in the anomalously rigid structure responsible for the linear [ positive anomaly. Intensity data from the August 31, 1886, Charleston earthquake and epicenters of recent events favor stress amplification as the more likely explanation for earthquake activity in the Summerville-Charleston epicentral [ zone. p Madeley, H.M. ,1972, Petrology of the Tuscaloosa Formation in ( west-central Georgia: Ohio State University, M.S. thesis, 93 p.
- This study had two objectives. The primary objective was to determine the environment of deposition of the Tuse:aloosi. ~
Formation where it is exposed in west-central Georgia. S[ In this area, the Tuscaloosa Formation unconformably overlies L granite, diorite, gneiss, and schist of the Georgia Piedmont. These same rock types are exposed north of the study area and are presumed to be similar to the rock types present there when the Tuscaloosa Formation was being deposited. A secondary objective of the study was to determine whether Folk's Empirical Quartz Classification System could profitably be employed in a study of the environment of deposition. Maher, D.H. ,1979, The Belair Belt of South Carolina and Georgia: Stratigraphy and depositional regime as compared to the Carolina (. slate belt: Geological Society of America (abs . ) , v. 11, no. 4, p . 18 4. A-45 c
I It is probable that the Carolina Slate Belt at.d the Belair Belt are depositionally correlative as part of an island-arc sequence. Manspelzer, W., Puffer, J.H., and Cousminer, H.L., 1978, Separation of Morocco and eastern Not th American A Triassic-Liassic I stratigraphic record: Geological Society of America Bulletin,
- v. 89, no. 6, p. 901-920.
Events leading to the separation of Africa and North America, and the subsequent spreading of the North Atlantic sea floor, are documented in rocks of Late Triassic to Early Jurassic age in eastern North America and Morocco. This paper presents new stratigraphic and geochemical data on the lower Mesozoic rocks of Morocco and establishes stratigraphic datums for l' E l trans-Atlantic correlations. These data are used to infer the sequence of events that led to the rif ting of Pangaea and the subsequent spreading of the North Atlantic sea floor. Marine, I.W., 1967, The permeability of fractured crystalline rock at g the Savannah River Plant near Aiken, South Caroli ta: U.S. Geological Survey Professional Paper 575-B, p. B203-B211. g The apparent permeability of finely fractured crystalline rock beneath the coastal plain sediments at the Savannah River Plant is estimated from swabbing tests to average about 0.0003 gallon per day per square foot. The apparent permeability of g zones of more open fractures is estimated from pumping tests 5 to average about one gallon per day per square foot. Marine, I.W.,1973, Geohydrology of the buried Triassic basin at the Savannah River Plant: Unpublished report presented at the International Symposium on Underground Waste Management and
- Artificial Recharge at New Orleans, Louisana, September 26-30, 1973, 20 p.
The Dunbarton Basin is 31 miles by 6 miles, and is 5,300 feet g thick. The permeability of the mudstone is low, with water-transmitting fractures virtually nonexistent. g Reflection seismic surveys show a sharp northwest boundary but do not indicate termination of the Triassic rocks where the southeast border was inferred from the aeromagnetic map. With scattered discontinuities (inferred faults) the contact of coastal plain beds and Triassic rocks could be followed by g reflection. The contact of Triassic and basement rock cou.'d g not be detected. Evidence from drill holes P12R and DRB 11 show that the inferred fault between them has not moved in 100 million years. The general trend in coastal plain sediments due to t(7 tonic tension has been indicated by downwarping. I A-46 I
5 - !5 - Furine, I.W.,1976a, Structural model of the buried Dunbarton Triassic Basin in South Carolina and Georgia, Geological Society of America, (a'bs . ) , v. 8, no. "l, p. 2 25. Seismic reflection surveys and model interpr(tation of
., gravity-magnetic sur'veys in the Dunbarton Triassic Basin i apparently indicated that the basin consists of fault blocks of different thicknesses and displacements. Drilling, however showed that apparent -displacement on the top of the Triassic was caused by a nasking of the reficction from the top of the Triassic. No fault. displacement has occurred on the top of the Triassic since aoout 100 p.illion years ago. Drilling information did not confirn or deny the displacement of the bottom of the Triassic.
Marine, I.W.,1976b, Structural and sedimentational model of the buried i Dunbarton Lasin, Scath Carolina and Georgia: Unpublished report presented at the 1976 Annual meeting of the Geological Society of America, Southeastern Section. _ No fault displacement has occurred since the development of the erosional surface en the top of the Triassic rock about
~
100 million years ago. Prior to intrabasinal faulting, while the basin was filling, a highland. existed to the northwent and was separated by a border tault, similar to those found in the Basin and Range Province. Two exploration wells, one on either side of an inferred introbasinal fault show no displacement of the surface, casting some doubt on the validity of the other inferred faults. The Dunbarton Basin may be wider than the 10 kilometers as previously reported I (Marine and Siple, 1974). The other intrabasinal faults inferred from the seismic data were also initially based on
, the displacement of the Triassic rock surface. They may also be caused by lensing of the masking reflector.
Marine, I.W., 1979a, Hydrology of buried crystalline rocks at the Savannah River Plant near Aiken, South Carolina: U.S. Dapartment of Energy DCE/SR-WM-79-2, 220 p. This Triassic basin may have faults at both borders, but the fault on the southeast may have a greater displacement causing the bottom of the basin to slope southeastward. [ All of the Triassic basins are bounded on one or both sides by large normal fault zones. Within the basins, normal faults are also common. There is no evidence of any compressional episodes in the form of metamorphism or intense folding since the deposition of the sediments. The reddish brown pre-Tascaloosa rocks encountered in wella PSR and DRB 9 are identified as Triassic on the basis of their lithologic composition, as no fossils were recovered from either well. The stratigraphic and structural position of A-47
I this body of rock as inferred from magnetic and seismic information also correlates well with a Triassic age assignment. Whereas definition of the boundaries are inexact, the steep magnetic gradient on the southeast, probably indicating a large normal fault, permits a more accurate placement of this boundary than the gentle and somewhat irregular magnetic gradient allows for the boundary on the northwest. l W Marine, I.W.,1979b, The use of naturally occurring helium to estimate g ground water velocities for studies of geologic storage of radioactive waste: Water Resources Research v. 15, no. 5, 3
- p. 1130-1136.
In a study assessing the potential for storing radioactive waste in metamorphic rock at the Savannah River Plant, the I
, rate of water movement was determined to be about 0.19 f t/yr by analyzing gas dissolved in the water. This water velocity is more applicable to the assessment of a geologic site for storage of radioactive waste than are velocities estimated from packer tests, pumping tests, or artificial tracer tests.
Marine, I .W. , and Fritz , S .J. , 1981, Osmotic model to explain anomalous hydraulic heads: Water Resources Research, v.17, no.1, p. 73-82. In the Dunbarton Basin it is suspected that osmosis causes the saline ~ water in the basin center to be slightly geopressurized l in relation to freshwater in the overlying coastal plain W aquifer. Wells penetrating the top and edge of the Triassic
, basin probably penetrate a zone where ion leakage gives rise g to less saline water,
. s
- g Marine, I .W. and Krapp, C.W. , 1976, Simulated seepage basin flow studies with soil-filled columns, M Crawford, T.V. , Ed. , Savannah l River Laboratory Environmental Transport and Ef fects Research, 5 Annual Report - FY 1975: U.S. Energy Resources Development Agency, DP-1412, p. 22-1 to 22-4.
During 1974, the fluid level in H Area Seepage Basin Number 4 began to rise while inflow remained approximately constant t indicating a decrease in seepage rate. To elucidate the causes and possible remedies for this undesirable situation, a series of soil column experiments were conductea using seepage basin soil and a variety of fluids. Marine, I . W. , and Root, R.W. ,1978, Geohydrology of deposits of Claiborne age at the Savannah River Plant: M Crawford, T.V., ed., Savannah River Laboratory Environmental Transport and Ef fects
, Research Annual Report - 1977: U.S. Energy Resources Development Agency, DP-1489, p. 57-59. ,
)
o In U.S. Geological Survey Bulletin 867 .(1936) Cooke considered all deposits of Claiborne age in the South Carolina Coastal l Plain to belong to the McBean Formation. In 1952, Cooke and A-48 l
I MacNeil raised the lower part of the deposits of Claiborne to formational status and called them the Congaree Formation and the Warley Hill :tarl. The Congaree Formation is a relatively high yielding aquifer; second only to the Tuscaloosa Formation in this area. It is probable that much of the water produced by high yielding wells (3,592 m3/ day; 660 gpm) reported to be pumping from the McBean Formation actually comes from the Congaree Formation. Marine, I.W., and Root, R.W., Jr., 1976, Summary of hydraulic I conductivity tests in the SRP separations areas, in Crawford, T.V., ed. , Se'rannah River Laboratory Environmental Transport and Ef fects Research, Annual Report - FY 1975: U.S. Energy Resources Development Agency, DP-1412, p. 21-1 to 21-4. In preparation for mathematically modeling the movement of water in the separations areas at the Savannah River Plant (SRP), hydraulic conductivities were calculated from existing data. This data was collected from laboratory tests of cores, pumping tests, water injection tests, injection-detection I tracer tests, and point dilution tracer tests. Marine, I.W. and Routt, K.R., 1975, A ground water model of the Tuscaloosa aquifer at the Savannah River Plant, M Crawford, T.V., ed. , Savannah River Laboratory Environmental Transport and Ef fects Research, Annual Report - 1974: U.S. Energy Resources Development Agency, DP-1374, p. 14-1 to 14-10. In areas of the South Carolina Coastal Plain within about 25 miles of the Fall Line, sand beds in the Tuscaloosa Formation form one of the major ground water supplies. Due to several additional planned ground water withdrawals from the Tuscaloosa Formation in the vicinity of SRP, a computer model D I of the Tuscaloosa aquifer was developed from existing information to obtain an estimate of the water flux through the system. ' Marine, I.W., and Siple, G.E. ,1974, Buried Triassic basin in the central Savannah Rwer area, South Carolina and Georgia: Geological Society of America, Bulletin v. 8 5, no. 2, p. 311-3 20. A basin filled with Triassic red beds, located on the South Carolina-Georgia line 20 miles southeast of Augusta, Georgia, I e is buried beneath 1,100 feet of Coastal' Plain sediments. An extensive aeromagnetic survey, seismic refraction and reflection surveys, and geophysical logs and samples from three wells define the extent and character of the basin. I - This basin, herein named the Dunbarton Triassic Basin, is 31 miles long, six miles wide, and trends northeast. g l s ,
I The northwest margin of the basin is well defined by the aeromagnetic survey, a seismic reflection traverse, and a well that passed through 1,600 feet of Triassic fanglomerate before entering the crystalline metamorphic rocks below. Near the l center of the Triassic basin, a well passed through 3,900 feet 5 of maroon Triassic mudstone and sandstone of fluvial origin without penetrating the bottom of the basin. Mar salis, W.E . , 1970, Petroleum exploration in Georgia: Georgia Geologic Survey Information Circular 38, 52 p. This information circular describes the oil and gas tests drilled in Georgia from 1903 through 1970. Most of the data has been compiled from the files of the Bepartment of Mines, E Mining and Geology, and from Geological Survey of Georgia g Bulletin 70. Marsalis, W.E . , and Fridell, M.S. , 1975, A guide to -selected Upper Cretaceous and lower Tertiary outcrops in the lower Chattahoochee River valley of Georgia: Georgia Geological Society Guidebook 15, 79 p. 3 The Chattahoochee River valley has excellent exposares of formations ranging in age from Late Cretaceous to middle Eocene. The geology is complicated by solution, overlap, and facies changes along strike and downdip, and also by cyclic deposits of Cretaceous age. Mayer, P.G., and Platt, R.B., 1971, The impact of BNFP's operation of ground water resources: Unpublished report No. EMP-102, 66 p. A comprehensive investigation of the quantitative and W qualitative aspects of ground water in the BNFP area. Mayer, P.G. ,1972a, Report of Emergency Cooling in Beacon Pond: Unpublished repor t No. EMP-103,18 p.
, 'An analysis of the effect of power failures on water l temperatures in Beacon Pond. M Mayer, P.G., 1972b, Impact of BNFP's' pr b.'ge from the Tuscaloosa o
g. aquifer on the ground water table: onpublished report number g EMP-104, prepared for Allied-Gulf Nuclear Services, v. III, page 6: Report on file at U.S. Geological Survey Poraville, Georgia 30360. . a s Adverse effects of pumpage from the Tuscaloosa on the water supply systems in the area were not observed. Pumpage from the Tuscaloosa aquifer d'id not result in any drawdown of the ' upper water table. The report concludes that the Tuscaloosa aquifer is safe from inflow of radionuclide-contaminated water that might be introduced accidentally into the upper table at
, BNFP.-
A-50 L
Mayer, P.G., 1973a, The Hydrology of the Barnwell Nuclear Fuel Plant area: Unpublished report No. EMP-106, 65 p. This is a detailed hydrologic study of the Barnwell Nuclear Fuel Plant including a hydrologic study of the Barnwell I Nuclear Fuel Plant including a hydrologic description of the site and facilities, as well as environmental hazards (flooding, dam failure, tsunami) . Mayer , P.G. ,1973b, The hydrologic studies at Allied-Gulf 's Barnwell Plant: Unpublished report no. EMP-110,14 p. A report of hydrologic studies presented to the Advisory Committee on Reactor Safeguards. The studies showed that accidentally introduced radionuclides.would produce no hazards. A safe, reliable water supply is available from wells in the Tuscaloosa aquifer, and withdrawal from the o Tuscaloosa aquifer will have little effect on piezometric levels in existing deep wells and no effect on wells in the McBean Formation. Mayer, P.G., 1974, Letter regarding review comments of AEC on S/F FSAR: Unpublished report no. EMP-ll8. Hydrologic engineering review comments on site drainage probable maximum flood potential, the effects of local maximum precipitation on the site drainage systems, and discussion of
- , a runof f model for the Barnwell Nuclear Fuel Plant. , Mayer , P.G. ,1975,' Letter regarding ground water at Barnwell Nuclear Fuel Plant: Unpublished report no. EMP-127.
I 1 Analysis of ground water elevations at the Barnwell Nuclear Fuel Plant and rainfall data from Columbia, South Carolina and Augusta, Georgia. Mayer, P.G., 1979, Review report on studies related to the Charleston, South Carolina earthquake of 1886, Unpublished report no. EMP-140, 11 p. , s . A review of studies relating to tectonic activity in the southeastern United States was made. The basis of the review I e was the U.S. Geological Survey Professional Paper 1028. The revis was made to assess the validity of the earthquake design criteria employed in the design of. the Barnwell Nuclear I Fuel Plant of the Allied-General Nuclear Services, Inc. of Barnwell, South Carolina. In ,the light of the present review, the earthquake design criteria employed at BNFP appear . shtisfactory. , a g
+
I McKee, E.D. and others,1959, Paleotectonic maps Triassic system: U.S. Geological Survey Miscellaneous Geological Investigations Map I-300, 33 p. , 9 pls. , 32 figs. , scale - 1: 5,o00,000 for pls.1-6, 8. Detailed discussions and maps of several fault bounded Triassic basins in the Atlantic Coastal Plain. Milton, C., and Hurst, V.J., 1965, Subsurface " basement" rocks of Georgia: Georgia Geologic Survey Bulletin 76, 56 p. This report describes all available specimens of rocks found as bottom cores or cuttings, by drilling below the Cretaceous or younger coastal plain sediments. This report also reviews what is known about buried Triassic rocks in states north of Georgia, and discusses the alteration of sandstones by igneous intrusions within the basins. Mitchell, G.D. ,1980, Potentiometric surface of the principal arteFian aquifer in Georgia-November, 1979: Georgia Geologic Survey ' Hydrologic Atlas 4, 2 sheets. Map covers the Coastal Plain of Georgia and small parts of Alabama, Florida, and South Carolina. Pctentiometric contours differ little from those shown in U.S. Geological Survey e Open-File Report 81-486 and Georgia Geologic Survey, Hydrologic 3 Atlas 6. - Mixon, R.B., and Newell, W.L., 1977, Stafford fault system: Structures documenting Cretaceous and Tertiary deformation elong the Fall Line
, in northeastern Virginia: Geology, v. 5, no. 7, p. 4?7-4 40.
Four en echelon northeast-trending structures, including southeast-dipping monoclines and northwest-dipping, high-angle reverse faults have been mapped along the inner edge of the Coastal Plain. Although displacements are small, the lB structures have an effect on the present thickness and distribution of coastal plain sediments in the area. Most of g the deformation took place in the Cretaceous and middle (?) g
., Tertiary, but more recent movement is possible. Similarities between the Stafford fault system and Brandywine fault system ,
suggest the two may be tectonically related. G Moye, F.,1976, Abstracts of theses on Georgia geology through 1974: Georgia Geologic Survey Bulletin 89, 94 p. Lists titles and abstracts of theses on the geology of Georgia.
- Murray, G.E., 1961, Geology of the Atlantic and Gulf Coastal Provinces
, of North America: Ha. per and Brothers, New York , 692 p.
A detailed, somewhat dated (pre-plate tectonics) discussion of the history, structure, stratigraphy and geography of the l W Atlantic and Gulf Coastal Provinces. 0 l A-52 s
t l Narasimhan, T.N. , Neuman, S.P. , and Witherspoon , P. A. , 1978, Finite B element method for subsurface hydrology using a mixed explici t-ir. flicit scheme: Water Resources Research, v.14, no. 5,
- p. 863-877.
The mixed explicit-implicit Galerkin finite element method developed previously by the authors is shown to be ideally suited for a wide class of problems arising in subsurface hydrology. These problems include confined saturated flow, unconfined flow under free surface conditions subject to the Dupuit assumption, flow in aquifers which are partly confined
'B and partly unconfined, axisymmetric flow to a well with storage, and flow in saturated-unsaturated soils. A single I
computer program, entitled FLUMP, can now handle all of these problems. The mixed explicit-implicit solution strategy employed in the program insures a high level of accuracy and computation efficiency in most cases. Noble, D.F.,1962, Origin of the expandable clay minerals in the Twiggs Clay of Eocene age: Florida State University, M.S. thesis, 85 p. The Twiggs Clay Member of the upper Eocene Barnwell Formation crops out along a zone extending from the central part of Houston County, Georgia northeastward to Wrens, Georgia, and I- probably into South Carolina. This member contains expandable clays of two derivations. One of these, degraded illite, has been derived from muscovite, the other, "true" I e montmorillonite, from non-micaceous materials. The results indicate that the degree of degradation of muscovite, illite, and contractible expanded clay may be used as a key to the rate of erosion and severity of weathering in the source area. O'Cbnnor, B.J. and Prowell, D.C. ,1976a, Post-Cretaceous faulting along the Belair fault zone near Augusta, Georgia: Geological Society of I 4 America (abn.) , v. 8, no. 2, p. 236-237. - Detailed outcrop and subsurface investigations have revealed , I that the Belair fault is a zone of significant early Tertiary faulting. The fault, which thrusts upper Precambrian (?) phyllites over suspected early Tertiary sands and gravels, is well exposed in several locations. Extensive auger and core
=. drilling data show that the fault zone is a series of northeast-trending en echelon breaks, where the eastern fault block has moved up and to the west relative to the western block.
O'Connor , B.J. , and Prowell, D.C. ,1976b, The geology of the Belair fault zone and basement rocks of the Augusta, Georgia area: I- Georgia Geologic Society Guidebook 16, p. 21-32.
; g " Basement" rock of the east-northeast trending Kiokee Belt in g , the Augusta area consists of high grade gneisses which are ~
intruded by a variety of granites. On the south the Kiokee I A-53 I -
~l
{ I Belt is in contact with low grade phyllites and related g metavolcanic and metasedimentary rocks of the Belair Belt of m the "Little River Series." The age of the Tuscaloosa Formation is critical because it is the youngest of the coastal plain sediments cut by the Belair fault. Definite correlation is difficult because of a paucity of fossils; palanological studies indicate an age as young as l middle Eocene in clays found in eastern Georgia. The " unconformity at the base of the Tuscaloosa is important because changes in its elevation are used to locate the Belair g fault zone. Bedding of the Tuscaloosa is slightly warped by 3 the fault within about 20 feet of the fault plane. Vertical separation of the unconformity across the zone increases from south to north, and the zone comprises more individual faults in the north. Because of poor exposure, deep weathering, and the lack of a persistent marker horizon, the unconformity at the base of the Eocene sediments is not mapped in detail. Also due to this poor exposure there are no documented faults in the Eocene sediments. The fault zone has ben delineated by surface and drilling using the base of the 9".caloosa as a g marker horizon. The eastern block was moving up and tilting g southward relative to the western block dur 8.ng faulting. In spite of the uncertainty of radiocarbon aat. s it is suggested l that an age of 1,500 to 2,000 years Before Pres. nt -isf proper for the reworked sediments and thus a minimum agA for late
, movement on the fault. The carbon flakes in tba gray lenses were deposited at the same time as the sands of the reworked sediments and that the radiocarbon ages deterrint J are the l
W depositional ages. The Belair Fault zone has been traced 13 miles by means of detailed surface mapping and extensive drilling It trends north-northeast and has as much as 100 feet of wrtical separation of the unconformity at the base of tbt Tusesloosa Formation. Surface exposures of the fault at to a;alities show that the basement phyllites have been thrust westward j over coastal plain sediments with at least two episodes of g l movement; one in the last few thousand years. E Oldham, R.W.,1981, Surface to subsurface geology of eastern Aiken, g western Orangeburg, northern Bamberg, and northern Barnwell g Counties and structural attitude and occurrence of the Black Mingo Formation in the subsurface between 'Se Santee and Savannah Rivers, South Carolina, University of South unrolina, M.S. thesis,111 p. The regional subsurface occurrence, structural e.ttitude, and lithostratigraphy of the Black Mingo Formation have beer. g mapped in the area of the Coastal plain of South Carolina g e located between the Santee and Savannah Rivers. Two A-34 9 I
r ,e subsurface formations are proposed. The Neeses Formation and -I Bamberg Formation represent shoreward and transitional lithofacies with respect to the seaward Santee Lirtestone I Formation and were deposited during the lower middle Eocene transgression, high stand and regression. A graben is mapped in Jasper and Beaufort Counties as an interpretation for displaced Black Mingo sediments. Faulting may have occurred as early as the Paleocene and as late as the Miocene. A fault is also mapped in north Bamberg County. Displacement is less than 100 feet and the upthrown side is to the east. I. Oliver, J. ,1977, Recent vertical crustal movements: The eastern United States: Quarterly progress report for period 9/1/76-1/1/77 to U.S. Nuclear Regulatory Commission. Preliminary results in the B'<3 Ridge and Piedmont Provinces indicate a regional northeast iard tilting of the ' Blue Ridge , belt; and a peak of relative velocity in North Carolina near Asheville, which corresponds to the Blue Fidge escarpment, marking the locus of the Atlantic Gulf drainage divide. These I data suggest dynamic uplif t of the Blue Ridge-Piedmont geologic boundary in the southern Appalachian orogen. Preliminary results of the first detailed transcontinental I ' profile of vertical crustal movements indicate thet movements in the western and eastern Ur.ited States are similar. Olsen, P.E., and Galton, P.M., 1977, Triassic-Jurassic tetrapod extinctions: Are they real?: Science, v. 197, no. 4307, p. 983-986. Terrestbial vertebrate fossils show that part of the Newark Supergroup of the eastern United States, all of the Glen Canyon Group of the southwestern United States, and the Upper Stormberg Group of southern Africa are Early Jurassic. This new correlation demonstrates that the supposed widespreaa tetrapod extinction at the Triassic-Jurassic boundary is an artifact of spurious correlation.
- Ormsby, M.R., 1980, Probability that another intensity X event could occur in the S.E. during a 200 year period: Georgia Institute of
. Technology, M.S. thesis,100 p.
Seismic risk computations for the relatively a seismic l I ' southeastern United States generally show that Charleston, South Carolina (and the southeast) have considerable potential for earthquake damage. The probability of the southeast sustaining another intensity X earthquake in the 200 year period following the 1886 Charleston, South Carolina has been ) calculated to be as high as 0.50. One reason for this high db risk calculation value is the inclusi.on of major aftershock I sequences. Using an af tershock time window to remove major aftershock sequences reduces the probability of recurrence to 0.12.
*' A-55 I .
I Padgett, G.G., 1980, Lithostratigraphy of the Black Mingo Formation in Sumter, Calhoun, and Richland Counties, South Carolina: University of South Carolina, M.S. thesis, 68 p. The purpose of this study is to extend the investigation of the Black Mingo Formation from type areas in Williamsbu{g County to Sumter, Calhoun, and Richland Counties. Correlation of geophysical logs and measured outcrops between the Congaree Bluf fs and the Lane, South Carolina drill holes and outcrops
- were made in order to tie previous field work in Lexington County to biostratigraphic studies from Lane and to the type sections of the Black Mingo Formation. An opaline claystone has been correlated within the Black Mingo Formation and interpreted as a marsh / lagoonal sequence of the Williamsburg g
g member. Depositional environments have been interpreted and a transgressive sequence with minor prograding and retrograding sequences within the Williamsburg Member of the Black Mingo Formation are proposed. An upper deltaic sequence underlying the Williamsburg Member is proposed to be within the Black Mingo Formation. Patterson, S.H., and Buie, B.F., 1974, Field conference on kaolin and fuller 's ear th, November 14-16, 1974: Georgia Geological Survey, g 53 p. g The kaolin deposits in the Macon-Gordon area, Georgia Are pa'rt of a belt of kaolin deposits extending along the inner / edge of the coastal plain from the Aiken district South Carolina, southwestward to the vicinity of Macon. - Pa tterson, S.H. , and Herrick , S.M., 1971, Chattahoochee Anticline, Appalachicola Embaymer't, Gulf Trough and related structural features, southwestern Georgia, f act or fiction: Georgia Geological Survey I O rmation Circular 41, 16 p. The original definition of the Chattahoochee Anticline is now known to be incorrect. The Gordon Anticline may exist in the southern part of the area originally thought to have been
, occupied by the Chattahoochee Anticline.
Some geologists have thought that the Ochlockonee fault of Sever forms the southeast side of the Gulf Trough. There is insufficient evidence to support this conclusion. The Gulf Trough may be a sediment-filled Tertiary strait or marine valley instead of a syncline or graben, and its structure may have been modified by carbonate solution. Petty, A.J. , Petrafeso, F. A. , and Moore, F.C. , Jr . ,19 65, Aeromagnetic map of the Savannah River Plant area. South Carolina and Georgia: U.S. Geological Survey Geophysical Investigations Map GP-489. g 1 sheet, scale: 1:250,000. g e A-56 I 3
I hA Aeromagnetic survey of the Savannah River Plant and surrounding area. The general outline of the Dunbarton Basin can be inferred. Pickering , S.M. , Jr. ,1971, Lithostratigraphy and biostratigraphy of the north-central Georgia Coastal Plain: Georgia Geological Society, Sixth Annual Field Trip. Field trip guide discussing the lithostratigraphy and biostratigraphy of the Tuscaloosa Formation, Clinchfield Sand, Ocala Limestone, Twiggs Clay, Irwinton Sand, Flint River Formation, McBean Formation, and the upper sands of the Barnwell Formation. Included is a description of the stratigraphy at Georgia Kaalin Co. mine no. 59 B. ~ Pirkel, W.A.,1981, Geology of the Limestone quadrangle, west-central South Carolina: South Carolina Geology, v. 25, no.1, p. 21-27. The Limestone 7.5-minute quadrangle is in the slate belt of west-central South Carolina. Rock units include argillites, felsic metavolcanics, and greenstones. These units occur in bands that trend northeast-southwest. A large granite intrusion is present in the western part of the quadrangle. The slate belt rocks of the area are a part of a regional syncline that trends northeast-southwest. Poag , C.W. ,1982, Biostratigraphy, sea level fluctuations, subsidence rates, and petroleum potential of the Southeast Georgia Embayment: _in, Arden, D.D. , Beck , B.F. , and Morrow, E. , ed. , Second Symposium on the Geology of the Southeastern Coastal Plain, p. 3-9. 9 . The age of sedimentary rocks in the GE 1 well ranges from Early Cretaceous to Pleistocene, and a variety of paleoenvironments are represented (e.g. , terrestrial, continental shelf, upper continental slope) . Eight major hiatuses represent intervals of erosion and nondeposition and are correlative with low stands of global sea level. I Conversely, the deepest water paleoenvironments correspond to high stands of global sea level. Pollard, L.D. and Vorhis, R.C. ,1980, Tne geohydrology of the Cretaceous I- . aquifer system in Georgia; Georgia Geologic Survey Hydrologic Atlas 3, 5 sheets. This report delineates aquifers and aquieludes in the Creteceous aquifer system and describes the quality and
, availability of the water in each of the aquifers. Structure I
contours t oss the Millett fault study area. Potentiometric contours cover only a small southern portion of the Millett fault study area. 1 I-A-57 r-i
# , W D
s - I Pooser, W.K. ,1965, Biostratigraphy of Cenozoic ostracoda from South l Carolina: University of Kansas Paleontological Contributions 8, W 60 p. The ostracodes proved to be a reliable means of determining the geologic age of the Cenozoic units, differentiating the strata into readily recognizable biostratigraphic units, and interpreting with a high degree of confidence the environments of deposition for strata as old as Miocene. Pooley, R.N., 1960, Basement configuration and subsurface geology of l eastern Georgia and southern South Carolina as determined by E seismic-refraction measurements, University of Wisconsin, M.S. thesis,, 47 p. This thesis supports the presence of the subsurface feature first postulated and named the Yamacraw Uplif t as_ first reported. This structure appears to be of tectonic origin but probably originated before the advent of Cretaceous time since, none of the overlying sediments show evidence of structural derangement. Popenoe, P., and Zietz, I. ,1977, The nature of the geophysical basement beneath the Coastal Plain of South Carolina and northeastern Georgia, in Rankin, D.W. , ed. , Studies related to the Charleston, South Carolina, earthquake of 1886 - A preliminary report: U.S. Geological Survey Professional Papet 1028, p. 119-137. Geophysical data delineate two distinctive crustal provinces beneath the Coastal Plain of Georgia and South Carolina. The province adjacent to and east of the Fall Line is a continuation of the Piedmont, composed chiefly of schist and g g gneiss units, which geologically and geophysically reflect the fabric of the Appalachian orogen. In structure and composition, the basement rocks are similar to those of the Carolina Slate Belt and the Charlotte Belt immediately west of the Fall Line. At least two small Triassic basins are present
,within the province and are clearly delineated by the magnetic l<
data. W Poppe, B., 1979, Historical survey of U.S. seismograph stations:' U.S. Geological Survey Professional Paper 1096, 389 p. A listing of seismograph stations, including information on operating organizations, instrumentation, and availability of seismograms. + = Pressler, E.D., 1947, Geology and occurrence of oil in Florida: American Association of Pettoleum Geologists Bulletin, v. 31, l 3 i no. 10, p. 18 51-18 62. l This report provides names for several framework features of the' Georgia Coastal Plain, among them are the Okeefenokee Embayment, Appalachicola Embayment, and Central Georgia Uplift. I C
+ . A-58 L
I I Prowell, D.C. , and O 'Connor , B.J. ,1978, Belair fault zones: Evidence 3 of Tertiary fault displacement in eastern Georgia: Geology, v. 6, no. 11, p. 681-684. The Belair faalt is the first well-documented Cenozoic fault I in this region. The southeast fault block has moved up and to the north, having a vertical of fset of 100 feet since Late Cretaceous time and 33 feet since the late Eocene. It consists of eight en echelon oblique-slip reverse faults and is at least 15 miles long; lateral displacement of 14 miles is recognized. I Prowell, D.C. , O 'Connor , B.J. , and Rubin, M. , 1975, Preliminary evidence for Holocene movement along the Belair fault zone near Augusta, Georgia: U.S. Geological Survey Open File Report 75-G80, 8 p. The unconformity at the base of the Tuscaloosa is the only easily recognized marker horizon offset by the fault. Bedding of the Tuscaloosa is slightly warped by the fault within about 20 feet of the fault plain. Vertical separation of the unconformity across the zone increases from south to north and I the zone comprises more individual faults in the north. Holocene faulting is indicated by the structural-stratigraphic relation exposed in a U.S. Geological Survey backhoe trench. I Rainwater, E.H. ,1964, Transgressions and regressions in the Gulf Coast Tertiary: Transactions of the Gulf Coast Association and Geologic Society v. 14, p. 217-230. The thick Tertiary section of the central and western Gulf Coast is composed of alternating sand and shale sequences and is characterized by an alternation of marine and nonmarine strata. It appears that eustatic sea level changes did not cause the advance and retreat of the shoreline, but that tectonics and variation in sediment supply caused the transgressions and regressions in tht9 area of terrigenous cla,s tics . 4 I E=ndazzo, A.F. , and Copeland, R.E. ,1976, The geology of the northern
' portion of the Wadesboro Triassic Basin, North Carolina:
Southeastern Geology, v.17, no. 3, p.115-138. - Clastic sediments representing alluvial fan and other fluvial =- deposits have been mapped in the northern portion of the Wadesboro Triassic basin. , Complex faulting and 'fanglomerate
' deposits occur along the ndrthwestern border of this basin, and a major normal fault forms the southeastern border.
Post-depositional movement along this fault has given the Triassic beds a southeasterly dip. 4 A-59 I
I Randazzo, A.F., Swe, W., and Wheeler, W.H., 1970, A study of tectonic influence on Triassic sedimentation, the Wadesboro basin, central Piedmont: Journal of Sedimentary Petrology, v. 40, no. 3,
- p. 998-1006.
The Wadesboro basin is defined by normal border faults with the basin representing the down dropped block. Many normal cross faults cut both Newark and pre-Newark rocks of the region. Newark rocks are cut by longitudinal faults which are also normal and trend northeast. Prominent fault scarps produced coarse-grained clastic rocks. Fine-grained sediments are found where faults are not rejuvenated. The eastern E margin has finer grained sediments which may have been deposited prior to activity of the eastern border fault or during a period of quiescence. Steep faults must have existed on the western border as indicated by the presence of fanglomerates . During sedimentation the source was periodically uplif ted as evidenced by alterations in the size of the sediments. The Wadesboro basin may represent a complete graben fitting the " Physiographic Coincidence Model". Rankin, D.W., 1975, The continental margin of eastern North American in the southern Appalachians: The opening and closing of the proto-Atlantic Ocean: American Journal of Science, v. 275-A, no. 3, p. 298-3 36. ' Two themes are developed within this paper; the first is the evidence in the southern Appalachians for an early episode of rifting. It appears that by about 800 m.y.B.P. ago a broad region more or less paralleling the Appalachian orogen was undergoing lateral extension accompanied by the emplacement of a nonorogenic bimodal plutonic volcanic group. The second theme developed is that the Blue Ridge and Piedmont Provinces represent different continental plates (the North Agerican plate and African plate, respectively) . Differences
-in lithology and deformational history of the two provinces led to this interpretation which also proposes that large +
masses of the African plate have been thrust onto the margin of the North American plate. Rankin, D.W., 1976, Appalachian salients and recesses: Lite g Precambrian continental breakup and the opening of the Iapetus Ocean: Journal of Geophysical Research, v. 81, no. 2, p. 5605-5619. The major thesis of this paper is that Appalachian salients I and recesses are inherited from the initial breakup of a continental mass by the intersection of rif t valleys radiating lj l from triple junctions at the start of the opening of the Wl
,Iapetus Ocean. Discussion focuses mainly on the Appalachian l E'O i A-60 'h
- I '
I orogen between Chattanooga, Tennessee, and Quebec City, Canada. Within this length, five major bends in Appalachian structural trends are candidates for plume-generated triple junctions. Rankin, D.F. , ed. ,19 77, Studies related to the Charleston, South Carolina earthquake of 1886 - A preliminary report: U.S. Geological Survey Professional Paper 1028, 204 p. l The crystalline basement beneath the Charleston-Summerville l area is not simply a seaward extension of crystalline rocks of l the Appalachian orogen that are exposed in the Piedmont to the l northwest, but has a distinctive magnetic signature that does 'g not reflect Appalachian orogenic trends. The area underlain g by this distinctive geophysical basement, the Charleston block, may represent a broad zone of Triassic and (or) Jurassic crustal extension formed during the early stages of the opening of the Atlantic Ocean. The Charleston block is characterized in part by prominent, roughly circular magnetic and gravity highs that are thought to reflect mafic or ultramafic plutons. The present stress regime of the Charleston-Summerville area appears to be one of northeast-southwest compression rather than of extension as it presumably was in the Mesozoic. The present stress regime seems similar to that of much of the eastern United States. Reagor, B.G. , Stover , C.W. , and Algermissen, S.T. ,1980, Seismicity map of the state of South Carolina: U.S. Geological Survey Miscellaneous Investigations Map MF-1225,1 sheet, scale I 1:1,000,000. This map contains earthquake data originally used in preparing i a report on seismic risks in the United States. Intensity !W values were updated from new and additional data sources that t were not available at the time of original compilation. Reichert, S.O., 1967, Summary report on the geology and hydrology of the 100 and 200 areas at Savannah River Plant for the period 1961-1966: E.1. duPont de Nemours and Co., 52 p. I This paper reports the results of monthly measuring the water level elevations of 52 wells in the 200 Areas, 15 in 100K I Area, 14 in 1000 Area, 18 in 100L Area, and 17 in 100P Area. It also summarizes the lithology by 10-foot increments of depth below the ground surface of 89 drill holes in the 200 Areas, and of the logs of drill holes in the 100 Areas that were used for water level measurements. A-61 I I
e I Peinhardt, J. , Gibson, T.G. , Bybell, L.M. , Edwards, L.E. , Fredericknen, ~ N.O. , Smith, C.C. , and Sohl, N.F. ,1980, Upper Cretaceous and lower W Tertiary geology of the Chattahoochee River valley, western Georgia and eastern Alabama: Geological Society of America Field Trip No. 20, p. 38 5-463. This report discusses the stratigraphy, depositional environment, and the biostratigraphy of both macrofossils and microfossils of the Chattahoochee River valley. Rhea, S. ,1981, South Carolina seismic program, Seismological data report: U.S. Geological Survey Open-File Report 81-362, 79 p. This paper reports data collected on the South Carolina Seismic Network from March 1973 thru July 1980. Hypocentral parameters were computed by the program HYPCELLIPSE. Rice, T.E. , Jr. ,1980, The Sabine Stage in the Georgia Coastal Plain: Emory University, M.S. thesis, 122 p. In the subsurface of the Georgia Coastal Plain, along the southern and southeastern margins, a relatively thick Sabine section overlies Gulfian (Upper Cretaceous) rocks. In the interior of the Coastal Plain a relatively thin Sabine section g overlies a significant thickness of Midwayan (lowest Tertiary) g rocks. Tectonism along a major south-southease fault system in the Georgia Coastal Plain is proposed to be responsible for these Midway-Sabine stratigraphic " structural relations. The Sabine deposits of the Georgia Coastal Plain are increasingly clastic in a northwestward, updip direction. The Sabine section at its extreme updip limit is comprised of nonmarine, clastic sediments of the Gravel Creek Member of the Nanafalia Formation. Ritter, D.E., 1979, Process Geomorphology: Dubuque, Wm. C. Brown Company Publishers, 603 p. General text in geomorphology containing detailed discussions of fluvial landforms. Root, R.W., 1979a, Computer modeling of ground water flow at the Savannah River Plant: Geological Society of America (abs.) , v.11, no. 4, 210 p. Using a three dimensional finite difference scheme, a ground water head model of the subsurface beneath a part of the Savannah River Plant is being developed. The study area is l underlain by unconsolidated and semiconsolidated sands, clays, E sandy clays, and clayey sands. The ground water system of A-62 I
interest is bounded on two sides by surface streams, on the third side by a piezometric high, on the top by the water table, and on the bottom by a permeable flow boundary. The presence of low conductivity clay layers causes definite vertical gradients of hydraulic head. Root, R.W.,1979b, A summary of exploration drilling in F Area for hydrogeologic information, in, Crawford, T.V. , ed. , Savannah River Laboratory Environmental Transport and Ef fects Research, Annual Report 1978: U.S. Department of Energy, DP-1489, p. 69-71. Analysis of undisturbed cores, continuous split-barrel e samples, and tests on permanent wells were used in developing a mathematical model of three-dimensional ground water flow beneath the Separations Areas and a conceptual geologic framework at the Savannah River Plant. Root, R.W., 3 , 1979b, Results of drilling a well cluster near F Area at SRP, in Crawford , T.V. , ed. , Savannah River Laboratory Environmental Transport and Effects Research, Annual Report - 1978: U.S. Depar tment of Energy, DP-15 26, p. 213-217. A cluster of five wells was drilled on the bluf f above Upper Three Runs Creek in the northwestern part of the Savannah River Plant Separations Areas to confirm the conceptual geohydrologic model in this area. The upward head gradient in the Congaree and Ellenton Formations suggests that water is discharging into Upper Three Runs Creek from these formations. This information is useful in developing a three-dimensional model of ground water movement and potential contaminant transport. Root, R.W. , Jr. ,1979c, Subsurface hydrology of coastal plain sediments in the SRP Separations Areas, in, Crawford, T.V. , ed. , Savannah River Laboratory Environmental Transport and Effects Research, Annual Repor: - 1978: U.S. Depar tment of Energy, DP-1526,
- p. 207-212.
The water table beneath the Savannah River Plant occurs primarily within the Barnwell Formation. The gradient in the I Congaree is low compared to the gradient of the water table and the McBean Formation. Root, R.W. , and Marine, I .W. , 1978, Water-level fluctuations in coastal plain sediments at SRP: in Crawford, T.V., ed., Savannah River Laboratory Environmental Transport and Ef fects Pesearch Annual Repor t - 1977 : U.S. Department of Energy, DP-1489_, p. 65-68. Water levels in all wells generally increase in elevation during the winter and early spring and decline for the remainder of the year. Water levels in the Barnwell Formation are higher than those in the McBean Formation; and these, in turn, are higher than the water levels in the Congaree Ib A-63
I Formation. Due to low clay content relative to the Barnwell and McBean Formations, the Congaree Formation conducts water more rapidly towards Upper 'Ihree Runs Creek, where it is discharged from the formation. The source of most of the water that moves down through the Barnwell and McBean l W Formations into the Congaree Formation is local precipitation. However, the Tuscaloosa Formation is recharged by precipitation northeast of the Savannah River Plant. Thus, the water levels in the Tuscaloosa Formation are not influenced by natural recharge or discharge at the Savannah River Plant. The amplitude of the water-level fluctuations are dampened with depth, but the response of the water levels in the deeper formations to rainfall is as immediate as that in the shallower formations. Sanover , A. , and Sower s, G.F. ,1967, Appendix A: Aerial photographic studies for Altamaha River Project, Georgie Power Company: Law Engineering Testing Company, Atlanta, Georgia,18 p. These studies provide an analysis of aerial photographs from the U.S. Department of Agriculture. The photographs were used to define geographic features such as drainage anomalies, Carolina Boys, sink holes and spring heads. Schilt, F.S. , Brown, L.D. , Oliver , J.E . , and Ka ufman, S. , 19 82, Subsurface structure near Charleston, South Carolina--results of COCORP reflection profiling in the Atlantic Coastal Plain: M Gohn, G.S., ed. , Studies related to the Charleston, South Carolina, earthquake of 1886-tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Report 82-134, p. 15-16. Seismic reflection survey lines in the Charleston-Summerville area showed that the top of the basement has as much as one kilometer of relief. The coastal plain sediments, basalt layer, and basement can all be traced with good continuity over much of the lines; they are cut by a reverse fault and possibly by a small fault-bounded grabe.n, each having an offset of a few tens of meters. Schmidt, R.G., 1962, Aeroradioactivity survey and areal geology of the Savannah River Plant area, South Carolina and Georgia ( ARMS-1) : g Civil Effects Study CEX-58.4.2, Civil Effects Test Operations, U.S. 3 Atomic Energy Commission, 51 p. This outdated aeroradioactivity survey shows no anomalies with regard to the Triassic basin. Schymm, S.A. and Khan, H.R.,1972, Experimental study of channel l patterns: Geological Society of America Bulletin, v. 83, no. 6, p. W 1755-1770. A seris of experiments was performed in a large flume to determine the effect of slope and sediment load on channel patterns. These experiments suggest that landforms may not A-64
always respond progressively to altered conditions. Ra ther , dramatic morphologic changes can occur abruptly when critical erosional and (cr) depositional threshold values are exceeded. Scrudato, R.J., 1969, Kaolin and associated sediments of east-central Georgia: University of North Carolina Ph.D. dissertation, 97 p. Lower Upper Cretaceous clastic sediments of east-central Georgia are characterized by coarse, cross-bedded, kaolinitic sands and gravels and high-quality, commercial, massive kaolin deposits. These deposits extend from Columbia, South Carolina, to the Ocmulgee River of central Georgia. Pollens indicate that major kaolin deposition was not restricted to early Late Cretaceous but also occurred during middle (?) Eocene. Associated pollen and spores indicate that climatic conditions were tropical to subtropical and therefore, probably conducive to extensive laterization of source Piedmont igneous and metamorphic rocks. Clay mineralogy of weathered igneous and metamorphic Piedmont rocks and of lower Upper Cretaceous, middle and upper Eocens, and Quaternary rocks differs significantly. Seismograph Service Corporation,1972, Report on seismorgraph surveys conducted in Barnwell, Aiken, and Allendale Counties, South Carolina, 41 p. The purpoces of this work were to obtain additional seismic information regarding the attitude of the surface and bedrock; to determine the position and outline of the Triassic basin; and to determine the strike of faults suggested as cutting previously established seismic survey lines. I Sever, C.W., 1965, Ground water resources Decatur, and Grady Counties, Georgia: Water-Supply Paper-1809 Q, 30 p. and geology of Seminole, U.S. Geological Survey Seminole, Decatur, and Grady Counties comprise about 1,350 square miles along the Georgia-Florida state line in the
, extreme southwest corner of Georgia. Structural contours drawn on the top of the Suwannee Li .estone, of Oligocene age, show the surface to be downwarped about 540 feet beneath the
, Tifton Upland. This downwarping affected the stratigraphy of l Eocene to Miocene rocks, the quality of their cont.ained water, E and the quantity of water available to wells tapping them. I Sever, C.W., 1966, Miocene structural movements in Thomas County, Georgia: U.S. Geological Survey Professional Paper 550-C,
- p. C12-C16.
( Rocks of Oligocene and Miocene age in Thomas County, in the Coastal Plain Province of southwestern Georgia, are gently fcided and transected by at least one northeast-trending A-65
fault. Maximum displacement along the fault is at least 190 feet and may be somewhat greater. Structural deformation began during Oligocene time, or at least before the Tampa Limestone (early Miocene) was deposited, and continued spasmodically through middle Miocene and possibly through late Miocene time. The trends of the Miocene structures parallel those of late Paleozoic structures in the Appalachian tectonic province of Georgia. The patallel trends suggest that the older Paleozoic structures have in some way controlled the Miocene structures. Sever , C.W. ,1967, Brief summary of the regional area and local geology as related to interpretation of seismology of the proposed site af a nuclear fueled power plant in south-central Georgia (report 2, , second draf t): Unpublished report, 28 p. Continuous cores, electrical resistivity logs, self potential logs and gamma radiation logs from more than 50 drill holes were used to determine the stratigraphy and structure .in the vicinity of the plant site. Sheridan, R.E. ,1974, Conceptual model for the block 'ault origin of the North American Atlantic continental margin gecoyncline: Geology, v. 2, no. 9, p. 465-468. A new interpretation of the basement structure of the Atlantic continental margin is proposed. The basins of the geosyncline are believed to be isolated fault bounded troughs with alignments more or less paralleling that of the continental slope. The apparent stress pattern can be explained by the clockwise rotation of a unit structural block encompassing the entire North American continental margin from Labrador to the Bahamas. Sheriff, R.E. ,1976, Interring stratigraphy from seismic data: Bulletin of the American Association of Petroleum Geologists,
- v. 60, no. 4, p. 528-542.
The conventional application of seismic data to mapping depth and attitude of reflecting interfaces has been supplemented in recent years by measurements of velocity and amplitude for g stratigraphic and lithologic information. Special attention 3 is given to: 1) resolution of events, 2) the measurement and interpretation of seismic velocity, 3) amplitude measurements, and 4) display, so as to help an interpreter grasp the interrelations of data elements. l l Siple, G.E. ,1946, Ground water investigations in South Carolina: l South Carolina Research, Planning and Development Board Bulletin 15, 73 p. Data from municipal water wells or springs was used to study the quality of the ground water of South Carolina. We lls in A-fG ll'
l l l I the coastal plain generally yield larger amounts of water than wells in the piedmont. A brief descriotion of the geology of the piedmont and coastal plain is included. Siple, G.E. ,1960, Piezometric levels in the Cretaceous sand aquifer of the Savannah River basin: Georgia Mineral Newsletter, v. 13, no. 4, p. 163-16 6. Ground water in Cretaceous deposits within 40 miles of Augusta, Georgia occurs under both water table and artesian conditions. Siple, G.E. , 2 967, Geology and ground water of the Savannah River Plant I and vicinity, South Carolina: Paper 1841, 113 p. U.S. Geological Survey Water-Supply The Savannah River Plant area is underlain by a sequence of I unconsolidated Upper Cretaceous, Tertiary, and Quaternary sediments that were deposited on an eroded basement of Precambrian (?) and Paleozoic igneous and metamorphic rocks. I The basement rocks contain a down faulted Triassic basin containing arkosic sandstone and siltstone. The Cretaceous and younger sediments form a wedge ranging in thickness from a few feet on the northwest side of the area to more than 1,200 feet on the southeast side. The principal aquifer beneath the Savannah River Plant I consists of the coarse sand and gravel of the Tuscaloosa and Ellenton Formations. Although the permeable zones in the two formations appear to be separated locally by interbeds of non-water-bearing silt and clay, the permeable zones are hydraulically connected owing to the discontinuity of the silt and clay beds. Consequently, the permeable zones in the two formations are considered to be a single ground water reservoir. The principal aquifer is recharged by leakage through the Tertiary sediments, and discharge occurs in the outcrop area of the Tuscaloosa Formation. Doubtless, water is also discharged from the principal aquifer by moving downdip toward the coast and thence leaking upward through the upper a confining beds. Siple, G.E. ,1969, Salt water encroachment of Tertiary limestones along coastal South Carolina: Sou th Carolina Geologic Notes, v.13, no. 2, p. 51-65. I Limestone of middle Eocene to early Miocene age, and clastic sediments of Paleocene to early Eocene age constitute the
-major water-bearing Tertiary formations along coastal South A-67 I .
Carolina which have been iniaded during recent and past geologic epochs by seawater. Upper zones of Eocene limestones, incised by estuaries during Pleistocene and Recent time, are now subject to salt water encroachment. Encroachment is also thought to occur alony the sub-sea level contact of the Eocene and Oligocene deposits. Smith, D.L. , Gregory, R.G. , and Emhof, J.W. , 1977, Heat flow in the southern Appalachians and southeastern Coastal Plain: Geological Society of America (abs.) , v. 9, no. 2, p. 18 5. Preliminary analyses of geothermal gradient determinations and thermal conductivity measurements from 28 borehole sites in Alabama, Georgia, South Carolina, North Carolina and eastern Tennessee yield new heat flow values which suggest regio.ially characteristic geothermal properties. Characteristic of the southeastern United States, the heat flow data are indicative of a mildly low thermal anomaly with areal variations probably related to major structural features and distributions of radioactivity in the crust. Sm ith , C. W. , III , 1979, Stratigraphy of the Aiken County Coastal Plain, South Carolina: South Carolina Geological Survey Open-File Report 19, 34 p. Six stratigraphic units are mapped in Aiken County: 1) Piedmont undifferentiated, 2) Cretaceous Middendorf Formation (?) , 3) Paleocene to mid-Eocene Huber Formation, 4) late Eocene Barnwell Group, 5) Miocene to pre-early Pleistocene Citronelle Formation, and 6) Plio-Pleistocene (?) to Recent alluvium. Also included is a geologic map. Sm ith , G.W. , III, 1980 Preliminary report on the geology of Lexington County, South Carolina: South Carolina Geological Survey Open-File Report 20, 45 p. Six lithostratigraphic units were mapped in the upper Coastal Plain of Lexington County, the: 1) Huber Formation, 2) Black Mingo Formation, 3) Tobacco Road Sand, 4) Dry Branch Formation, 5) Citronelle(?) Formation, and 6) Pinehurst Formation. Smith, J.W. , Wampler , J.M. and Green, M.A. ,1968, Isotopic dating and metamorphic isograds of the crystalline rocks of Georgia: Georgia Geologic Survey Bulletin 80, p. 121-139. Micas in Georgia crystalline rocks date from about 250 million years on the southeast to 350 million years on the northwest side. The metamorphic isograds indicate one period of metamorphism spanning both the Acadian and Alleghanian orogenies. Granitic intrusion and/or granitization may have occurred during the Taconic orogeny. A-68
Snipes, D.S., 1965, Stratigraphy and sedimentation of the Middendorf Formation between Lynches River, South Carolina and the Ocmulgee River, Georgia: University of North Carolina Ph.D. dissertation, 14 0 p. The outcropping basal Upper Cretaceous bedt between the Lynches River, South Carolina, and the Ocmulgee River, Georgia, are assigned 'to the Middendorf Formation. These beds, which are very similar to strata exposed at the type section of the Middendorf Formation, near Middendorf, South Carolina, previously have been referred to as the Tuscaloosa Formation, but their lithology differs appreciably from typical Tuscaloosa strata exposed near Tuscaloosa, Alabama. I Evidence obtained from studies of sedimentary structures, clay minerals and heavy minerals indicates that the Middendorf clastics were derived from the Piedmont Province. These I studies, together with studies of size analyses and thin sections, indicate that the Middendorf Formation is dominantly fluvial. It was deposited by streams of high viscosity and density on the upper part of river flood plains, which were located immediately south of the Cretaceous Fall Line. Snoke, A.W. , Secor , D.T. , Jr . , and Me tzgar , C.R. , 1977, Batesburg - Edgefield cataclastic zone: A fundamental tectonic boundary in the i South Carolina piedmont: Geological Society of America (abs.),
- v. 9, no. 2, p. 185.
Between Lake Murray, South Carolina, and the Savannah River, the boundary between the Carolina Slate and Kiokee Belts is a steep northwest dipping fault. Structures here such as flattening foliation, associated elongation lineation and intersecting cleavages suggest a polyphase history for the Batesburg - Edgefield cataclastic zone which began during infrastructural upwelling but subsequently evolved into strike-slip faulting. Snoke, A.W. , Kish, S.A. , and Secor, D.T. Jr., 1980, Deformed Hercynian granitic rocks from the Piedmont of South Carolina: American Journal of Science, v. 280, no. 10, p. 1018-1034. I Granitic magmatism, amphibolite facies regional metamorphism, and penetrative deformation provide documentation of a complex late Paleozoic (Hercynian) orogeny, which is widespread in the Kiokee Belt of South Carolina and Georgia. Late stage effects of this orogenic episode include east-west cronulation cleavage and brittle faulting. Movements along thase brittle faults probably began no sooner than Late Cretaceous, perhaps even Permfan, time. Such data substantiate the role of ' compressional tectonics in the evolution of this portion of the southern Appaiachian orogen during the late Paleozoic. I A-69 8
I Staheli, A.C. ,1977, Geologic significance of riverine swamp ' distribution on the Georgia Piedmont: Geological Society of America (abs . ) , v . 9, no. 2 p . 18 6. Numerous swamps occur en the floodplains of major piedmont streams and their tributaries in the southeastern United States. Classification of over 1000 riverine swamps showed g that ninety percent of all piedmont swamps occur southeast of 3 the Brevard Zone in drainage basins of streams that flow normal to regional structures. The greatest concentration of swamps southeast of the Brevard Zone and most of the largest swamps on the Georgia Piedmont are found in an area bounded by: the upper Chattahoochee River basin or Brevard lineament on the north; the lower Chattahoochee River basin on the west; the Savannah River Basin on the east; and the Pine Mountain structure on the south. Stephenson, D.E. , and Pra tt, H.R. ,1981, In_ situ stress field in the southeastern United States and its implication: Southeastern Geology, v. 22, no. 3, p.115-121. In the Coastal Plain of the southeast, h situ stress measurements show the major principal stress component to be in the vertical direction, w'lich indicates normal faulting, g Fault plane solutions for the Coastal Plain indicate both a normal and reverse faulting. The solutions are not well constrained, and the exact mechanism is dif ficult to determine. Recent studies indicate normal faulting in coastal plain sediments near Charleston, South Carolina; however, thrust faulting may be present in the crystalline basement. Stephenson, L.W., 1928a, Major marine transgressions and regressions and structural features of the Gulf Coastal Plain: American Journal of Science, Fifth Series, v. 16, no. 94, p. 281-298. A general discussion of the history of the transgressions and regressions that occurred from Comanchean time through the Quaternary. Stephenson, L.W.,1928b, Structural features of the Atlantic and Gulf Coastal Plain: Geological Society of America Bulletin, v. 39, no. 4, p. 8 87-900. l 3 Discusses the general features and extent of the Atlantic and Gulf Coastal Plains. The structure of the region is summed up I as a gentle monocline including all formations from Cretaceous to Holocene. l Stewart, D.M., Ballard, J.A., and Black, W.W., 1973, A seismic estimate of depth of Triassic Durham Basin, North Carolina: Sou theastern Geology, v. 18, no. 2, p. 93-103. A seismic measurement of depth to bacement was been made near tb: center of the Triassic Durham Basin and indicates that the g , probable depth of sediments at that point is 6,000 + 500 feet, _ g A-70 '
I Stover , C.W. , Reagor , B .G. , Algermissen , S.T. , and Long , L.T. , 1979, l Seismicity map of the State of Georgia: U.S. Geological Survey Miscellaneous Field Studies Map MF-1060, 1 sheet, scale 1:1.000,000. Contains earthquake data originally used in preparing a report on seismic risks in the United States. Intensity values were up dated from new and additional data sources that were not available at the time of the original compilation. I Straley, H.W., III, 1966, Magnetic anomalies and epicentral lines on the South Carolina Coastal Plain: Tectonophysics, v. 3, no. 5,
- p. 3 81.
I The history of magnetic geophysical investigations upon the southern Atlantic Coastal Plain is traced, an incomplete map of part of South Carolina is presented, and a few hypothetical I geological structures or litholigical alignments that may be reflected in the plotted magnetic data are pointed out. Stringfield, V.T., 1966, Artesian water in Tertiary limestone in the I southeastern states: U.S. Geological Survey Professional Paper 517, 226 p. I In Florida, southern Georgia, and adjacent parts of Alabama and South Carolina an artesian aquifer system of Tertiary age is the source of some of the largest ground water supplies in the United States. The aquifer system consists of as many as eight formations, chiefly limestone. The area of the system discussed in this report includes all of Florida and most of the Coastal Plain of Georgia as well as adjacent parts of South Carolina and Alabama. It extends from the Atlantic coast to as far inland as the Fall Line in a few places. I Swift, D.J.P., 1966, The Black Creek-Peedee contact in South Carolina: South Carolina Geologic Notes, v.10, no. 2, p.17-36. The upper Black Creek Formation of Late Cretaceous age in the Peedee River valley, South Carolina, consists mainly of laminated sands and clays deposited in a fluviomarine environment. Lenses of clean sand at the top of the formation are littoral and nearshore sand bodies. The overlying Peedee Formation is a muddy shelf sand. The Pecdee - Black Creek contact is a ravinement or disconformity cut by the transgressing Peedee Sea. Talwani, P. ,197ba, Crustal structure. of South Carolina: Second Technical Report to U.S. Geological Survey, Contract No. 14-08-0001-14553, 79 p. l l This report documents advances made in the study of crustal structure of South Carolina. By monitoring quarry blasts the velocity structure, both underneath the Piedmont and under the l I A-71 l l l
I Coastal Plains has begun to emerge, and the possible < .tstence of a buried sedimentary basin under the Coastal Plains is indicated. Macroscopic and instrumental data were obtained for five earthquakes felt in the state. Both seismic and other geophysical data have helped in the delineation of the Goat Rock fault. Talwani, P. ,1975b, Crustal structure of South Carolina: Semi-Annual Technical Report to U.S. Geological Survey, Contract No. 14-08-001-14 553, 34 p. During the reporting period, quarry blasts were monitored and an aftershock investigation following the August 2, 1974 earthquake on the South Carolina-Georgia border was carried out. This ear thquake was predominantly strike-slip. The fault plane strikes northeast, parallel to the regional geological trend. Talwani, p.,1977, Recent earthquakes in the South Carolina coastal , plains and their tectonic significance: Geological Society of America (abs. ) , v. 9, no. 2, p. 18 9. The Trenton Earthquake of 4/29/76 was probably associated with the contact between the Kiokee Belt and the Belair Belt. Fault plane solution suggests thrust faulting with the southeastern block overthrust. Four events on 9/22-23/76 located near Bowman, may be associated with a postulated buried Triassic basin near Orangeburg. (5 Talwani, P., 1979, Induced seismicity and earthquake prediction studies g in South Carolina: Eighth Technical Report to U.S. Geological g Survey, Contract No. 14-08-0001-14553, 36 p. This report includes induced seismicity studies at Lakes Jocassee and Keowee, and Monticello and Clark Hill reservoirs. It also includes results from earthquake prediction studies at Lake Jocassee and seismic refraction studies in South Carolina. Talwani, P., Amick, D., and Stevenson, D., 1979, Crustal structure studies in South Carolina Coastal Plain: Ninth Technical Report to U.S. Geological Survey, Contract No. 14-08-0001-17670, 81 p. Refraction, gravity and borehole data suggest that the shallow crustal structure in the Charleston area is complicated. The l W northeast-southwest direction of major axis of compressive stress suggests that the tectonic stresses responsible for the g formation of the Cape Fear Arch to the northeast and the g Peninsular Arch to the south are still active. The presence of tensional Mesozoic features in the Charleston area such as basalts and red beds suggests that the present day stresses are being released along preexisting zones of weakness. A-72
Taiwani, P., Rastogi, B.K. , and Stevenson, D. , 1980, Induced seismicity and earthquake prediction studien in South Carolina: Tenth Technical Report to U.S. Geological Survey, Contract No. 14-08-0001-17670, 212 p. This report presents data on duced seismicity studies in South Carolina up to September 1979. The seismicity 1) is shallow (1.25 miles) , 2) spreads in discrete jumps due to the heterogeneous nature of the rocks, 3) spreads along existing joint and fracture planes, 4) is caused by changes in pore pressures at hypocentral depths, and 5) suggests the existence of large horizontal stresses at shallow depths. Talwani, P., Stevenson, D. , Chiang , J. , Sauber , J. , and Amick , D. , 1977, The Josassee Earthquake ; March-May '77) A Progress Report: Fif th Technical Report to U.S. Geological Survey, Contract No. 14-08-0001-14553, 49 p. Between March and May 1977 low level, low magnitude, and shallow seismic activity was recorded in the vicinity of Lake Jocascee. A comparison of water level fluctuations in the lake over a two year period suggests that the observed seismicity may be associated with sustained periods of increase in water level. Tarr, A., 1982, Detection and location capability of the southeastern United States Seismic Network: Southeastern U.S. Seismic Network Bulletin No. 9, p. 36-4 2. Discusses the methods for obtaining the theoretical detection and location capabilities of the southeastern United States Seismic Network. I Tarr, A., Talwani, P., Rhea, S. , Carver , D. , and Amick , D. , 1981, Results of recent South Carolina seit,mological studies: Bulletin of the Seismological Society of America, v. 71, no. 6, p.1883-1902. Results of recent geophysical and geological studies, when combined with the seismological results, indicate two seismic regimes in South Carolina. The first regime covers the buried basement structure of the middle and lower Coastal Plain Province, which has been shown by geophysical studies to be quite unlike Piedmont Province structures to the northwest. The second regime covers the exposed Piedmont Province and the upper coastal plain. Earthquake activity may be associated with strain release on or near mapped faults or contacts between metamorphic belts. Taylor, P.T., Zietz, I. , and Dennis, L.S. ,1968, Geologic implications of aeromagnetic data for the eastern continental margin of the United States: Geophysics, v. 33, no. 5, p. 755-780. Aeromagnetic data suggests that Florida and part of Georgia I were added to the paleocontinent of North America in pre-Paleozoic time. A-73
Thayer, P.A., 1970, Geology of Davis County Triassic Basin, North Carolina: Southeastern Geology, v.11, no. 3, p.187-198. The Davis County Basin is believed to be an outlier of the Dan River Basin. Upper Triassic nonmarine strata within the basin can be divided into two intertonguing facies: 1) basin margin conglomerate, and 2) b,asin center candstone-siltstone. Lithofacies distribution indicates that the basin was filled from the eastern and western sides, and that the sediment was dominantly derived from nearby medium and high rank metamorphic sources. Thayer, P.A. ,1970, Stratigraphy and geology of Dan River Triassic Basin, North Carolina: Sou theastern Geology, v.12, no.1, p.1-31. Dan River basin, a northeast-trending asymretrical fault trough located in Stokes and Rockingham Counties, North Carolina, contains up to 15,000 feet of nonmarine clastic strata (Dan River Group) . On the basis of distinctive sedimentary features and stratigraphic position this thick sequence can be divided into three formations. Environments of deposition include alluvial fan, floodplain, lacustrine and swamp environments. Movements along basin-margin fault zones initiated and accomnanied sedimentation, and erosion of uplif ted fault blocks provided most of the detritus to the subsiding trough. Af ter sedimentation the strata were tilted to the northwest and folded, faulted, an<l intruded by dolerite dikes. Thomas, W. A. , Tull, J.F. , Bearce, D.N. , Russell, G. , and Odom, A.L. , 1979, Geologic synthesis of the southernmost Appalachians, Alabama, and Georgia: in Wones, D.R., ed. , Proceedings on the "Caledonides W in the USA" (I.G.C.P. project 27: Caledonide orogen): Virginia Polytechnic Institute and state university, Department of Geological Sciences, Memoir no. 2, Blacksburg, Virginia, 24061,
- p. 91-9 7.
The Appalachian orogen is within the regional Alabama structural recess between the Tennessee Appalachian structure salient and the Ouachita structural salient. The orogen includes a belt of folded and thrust faulted Paleozoic l sedimentary rocks on the nor thwest, and a belt of Precambrian W and Paleozoic metamorphic rocks. Included are discussions involving the Appalachian fold and thrust belt, the piedmont northwest of the Brevard Zone, and the rocks southeast of the Brevard zone. Thornbury, W.D., 1965, Regional geomorphology of the United States: New York, John Wiley & Sons, Inc., 609 p. Included in the chapter on the Coastal Plain Province are sections on the geology, characteristics and descriptions of geomorphic sections, and geologic history. A-74
I Toulmin, L.D. ,1955, Cenozoic geology of southern Alabama, Florida, and Georgia: Bulletin of the American Association of Petroleum Geologist, v. 39, no. 2, p. 207-235. The outstanding feature of the geology of the Coastal Plain of the southeastern states is the presence of two distinct I sedimentary provinces, one in the northern Gulf Coast area extending basins or embayments of the two provinces are more or less separated structurally by the Peninsular Arch. The provinces are distinct lithologically in that the northern I Gulf Coast Province contains in the Cenozoic section, marine clastic deposits chiefly, with a minor proportion of carbonates, mostly upper Eocene and Oligocene in age. The I Florida Peninsula sediments, on the other hand, consist almost entirely of organic limestones, from the basal clastics of the Lower Cretaceous throughout the section to the Miocene. Miocene and later deposits, however, make up a very small part of the total Cenozoic section. Finally, the two provinces are distinct faunally, as the fauna of the Florida Peninsula is more clo'sely related to that of the Caribbean than it is to that of the northern Gulf Coast Province. Tuohy , M.A. , Gardinier , C.L. , Brown, S.E. , and Karp, H.C. , 19 81, Well I log location maps for the Pliocene to Recent, Miocene, principal artesian, and Cretaceous aquifers: Gecrgia Geologic Survey Hydrologic Atlas 7, 4 sheets. Map covers the Coastal Plain of Georgia'. Four sheets are included (Pliocene-to-Recent, Miocene, principal artesian, and Cretaceous aquifers) . Well location and log type (g eolog ic, I driller 's or lithologic, electric G.S.P. and resistivity, and gamma ray) are shown. Turner, P. A. ,1959, Sedimentation in the Upper Cretaceous of east-central Georgia: -Cornell University, M.S. thesis, 80 p. Upper Cretaceous sediments were derived from the crystalline Piedmont of Georgia. The lower part was transported and deposited rapidly on a flood plain close to the shore line. The upper part of the Upper Cretaceous section was depos',ted I in a lagoonal environment separated from the ocean by barrier beaches that extended approximately east-west through Georgia. Tschudy, R.H., and Patterson, S.H., 1975, Palynological Evidence for Late Cretaceous, Paleocene, and early and middle Eocene ages for strata in the Kaolin Belt, central Georgia: Journal of Research of the U.S. Geological Survey, v. 3, no. 4, p. 433-44 5. Beds assigned to the Tuscaloosa Formation are now known to be at least as old as Late Cretaceous and as young as middle Eocene (Claiborne) . The Tuscaloosa Formation in central Georgia contains strata considerably younger than does the A-75
I formation at the type locality. The beds assigned to this formation in central Georgia contain considerable evidence for what could be called intraformational unconformities, such as channel-fill deposits, lenticular units, and irre1ular and undulating contacts between units of different lithologies. Some of these features may be found to represent stratigraphic breaks that can be recognized throughout the region. Tull, J.F., 1979, Overview of the sequence and timing of deformational events in the southern Appalachians: Evidence from the crystalline rocks North Carolina to Alabama: irl Wones, D.R. , ed. , Proceedings on the "Caledonides in the USA" (I.G.C.P. Project 27: Caledonide orogen): Virginia Polytechnic Institute and State University, g Department of Geological Sciences, Memoir no. 2, Blacksburg, Virg in ia , 240601, p. 167-177. g The purpose of this paper is to examine some of the pertinent l data relating to the timing of southern Appalachian W deformational events affecting crystalline rocks, and to exclude from this discussion stratigraphic and structural relationships which have been documented in the Appalachian Valley and Ridge and Plateau Provinces to the northwest. U.S. Army Corps of Engineers, Charleston District, 1952, Geologic engineering investigations Savannah River Plant: Waterways Experiment Station, Corps of Engineers, U.S. Army, Vicksburg, MS, 45 p. This report presents the results of the geological investigation of the foundation areas of the Savannah River Plant, and an interpretation of the engineering significance of the geological features. The geological work also included the investigation of ground and surface water supplies, drainage conditions, and sources of aggregate for construction. U.S. Army Corps of Engineers, Savannah District, 1980, Navigation charts, Savannah River, Georgia and South Carolina, Savannah to Augusta: Corps of Engineers, U.S. Army Savannah, GA, 57 p. Aerial photography atlas of the Savannah River between Augusta and Savannah. Depths lister used to determine the thalweg of the Savannah River. U.S. Atomic Energy Commission, Division of Materials and Licensing,1970, Allied-Gulf Nuclear Services Barnwell Nu:.iear Fuel u Plant, Docket No. 50-332, 146 p. An evaluation of the geology, hydrology, and seismology of the Barnwell Nuclear Fuel Plant site. I A-76
I U.S. Geological Survey,1976a, Probable recent fault movement in Georg ia: Department of Interior News Release, January 12. I This news release proposed that movement on the Belair fault zone has probably occurred within the last 2,500 years. The sediments dated as less than 2,500 years old, were found to be offset at least three feet. Older strata, between 65 and 100 million years old (Lath Cretaceous age), were found to be of fset 55 feet, which shows that che fault has moved more than once. U.S. Geological Survey, 1976b, Fault movertant in Georgia not as recent as believed: Department of Interior News Release, November 18. Movement along the Belair fault may not have taken place within the last 2,500 years, but has occurred within the past I
~ ,.
50 million years. Radiocarbon dates reported earlier did not give accurate data on the last fault movement. U.S. Geological Survey, 1977, Preliminary report on Belair exploratory trench no.10-76 near Augusta, Georgia: U.S. Geological Survey Open-File Report 77-441, 20 p. Exploratory trench no.10-76 showed several fault planes and shear zones in the vicinity of Augusta, Georgia. There is absence of evidence of fault movement for at least the past 2,000 years, but no direct evidence of fault history over the past 100 million years. No offset, shear or other deformation was observed in the post-Tuscaloosa sediments. U.S. Geological Survey, 1980, Water resources investigations, Georgia District, 1980, 45 p. This report contains a brief description of the water-resource investigations in Georgia in which the Geological Survey participates, and a list of selected references. U.S. Nuclear Regulatory Commission,1973, Seismic and geologic siting criteria for nuclear power plants, Appendix A to 10 CFR 100: Federal Registrar, 38 FR 31279. Geologic and seismic citing criteria for nuclear electric generating stations. Va il, P.R. , and Mitchum, R.M. Jr . ,1978, Global cycles of relative changes of sea level from seismic stratigraphy: American Association of Petroleum Geologists Memoir 29, p. 469-472. The evidence for cycles of relative change of sea level on a global scale, is based on the fact that many regional cycles determined on different continents are simultaneous, and that the relative magnitudes of the changes generally are similar. I A-77
I Because global cycles are records of geotectonic, glacial, and other large-scale processes, they reflect major events of Phanerozoic history. Van Houten, F.B., 1969, Late Triassic Newark Group, north central New Jersey and adjacent Pennsylvania and New York: in Subitz ky, ed. , I Geology of selected areas in New Jersey and eastern Pennsylvania, g Geological Society of America Guidebook of Excursions, Field Trip B No. 4, p. 314-331. The Newark Grcup consists of 16,000-20,000 feet of nonmarine sedimentary rocks and associated intrusive and extrusive basic rocks. Their strike generally parallels the trend of the basin and they dip 10-20*NW. Along the northwestern margin these rocks are bounded by Precambrian and Paleozoic rocks. Most of this boundary is a system of high-angle faults, but intermittently the Triassic deposits overlap on rocks of the upland terrane. Within the basin, Newark strata lie on Paleozoic and subordinate Precambrian rocks of the Blue Ridge and Piedmont Provinces. Along the southeastern margin Newark deposits overlap on Precambrian and Paleozoic rocks of the Piedmont Province. Newark strata, in turn, are overlapped by Cretaceous and younger deposits of the Coastal Plain Province to the southeast. Van Houten, F.B., 1977, Triassic-Liassic deposits of Morocco and eastern North America: Comparison: Bulletin of the American Association of P9troleum Geologists, v. 61, no. 1, p. 79-99. This study examines fault basins that developed on the broad flanks of a central Atlantic arch and focuses on four tectonic l provinces that frame the present North Atlantic Basin, namely, l the African platform and Variscan domain in Morocco, and the southern Alleghenian, and northern, Acadian, domains in g eastern North America. The review involves the record of 5 events from early fragmentation about 215 m.y.B.P., to initial separation and opening of the Mid-Atlantic Rif t about 175 m.y.B.P. Veatch, J.D. , and Stephenson, L.W. , 1911, Preliminary report on the Geology of the Coastal Plain of Georgia: Georgia Geologic Survey Bulletin 26, 466 p. This report contains much of the initial stratigraphic and g structural work done on the Coastal Plain of Georgia. The E Okeefenokee Embayment was originally mapped in this report based on changes in key horizons in the subsurface, but lack of deep well data prevented the establishment of the extent of the basin. " A-78
I Warren, M.A., 1944, Artesian water in southeastern Georgia: Georgia Geological Survey Bulletin 49, 140 p. The rocks of the principal artesian aquifers in southeastern Georgia are limestones of Eocene and Oligocene age. Most of the recharge of these aquifers lies five to 120 miles south and southeast of the Fall Line. The transmitting capability of the aquifers increase in the southern part of the state. Warren, M.A., 1945, Artesian water in southeastern Georgia: Georg ia I Geologic Survey Bulletin 49A, 83 p. Lists data on location, owner , driller , diameter, depth, completion date, and yield of artesian wells in Georgia. Weaver , C.E . , and Beck , K.C. ,1977, Miocene of the S.E. United States: A model for chemical sedimentation in a peri-marine environment: Sedimentary Geology, v. 17, nos. 1 and 2, p. 1-234. Discusses a geochemical model for the deposition of the commercial deposits of clay and phosphate. Weaver, C.E. , and Beck, K.C. ,1982, Environmental implications of I palygorskite (attapulgite) in Miocene of the southeastern United States: h Arden, D.D., Beck, B.F., and Morrow, E., ed., Second Symposium on the Geology of the Southeastern Coastal Plain,
- p. 118-125.
During early Miocene time palygorskite formed in the southeastern United States in shallow, brackish-water coastal lagoons. It altered from montmorillonite by the addition of silicon and magnesium. It formed in a humid, subtropical to tropical climate that was modified by ocean currents controlled by the movement of continental plates. It is unlikely that the palygorskite formed in a normal marine i environment. Wentwor th , C.M. , and Mergner-Keefer , M. , 1981, Reverse faulting along j the eastern seaboard and the potential for large earthquakes: M , Beavers, J.E. , ed. , Earthquakes and Earthquake-Engineering , Eastern U.S., v. 1, p. 109-128. l The origin of earthquakes along the eastern seaboard has long been a problem, as neither active faults or earthquake-related surface faulting has been recognized. The absence of surface deformation in the Quaternary, despite the occurrence of earthquakes as shallow as those expressed at the surface in the west, suggests that the rates of deformation in the east are low. Reverse faults with small Cretaceous and Cenozoic of fsets exist, and earthquake focal-mechanism solutions also show reverse fault geometries. A-79 I
I Wentworth, C.M., and Mergner-Keefer, M., 1982a, Regenerate faults of small Cenozoic offset - probable earthquake sources in the southeastern United States: in Gohn, G.S., ed., Studies related to the Charleston, South Carolins earthquake of 1886 - tectonics and seismicity (collected abstracts): U.S. Geological Survey Open-File Report 82-134, p. 34-35. The principal style of Cenozoic faults and earthquake l 5 focal-mechanism solutions known along the eastern seaboard suggests that a domain undergoing northwest-southeast compression extends along the eastern seaboard between the continental margin and the front of the Appalachian Mountains. In the southeast, several mapped no-theast-trending zones of high-angle reverse faults and many faults in isolated exposures of fset coastal plain deposits as much as 325 feet; the youngest recognized offset is one foot in probable Pliocene or Pleistocene surficial gravels in the Staf ford fault zone in Virginia. The extent of the domain is inferred from 1) reverse faults known in South Carolina and along the Fall Line from Georgia to New Jersey, 2) earthquake source mechanisms, particularly in coastal New England, and 3) the broad distribution of early Mesozoic normal faults in the exposed piedmont terrain and beneath the coastal plain and of fshore. The authors suggest = that, to a large extent, the reverse faults reuse parts of these early Mesozoic faults. Wentworth, C.M., and Mergner-Keefer, M., 1982b, Regenerate faults of small Cenozoic offset as probable earthquake sources in the southeastern United States: U.S. Geological Survey Professional Paper 1313, in press. An analogy is made between the western foothills of the Sierra Nevada and the Piedmont, to reinforce parts of the reverse fault hypothesis. The analogy is made given the lithologic similarity between the two regions. Of fsets in the younger
- rocks of the Sierra foothills indicate that normal faulting i
along pre-existing faults has been underway since the Miocene, but has accumulated relatively small of fsets. The foothills example suggests that much more evidence of Cenozoic faulting may be found in the scattered surficial deposits in the piedmont. Of the alternative sources of earthquakes that have been proposed, the Appalachian decollement has the most direct relation to the reverse-fault hypothesis. Although there is no geologic evidence that such a decollement has moved at all since the Paleozoic, some of the early Mesozoic extension could have reused such a decollement as a sole, and the reverse faulting might be a shallow expression of more recent decollement movement in a compressional regime. A-80 I
A I White, W.A., 1952, Post-Cretaceous faults in Virginia and North Carolina: Geological Society of America Lulletin, v. 63, no. 7,
- p. 745-748.
At several localities in Virginia and North Carolina faults of small displacement cut young fluvial gravels. Some of these faults are normal; others are reverse. Whitney, J. A. , Paris, T. A. , Carpenter, R.H. , and Hartley, M.E. III, 1978, volcanic evolution of the southern slate belt of Georgia and South Carolina: A primitive oceanic island arc: Journal of Geology, v. 86, no. 2, p. 173-192. The Carolina Slate Belt is recognized as a major metavolcanic tectonic province of the southern Appalachians. The lower stratigraphic sequence is composed of "metadacite." These are overlain by a sequence of tuffs which grade vertically into I argillites. The petrographic suite is similar to that found in primitive island arcs. Modern day analogs suggest a model for the slate belt during this volcanic phase in which the primitive island arc formed separated from a continent by a marginal basin. Wigley, P.B. , ed. ,1981, Latest thinking on the stratigraphy of selected areas in Georgia: Georgia Geologic Survey Information Circular 54-A, 67 p. This report consists of three papers which provide interpretations regarding the stratigraphy of selected areas in the Blue Ridge and Piedmont of Georgia and adjacent parts I of Alabama. Two features which are especially significant about all three of these reports are: 1) they present stratigraphic interpretations ir structurally complex areas where multiple deformation plays an important role in the orientation of stratigraphic sequences, and 2) there is movement away from the old " belt" concept first introduced in Georgia by G.W. Crickmay in 1952. Winker, C.D., and Howard, J.D., 1977, Correlation of tectonically deformed shorelines on the southern Atlantic Coastal Plaint Geology, v. 5, no. 2, p.123-137. Warping of the Atlantic Coastal Plain has continued through I the Pleistocene following previously established Cenozoic structural features. These results are based on the maximum transgression of sea level. Woolard, G.P., 1955, Preliminary report on seismic investigation in Tif t and Atkinson Counties, Georgia: Georgia Mineral Newsletter,
- v. 8, no. 2, p. 6 7-7 7.
Reflection and refraction studies were carried r at in Tif t and Atkinson Counties, Georgia. At the time of publication the results of the studies were still being tabulated. A-81 )
I Yor k , J.E . , and Oliver , J .E . , 1976, Cretaceous and Cenozoic faulting in eastern North America: Geological Society of America Bulletin,
- v. 87, no. 8, p. 110 5-1114.
Cretaceous and Cenozoic faults in eastern North America provide evidence of modest intraplate tectonic activity in this region. Gravity and thrust faults with inconsistent trends are present, thus indicating that stresses that vary spatially and (or) temporally rather than a single stress field acting steadily throughout the entire North American plate, are responsible for causing this intraplate tectonic = activity. Strike-slip, movement is not demonstrable, but could have occurred in some places. Zen, E.A., 1981, An alternative model for the development of the allochthonous southern Appalachian piedmont: American Journal of Science, v. 281, no. 9, p.1153-1163. The recent COCORP deep seismic profile revealed that a clearly recognizable though possibly composite seismic horizon, interpreted as a structural discontinuity in the rocks, exists in the crust underlying this transect at least as far east as the Kings Mountain Belt. It is proposed that both the rocks are allochthonous by overthrusting, and the rocks east of it, for which the seismic evidence for discontinuity is weaker, may be parts of an aggregated terrain consisting of microplates. Zietz, I., and Gilbert, F.P. ,1980, Aeromagnetic map of part of the southeastern United States: In color: U.S. Geological Survey Geophysical Investigations Map GP-936, 1 sheet, scale 1:2,000,000. E W Aeromagnetic map covering the Atlantic Coastal Plain and Piedmont from northern Florida to southern Pennsylvannia. Map is based on Aeromagnetic surveys conducted between 1965 and 1979. Dunbarton Triassic Basin appears on this map. Zimmerman, E.A., 1977, Ground water resources of Colquitt County, Geor g ia: U.S. Geological Survey Open-File Report 77-56, 41 p. The principal artesian aquifer is made up of limestone beds of Eocene, Oligocene and lower Miocene age. The Swannee Strait traverses Colquitt County from near the southwest corner to the northeast corner. In this strait, limestone in the principal artesian aquifer is partly replaced by fine-grained clastic sediment, impairing transmissivity and making wells hard to construct. The transmissivity is much lower northwest of the strait than it is coutheast, probably because of tacles changes in the aquifer. The clastic beds of Miocene age are of little importance in the ground water picture because g larger yields can be obtained from the underlying principal g artesian aquifer. A-82 I I
I I Zoback, M.D.; Healy, J.H.; Roller, J.C.; Gohn, G.S.; and Higgins, B.B., 1978, Normal faulting and h situ stress in the South Carolina Coastal Plain near Charleston: Geology, v. 6, no. 3, p. 147-152. Evidence presented suggests that normal faults in coastal plain sediments near Charleston, South Carolina are currently active. Hydraulic fracture studies were carried out in I Clubhouse Crossroads wells #2 and #3 which are located on the edge of the Charleston meizoseismal zone. The magnitude of the least-principal stress in coastal plain sediments in the I Clubhouse Crossroads wells is significantly less than the overburden stress. Incipient normal faulting might occur if the difference between these stresses were large enough. Such a fault would strike northwest-southeast and dip about 60'. Zoback , M.L. , and Zoback , M. , 1980, State of stress in the conterminous United States: Journal of Geophysical Research, v. 85, no. Bll,
- p. 6113-6156.
Northwest-southeast to west-nor thwest-east-southeast compression characterizes the Atlantic Coast stress province, which includes the Atlantic Coastal Plain, the Piedmont Province of the southern Appalachians, and the entire Appalachian fold belt in the northeast. Earthquakes in the Atlantic Coast Province of ten have components of both thrust and strike-slip motion. Such oblique motion is expected because the earthquakes seem to occur on favorably oriented preexisting structures. For modern earthquakes associated with northeast striking normal faults which bound Triassic basins, the current sense of motion on the fault (reverse) is exactly opposite to the motion that created the faults. I I I I I A-83 I
--_a - -
4 4 I l I I l APPENDIX B OBSERVATION HELL LOGS l I
, I
l APPBNDIX B The following logs show the well construction for holes drilled as part of this study. A description of the observation well installation is in Section 6.4. i i I '
O PROJE CT WE LL NO I OBSERVATION WELL JOS NO 9510
$s TE Postulated Millett Fault V0GTLR ELECTRIC GENER m NG PIANT
.X) ORDINATE $
N 1120358.26 E 660009.14 VG-1 3E(,gpe COMPL E TE D PAEPARED tv REFEREN(f POtN1 f On ME ASUREMENTS 5/16/82 5/26/82 Ron Wood (GPC) Top of Surface Casing 4 Steel Posts DEPTH ELEV.
& Locking ELEV. - TOP OF SURF ACE CAStNG:
157.6 4 Steel
,IPlate Concrete Slab . .. . .
'd,.j.y --
) f. - . . ELEV. -TOP DF RISER CA$ LNG:
GENE R All2ED GEOLOGIC LL'G ,f;' f,h' y GROUND SUR F ACE *O 156.6 reb KAx4f * ~ ' ,
,,.e in gy m f.A;'
r, 4 g. I ? e
; ./
(y aa. aa
. (s hi d'
I 'oiA. 6" TYPE- Carbon Steel
$URF ace CASING y - r d '* =' ;2 2*0 154*6
#8 4 f
' E f: BOTTOM OF SURF ACE CASING ; - _ - -_ _ . _
4 a aa aa BACKFILL MATE RIAL TYPE. Cement Grout F. (Placed Through 1" $ Tremie) E E
',' ~ 6" O Hole aa s* RISE R CASING s a aa
=- oiA- 2"
,. ,', TYPE: Carbon Steel e
' TOP OF SE AL h17.3-439 2 ' . 'J h25.0 -268.h Sand *
*~
( 1/h" Steel Plate 3" 6 ( - - - ---- (Welded to Riser Casing) 439.2-h58.5 Clay FILTE R PACK h58.5-512.0 TYPE: Caved Sand Interbedded Sand / Clay -+-- T0P 08 SCRE EN 507.0 -350.4 SCREEN. Continuous Slot oiA 2" TYPE: Stainless Steel i
-- OPENINGS. WIDTH. O,Q20 r TYPE Johnson Manf. Well Point Screen ,
- BOTTOM OF SCREEN :
512.0 -355.4 - V- : 7\<
,, Top of Cement Grout ' 512.0 -355.k BOTTOM OF HOLE :
565.0 -h08.h l
---, r HOtEoiA _3" d l 1
O PR OJE CT et LL No V0GTLE ELECTRIC GENERATING PLANT VG-2 OBSERVATION WELL .K)NO sate COORDeN AT E S 9510 Postulated Millett Fault N 1122608.99 E 650596.85 GEGUN COedPL &TED PREPARED BY REF E REosCE POINT FOR WEASUREMENT5 5/14/845/20/82 E. Vanek Top of Surface Casing y Steel Posts DEPTH ELEV Locking 253.8 { y Steel -ELEV. - TOP OF SURF ACE CASING: k
,f Plate 2 2 ~ N.A.
Concrete Slab % ., ,4
.. z gi, 49: -ELEV. - TOP OF RISE R CASING:
g GENE R All2EO GE OLOCsC ax m LNs*1**
~
j r i e'
"s w a-y GROUNO SURF Act 0 253.1 y# ,. .- .
e .g ..
/ ',' f SURF ACE CASING
* =
=
., o,A. 6" H,
* 's o
- i TvrE : Carbon Steel e r 6
* ' :L
=; BOTTOM OF SURF ACE CASING 2 3.0 250.1 3 e e.
4 4 ea .. 8ACKFILL MATE RIAL
. . . TYPE: Cement Orout
. .F (Placed Through 1" 6 Tremie)
" 6" O E
** RISE R CASING e a ea e* DIA 2"
- e. .. TYPE CarDon Steel s e ea a ..
** e TOP OF SE AL ANNULARSEAL _5_5_3.{ -2_99._9 TveE- 1/h" Steel Plate 3" 6 (Welded to Riser Casing)
FILTE R PACK 52h.0-610.0 MPE: Caved Sand 4-- Clayey Sand 610.0-620.0 - 6 61ji .C --3 ~1.9~ E Sand SCREEN Continuous Slot h D'A- 2" TYPE Stainless Steel OPENINGS wioTH 0.020 1 TvrE Johnson Manf. Well Point Screen 1 - 80TTOM OF SCRE EN : Y1
- BOTTOM OF SUMP W W
< HOLE DIA 3" 6 I
O PROJECT vrE L L NO OBSERVATION WELL V0GTLE ELECTRIC GENERATING PLANT VG-3 JOc ho $s t & COORDies AT E s 9510 Postulated Millett Fault N 1121183.52 E 655725.83 SEGvh Coup 6 4itD Pageanto tv ngpgat**CE POikT FOm adE AsumEMEN15 5/15/82 5/17/& E. M. Fanelli Top of Surface Casing p Steel Posts DEPTH E Li v. I Concrete Slab % p, ,,.;. ,, , ge J Plate - c 8
- tLtv. - Tor or SURF ACE "A5i.dC:
p e..: , tLav.-Toe or RistR CASING: IbI*1
-- 165*7 j ,,.,,..,
GENE R AU2E D GE OLOC'C IG- ,44,k y GROUND st,R r ACE O 165.7
- a. an .;;. z
-y ,- mwm ~~~ ~~~~
p' g P.' .. g. I y, f sums Act casing q , ,
/ j. ..
9 oir; 6" 6 , a * >j
; ;1 **,
, TYPE: Carbon Steel U
U: seriou er suRrAct Casing : 10 162._] 4 .
.. .. eACKilLL MAT E 814 AL
.. . . TvPE: Cement Grout
. P (Placed Through 1" 6 Tremie)
I 88 a 88 H pl5E R CA$1NG h63.0-529 9 '
- o'A. 2" Clay " , :'
. ., Tver: Carbon Steel s ..
** e top or SE AL 529 9-541.8 $ 'ZL / ^~~u'^aSt^' h_hlhh3gL h_
Sand I Tves. 1/h" Steel Plate 3" O (Welded to Riser Casing) 5hl.8-563.0 ,,,,,,,,c, Clay Tvrt: Caved Sand 563 0-57h.3 Sand , 533.'i-368.0
.- Toe or seRrra. :
T SC"""-Continuous Slot 57h.3-57h.1 E - o,A: 2" Tver. Stainless Steel Clay I I C h OPENINGS WIDTH 0.020 vver Johnson Manf. Well Point Screen soTToM oF SCREEN - 539.0 -373.3 soTTow or suu, . 57h.9 -h09.2
=.--3m
< HOLE DIA 3" 0 I
O rRe,Ec, E m .e OBSERVATION WELL l V0GTLE ELECTRIC GEIERATING PLART VG-4 Joe No Sa T E COOROs%ATES 9510 Postulated Millett Fault N 1124629.k1 E 6hh971.51 SECUN COMPL E T E D PREPAR10sv Rif kREh0E POthi FOR WE ASUREWENTS 5 / 2 7 / 82 5/31/82 Thackaberry/ Crosby Center of Pressure Gauge in DEPTH ELEV. s Elev. - Pressure Gauge 153.56 Locking Plate - N E LEV. - TOP OF RISE R CASING : 153.20 CENE RAL'ZE o GEOLOGIC LCG p - _ y GROUND SURF ACE O 150.2d w wwa , 6;>.,9 m ,e fj,: w as UK' m "s t l ' , ' w. 5y b .* "
$b SURF ACE CASING s
y , o,A. 6"
, g',
.. .. ;/j TYPE: Carbon Steel n' . .
e s : BOTTOM OF SURF ACE CASih;G 2
- s. ..
4 a
.. sa BACKFILL MATE RIAL TYPE: Cement Grout Y--
(Placed Through 1" @ Tremie) s . sa ss
. . 6" 4a s. g,$g g 4A$gNg
.. oia 2" $
.. .. TYPE- Carbon Steel a .
TOPOFStAL ANNULAR SE AL _h Sj-2_9h_.y h29 0-459 0 TvrE: 1/h" Steel Plate 3" O Clayey Sand (Welded to Riser Casing) 459 0-47h.6 FiLTE R PACx Clayey Silt TvPE: Caved Sand l - b7h.0-504.0 Ul*7 530.C-379.71 504.0-513.0 #
- E- '
} Sand SC"E** Continuous Slot E o,A 2" I.D. Type Stainless Steel 513.0-524.0 Sandy Clay i +-- OPENINGS wioTH 0.020 T yrf . .Iohnson Manf. Well Point Screen 52h.0-570.0 --- BOTTOM OF SCREEN 535.0. 38h.7.h Sand
~
i _=- k7 Top of Cement SJ11 - _38h . 8h BOTTOM OF HOLE t .
.m ,
8., y g h" 0
i l @ ! wtLL NO OBSERVATION WELL i l PROJECT v00rts stzCra1C czuzairtua Ptrur vo_s Joe NO saia CoonoNATES 9510 etGvh Postulated COMP L if t0 Millett Fault. PREPAREDSv N 1116669.12 E_665818.68 ! RE Ft AENCl POeNY FOR WE A5umEMENT E j 5/13/82 6/15/82 R. J. Kelleher Center of Pressure Gauce en OEPTH E LE V.
*** ~ #* *#* ""8 I
Locking Plate -\kN _ ELEv. - TOP OF riser CASING : 96.9 cENE RAUMO GEOLOGIC LOG p - - y GROUNO SURF ACE O 94.5 m ww ww gy. =
* .o;,: amwm "a ', '"
- w. 5:?
1' l'l ,a , a' ' surf ACE CAs NG s u h
.. s
. g ,
0,A- 6"
.. .. g TvPE- Carbon Steel p{
P
,. ,. 2.1 92.h O a a
- 8OTTOM OF SURF ACE CASING 1 se ae 4 a I
ea .. B ACKFILL MATERIAL 112.0-186.8 , . . . TYPE: Cement Grout Calcareous Siltstone . I (Placed Through 1" @ tremie) (Marl) ',' , se sa 3 4 aa a* RISE R CA$iNG I 186.8-202.0 Fossiliferous Limestone D'A TYPE: 2" Carbon Steel 8 4 4 0 TOPOFSEAL
- A%~utAR sE AL 120.0 - 25.5 I 202.0-232.0 Foss. Calcareous Sand TvPE-1/h" Steel Plate h" @
(Welded to Riser Casing)
" ' " ^ '
- 232.0-282.0 Non-Cale. Sand Tv"I Caved Sand l -
TOP OF SCREEN :
=
-;_ SCREEN Continuous Slot OiA- 2" TYPE. Stainless Steel
~_*"<W OPENINGS MOTH: 0.020
,{ Tv >E Johnson Manf'. Well Point Screen 2h2.0 -147.5 7 BOTTOM OF SCREE N
{,[ f Top of Cement 2bDE307.5_
'. soTTOu CF wOtE ; SDL Q: M .S.
I a,, e e, Sy e ,, y t 3" 0
O PROJE CT l WE L L NO OBSERVATION WELL V0GTLE ELECTRIC GENERATING PLANT VG-6 c ho SITE COORDsNATE$ 9510 Postulated Millett Fault N 1110896.34 E669643.15 SEGuN COMPLETED PAEPARED BY RE FE AENCE POINT FOR WE ASUREWENT$ 6/11/826/12/82 Robert J. Kelleher Top of Surface Casing b Steel Posts y DEPTH ELEV c ng f ELEv. - TOP OF SURF ACE CASING: g Concrete Slab IPlate /l 14 -. ELEV. -TOP OF RISER CASING: GENERAltZEO GEOLOGIC mag [O'G
*;s T/tk)
A.'.s, .,s m w a. y GROUND SURF ACE - 217,1
; V- ~ is; .
's ! 1, <. g
# d' A~ SURF ACE CASING D .[=
i.
- p.
z, DIA: h" (
,.7 ... .- TYPE. Carbon Steel w
4 . , 2 6
=*
8 Ii 2 : 17 215.4 80TTOM OF SURFACE CASING 1
- . ea 4 a
.. .. BACKFILL MATERIAL TYPE Cement Grout
. .I"'"- (Placed Through 1" D Tremie) s a aa
. 'l
- ea 6" O Hole RISE R CASING A 8 a -
a
- OIA 2"
.. .. T 6 tCarbon Steel ss TOP OF SE AL 237 5-328.2 A b) 1/4,, Steel Plate 3,, 0 ( 2h2.0 - 2h.9 Calcareous Siltstone L (Welded to Riser Casing)
(Marl) 328.2-3h0 5 Fossiliferous Limestone .e--- TvPE: Caved Sand 3h 0. 5-388. 3 422.0 404.9 Fossiliferous Sandstone -
**""" ~~~ ~ ~ - ~
{ SCREEN Continuous Slot Q o'^ 2" TvPE: Stainless Stee2 388.3-h28.0 Z o,E N,NGS ,,ot H 0.020 Non-Calcareous Sand 1 TvPE- Johnson Manf. Well Point Screen b 80TTOM OF SCRE E N : *
- Top of Cement Grout -
D E.SO9*9-8 8 BOTTOM OF HOLE 1 b O-
====-p 7 HOLE OIA
O ag g ,,o OBSERVATlDN WELL ; {PmOJtC1 v0GTLE ELECTRIC GENERATING PLANT VG-7 Jut NO la t t COORDehafts 9510 Postulated Millett Fault N 11272h5.60 E 640322.37 etGvh COMP L IftD PAIPAAf D tv at f a mise C4 POINT FOn ut A$uatutNis 5/25/82 6/25/82 S. Balone Top of Surface Casing
% Steel Posts otrTs totv
} Locking
! Steel F lev. -TOP OF surf ACE CAstNG:_ 251 * ~'
Concrete Slab , ' Plate h ).4 ;y;p M " i 4.<-
,,}, ELEV.-TOP OF riser CAslNG:
251.1 GENE RAll2Eo GEOLOGIC L O'G ;* (k. ua rear y GROUNo SURF ACE O 250.6 w u# s~ x' _ _ f r. ** d' g
/ , f- suRe Act cAsmG d IA a* .e $ OtA: fu
*- , . . gi a *
=.as
,o TvPE Carbon Steel I l W ','
4 8 h E: a BOTTOM OF surf ACE CAstNG 6.0 2h5.1 ae ea BACKFILL MATE Ri A6 TvrE: Cement Grout
. (Placed With 1" % Tremie)
' , '~ 6" Hole a' '
Rise R cAsmG
o'^-
211.6-225 0 ' 2" Clayey Silt ,, ,', TveE Carbon Steel 225 0-282.7 . Caleareous Siltatone ,', TO,0, se At p j (Marl) 36.6 g (_21h .0 1 1/h" Steel Plate 282.7-286.) Fossil Shells 286.5-372.0 Sand VVPE' Caved Sand
.~
372.0-392.0 Clay 357.5 -106.9
,,,,,,c,,
{
~
sCRet* Continuous Slot o'A 2" TYPE Stainless Steel
= -
=
9 I r octNiNGs wioTs 0.020 tver Johnson Manf. Well Point Screen BOTTOM O5 sCRE EN : 3b2[,-111 2
- Top of Cement Grout s 363.c -112.4
' ,', BOTTOM O8 HOLE : 392 -31.A
'L W f MOLE OIA 3" N
O .E m e l i P.mE C, OBSERVATION WELL l V0GTLE ELECTRIC GENERATING PLANT VG-8 Jos NO $416 COOADINATES 9510 Postulated Millett Fault N 110hhh6.34 E 6787hh.09 begun COMPL E TE D PREPARED 87 REFERENCE Poih1 FOR ME A&vREMENT5 6/Eh/82 6/25/82 S. Balone Center of Pressure Gauge 3 DEPTH ELEY-Locking Plate - g ev. - ressee Ga w 107.6
+ 3.9 107.6
- ELEV.-TOP OF RISER CASING:
GENE R All2ED GEOLOGIC LOGp - ~ p- GROUND SURF ACE O 103.7 euww,p .
.. .c w un w uw
. : - ,, . y
* 8 SURF ACE CASING a{* *. ...* ~
o,A. 6" 6
$ ** **,, s
, W M TYPE: Carbon Steel
, ?, , . ,
1.. .. , 2.1 101.6 L a 8 L : 80TTOM OF SURF ACE CASING = se er ie .a BACKFILL MATERIAL
. , . TYPE: Cement Grout
. F (Placed Through 1" @ Tremie) 1h3.6-222.2 Calcareous Siltstone '[ '.' 6" O Hole (Marl) *'
',' a'5E a CA5'NG 0
.. DiA. 2" 222.2-2h0.1 '
TYPE. Carbon Steel Limestone , , 2h0.1-285.2 '.' '.' ' Interbedded Sand ad ANNULAR $t At 147.C
- 43.3 and Limestone -
,b TvrE: 1/h" Steel Plate 3" 6 (Welded to Riser Casing) 285 2-335.0 Sand F,LTE R PACK TYPE: Caved Sand l-
. TOP OF SCREEN :
I:- SCREEN Continuous Slot 335.0-336.h ,,,. 2" TYPE Stainless Steel Limestone -
=
336.h-355.h
-T 5 PENINGS unDTH 0.020 TvrE. Johnson Manf. Well Point Screen Clay 312.0-208.3
'5 soTTou oF SCREEN :
--# [
M, - Top of Cement i 312.0-208.3 f 5 soTTou or Hott : 3.3U-2)11 - 4 4 8 8 g
'8e a 8, y 1; 3" 0 1
I & ~ wtLL NO I OBSERVATION WELL lPROJEC1 JOS feO 9510
$411 Postulated Millett Fault j V0GTLE ELECTRIC GENERATING PLANT COOADINAf t$
N 1134867 0h E 679h23.1 VSC-1 I 6tGuN COMPLiftD PREPAmtD tv REFlathCE POINT FOR utasvainsimig 6/lk/82 6/17/82 K. Wornick Top of Surface Casing DEPTH ELEV. ELEV.-TOP OF SURF ACE CASING: 220.p5 Locking Screw Cap w L'.;' E ELEV.-TOP OF RISER CASING: 220.95
% 0 219.0 cENE R AUZED GEOLOGIC LOG w ma .a g
( 9
-f{ . y,emwm
- p. GROUND SURF ACE
.. g: '
h t a1;j ' , ' ",']
- surf ACE CASING
- - > oiA 6"
* ) - a
, ,j ea a a pj TYPE: Carbon Steel
' s a 3
sj '- a h. 30 216.0 6 a 8 L: BOTTOu OF SURF ACE CA$iNG 1 _ ss 4 a , aa . . BACKFILL uATE RI AL s s TYPE. Cement Grout I (Placed Through 1" O Tremie) a a sa sa a a
~
** ** RISE R CASING 106.8-186.5 *
- oiA- h" I.D.
Fossiliferous Calc. ,', ,' . TYPE: PVC Sandstone /Foss. . . Limestone ',* '= 186.5-267.2 ,", .'., 186.0 33.c Calcareous Siltstone - - (Marl) '
] TDP OF FILTER PACK f
FILTER PACK T"E : Caved Sand 267 2-366.h ,__ Fossiliferous Calc. Sand
- TOP oF SCREEN : 3M.0 -126.C
{ SCREEN Continuous Slot 366.h-423.4 I o'^ h" I.D. TYPE PVC Sandy Clayey 5_ - I Siltstone h OPENINGS' WIDTH TYPE 0.015 soTTou oFsCREEN : 350.C-131.0 ,
- 4 2.0' Ball Valve (Down Pump Only) 366.C -lh7.C
.U. Top of Grout
. . soiTou oF woLE NOdJE6aC w
.-: -: :/ .
woLE oiA 6.5" 6
@ we gg no l
PMOJE C T OBSERVATION WELL v0crtz stscra1C cenzairino Ptinr vSC-2 JCO NO Sa TE COOADINATES 9510 Postulated M!.11ett Fault N 11h1512.71 E 67349.62 SEGuh COMPLETED PAEPAREOev af f E8ENCE POihi FOR ME ASUREME NTE 6/1h/&6/lk/82 K. Wornick/(R. Wood Top of Surface Casing E Steel Posts" l OEPTH ELEV. 1 Locking i
-.ELEV. - TOP OF SURF ACE CASING:
202.6
! Steel l Plat,e /!
Concrete Slab - 202 6
,4,',$ f'
- I.'.. E LE V. - TOP OF RISE R CASING :
ya a: 6.s: . . GENERALIZED GEOLOGIC 8 y GROUND SURF ACE O 201.7 was LO'G ';9, *. ' 3.s . .s.'ha.s se u. - - - - ---- [i { [ k' [ (* , 'f SURFACE CASING
,r,# g .e s- "
e. a DIA: b" H .. .. W,: TYPE: Carbon Steel
- yh
]s' *= '
6
- M
-f 2.1 199.6 BOTTOM OF SLRF ACE CASING 1 =
,e ae 4 a aa a a BACKF ILL MATE RI AL Geology based on ,', '
,'.- TYPE: Cement Grout Georgia Power Comp. .
(Placed Through 1" $ Tremie) Boring Log == == r s n
'l ~
6" 0 Hole RISE R CASING a* DIA 2"
.. .. TYPE. Carbon Steel a
TOP OF SE AL 152.0-256.5 Calcareous Siltstone E' ' , .,;:) 1/ho Steel Plate 3,, 0 (160.0 bl.7 (Marl) (Welded to Riser Casing) 256.5-316.0 ""' Sand TYPE- Caved Sand 316.0-362.8 Clay TOP OF SCREEN : 310.0 -108.3 L SCREEN Continuous Slot 6 *-- OiA 2" I.D. TYPE: Stainless Steel r OPENINGS. wioTH 0.020 7 TYPE Johnson Manf. Well Point Screen
; sOTTOu Os SCREEN : 315_.0 _-113; 3_
',', Top of Cement Grout 3.lL.0 -115_.,3_
' ,', BOTTOM OF HOLE 1 600.,1MQ1
-.L
- HOLE DIA 3" 0
i O , oxc1 jeto I ' OBSERVATION WELL Jos NO 9510 sit E Postulated Millett Fault V0GTLE ELECTRIC GENERATING PLANT COORDINAT E1 N 1138356.8h E 67625h.55 i VSC-3 I
#EGUN COMPL E TE D PREPAREDSV REfiRENCE POINT FOR ML AsuntutN11 6/29/82,6/30/@ Ron Wood (GPC)
~
Top of Surface Cat:ing y Steel Posts y DEPTH E LE V. g Locking i 166*7 I Concrete Slab w .,.a.. g o Steel
,f Plat,e
, /l n/e l-ELEV. - TOP OF SURF ACE CASINC:
166.6 4 ,.g 6 , , , , , ,
, ELEV. - TOP OF RISE R CASING :
GE NE R ALIZED GEOLOC'C L(k.s
- 1 8 k.'
, y GROUND SURF ACE O 165.7 mm '~ ; ~s w a.
_x .,.-.
) <
SURF ACE CAS4NG s
.. .. g. o,A. 6"
. . g,
; p *,'
TYPE: Carbon Steel i .. .. ? U
- U
* : BOTTOM OF SURF ACE CASING 1 -
4 a
.. .. BACKFILL MATE RIA.,
I .. a .F TYPE; Cement Grout (Placed Through 1" 6 Tremie) I s . 6" $ Hole
*' ** RISE R CASING
** DIA. 2"
[. .. TYPE: Carbon Steel TOP DF SE AL ANNULAR SE AL (_32.5.0,-159 3 TYPE- 1/k" Si, eel Plate 3" @ (Welded to Riser Casing)
"'""'^C" 318.0-338.0 Clay TYPE: Caved Sand 4--
338.0-560.0 "7 "" "" __ 6 TOP OF SCRE EN ! 565.C-399.3 . ! 560.0-570.0 E SC" " Sand -- . Continuous Slot oiA: 2" TYFE: Stainless Steel e
=
I . 1 a OPENINGS WIDTH- 0.020 TYPE Johnson Manf. Well Point Screen eOTTOM OF SCREEN -
* ~
- sOTTOu OF Suur - 578.C -h12.3
.y. .
< HOLE DIA 3" 0 I
O l OBSERVATION WELL v00Ttt lPAOJECT tttCTarC ornzRAT1xo PtanT ECThi JOa NO sit t coonD8 NATES 9510 Postulated Millett Fault N 1130601.87 t 683297.22 SEGum COs**t E T E D PetranED 87 mEFEaENCE PosNT Fon uf ASumEutNTS Center of Pressure cauge 7/21/82 7/28/82 R. J. Kelleher DEPTM ELEV Pressure Gauge [- Steel Post Relief Valve _ 158.0 _f ELEv.-top or riser CASING: GENE RAL12Eo GEOLOGIC log y GROUND sVRF ACE O 156.7 m aw.ia., g r,.; ;,,. g
.. . ya m ua
~
' .w h '
'=:) '
8 8 surf ACE CASING r
,i ', ,': ./ 3 s : , O. ' ,a
.k' oiA: Surface shelter vill be built
.' ; .. b TvPE. by land ovner.
'*'s'. *'
a y'j ,
? E,
- a 's j
'* 8 L '
soTTOM OF SURF ACE CAstNG 1 -- --- g se ae 4 m aa aa eACKFILL MATERI AL a s
.. TYPE: Cement Grout
= ,I."'- (Placed through 1" 0 Tremie)
B B 30 88 s a
"' Rise h CASING na ** DIA h" E 271.9-323.6 -
TYPE: PVC Sch. 80 g Non-Calcareous Sand , , E 8
- 360.0 203.3 323.6-378.6 .: ____ _ _ _ _
Clay ;. yopo,,,tyg,,,cx FILTE R PACK TYPE: Fine Aggregate Sand for
+- Concrete Placed Through 1" $
378.6-h90.0 Sand Tremie l 465.0 -308.3
= s top OF SCREEN :
SC " " " Continuous Slot
- 3. g
-i oiA- h" I.D. TYPE. PVC g
=
=. -
{, OPENINGS WIDTH 0.015 TYPE-
- M soTTou oF SCREE N -
h80.0 -323.3 2.0' Ball Valve (Down Pump Only) g b' eorrow orsuw, _
. h82.0 -325.3 3 ,,
sorTou oF Note : LSQ.a=331 3 . 8" 0 W 4 : OLE DIA: I
n, g aa"'A- -- s ---. -
< --~ ~ - - - - -
I I I I I APPENDIX C TABULATION OF EXISTING WATER ELL AND DRILL HOLE DATA l I I . I I
APPENDIX C WATER WELL AND DRILL HOLE IWEN'IORY This appendix provides a tabular listing of available information from numerous water wells and exploratary borings drilled throughout the study area. This typically includes such general information as the well location, depth and surface elevation. The availability of additional information is indicated by a check in the appropriate column. Such information may include a geologist's log, a driller's log, geophysical logs spontaneous potential, resistivity, gamma ray and/or neutron, water level data, water quality data, well test and/or construction reports,
, and governmental agency reports. The primary sources for this drill hole data are state and federal geological surveys, state and county water resources agencies, and local plant sites such as Vogtle Electric Generating Plant, Savannah River Plant and Barnwell Nuclear Fuel Plant.
l
TABLE NO. C-1 (SHEET lA OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER lELL DATA BURKE COUNTY, GEORGIA l DATA AVAILABLE SURFACE GEOPHYSICAL LOGS HE LL ELEVATION GEOLOGIST'S DRILLER 'S SP/ GAMMA / NUMBER LOCATIOP. DEPTH (FT.) (FT.) LOG LOG RESISTIVITY PEUTRON B-1 33* 13' 38" N X 81* 49' 35" W B-3 33' 13' 28" N X 81* 49' 50" W B-4 33' 13' 13" N X 81* 49' 51" W B-6 33* 13' 03" N X 81* 49' 41" W B-7 33* 12' 55" N X 81* 49' 12" W B-8 33' 13' 33" N X 81* 49' 40" W b-10 33' 13' 29" N X 81* 50' 20" W B-11 33* 13' 04" N X 81* 50' 24" W B-12 33' 09' 45" N X 81* 46' 21" W B-13 33' 14' 22" N X 81* 51' 50" W B-14 33' 1A' 03" N X 81* 2A' 28" W B-15 33* ll' 22" N X 81' 52' 19" W B-16 33* 09' 26" N X 81' 46' 46" W l B-2 5 33* 08' 27" N X 81* 44' 50" W B-26 33' 08' 09" N X 81* 44' 37" W I C-1
- m m M
M M - M M M M TAB 2 NO. C-1 (SHEET 1B OF 88) INVENTORY OF EXISTING DRILL EOLE AND KATER NELL DATA BURKE COUNTY, GEORGIA DATA AVAILABLE NELL CONSTRUCTION W LL WATE R WATE R AG NCY* NUMBER LOCATION REPORT TEST GVEL QUALITY REPORT REMARKS B-1 33* 13' 38" N Split spoon samples 81* 49' 35" W only B-3 33* 13' 28" N Split spoon samples 81* 49' 50" W only B-4 33* 13' 13" N Split spoon samples 81* 49' 51" W only B-6 33' 13' 03" N Srt.c spoon samples 81* 49' 41" W only B-7 33* 12' 55" N Split spoon samples 81* 49' 12" W only B-8 33* 13' 33" N Split spoon samples 81* 49' 40" W only B-10 33* 13' 29" N Split spoon samples 81* 50' 20" W only B-ll 33* 13' 04" N Split spoon samples 81* 50' 24" W only B-12 33* 09' 45" N Split spoon samples 81* 46' 21" W only B-13 33* 14' 22" N Split spoon samples 81* 51' 50" W only B-14 33' '1' 03" N Split spoon samples 81* 51' 28" W only B-15 33* 11' 22" N Split spoon samples 81* 52' 19" W only B-16 33* 09' 26" N Split spoon samples 81* 46' 46" W only B-25 33' 08' 27" N Split spoon samples 81* 44' 50" W only B-26 33' 08' 09" N Split spoon samples 81* 44' 37" W only
- Well record obtained from USGS, state or county agency.
i C-2 l l
TABLE NO. C-1 (SHEET 2A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA BURKE COUNTY, GEORGIA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS 5E LL ELEVATION GEOLOGIST'S DRI LLE R 'S SP/ GAMMA / NUMBER LOCATION DEPTH (PT) (PT) LOG LOG BESISTIVITY NEUTRON B-35A Alvin W. Vogtle Site 70 94.4 X B-36A Alvin W. Vogtle Site 70 98.3 X B-36B Alvin W. Vogtle Site 150 98.4 X B-45 18,100 N.E. of 36
- 370 273.5 X B-136 N 1,14 2,996.2 (a) 300 209.5 X E 623,848.8 B-147 33' 08' 37" N X 81* 45' 37" W F,-15 2 N 1,13 3,8 30.7 (a) 200 152.'. X E 633,343.7 B-156 N 1,131,584.1 (a) 260 237.7 X E 642,340.1 B-246 N 1,145,531.6 (a) 400 210.4 X E 620,553.1 B-346 N 1,137,351 (a) 26.5 108 X E 628,477 CW-1 N 69+13 (b) 251 X E 89+19 GGS***131 33' 14' 11" N 620 129 X 81* 56' 46" W GGS 220 33' 11' 20" N 1002 X 81* 55' 30" W GGS 316 33' 10' 10" N 1003 276 X 81' 56' 55" W GGS 391 32' 49' 41" N 250 229 X 82* 14' 26" W i
- See remarks
- Georgia Geologic Survey (a) Georgia state grid (b) Vogtle plant grid C-3 E E
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TABLE NO. C-1 (SHEET 3A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA BURKE COUNTY, GEORGIA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS iE LL ELEVATION GEOLOGIST'S DRI LLER 'S SP/ GAMMA / NUMBEh LOCATION DEPTH (PT.) (FT.) LOG LOG RESISTIVITY NEUTRON dGS 392 33' 03' 19" N 175 230 X 81* 43' 40" W GGS 520 33' 0 33" N 700 300 X 82* 014 00" W GGS 1171 33' 05' 53" N 187 X X X (Burke #1) 81* 42' 40" W GGS 1172 33' 07' 00" N 150 100 X (Barke #2) 81* 42' 15" W GGS 1176 33' 09' 46" N 150 300 X X X - (Burke #4) 81* 54' 25" W GGS 2136 32' 49' 37" N 405 X (Burke #2) 82' 09' 14" W GGS 3169 33' 08' 29" N 378 X X XX 81* 45' 38" W GGS 3354 33' 00' 34" N 410 268 X X 82* 06' 23" W GGS 3444 32' 52' 32" N 1530 268 X X X 82* 13' 15" W MU* #1(# 5) N 1,14 4,4 24.7 (a) 851 197 X X X E 624.530.7 MU* #2(#6) N 1,144,500 (a) 850 214.5 X X E 623,135 TW-1 33* 08' 24" N 928 219 X XX X 81* 45' 41" W Sardis il 32' 58' 25" N 300 81* 45' 32" W Sardis #2 32' 58' 10" N 300 81* 45' 07" W
- Makeup (a) Georgia state grid C-5 M QS M
M C m m TABLE NO. C-1 (SKEET 3B OF 88) INVENTORY OF EXISTING DRILL HOLE AND KATER ELL DATA BURKE COUNTY, GEORGIA DATA AVAILABLE WELL CONSTRUCTION WELL WATER WATE R AGE NCY NUMBER LOCATION REPORP TEST IEVE L QUALITY REPORT REMARKS GGS 392 33' 03' 19" N X 81* 43' 40" W GGS 520 33* 05' 33" N 82* Ol' 00" W GGS 1171 33* 05' 53" N (Burke #1) 81* 42' 40" W GGS 1172 33' 07' 00" N (Burke #2) 81* 42' 15" W GGS 1176 33* 09' 46" N (Burke #4) 81* 54' 25" W GGS 2136 32' 49' 37" N (Burke #2) 82* 09' 14" W GGS 3169 33' 08' 29" N 81* 45' 38" W GGS 3354 33' 00' 34" N 82* 06' 23" W GGS 3444 32' 52' 32" N Temperature, acoustic 82* 13' 15" W velocity, caliper, and fluid logs MU* #1(#5) N 1,14 4,424.7 (a) X X X X E 624,530.7 MU* #2(96) N 1,144,500(a) X X X E 623,135 TW-1 33* 08' 24" N X Loga of interval 81* 45' 41" W velocity, elastic moduli, bulk density and Poisson's ratio Sardis il 32' 58' 25" N X X 81* 45' 32" W Sardis #2 32' 58' 10" N X X 81* 45' 07" W
- Ma'seup (a) Georgia state grid C-6
TABLE NO. C-1 (SHEET 4 A OF 88 ) INVENTORY OF EXISTING DRILL HOLE AND W\TER ELL DATA BURKE COUNTY, GEORGIA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL EIEVATION GEOLOGIST'S DRI LIER 'S SP/ GAMMA / NUMBE R LOCATION DEPTH (PT.) (FT.) LOG LOG RESISTIVITY NEUTRON Waynesboro #2 South side of 300 256 Waynesboro EFFINGHAM COUNTY, GEORGI A GGS 3108 32' 34' 22" N 198 X (Ef fingham 81* 25' 03" W
#10)
GGS 3109 32* 33' 07" N 188 X (Ef fingham 81* 22' 34" W
#11)
GGS 3110 32' 31' 47" N 210 X (Effingham 81* 19' 57' W
#12)
EMANUEL COUNTY, GEORGI A Georgia Oil 32' 35' 00" N 2232 Co. 82* 08' 00" W* GGS 172 32* 48' 00" N 1833 200 82* 14' 00" W*
- See remarks
- Not shown on Figure 7-1 C-7 E E E E
M . M M M M M M TABLE NO. C-1 (SHEET 4B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA JEFFERSON COUNTY, GEOHGIA DATA AVAILABLE ELL CONSTR'JCTION ELL WATER WATER AGENCY NUMIER LOCATION REPORT TEST LEVE L QUALITY , REPORT BEMARKS X ** Waynestoro #2 South side of X Waynesboro EFFINGHAM COUNTY, GEORGIA GGS 3108 32' 34' 22" N (Effingham 81* 25' 03" W
#10)
GGS 3109 32' 33' 07" N (Effingham 81* 22' 34" W
#11)
GGS 3110 32' 31' 47" N (Effingham 81* 19' 57" W
#12)
EMANUEL COUNTY, GEORGI A Georgia Oil 32' 35' 00" N X Approximate location Co. 82* 08' 00" W* GGS 172 32* 48' 00" N X Approximate location 82* 14 ' 00" W*
- See remarks
** Not shown on Figure 7-1 C-8
TABLE NO. C-1 (SHEET SA OF 88) INVENIORY OF EXISTING DRILL HOLE AND WATER ELL DATA JEFFERSON COUNTY, GEOPGI A DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL ELEVATION GEOLOGIST'S DRI LLE R
- S SP/ GAPEA/
NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON Ash 41 Near Monticello* 103 X City of Wadley, Georgia 491 X Wa dley Geor g ia 32' 59' 00" N 1143 445 Petroleum Co. 82* 27' 00" W* GGS 133 32' 12' 20" N 549 445 X 82* 23' 40" W GGS 480 33* 03' 40* N 750 355 X 82* 23' 35" W GGS 532 32' 53' 54" N 410 265 X 82* 23' 22" W GGS 554 32' 59' 44" N 370 57 X 82* 24' 40" W GGS 1192 32' 54' 15" N 253 X X 82* 23' 45" W Joiner #1 SE/4 NW/4, 168 X sec.6 T2N R6E Sasser #1 SW/4 NW/4 270 X sec.36 T2N R3E Wooten #2 Center sec. 5, 162 X T2N, RSE
- See remarks
** Not shown on Figure 7-1 C-9 E E E E E E E E E E
M M M M M M M M TABLE NO. C-1 (SHEET SB OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA JEFFERSON COUNTY, GEORGI A DATA AVAILABLE ELL CONSTRUCTION ELL WATE R WATE R A2 NCY NUMBER LOCATION REPORT TEST LEVEL QUALITY REPORT BEMARKS Ash il Near mnticello* 0.2 mi. west of SE corner of Section 1, T2N, R6E*" City of Wadley, Georgia X X X X ** Wadley Georg ia 32' 59' 00" N X Approximate location Petroleum Co. 82* 27' 00" W* ** GGS 133 32* 12' 20" N ** 82* 23' 40" W GGS 480 33* 03' 40" N ** 82* 23' 35" W GGS 532 32' 53' 54" N ** 82* 23' 22" W GGS 554 32' 59' 44" N ** 82* 24' 40" W GGS 1192 32* 54' 13" N ** 82* 23' 45" W Joiner #1 SE/4 NW/4, ** sec.6 T2N R6E Sasser il SW/4 NW/4 ** sec.36 T2N R3E Wooten #2 Center sec. 5, ** T2N, R5E
- See remarks
** Not shown on Figure 7-1 C-10
TABLE NO. C-1 (SHEET 6A OF 88) ZNVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA JENKINS COUNTY, GEOBGIA DATA AVAILABLE SURFACE GEOPHYSICAL LC3S E LL ELEVATION GEOLOGIST'S DRILLE R'S SP/ MA/ NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY h LTRON GGS 227 32' 52' 42" N 81* 57' 42" W GGS 1032 32' 52' 59" N 81* 57' 12" W GGS 3442 32* 48' 24" N 400 X 81* 53' 55" W Magnolia Magnolia Springs 480 X Springs il State Park, Millen Magnolia C.C.C. camp at 357 210 X Springs 62 Magnolia Springs State Park
- RICHMOND COUNTY, GEORGIA Kimberly Clark 33* 16' 37" N 700 290 X X test well 81* 56' 00" W SCREVEN COUNTY, GEOBGI A B*** 1 Newington, 199 Georg ia B-3 32' 36' 49" N 202 X 81* 24' 37" W B-4 Newing ton , 162 Georgia B-5 Newington, 104.5 Georgia
- See remarks
*** Boring C-ll M M M M M M M M M M M M
M M M M M M M M M M M M M
., TABLE NO. C-1 (SHEET 6B OP 88)
INVENTORY OF EXISTING DRILL HOLE AND WATER WELL DATA JENKINS COUNTY, GEORGIA DATA AVAILABLE TELL CONSTRUCTION ELL WATER WA1E R AGENCY NUMBE R LOCATION REPORT TEST LEVEL QUALITY REPORT RE MARKS GGS 227 32' 52' 42" N 81* 57' 42" W GGS 1032 32' 52' 59" N 81* 57' 12" W GGS 3442 32' 48' 24" N 81* 53' 55" W Magnolia Magnolia Springs X X X ** Springs il State Park, Millett Magnolia C.C.C. camp a t X Springs #2 Magnolia Springs 4-1/2 miles north of State Park
- Millen**
RICHMOND COUNTY, GEORGIA Kimberly Clark 33* 16' 37" N X Acoustic velocity log test well 81* 56' 00" W SCREVEN COUNTY, GEORGIA B*** 1 Newington, Boring log ** Georg ia B-3 32' 36' 49" N Boring log 81* 24' 37" W B-4 Newing ton , Boring log ** Georgia B-S Newington, Boring log ** Georgia
- See remarks
** Not shown 'n Figure 7-1 *** Boring C-12
TABLE NO. C-1 (SHEET 7A OF 82) INVEN'IORY OF EXISTIE DRILL HOLE AND WATER ELL DATA SCREVEN COUNTY, GEOBGIA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS NE LL ELEVATION GEOLOGIST'S DRI LLER 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON B-21 32' 37' 13" N 203 X 81* 25' 00" W B-22 32' 37' 50" N 202 X 81* 25' 33" W B-23 Screven/E f f ingham border B-31 32' 48' 46" N 248.2 X 81* 28' 50" W B-32 32' 54' 14" N 253.2 X X 81* 30' 32" W B-33 32* 57' 31" M 273.2 95 X X 81* 32' 29" W B-34 33' 00' 59" N 273.3 X X 81* 34' 35" W B-3 5 33' Ol' 28" N 203.5 X 81* 31' 56" W B-36 32* 41' 34" N 173.3 X 81* 26' 32" W B-37 32' 41' 10" N 233.1 X X 81* 27' 36" W B-38 32* 38' 32" N 212.4 X X 81' 27' 30" W B-40 2 miles north of 190.5 X X Clyn, Ga.* B-41 4 miles south of 232 X X Clyo, Ga.*
- See remarks C-13 M M M M M M M M M M
m M M M M M M M M M M TABLE NO. C-1 (SEEET 7B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA SCREVEN COUNTY, GEORGIA DATA AVAILABLE ELL CONSTRUCTION W LL WATE R WATE R AGENCY NUMBER LOCATION REPORT TJST LEVEL QUALITY REPORT RE MARKS B-21 32' 37' 13" N Boring log 81* 25' 00" W B-22 32' 37' 50" N Boring log 81* 25' 33" W B-2 3 Screven/E f fingham X X ** border B-31 32' 48' 46" N 81* 28' 50" W B-32 32' 54' 14" N 81* 30' 32" W B-33 32' 57' 31" N 81* 32' 29" W B-34 33' 00' 59" N 81* 34' 35" W B-35 33' Ol' 28" N 81* 31' 56" W B-36 12' 41' 34" N 82* 26' 32" W B-37 32' 41' 10" N 81* e?' 36" W B-38 32' 38' 32" N 81* 27' 39" W B-40 2 miles north of 400 ft east of GA. Clyo, GA.* highway 91, ** B-41 4 miles south of Along Stillwell Rd., Clyo, GA. * **
- See remarks
** Not shown on Figure 7-1 C-14
TABLE NO. C-1 (SHEET 8A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER HELL DATA SCREVEN COUNTY, GEORGIA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS HE LL E LEVATION GEOLOGIST'S D RI LLE R'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON BFL 4-2 Millhaven 790 180 X XX Plantation GGS 295 32' 45' 26" N 490 202 X 81* 38' 29" W GGS 413 32' 45' 54" N 216 210 X 81* 34' 54" W GGS 590 32' 55' 59" N 374 95 x 81* 32' 14" W GGS 855 32* 35' 00" N 2677 130 X XX 81* 25' 40" W GGS 940 32' 53' 06" N 81* 39' 31" W GGS 974 32' 45' 04" N XX X 81* 35' 29" W GGS 979* 32' 36' 25" N #1 - 1336 160 X 81* 44' 40" W #2- 670 X 63 - 1331 GGS 1007 32' 49' 31" N 260* X XX X 81* 46' 53" W GGS 1047 32' 55' 32" N 81* 40' 18" W GGS 1170 32' 38' 07" N 340* X xx x 81* 25' 29" W GGS 1174 33' Ol' 17" N 81* 34' 35" W GGS 1175 32' 55' 59" N 295 X XX X 81' 31' 15" W GGS 3032 32' 41' 18" N X X 81* 30' 54" W
- See remarks C-15 m W W W W W W W W W W W W W
g 7 o C g l n i a g
- r , m o
- u2 m l t4 a -
c g E S g a , K o f1 m m R l u# o o A n r r M r ay f f E e p Mn3 R h i gpa4 t h t l nmd p p a e e E C ion KCa D
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N TE I SR N O C E NW NW NW NW NW NW NW NW NW NW NW NW N
"6 "9 "4 4 9 "4 00 "61 03 "4 "9 02 "50 1 "3 35 2
31 "8 "79 02 95 51 "8 15 4 1 22 55 51 04 24 O n - I no ' ' 7 T ' ' A ei vt aa 58 5 4 52 '55
'3 '9 5 '5 '6 '4 '96 '5 '0 '8 '5 '51 1 0 e r
C 43 4 3 53 32 53 43 3 4 44 54 32 53 4 3 O ht u L l n g l a il MP 21 21 21 21 21 38 21 38 21 38 21 21 3 8 2l 3 B
'21 38 2 1 3 8 i
F E 38 38 38 38 38 so k n r n aw mo eh .E R 2 5 9 3 1 0 9 5 5 0 4 4 7 9 7 7 0 0 7 4 0 0 7 1 5 7 1 2 3 0 r s et LE 4 2 4 5 8 9 9 9 1 1 1 1 3 eo SN LI M L S S S S S S S S S S S S EU N F B G G G G G G G G G G G G G G G G G G G G G G G G
- E E
TABLE NO. C-1 (SHEET SA OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA SCREVEN COUNTY, GEORGIA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS lE LL ELEVATION GEOLOGIST'S DRI LLE R 'S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (PT.) LOG LOG FESISTIVITY NEUTRON GGS 3095 North Screven 75 X County
- GGS 3198 32' 41' 25" N 212 X 81* 30' 29" W WASHING % N COUNTY, GEORGIA GGS 223 32' 59' 25" N 605 480 X 83' 00' 15" W
- See remarks 4
C-17 E E E E E E E E E E E E E
E E E E E E E TABLE NO. C-1 (SHEET 9B OP 88) INVENTORY OF EXISTING DRILL HOM AND WATER ELL DATA SCREVEN COUNTY, GEORGI A DATA AVAILABLE ELL CONSTRUCTION ELL WATE R WA'IE R AGENCY NUMEER LOCATION REPORT TEST LEVEL QUALITY EPORT EMARKS GGS 3095 North Screven East of Hitonia** Countv* GGS 3198 32* 41' 25" N 81* 30' 29" W WASHINGTON COUNTY, GEOEGIA GGS 223 32* 59' 25" N 83* 00' 15" W
- See remarks
** Not shown on Figure 7-1 C-18 l
WN KT O R X W AU S GE G N O L L A C I Y S T Y I H P /I O PT E SS V X X W E G I L S B E A E A T A D L I A V W A S L L A 'R T EG ) E W R A D LO LL I R X X X X X X X X X X m 8 E 8 TA D AN F WI O A DO NR AA L S m 0 1 C 'T E S LH I G T E HU OT GO OL E H S LS ( L O L O E 9 1 C m I , G 1 RY
- DT C GUN 1 - .NO EL)
O I T C CI . N SN ATT b 0 4 9 0 0 2 0 2 7 5 . E I E FAF 1 6 5 4 9 2 2 3 4 4 3 d L XK RV( 4 4 2 1 4 i B EIA UE r A F TO SL E
)
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- e e r NW n NW NW r r e d o e e v o t d d s N
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- ae
)
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)
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' ' ' ' ' ' l T 13 f 92 94 f f f f a f n 45 25 64 25 02 A.
- oar 25 o 2 5 14 o o o o s O 36 97 04 86 70 r L 4d 26 91 13 82 01 y n n n n e
/a 74 64 *
- 74 64 74 t * * *
- w w w w v E u 31 i 31 31 o o o o i SQ NE NE 3 8 NE NE NE C 3 8 38 T T T T sn k U r
ad me ei rf i ed eo R 3 3 6 8 9 0 8 0 7 8 3 4 SM 6 6 8 2 3 3 3 5 5 LE 3 9 8 0 6 2 3 4 4 4 4 4 4
- LB 2 2 1 2 2 2
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E E E E E E E E E E TABLE NO. C-1 (SHEET 10B OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WATER ELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGE NCY NUMDER LOCATION REPORT 'IE ST LEVEL QUALITY REPORT BEMARKS AK-23 SE/4 of Oakwood X 2 miles past Aiken Quadrangle
- St. Park boundary to the west on SC-53**
AK-29 N 723.4 (c) X X X ** E 466.5 AK-183 N 699.2 (c) X X X E 417.5 AK-203 33* 26' 01" N X X X X 81* 54' 43" W AK-266 N 710.2 (c) X X X ** E 434.5 AK-268 N 688.0 (c) X X X X E 426.2 AK-269 N 707.1 (c) X X X ** E 410.3 AK-380 City of Ellenton* X X X Corner of Oak and Boatner St.** _AK-428 33* 29' 40" N X X ** 81* 52' 05" w AK-430 33* 19' 40" N X 81* 44' 35" W AK-437 Town of Ba th X X X ** AK-438 Town of Bath
- X Under .e water tank along Co. road 20**
AK-453 Town of Belvedere X ** AK-454 Town of Belvedere X X X X **
- See remarks (c) Modified Universal Transverse Mercator (UTM) grid.
C-20
TABLE NO. C-1 (SHEET llA OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WATER 1 ELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WELL ELEVATION GEOLOGIST'S DRILLER'S SP/ GAMMA / NUMBE R LOCATION DEPTH (PT.) (FT.) LOG LOG IE SISTIVITY NEUTRON AK-456 Town of Belvedere 118 X AK-459 Town of Clearwater 195 X AK-461 Town of Clearwater 172 X X DRB 1 33' 17' 56" N 1900 261.62 X 81* 40' 18" W DRB 2 33' 16' 39" N 1982 281.6 X X 81* 39' 48" W DRB 3 33' 17' 14" N 1941 285.3 X X 81* 39' 49" W DRB 4 33* 16' 39" N 1938 250.75 X XX 81* 38' 03" W DRB 5 33' 17' 40" N 1838 286.7 X XX 81* 39' 37" W DRB 6 33' 17' 29" N 1913 269.08 X XX 81* 39' 21" W DRB 7 33* 17' 17" N 1969 277.9 X XX 81* 40' 28" W DRB 8 33' 16' 54" N 1965* 81* 38' 54" W LA-8 33' 17' 01" N 629 274 X 81* 43' 09" W
- See remarks C-21 g W E E E E E E E E E
m M M M W W W W W W m m W TABLE NO. C-1 (SHEET llB OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE NELL CONSTRUCTION HELL WATE R WATER I AGE NCY NUMBER LOCATION REP _ ORT TEST LEVE L QUALITY REPORT REMARKS AK-456 Town of Belvedere X X X AK-459 Town of Clearwater X ** AK-461 Town of Clearwater X X DRB 1 33* 17' 56" N 81* 40' 18" W DRB 2 33* 16' 39" N i Directional, sonic, 81* 39' 48" W temperature, micro-lateral logs DRB 3 33* 17' 14" N Microlateral log 81* 39' 49" W DRB 4 33* 16' 39" N Caliper & sonic logs 81* 38' 03" W DRB 5 33* 17' 40" N Caliper, sonic and 61* 39' 37" W microcaliper logs DRB 6 33* 17' 29" N Directional, sonic, 81* 39' 21" W temperature, micro-lateral logs DRB 7 33* 17' 17" N Caliper & sonic logs 81* 40' 28" W DRB 8 33* 16' 54" N X X Depth taken from cross-81* 38' 54" W section of NW border of Triarsic basin ***.1 LA-8 33* 17' 01" N X X X X 81* 43' 09" W
** Not shown on Figure 7-1 *** Cross section with lithologies 1 From Marine,1979a C-22
TABLE NO. C-1 (SHEET 12A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA'AVAILABLE SUGACE GEOPHYSICAL LOGS E LL EiVAT ION GEOLOGIST'S DRILE R'S SP/ GAMMA / NUMBER LOCATION DEPTH (PT.) 'FT.) LOG LOG IESISTIVITY NEUTRON LA-31 33' 20' 16" N 685 X 81* 43' 51" W P- A N 75,444 (d) 920 267.9 X X E 56,848 P-1B N 75,443 (d) 555 289.1 E 56,818 P-lC N 75,4 65 (d) 368 289 E 56,797 P-2A N 73,896 (d) 843 249.9 X X E 53,316 P-2B N 73,895 (d) 532 250.3 X E 53,3.35 P-2C N 73,893 (d) 350 249 X E 53,281 P-3A N 72,800 (d) 936 277.7 X X E 60,100 P-3B N 72,800 (d) 548 277.6 E 60,130 P-3C N 72,826 (d) 410 278 E 60,115 P-7A 33* 20' 00" N 725* 273.5 X 81* 35' 54" W P-4R N 90,559 (d) 765 105.3 X E 14,902 SCGS*** Central portion 100 503 X Butler il of North Augusta 7.5' Quad *
*See remarks * ** South Carolina Geological Survey (d)Scvannah River Plant (SRP) grid C-23 M M M M M M M M M ' '
M M
E E E E E E E E E TABLE NO. C-1 (SEEET 12B OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WA'IER ELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE WELL CONSTRUCTION HELL WATER WATER AGE NCY NUMEER LOCATION REPORT TEST LEVE L QUALITY EPORT REMARKS LA-31 33* 20' 16" N X X X X 81* 43' 51" W P-1A N 75,444 (d) X X Driller's log of E 56,948 piezometers; caliper loo P-1B N 7 5,443 (d) X X X E 56,818 -- P-lC N 75,4 65 (d) X X X E 56.797 P-2A N 73,896 (d) X X Driller's log of E 53,316 ciezometers P-28 N 73,895 (d) X X X E 53,335 P-2C N 73,893 (d) X X X E 53,281 P-3A N 72,800 (d) X X Driller's log of E 60,100 nfarnmatars P-3 B N 72,800 (d) X X X E 60,130 P-3C N 72,826 (d) X X X E 60,115 P-7A 33* 20' 00" N X X Caliper log available; 81* 35' 54" W depth from caliper ing** P-4R N 90,559 (d) X Driller's log of E 14,902 nierneaters SCGS*** Central portion 0.38 miles NW cf inter-Butler il of North Augusta section of I-20 and 7.5' Quad
- US-25**
- See remarks
** Not shown on Figure 7-1
- South Carolina Geological Survey (d) Savannah River Plant (SRP) grid C-24
TABLE NO. C-1 (SHEET 13A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WA'IER ELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL ELEVATION GEOLOGIST'S DRILLER ' S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON SCGS Huber Hollow Creek 408 X
#1 7.5' Ouad*
SCGS NE/4 of Windsor 60 350 X McGriff 7.5' Quad
- Site 52 SCGS McNeil SE/4 of Augusta 100 180 X
#2 East 7.5' Quad
- SCGS Same as AK-23 73 418 X Oakwood #1 (Sheets 10A & 10B)
SCGS NW/4 of Oakwood 63 500 X Oakwood #2 7.5 Quad
- SCGS SE/4 of Augusta 30 175 X Washington East 7.5' Quad
- Corp. 41 SCWIC * *
- 33* 29' 11" N 505 39V-b1 81* 41' 30" W SCWIC 33* 29' 10" N 240 505 39V-b2 81* 41' 31" W SCWIC 33* 29' 09" N 239 505 x 39V-b3 81* 41' 32" W SCWIC (No location) 20C* X 40X-ml T-1 Savannah River 801 270 X Plant W-1 33* 12' 42" N 152 96 81* 46' 46" W*
- See remarks
*** South Carolina Water Resources Commission C-25 E E E E E
~
E E
E TABLE NO. C-1 (SHEET 13B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE WELL CONSTRUCTION HELL WATE R KATE R AGE NCY NLHER LOCATION IEPORT TEST IEVEL QUALITY RE PORT IEMARKS SCGS Huber Hollow Creek At junction of S-2-145 41 7.5' Quad
- and S-2-146** ~--
SCGS NE/4 of Windsor 1.5 miles SE of McGriff 7.5' Quad
- Tarrants Mill Pond **
Site 42 SCGS McNeil SE/4 of Augusta X 0.1 miles NE of MM 42 East 7.5 Quad
- 148**
SCGS Same as AK-23 X Oakwood il (Sheets 10A & 10B) SCGS NW/4 of Oakwood X 0.5 mi. down dirt road Oakwood 42 7.5 Quad
- off SC-29**
SCGS SE/4 of Augusta X 0.47 mi. NW of Silver Washington East 7.5' Quad
- Bluff Church **
Corp. 91 _, SCW FC * *
- 33* 29' 11" N X 39V-b1 81* 41' 30"_ W bCW RC 33* 29' 10" N X **
39V-b2 81* 41' 31" W _ SCW FC 33* 29' 09" N X 39V-b3 81* 41' 32" W SCWRC (No location) X Caliper log; depth from 40X-ml gamma log ** T-1 Savannah River Plant W-1 33* 12' 42" N Well lithologies and 81* 46' 46" W* local geology available from graphic logs, CDCE****, 2, approx. location
- Se e r e mar k s
** Not shown on Figure 7-1 *** South Carolina Water Resources Commission * * *
- Charleston District Cos es of Engineers 2 Corps of Engineers, Geologic-Engineering Investigations (1952)
C-26
TABLE NO. C-1 (SHEET 14A CF 88) INVEN'!ORY OF EXISTING DRILL HOLE AND WATER ELL DATA AIKEN COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL EEVATION GEOLOGIST'S DRILLER 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON X-M-16 33' 19' 06" N 354 354 81* 44' 08" W 21-F Savannah River Plant 790* X 54-R Savannah River Plant 460* X 55-P Savannah River Plant 570* X 905-68A 33' 20' 34" N 384 X 81* 20' 34" W 905-37F 33' 17' 00" N 773 299.5 X 81* 40' 28" W 905-35H 3 17' 13" N 824 298.7 X 81* 38' 36" W 905-93P i Save.nnah River Plant 610* X l ALENDALE COUKTY, SOUTH CAROLINA AL-1 32' 57' 24" N 750 140 81* 14' 15" W AL-2 33' 00' 13" N 800 200 81* 18' 21" W
- See remarks C-27 E -
E E E E
a TABE NO. C-1 (SHEET 14 B OF 88 ) INVEN'IORY OF EXISTING DRILL HOE AND WATER ELL DATA AIICEN COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WAE R AGENCY NUMBER LOCATION REPORT EST EVEL QUALITY EPORT EMARXS X-M-16 33* 19' 06" N Well lithologies and 81* 44' 08" W local geology avail-able from graphic logs, CDCE, 2 21-F Savannah River Plant Depth from E-log ** 54-R Savannah River Plant Depth from E-log ** 55-P Savannah River Plant Depth from E-log ** 905-68A 33* 20' 34" N X X X 81* 20' 34" W 905-37F 33* 17' 00" N X X X X 81* 40' 28" W 905-35H 33* 17' 13" N X X X 81* 38' 36" W 90 5-9 3P Savannah River Plant Depth from E-log *
- ALENDALE COUNTY, SOLTTH CAROLINA AL-1 32' 57' 24" N X X 81* 14' 15" W AL-2 33' 00' 13" h X X 81* 18' 21" W
- Not shown on Figure 7-1 2 Corps of Engineers, Geologic-Engineering Investigations (1952)
C-28
TABLE NO. C-1 (SHEET ISA OF 88) INVENWRY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS TE LL ELEVATION GEOLOGIST'S DRI LLER 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG PESISTIVITY NEUTRON AL-3 Peeples 7.5' Quad
- 40 X AL-5 32' 57' 38" N 700 140 81* 14' 29" W AL-6 32" 57' 33" N 750 140 81* 14' 29" W AL-8 33* 02' 08" N 600 151 81* 13' 21" W AL-9 32' 57' 27" N 660 140 81* 14' 12" W AL-10 32' 57' 28" N 635 140 81* 14' 15" W AL-11 33' 05' 52" N 84 81* 30' 04" W AL-12 33' 00' 38" N 648 215 X 81* 19' 07" W AL-13 33* Ol' 35" N 371 300 81* 23' 02" W AL-14 33* 02' 40" N 150 X 81* 22' 00" W AL-15 33' 04' 35" N 210 120 81* 28' 56" W AL-16 33' 04' 55" N 210 120 81* 29' 08" W AL-17 33' 04' 56" N 210 120 81* 28' 04" W
- See remarks C-29 E
E - E TABLE NO. C-1 (SHEET ISB OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER HELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION HELL WATER WATE R AGENCY NUMIER LOCATION TEST LEVEL l BEPOT:T BEMARES REPORT QUALITY AL-3 Peeples 7.5' Quad
- 2.8 miles NW of Pilletville**
AL-5 32' 57' 38" N X 81* 14' 29" W AL-6 32' 57' 33" N X 81* 14' 29" W AL-8 33* 02' 08" N X X 81* 13' 21" W AL-9 32' 57' 27" N X 81* 14' 12" W AL-10 32' 57' 28" N X X 81* 14' 15" W AL-ll 33' 05' 52" N X X 81* 30' 04" W AL-12 33* 00' 38" N X X X X X 81* 19' 07" W AL-13 33* Ol' 35" N X 81* 23' 02" W AL-14 33' 02' 40" N X X X 81* 22' 00" W AL-15 33* 04' 35" N X 81* 28' 56" W AL-16 33' 04' 55" N X X 81* 29' 08" W AL-17 33' 04' 56" N X 81* 28' 04" W
- See remarks
** Not shown on Figure 7-1 C-30
TABLE NO. C-1 (SEEET 16A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS Nd LL E LEVATION GEOLOGIST'S DRI LLE R 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RSSISTIVITY NEUTRON AL-18 33* 05' 49" N 218 120 81* 31' 32" W AL-19 33* 04' 30" N 760 161.5 X X 81* 26' 48" W A L-20 33' 06' 18" N 200+ 140 81* 33' 05" W AL-21 33' 04' 48" N 100 120 81* 25' 25" W AL-22 32' 57' 58" N 830 148 X X 81* 15' 05" W AL-23 33* Ol' 08" N 889 210 X 81* 18' 07" W AL-2 4 33' 00' 13" N 740 200 81* 18' 21" W AL-27 See Sandoz ll, Sheet C-52 AL-2 8 32' 48' 05" N 480* 140 X X 81* 18' 56" W AL-29 32' 57' 31" N 668 140 X X 81* 14' 18" W A L-30 32' 57' 00" N 81* 11' 41" W AL-32 32' 57' 08" N 260 100 81* 26" 54" W AL-3 3 33' 02' 18" N 800 180 X X X 81* 17' 22" W l
- See remarks C-31 m W
TABG NO. C-1 (SIEET 16B OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WATER M:LL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABIE ELL CONSTRUCTION NELL WATER WATER AGENCY NUMBER LOCATION REPORT TEST EVEL QUALITY REPORT REMARKS AL-18 33' 05' 49" N X 81* 21' 32" W AL-19 33' 04' 30" N X X X 81* 26' 48" W AL-20 33' 06' 18" N X X 81* 33' 05" W AL-21 33' 04' 48" N X X 81* 25' 25" W AL-22 32' 57' 58" N X X X 81' 15' 05" W AL-23 33' Ol' 08" N X X X X 81* 18' 07" W AL-24 33' 00' 13" N X 81* 18' 21" W AL-27 See Sandoz i1, Sheet C-52 AL-28 32' 48' 05" N X Caliper 109, depth 81' 18' 56" W taken from E-log AL-29 32' 57' 31" N X X X Caliper log 81* 14' 18" W AL-30 32' 57' 00" N 81* 11' 41" W AL-32 32' 57' 08" N X X 81* 26" 54" W AL-33 33' 02' 18" N X Samples stored at 81* 17' 22" W SCWRSR*** See remarks
*** South Carolina Water Resources Sample Repositcry C-3 2
TABLE NO. C-1 (SHEET 17A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE CEOPHYSICAL LOGS NE LL ELEVATION GEOLOGIST'S DRILLE R'S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON AL-36 32' 58' 45" N 667* 160 X X Ol' 17' 14" W AL-3 7 32' 45' 52" N 154 81' 21' 29" W AL-3 8 32' 56' 53" N 298 100 81* 26' 39" W AL-39 33* 04' 08" N 200 80 81' 28' 37" W AL-40 33' 07' 18" N 755 240 X X 81* 33' 19" W AL-41 33' 04' 49" N 500 140 X 81* 32' 12" W AL-44 32' 58' 50" N 856 162 X X 81' 17' 45" W A L-4 5 33' 02' 14" N 758 X 81* 17' 15" W AL-4 6 32' 59' 35" N 908 X 81' 17' 50" W AL-47 32' 46' 39" N 170 60 X X X 81* 22' 27" W AL-48 33' 05' 18" N 310 186* X 81' 14' 27" W AL-49 32' 58' 40" N 849 240 X X 81* 21' 45" W AL-51 32' 02' 10" N 240 270 81* 22' 13" W
- See remarks C-33 E
M M M M M M TABLE NO. C-1 (SHEET 17B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION NELL WATER WATER A2 NCY NUMBER, LOCATION REPORT TEST LEVEL QUALITY REPORT REMARKS AL-36 32' 58' 45" N X Depth from gamma log, 81* 17' 14" W samples stored at SCWRSR AL-37 32' 45' 52" N X 81* 21' 29" W AL-3 8 32' 56' 53" N X Samples stored at 81* 26' 39" W SCWRSR AL-39 33' 04' 08" N X 81* 28' 37" W AL-40 33' 07' 18" N X Samples stored at 81* 33' 19" W SCWRSR AL-41 33' 04' 49" N X 81* 32' 12" W AL-44 32' 58' 50" N X 81* 17' 45" W AL-4 5 33' 02' 14" N
- 61* 17' 15" W AL-46 32' 59' 35" N X 81* 17' 50" W A L-4 7 32' 46' 39" N X X X Samples stored at 81* 22' 27" W SCWRSR AL-4 8 33' 05' 18" N X X X X X Sand analysis, log-81* 14' 27" W ging depth is 800 ft.
AL-49 32' 58' 40" N X X Samples stored at 81* 21' 45" W SCWRSR AL-51 32' 02' 10" N X Samples stored at 81* 22' 13" W SCWRSR C-34
TABLE NO. C-1 (SEEET 18A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER lELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL ELEVATION GEOLOGIST'S D RI LLE R 'S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RE SISTIVITY NEUTRON AL-5 2 33' 02' 10" N 330 270 81* 22' 13" W AL-5 3 33' 04' 34" N 783 200 80* 26' 45" W AL-5 4 33' 04' 34" N 200 80* 26' 45" W AL-5 5 32' 58' 56" N 220 81* 20' 39" W Al-56 32' 58' 55" N 220 81* 20' 42" W AL-57 32' 58' 40" N 240 81* 21' 58" W AL-58 32' 58' 22" N 240 81* 22' 03" W AL-59 32' 58' 12" N 200 81* 22' 50" W AL-60 32' 58' 19" N 220 81* 21' 48" W AL-61 32' 58' 20" N 220 81* 21' 32" W AL-62 32' 57' 52" N 280 81* 21' 38" W AL-6 3 33' 06' 54" N 220 81* 33' 13" W AL-6 4 33' 06' 29" N 170 81' 33' 51" W . C-35 EEEE BEERI
E E E E E TABLE NO. C-1 (SHEET ISB OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION NELL WATER WATER AGENCY NUMBER LOCATION REPORT TEST LEVEL QUALITY REPORT RE MARXS AL-52 33* 32' 10" N X 81* 22' 13" W AL-5 3 33* 04' 34" N X 80* 26' 45" W AL-5 4 33* 04' 34" N X 80* 26' 45" W AL-5 5 32' 58' 56" N X 81* 20' 39" W Al-56 32' 58' 55" N X 81* 20' 42" W AL-57 32* 58' 40" N X 81* 21' 58" W AL-58 32' 58' 22" N X 81* 22' 03" W AL-59 32' 58' 12" N X 81* 22' 50" W AL-60 32' 58' 19" N X 81* 21' 48" W AL-61 32' 58' 20" N X 81* 21' 32" W AL-6 2 32' 57' 52" N X 81* 21' 38" W AL-6 3 33* 06' 54" N X 81* 33' 13" W AL-64 33' 06' 29" N X 81* 33' 51" W C-36
TABLE NO. C-1 (SHEET 19A OF 80) INVENTORY OF EXISTING DRILL HOLE AND WATER lELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL ELEVATION CEOLOGIST'S DRI LLE R'S SP/ GAMMA / NUMBEa LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON AL-6 5 33* 06' 23" N 156.79 81* 34' 07" W 55" 800 202.23 X X X XX AL-6 6 33' 06' N 81* 33' 56" W AL-67 33' 06' 48" N 175 81* 34' 26" W AL-6 8 33* 05' 59" N 210 81* 32' 34" W AL-69 33* 05' 47" N 190 81* 32' 43" W AL-70 33' 05' 37" N 180 81' 32' -55" W AL-71 33' 04' 56" N 140 81* 32' 38" W AL-7 2 33' 04' 53" N 140 81* 32' 49" W AL-73 33' 04' 53" N 140 81' 32' 13" W AL-74 33' 04' 50" N 140 81* 32' 10" W AL-75 33' 05' 20" N 200 81' 31' 45" W AL-7 6 33' 05' 25" N 210 81* 31' 51" W AL-77 33' 05' 52" N 160 81' 30' 05" W C-37 m - M M M M M - m
m W W . m W W W W TABLE NO. C-1 (SHEET 19B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATE R WAE R AGENCY NUMBER LOCATION REPORT TEST LEVEL QUALITY REPORT REPARKS AL-65 33' 06' 23" N X 81* 34' 07" W AL-6 6 33* 06' 55" N X X Samples stored at 81* 33' 56" W SCWRSR AL-6 7 33* 06' 48" N X 81* 34' 26" W AL-68 33' 05' 59" N X 81* 32' 34" W AL-69 33' 05' 47" N X 81* 32' 43" W AL-70 33' 05' 37" N X 81* 32' 55" W AL-71 33* 04' 56" N X 81* 32' 38" W AL-72 33* 04' 53" N X 81* 32' 49" W AL-7 3 33* 04' 53" N X
, 81* 32' 13" W AL-7 4 33' 04' 50" N X 81* 32' 10" W AL-7 5 33* 05' 20' N X 81* 31' 45" W AL-76 33* 05' 25" N X 81* 31' 51" W AL-77 33' 05' 52" N X 81* 30' 05" W C-38
E
/ N AO MR MT AU S GE G N O
L L A C I Y S T Y I H V P /I O PT E SS E G I E L S B E A R A L T I A A D V A S L L A 'R T EG E A LO D LL ) RA I 8 EN R 8 TI D AL F WOR O DA A NC S 0 A H 'T 2 ET S LU I G T OO E HS GO OL E 9 H L 3 S L O ( LY I T E G C E 1 RN
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- 4 6 N F 0 3
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- E R D
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'27 01
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- 21 21 31 3'
38 1 21 38 31 38
'31 38
'21 38 21 38 21 38 21 38 p 38 38 38 38 38 se kd r
ad me et r r ep o R ee LE 8 9 0 3 5 6 7 8 9 0 1 2 3 SR LB 7 7 8 8 8 8 8 8 8 9 9 9 9 E M NU N L A A L L A L A L A L A L A L A L A L A L A L A L A
- E E
M TABLE NO. C-1 (SHEET 20B OF 88) IWENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDAIE COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUC"ICN E LL WATER WA'IE R AT NCY NUMEER LOCA*A . 'N HEPORr TEST LEVEL QUALITY REPORT EMARKS AL-78 33* 05' 54" d X 81* 30' 05" W AL-79 33' 05' 53" N X 81* 32' 26" W AL-80 32' 48' 03" N X 81* 18' 56" W AL-83 32' 48' 13" N X 81' 18' 44" W AL-8 5 33' 02' 18" N X X 81' 17' 22" W AL-8 6 33' 02' 43" N X X Depth cited is a 81* 17' 27" W measured depth AL-8 7 32' 02' 44" N X 81' 17' 46" W AL-88 33' 02' 39" N X 81' 17' 52" W AL-89 33' 02' 39" N X 81' 17' 56" W AL-90 32' 49' 24" N X 81* 21' 40" W AL-91 32' 49' 13" N X Bl* 21' 33" W AL-9 2 32* 48' 44" N X 81* 21' 46" W AL-93 32' 46' 39" N X 81* 21' 23" W C-40
TABM NO. C-1 (SHEET alA OF 88) INVENMRY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL ELEVATION GEOLOGIST'S DRILLE R 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON AL-94 32' 47' 54" N 90 81* 22' 01" W AL-95 32' 48' 30" N 100 81* 22' 23" W AL-96 32' 48' 55" N 110 81* 22' 31" W AL-97 32* 49' 09" N 110 81* 22' 18" W AL-98 32* 49' 07" N 120 18* 22' 52" W AL-99 32' 49' 47" N 110 81* 22' 12" W AL-100 32' 49' 45" N 110 81* 22' 24" W AL-101 32' 49' 59" N 115 81* 22' 11" W AL-102 32' 49' 53" N 140 81' 21' 45" W AL-103 32' 49' 49" N 150 81* 21' 28" W AL-104 32' 49' 47" N 130 81* 21' 57" W AL-105 32' 49' 37" N 120 81* 21' 58" W C-41 E E E E
~
S K R A M E R YT CR M NO EP X X X X X X X X X X X X GE AF A T A D lI lI L L Y E T W E RI L EL
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C NGC LT O .I E LS N TL SA EE h T I D MXN E EE L A FL T OA Y N R O O I T TT N CR E UO V RP N TE I SR N O C NW NW NW NW NW NW NW NW NW NW NW NW "4 "1 03 "51 "9 "8 7 2" 72 5 "4 91 3 "5 "9 "8 77 78 N 50 32 53 01 05 41 42 51 54 42 45 35 O I T ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' ' A 72 82 82 92 92 92 92 92 91 91 91 91 C 42 42 42 42 42 42 4 2 42 42 4 2 42 42 O L 21 21 21 21 21 21 21 21 21 21 21 21 38 38 38 3 8 38 38 38 38 38 38 38 38 R 0 1 2 3 4 5 L LI E 4 9 5 9 6 9 7 9 8 9 9 9 0 1 0 1 0 1 0 1 0 1 0 1 M - - - - - - - - - - - - EU N L A L A L A L A L A L A L A L A r A L A L A L A
TABLE NO. C-1 (SHEET 22A OF 80) INVENTORY OF EXISTING DRILL HOLE AND WATER BELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL ELEVATICN GEOLOGIST ' S DRI LLER 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG IESISTIVITY NEUTRON AL-106 32' 49' 23" N 100 81* 22' 12" W AL-109 33' 07' 21" N 210 81* 33' 05" W AL-lli 33' 07' 14" N 230 81* 33' 10" W AL-ll3 32' 07' 15" N 240 81* 33' 30" W AL-ll4 32' 07' 08" N 220 81* 33' 05" W AL-120 32* 57' 32" N 220 81* 21' 40" W AL-132 33* 04' 02" N 150+ 110 81* 28' 35" W AL-141 33* 02' 45" N 125 260 81* 26' 43" W AL-156 33' 05' 42" N 590 190 81* 28' 30" W AL-165 33' 05' 51" N 275 170 81* 30' 47" W AL-209 33' 06' 05" N 73 190 81* 30' 31" W AL-211 33' 06' 33* N 108 250 81* 29' 28" W AL-251 33' 08' 30" N 320 81* 31' 30" W AL-268 33* 05' 50" N 175 81* 30' 18" W C-4 3
S K R A M E YT CR NO X X X X X X X X X X X X X X EP GE AR A T A D L L Y T E E RI L EL
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'31 38 31 38 31 38 31 38 31 38 31 38 R 6 9 l 3 4 0 2 1 6 5 9 1 1 8 L 0 0 l l l 2 3 4 5 6 0 1 5 6 LE M 1
1 l l l 1 1 1 1 1 2 2 2 2 EU N L A L A L A L A L A L A L A L A L A L A L A L A L A L A
TABLE NO. C-1 (SHEET 23A OF 88) INVENERY OF EXISTING DRILL HOM AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS W.LL ELEVATION GEOLOGIST'S DRI LLE R'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON AL-269 33' 05' 30" N 120 81* 30' 42" W AL-270 33' 05' 52" N 170 81* 30' 51" W AL-271 33* 05' 51" N 500+ 170 81* 30' 47" W AL-272 33* 05' 41" N 240 15 81* 29' 32" W AL-273 33' 08' 30" N 320 81* 31' 30" W AL-274 33* 00' 18" N 190 81* 19' 50" W AL-275 33' 04' 35" N 160 81* 13' 12" W AL-276 33' 04' 50" N '360 81* 13' 20" W AL-277 33' 04' 20" N 160 81* 13' 10" W AL-279 33' 03' 22" N 140 81* 12' 48" W AL-280 33' 03' 30" N 140 Bl* 12' 49" W AL-281 33' 03' 22" N 140 81* 12' 48" W AL-282 33' 03' 22" N 140 81* 12' 48" W AL-263 33' 04' 37" N 620 160 81* 12' 32" W ___. C-4 5 m W W
M S X R A M E M M YT CR M NO EP X X X X X X X X X X X X X X A GE A T A D M L Y L T E E RI L EL
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_M 5 6 7 9 0 1 2 3 R 9 0 1 2 3 4 8 8 8 8 LE LI 6 2 7 2 7 2 7 2 7 2 7 2 7 2 7 2 7 2 7 2 2 2 2 2 M - - - - - - - - - - - - - - EU L L L L L L L L L L L L L L N A A A A A A A A A A A A A A
1 ABLE NO. C-1 (SHEET 2 4 A OF 88 ) INVENTORY OF EXISTING DRILL HOLE AND WATER 1 ELL DATA ALENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WELL ELEVATION GEOLOGIST'S DRILLE R' S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON AL-284 33' 04' 37" N 165-185 160 81* 12' 32" W AL-285 33* 04' 37" N 160 81* 12' 32" W AL-286 33' 05' 32" N 160 81* 13' 03" W AL-289 33' 02' 43" N 290 250 81* 26' 48" W AL-290 32' 55' 13" N 120 81* 25' 23" W AL-291 32' 55' 30" N 60-70 130 81' 25' 50" W AL-292 33' Ol' 12" N 200 140 81* 13' 21" W AL-295 33' 03' 04" N 140 81* 08' 56' W AL-296 33' 02' 55" N 150 200 81* 18' 59" W AL-297 33' 02' 55" N 200 81* 18' 59" W AL-298 illegible N 1030 140 81* 20' 34" W AL-299 32' 57' 28" N 315 60 81' 26' 42" W AL-300 33' Ol' 23" N 140 81* 15' 02" W AL-301 33' 02' 27" N 340 230 81* 21' 52" W C-47 E E - E E E
M t a d S e K r R o A t M s E s eR l S pR mW aC SS M YT CR NO X X X X X X X X X X X M E P GE AR A T A D L L Y T E E RI L EL
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O C NW NW NW NW Nh NW NW NW NW NW NW NW NW NW 72 72 2 "3 3 "8 33 00 21 "46 59 59 4 82 32 72 N 33 33 30 4 4 12 35 12 05 55 55 3 24 20 25 O I e T ' ' ' ' ' ' ' ' ' ' ' ' l' ' ' ' A 4 2 4 2 '5 '3 2 6 '5 '5 '5 '5 13 38 28 '2 '8 b0 76 l '5 '2 '1 C 01 01 01 02 52 52 01 00 01 01 i 2 52 O1 02 O g L e
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- 31 3' 1 3 1 3' 1 2 1' 21 31 3' 1' 31 31 l1 21 31 3' 1 M 38 36 38 38 3 8 38 38 38 38 38 i 8 38 3 8 38 R 4 5 6 9 0 1 2 5 6 7 8 9 0 1 LE 8 8 8 8 9 9 9 9 9 9 9 9 0 0 LB 2 2 2 2 2 2 2 2 2 2 2 2 3 3 M - - - - - - - - - - - -
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L L A M C I Y S T Y I H V P /I O PT E SS E G I L S B B A R A L T I A A D V A S L L A 'R T EG E A LO ) RA D LL I R M 8 EN D 8 TIAL F WOR O DA S M A NC 5 A 2 H 'T ET S LU I G T E HS OO GO OL E 9 H L , S LY ( L O E 4 C
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D NW NW NW NW NW NW NW NW NW NW NW NW NW NW 98 2 "8 2 "8 1 "0 31 7 "9 52 "51 "
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8 "8 "2 "7 "31 N 4 4 11 11 22 22 21 53 53 00 50 05 40 4 4 42 O I '
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- M 21 31 31 '21 38
'21 38 21 38 21 38
'21 38 31 38 31 38 38
'3 1' 38 31 38 31 38 38 38 38 s
k r a m M e r R 2 3 4 5 6 7 8 9 0 1 2 3 4 6 LE 0 0 0 0 0 0 0 0 1 1 1 1 1 1 e e LB E M WU 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L 3 L
- S M N A A A A A A A A A A A A A A
- E E E E E E E E E TABLE NO. C-1 (SHEET 25B OF 88)
INVEN'IORY OF EXISTI!G DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE hdLL CONSTRUCTION NELL WATER WYDER AGE NCY NUMIER LOCATION 1EPORT TEST LEVEL QUALITY REPORT BEMARXS AL-3 0 2 32' 56' 49" N X 81* 17' 48" W AL-303 33* 05' 12" N X 81' 20' 18" W AL-30 4 33* 05' 12" N X X 81* 20' 18" W AL-3 0 5 32' 55' 21" N X 81* 14' 20" W AL-306 32' 55' 23" N X 81* 14' 21" W AL-307 32' 55' 27" N X 81* 14' 19" W AL-308 32* 58' 55" N X X 81* 18' 32" W AL-3 0 9 32' 58' 55" N X 81* 18' 31" W AL-310 33* Ol' 08" N X Test hole depth - 239 f t, 81* 18' 07" W samples stored at SCWRSR AL-311 33' 57' 56" N X 81* 14' 02" W L-312 33' 02' 02" N X X 81* 16' 52" W AL-313 33' 05' 48" N X X 81* 25' 08" W AL-314 33* 05' 42" N X X 81* 25' 47" W AL-316 33* 03' 43" N X X 81* 17' 21" W C-50
TABM NO. C-1 (SHEET 26A OF 88) INVENTORY OF EXISTING DRILL HOM AND WATER ELL DATA ALENDAM COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL E MVATION GEOLOGIST'S DRI LLER'S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG EESISTIVITY NEUTRON AL-317 33* 05' 56" N 230 97.12 81* 36' 06" W New Googe Googe Street, City Street of Allendale Sandoz 01 33* 02' 23" N 790 186.5 X X 81* 29' 18" W SCGS AL-1 33* 04' 52" N 65 145 X 81* 33' 44" W SCGS AL-2 33* 04* 59" N 45 150 X 81' 34' 29" W SCCS AL-3 33' 05' 0:" N 10 150 X 81* 34' 30" W SCGS AL-10 NE/4 of Peepples 75 90 X 15' Quad
- SCGS Al-15 32' 50' 56" N 50 80 X 81' 24' 21" W S'GS AL-16 32' 55' 42" N 65 70 X 81* 29' 16" W SCGS AL-17 32' 55' 48" N 70 90 X 81' 28' 30" W SCGS 33* 04' 43" N 90 140 X Dunbar 84 81* 33' 18" W SCGS 33' 04' 26" N 40 92 X Dunbar 414 81* 34' 13" W SCGS NE/4 of Millet 60 140 X Dunbar #15 7.5' Quad.*
SCGS 33' 03' 08" N 64 82.8 X McNa ir 8 3 81* 30' 12" W l
- See remarks C-51 E -
M M M M M M M
M M M M M M M M M M TABLE NO. C-1 (SEEET 25B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDA 2 COUNTY, SOUTH CAROLINA DATA AVAILABLE WELL CONSTRUCTION WELL WATER WATER AGENCY NUMBER LOCATION REPORT TEST LEVEL QUALITY REPORT REMARKS AL-317 33' 05' 56" N Boring log 81* 36' 06" W New Googe Googe Street, City X X ** Street of Allendale Sandoz el 33' 02' 23" N Same location as AL-27; 81* 29' 18" W depth f rom E-log SCGS AL-1 33' 04' 52" N 81* 33' 44" W SCGS AL-2 33* 04' 59" N 81* 34' 29" W , SCGS AL-3 33' 05' 05" N 81* 34' 30" W SCGS AL-10 NE/4 of Peepples On dirt road 2.3 mi. 15' Quad
- SE o f Ba r ton *
- SCGS Al-15 32' 50' 56" N 81* 24' 21" W SCGS AL-16 32' 55' 42" N 81* 29' 16" W SCCS AL-17 32' 55' 48' N 81* 28' 30" W SCCS 33' 04' 43" N Dunbar 44 81* 33' 18" W SCGS 33' 04' 26" N Dunbar #14 81* 34' 13" W SCCS NE/4 of Millet Same location as SCCS Dunbar $15 7.5' Quad.* Dunbar $3**
SCGS 33' 03' 08" N X McNa ir 4 3 81* 30' 12" W
- See remarks
** Not shown on Figure 7-1 C-52
TABLE NO. C-1 (SEEET 27A OF 88) INVENMRY OF EXISTING DRILL HOIE AND WATER ELL DATA BAMDERG COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL ELEVATION GEOLOGIST'S DRI LUS R'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON Ba m-1 33* 19' 14" N R240 244 81* 08' 39" W Bam-2 33* 19' 26" N R240 248 81* 08' 38" W Bam-3 33' 19' 22" N R240 248 81' 08' 39" W Ba m-6 32' 17' 45" N 584 170 X 81* 02' 15" W Ba m-7 33* 17' 45" N 435 170 X X 81' 02' 15" W Ba m-8 33* 17' 15" N 160 150 81* 02' 23" W Ba m-9 33' 05' 42" N 596 120 81* 00' 43" W Bam-10 33' 05' 50" N 596 146 81* 00' 50" W Ba m-14 33' 18' 59" N R473 244 X 81* 08' 45" W Ba m-15 33' 17' 42" N R200 120 81* 02' 14" W Ban-16 33* 17' 45" N 195 120 81* 02' 14" W Ba m-18 33' 18' 11" N R284 220 X X 81* 08' 35" W Ba m-19 33' 17' 45" N 500-550 170 X X 81' 02' 15" W C-53 M M M M M M M M M
m M M M M M M M M M TABLE NO. C-1 (SHEET 27B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ALLENDALE COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGENCY NUMBER LOCATION REPORT TEST LEVE L QUALITY REPORT REMARKS Ba m-1 33' 19' 14" N X X 81* 08' 39" W Ba m-2 33* 19' 26" N X 81* 08' 38" W Ba m-3 33* 19' 22" N X X 81' 08' 39" W Ba m-6 32* 17' 45" N X X Caliper log ** 81* 02' 15" W Bam-7 33' 17' 45" N X X Fluid, temperature, and 81* 02' 15" W caliper logs ** Ba m-8 33' 17' 15" N X ** 81' 02' 23" W Ba m-9 33' 05' 42" N X X ** 81' 00' 43" W Ba m-10 33* 05' 50" N X ** 81* 00' 50" W Ba m-14 33* 18' 59" N X X X Sanitary survey 81* 08' 45" W Ba m-15 33' 17' 42" N X ** 81* 02' 14" W Ba m-16 33' 17' 45" N X X ** 81' 02' 14" W Ba m-18 33' 18' 11" N X X X ** 81* 08' 35" W Ba m-19 33' 17' 45" N X Fluid, temperature, and 81* 02' 15" W caliper logs **
** Not shown on Figure 7-1 C-54
TABLE NO. C-1 (SHEET 28A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WA'IT.R ELL DATA BAMBERG COUNTY, SOU'M CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS HE LL E LE'v ATION GEOLOGIST'S DRILLER 'S SP/ GAMMA / NUMBER LOCATION DEPTH (PT.) (FT.) LOG LOG RESISTIVITY NEUTRON Bam-20 ??' 17' 43" N 399 170 ol* 02' 15" W Bam-21 33' 17' 45" N 169 170 X 81' 02' 15" W Bam-2 2 33' 18' 56" N 302 220 X X X 81* 08' 20" W Bam-23 33' 19' 27" N R296
- 244 X X X 81* 08' 25" W Bam-24 33' 17' 15" N 551* 147 X X 81* 02' 15" W Ba m-2 5 33' 13' 19" N R250 240 X X 81* 10' 21" W Ba m-26 33' 06' 05" N 400 140 X X 81* 00' 41" W Bam-27 33' 17' 15" N 550 147 X X 81* 02' 25" W Bam-28 33' 19' 56" N R34 0
- 260 X X 81* 11' 17" W Ba m-29 33' 13' 20" N RISO 240 81* 10' 30" W Bam-30 33' 05' 40" N 120 81* 00' 45" W Bam-31 33* 17' 46" N 176 120 X 80* 02' 13" W Bam-34 33' 13' 15" N R175 200 80* 07' 49" W
- See remarks C-55 E E E E E E E E E E E E E
^
TABIE NO. C-1 (SHEET 28B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA BAMIERG COUNTY, SOUTH CAROLINA DATA AVAILABLE lELL CONSTRUCTION ELL WA1TR WATER AGENCY NUMIER LOCATION REPOIC TEST LEVEL QUALITY REPORT REMARXS Bam-20 33' 17' 43" N X ** 81* 02' 15" W Ba m-21 33' 17' 45" N X Caliper log ** 81' 02' 15" W Bam-22 33* 18' 56" N X X X X ** 81* 08' 20" W Bam-23 33' 19' 27" N X X X X Total depth is 310 ft, 81* 08' 25" W sanitary survey Bam-24 33' 17' 15" N Depth from gamma log, Pl* 02' 15" W ** Ba m-2 5 33' 13' 19" N X X X X 81* 10' 21" W Ba m-2 6 33* 06' 05" N X X X X Sand analysis performed 81' 00' 41" W ** Ba m-2 7 33' 17' 15" N X Sample stored at 81' 02' 25" W SCWRSR** Bam-28 33' 19' 56" N X X Completed depth 500 ft, 81* 11' 17" W sample stored at SCWRSR Ba m-29 33' 13' 20" N X 81' 10' 30" W Ba m-3 0 33' 05' 40" N X ** 81* 00' 45" W Bam-31 33' 17' 46" N X X X ** 80' 02' 13" W Ba m-3 4 33* 13' 15" N X X 80' 07' 49" W
** Not shown on Figure 7-1
)
C-56
TABLE NO. C-1 (SHEET 29A OF 98) IN'ENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA BAMBERG COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS 1CLL EIEVATION GEOLOGIST'S DRI LLER 'S SP/ GAMMA / h0MBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON Bam-36 33' 04' 35" N R220 131 81* 06' 53" W Bam-37 33" 11' 15" N 144 81* Ol' 15" W Bam-38 33' 11' 07" N R300 143 80* 55' 58" W Ba m-4 0 33' 11' 19" N 147 80* 53' 32" W Bam-41 33* 17' 39" N 210 81* 11' 35" W Bam-42 33' 22' 26" N R140 194 81* 07' 04" W Bam-43 33' 07' 52" N R16 5+ 126 80* 55' 35" W Bam-45 33' 08' 30" N 175 81* 09' 30" W Ba m-49 33' 22' 04" N 500 260 81* 11' 22" W City of City of Denmark 470 X Denmark A City of City of Denmark Denmark B City of City of Denmark 300 Denmark C City of City of Denmark 340 X Denmark D City of City of Denmark Denmark E
- See remarks C-57 E E E E E E
E E E E E E E E E E E E TABM NO. C-1 (SHEET 29B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA EAMIERG COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGENCY NUMIER LOCATION REPORT TEST EVEL QUALITY REPORT REMARKS Ba m-3 6 33' 04' 35" N X X 81* 06' 53" W Bam-37 33' 11' 15" N X X ** 81* Ol' 15" W Ba m-3 8 33' 11' 07" N X X ** 80* 55' 58" W Ba m-4 0 33' 11' 19" N X X ** 80' 53' 32" W Ba m-41 33' 17' 39" N X X 81* 11' 35" W Ba m-4 2 33' 22' 26" N X X 81* 07' 04" W Bam-4 3 33' 07' 52" N X X ** 80* 55' 35" W Ba m-4 5 33' 08' 30" N X Sample stored at 81* 09' 30" W SCWRSR Bam-49 33' 22' 04" N X X 81* 11' 22" W City of City of Denmark X X ** Denmark A City of City of Denmark Installation report ** Denmark B City of City of Denmark X X ** Denmark C City of City of Denmark ** Denmark D City of City of Denmark
- X Behind Denmark ware-Denmark E house, installation report **
- See remarks
** Not shown on Figure 7-1 C-58
TABLE NO. C-1 (SKEET 30A OF 88) INVENTORY OF EX2STZNG DRILL HOLE AND WATER ELL DATA BARNNELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL ELEVATION GEOLOGIST'S DRILLER'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON B-36 33' 09' 54" N X 81* 43' 32" W B-45 33* 11' 54" N 81' 41' 54" W Blackville Town of Blackville 470 fl
- B W-2 33' 14' 38" N R200 220 81* 21' 17" W B W-3 33' 14' 38" N R180 220 81* 21' 17" W BW-4 33' 14' 38" N 180-185 220 81* 21' 17" W B W'S 33' 21' 18" N 200 81* 16' 20" W B W-6 33' 21' 14" N 350 290 81* 16' 12" W BW 7 33* 21' 30" N(?) 300+
81* 16' 45" W B W-8 Town of Williston* 150 Bhh9 33' 24' 15" N 150 81* 24' 50" W ___BW-10 33* 24' 05" N 150 81* ?4' 45" W B W-ll Barnwell Air Base 200 231 B W'-12 North side of ice plant
- Bhbl3 33' 14' 38" N 165 220 81* 21' 17" W
- See remarks C-59 m '
m m m m M . W W m m m m
m m m W ' W m m m m m m M M TABLE NO. C-1 (SHEET 30B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNELL COUNTY, SOUTH CAROLINA l DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGENCY NLHIER LOCATION REPORT TEST LEVEL QUALITY REPORT REMARKS B-36 33' 09' 54" N 81* 43' 32" W B-45 33' 11' 54" N 81* 41' 54" W Black ville Town of Blackville X X X Under water tank near
#1
- railroad **
BW-2 33* 14' 38" N X X 81* 21' 17" W BW-3 33* 14' 38" N X X 81* 21' 17" W BW-4 33* 14' 38" N X 81* 21' 17" W B W-5 33* 21' 18" N X 81* 16' 20" W B W-6 33* 21' 14" N X 81* 16' 12" W BW-7 33* 21' 30" N(?) X 81* 16' 45" W B W-8 Town of Williston* X West of tank ** B W-9 33* 24' 15" N X X 81* 24' 50" W B W-10 33* 24' 05" N X X 81* 24' 45" W BW-ll Barnwell Air Base X ** BW-12 North side of X West of railroad ice plant
- tracks **
B W-13 33* 14' 38" N X X 81* 21' 17" W
- See remarks
** Not shown on Figure 7-1 C-60
TABLE NO. C-1 (SHEET 31A OF 88) INVENTORY Ol' EXISTING DRILL HOLE AND WATER NELL DATA BARNKELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL EIEVATION GEOLOGIST'S DRILLER'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON BW-14 Town of Barnwell* 160 BW-15 North side of 200 plant
- B W-16 Town of Barnwell 145-150 BW-17 Elko public school 24 BW-19 Town of Dunbarton* 137 B W-20 33' 11' 50" N 217 120 81* 43' 20" W BW-21 Town of Dunbarton BW-24 0.3 mi. S of EC-40 196 250 0.3 mi. SW of SC-54 BW-2 5 Williston dorms
- 142 355 BW-26 Town of Blackville 306 350 BW-28 0.95 mi. south of 68 210 SC-6 4 on SC-3 BW-30 Old section houses 95 270 at Ashleigh*
BW-31 Ritz drive-in 140 240 theater
- See remarks C-61 E E E E E E E E E E E
M M M M M M M M TABLE NO. C-1 (SHEET 31B OF 88) INVENIORY OF EXISTING DRILL HOLE AND WATER NELL DATA BARNELL COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGENCY NUMIER LOCATION REPORT 'ITST LEVE L QUALITY REPORT REMARXS BW-14 Town of Barnwell* X 20 ft SE of reservoir ** BW-15 North side of X Near railroad plant
- tracks **
BW-16 Town of Barnwell X 10 ft north of reservoir ** BW-17 Elko Public School X ** BW-19 Town of Dunbarton* X 2 blocks south of railroad tracks ** BW-20 33* 11' 50" N X X 81* 43' 20" W BW-21 Town of Dunbarton X ** BW-2 4 0.3 mi. S of SC-40 X ** 0.3 mi. SW of SC-54 BW-25 Williston dorms
- X 1.75 mi. west of Rt-39 at Williston on US-78**
BW-2 6 Town of Blackville X ** BW-2 8 0.95 mi. south of X ** SC-64 on SC-3 BW-30 Old section houses X Southern sailroad at Ashleigh* Barnwell and Blackville** BW-31 Ritz drive-in X ** theater
- See remarks
** Not shown on Figure 7-1 C-62
TABLE NO. C-1 (SHEET 32A OF 88) INVENTORY OF EXISTING DRILL HOLE AND KATER M:LL DATA BARNhELL COUNTY, SOUTH CAROLINA DATA AVAILABLE _ SURFACE CEOPHYSICAL LOGS NE LL ELEVATION GEOLOGIST'S DRI LLE R'S SP/ GAPJ1A/ NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON BW-32 Schumport store
- 80 340 BW-3 3 0.85 mi. east of 85 244 SC-3 on T-78 BW-3 4 1.9 mi. south of 98 220 Salrathie Rur on T-7 3 BW-3 5 0.45 mi. SE of 98 320 Rt. 39 on SC-163 B W-3 6 On SC Rt. 39 approx. 340 3.75 mi. south of US-78 BW-3 7 East of Dunbarton 136 BW-38 Tri Ct. across BW Co. 130 220 Airport, on Elko Rd.*
BW 39 33* 14' 17" N 230 215.7 X 81* 21' 54" W B W-4 0 33' 09' 20" N 960 240 81* 16' 20" W BW-41 33* 21' 55" N 290 280 l 81* 19' 44" W I BW-4 2 33' 21 ' 55" N 270 280 l 81* 19' 44" W BW-4 3 33* 21' 26" N 250 300 81* 18' 04" W I
- See remar ks i
t C-63 M M M M M M - M M M M
E E E E i i TABLE NO. C-1 (SHEET 32B OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNELL COUNTY, SOUTH CAROLINA i l DATA AVAILABLE ELL CONSTRUCTION ELL WATER WA'IE R AGENCY NUMEER LOCATION REPORT TEST IEVEL QUALITY REPORT REMARKS BW-3 2 Schumpart store
- X East of Elko on US-78**
BW-33 0.85 mi. east of X ** SC-3 on SC-7 8 BW-3 4 1.9 mi. south of X ** Salrathie Rur on SC-73 BW-3 5 0.4 5 mi. SE pf Rt. 39 X ** on SC-163 BW-3 6 On SC Rt. 39 approx. X ** 3.75 mi. south of US-78 BW-3 7 East of Dunbarton X By railroad tracks ** BW-38 Tri Ct. across BW Co. X 1.1 mi. N Air por t , on El ko Rd .
- intersection on Elko Rd.* W SC-64,**
BW-3 9 33* 14' 17" N X X X 81* _21' 54" W BW-4 0 33' 09 ' 20" N X X Al* 16' 20" W BW-41 33* 21' 55" N X X 81* 19' 44" W BW-4 2 33* 21' 55" N X 81* 19' 44" W BW-4 3 33* 21' 26" N X 81* 18' 04" W
- See remarks
** Not shown on Figure 7-1 C-64
TABLE NO. C-1 (SHEET 33A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNhELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL E LEVATION GEOLOGIST'S DRILIE R 'S SP/ GAPJtA/ NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG IESISTIVITY NEUTRON BW-44 33' 24' 08" N 820 352 X X 81* 24' 53" W BW-45 33' 14' 25" N 246 220 81* 22' 58" W BW-46 33* 21' 22" N R246 290 81* 16' 19" W BW-47 Barnwell dorms
- 230 BW-4 9 2.5 mi. NW of 112 280 Rt. 39' BW-50 0.65 mi. west of 112 T-3 3 or. T-ll2 B W-51 33' 12' 36" N R4007 160 81* 21' 59" W BW-5 2 Owens Rd., City R176 of Barnwell BW-5 3 0.2 mi. seauth 84 on Woids Rd.*
BW-5 4 33' 24' 45" N 136 350 81* 25 ' 00" W BW-5 5 33' 14* 10" N 280 150 X 81* 21' 54" W B W-5 6 33' 3 4 ' 06" N 285 150 X Bl* 22' 06" W
- See remarks C-65 E E E E E E
M M - M M M TABLE NO. C-1 (SHEET 33B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA BARNhELL COUNTY, SOUTH CAROLINA DATA AVAILABLE WELL CONSTRUCTION lELL WATE R WATE R AGENCY' NUMBER LOCATION REPORT TEST IEVEL QUALITY REPORT REMARKS BW-4 4 33* 24' 08" N X X X X X 81* 24' 53" W BW-4 5 33* 14' 25" N X X Gl* 22' 58" W BW4 6 33* 21' 22" N X 81* 16' 19" W BW-4 7 Barnwell dorms
- X 1.3 mi. south of SC-64 on side road 0.4 mi. west of SC-3**
BW-49 2.5 mi. NW of X At Williston Rd., Rt. 39* north side of railroad track s*
- BW-50 0.65 mi. west of X **
SC-3 3 on SC-112 BW-51 33' 12' 36" N X 81* 21' 59" W BW-5 2 Owens Rd., City X ** of Barnwell BW-53 0.2 mi. south X 0.2 mi. east of or. Woids Rd.
- Stringefellow Gallon SC-62**
BW-54 33* 24' 45" N X X 81* 25' 00" W B W-5 5 33* 14' 10" N X X 81* 21' 54" W BW-5 6 33* 14' 06" N X X X X 81* 22' 06" W
- See remarks
- Not shown on Figure 7-1 C-66
TABLE NO. C-1 (SEEET 34A OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WATER lELL DATA BARNWELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SU RFACE GEOPHYSICAL LOGS WE LL E LEVATION GEOLOGIST'S DRILLE R 'S SP/ GAMMA / NUMBER LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON B W-57 33* 14' 10" N 336 190 X 81* 22' 45" W B W-58 33* 14' 43" N 345 230 81* 21' 05" W B W-5 9 33* 13' 58" N 252 150 X 81* 21' 48" W BW-60 33* 14' 07" N 330 150 X 81* 21' 59" W B W-61 Barnwell Mills, 0.2 343 X mi. behind water tank B W-6 2 33* 13' 38" N 271 X 81* 21' 40" W BW-6 3 City of Barnwell BW-64 33* 21' 10" N 184 285 81* 19' 20" W BW-65 City of Barnwell 85 BW-66 33* 13' 59" N 262 150 61* 21' 57" W BW-6 8 33' 15' 40" N 81* 29' 10" W B W-6 9 Town of Hilda 338 B W-7 0 33* 15' 15" N 886 X Bl* 28' 25" W C-67 m . M M
m ~ M TABLE NO. C-1 (SHEET 34B OF 88) INVEN70RY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNWELL COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGENCY NUMIER LOCATION REPORT TEST LEVE L QUALITY REPORT REMARXS BW-5 7 33* 14' 10" N X X X X 81* 22' 45" W BW-5 8 33' 14' 43" N X 81* 21' 05" W BW-59 33' 13' 58" N X X X X 81' 21' 48" W BW-60 33' 14' 07" N X X X X 81* 21' 59" W BW-61 Barnwell Mills, 0.2 X X X ** mi. behind water tank BW-6 2 33* 13' 38" N X X X 81* 21' 40" W BW-6 3 City of Barnwell X X ** BW-64 33' 21' 10" N X X 81* 19' 20" W BW-6 5 City of Barnwell X ** B W-6 6 33' 13' 59" N X 81* 21' 57" W BW-6 8 33' 15' 40" N X 81* 29' 10" W BW-6 9 Town of Hilda X ** BW-70 33' 15' 15" N 81* 28' 25" W
*
- Not shown on Figure 7-1 C-68
TABLE NO. C-1 (SHEET 35A OF 88) INVENMRY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNWELL COUNTY, SOUTH CAROLINA l DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL ELEVATION :EOLOGIST'S DRI LLER 'S SP/ GAP W NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON BW-71 33* 15' 30" N 81* 28' 45" W BW-7 5 32* 21' 40" N 465 293 X X X 81* 15 40" W BW-7 6 0.04 mi. east of 255 X X X P coordinates
- BW-7 7 City of Barnwell 312 X B W-78 26 ft S of West St., 808* X X 41 f t E of Elko St.
BW-79 33* 24' 05" N 785* X X 81* 24' 24" W BW-80 33* 22' 46" N 140 345 81* 22' 49" W ____. BW-81 33* 24' 46" N 350 81* 22' 49" W BW-8 2 33* 15' 53" N 34 248 81* 27' 06" W BW-8 3 33* 21' 25" N 367 X X X (14 5) 81* 16' 33" W BW-8 4 33* 21' 02" N 315 290 X 81* 18' 52" W BW-8 9 33* 15' 18" N 41.5 238 81* 27' 13" W B W691 33* 15' 55" N 61.5 262.8 X 81* 27' 46" W
- See remarks C-69
E TABLE NO. C-1 ' SHEET 35B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNE LL COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL HATER WATER ATNCY NUMBER LOCATION EPORT TEST LEVEL QUALITY REPORT EMARKS BW-71 33* 15' 30" N X 81* 28' 45" W BW-7 5 32* 21' 40" N X X X X X 81* 15' 40" W BW-7 6 0.04 mi. east of South 1012 - West P coordinates
- 403 (BNF**
coordinates) B W-7 7 City of Barnwell* X Under water tank ** BW-7 8 26 ft S of West St., Depth from gamma 41 f t E of Elko St. 10a** BW-7 9 33' 24' 05" N Depth from gamma 81* 24' 24" W log BW-80 33' 22' 46" N X X X 81* 22' 49" W BW-81 33' 24' 46" N X 81' 22' 49" W BW-8 2 33' 15' 53" N X X X 81* 27' 06" W BW-8 3 33' 21' 25" N X X X (145) 81* 16' 33" W BW-8 4 33' 21' 02" N X X X Sample stored at 81* 18' S2" W SCWRSR BW-89 33' 15' 18" N X X X 81* 27' 13" W BbF91 33' 15' 55" N X X Sample stored at 81* 27' 46" W SCWRSR
- See remarks
** Not shown on Figure 7-1
- Barnwell Nuclear Fuel Plant C-70
TABLE NO. C-1 (SEEET 36A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER NELL DATA BARNWELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL E LEVATION GEOLOGIST'S D RI LLE R ' S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON BW-9 9 33* 15' 38" N 308 251.4 81* 27' 48" W BW-106 33' 20' 12" N R80-100 310 81* 19' 46" W B W-107 33' 20' 46" N 79 290 81* 15' 46" W : BW-10 8 33* 20' 28" N 300 81* 18' 55" W l B W-10 9 33* 20' 45" N 290 81* 18' 25" W B W-111 33* 21' 30" N 295 81* 18' 45" W BW-13 6 33* 15' 34" N l 32.5 247.5 81* 27' 48" W I BW-14 5 33* 21' 25" N l 410 X X X 81* 16' 15" W l City of 33* 16' 35" N 330 Hilda 81* 14' 45" W C-5 33* 14' 59" N a pprox. appr ox . 81* 40' 16" W 250 283 D-15 33* 12' 12" N approx. approx. 81* 43' 33" W 150 135 D RB-9 33* 15' 00" N approx, approx. X 81* 36' 58" W 2700 300 DRB-10 33* 12' 15" N 1280 X 81* 34' 48" W
- Se e r e mar k s C-71 E E
E E ' E TABLE NO. C-1 (SREET 36B OF 88) INVENTORY OF EXISTItG DRILL HOLE AND WATER NELL DATA BARNELL COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATER AGENCY N UM BE R LOCATION REPORT TEST LEVE L QUALITY FEPORT RE MARKS BW 99 33* 15' 38" N X X 81* 27' 48" W BW-106 33' 20' 12" N X 81' 19' 46" W BW- 107 33* 20' 46" N X X X 81* 15' 46" W B W-108 33' 20' 28' N X 81* 18' 55" W BhF109 33* 20' 45" N X 81* 18' 25" W BW-lli 33' 21' 30" N X 81' 18' 45" W BW-13 6 33* 15' 34" N X X X 81* 27' 48" W BhF14 5 33' 21' 25" N X X X X X Sand analysis 81* 16' 15" W City of 33' 16' 35" N X Hilda 81* 14' 45" W C-5 33* 14' a
'9" N Approximate location 81* 40' 16" W given, graphic log D-15 33' 12' 12" N Approximate location 81* 43' 33" W qiven, graphic log D RB-9 33* 15' 00" N X X Sample analysis by thin 81* 36' 58" W section and X-ray diffraction DRB-10 33* 12' 15" N Sample analysis by 81* 34' 48" W x-ray diffraction
- See remarks C-72
TABLE NO. C-1 (SHEET 37A OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA PARNELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SU RFACE GEOPHYSICAL LOGS WE LL E LEVATION GEOLOGIST'S DRI LLE R 'S SP/ GAMMA / N UMBE R LOCATION DE PTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON D RB-ll 33* 13' 18" N 1012 X 81* 35' 42" W DU-4 2 33* 12' 44" N R80-100 81* 43' 51" W* DU-4 7 33* 12' 31" N 79 81* 43' 14" W* H-12 33* 13' 26" N 81* 35' 48" W K-5 33* 13' 02" N approx. a ppro x . 81* 39' 57" W* 350 273 LA-2 33* 12' 15" N 573 128 X 81* 44' 26" W LA-3 33* 14' 49" N 575 290 X 81* 38' 56" W LA-33 33* 12' 27" N 644 297 X 81* 39' 29" W PG-4 33* 13' 08" N 413 321 81* 34' 05" W Ph2-2 33' 11' 50" N 81* 45' 18" W* P-5 33* 13' 34" N approx . appr o x. 81* 34' 58" W* 270 316 P-15 33* 13' 23" N 81* 34' 50" W* P-5R 33* 08' 57" N 1312.9 207.95 X X 81* 36' 57" W
- Se e r e na r k s C-73 M M M M '
m m m m M TABLE NO. C-1 (SEEET 37B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WMER ELL DATA BARN) ELL COUNTY, SOUTH CAROLINA DATA AVAILABLE WELL CONSTRUCTION WELL WATER WATE R AGENCY NUMIER LOCATION REPORT TEST LEVEL QUALITY REPORT REMARKS DRB-ll 33* 13' 18" N Sample analysis by X-ray 81* 35' 42" W diffraction DU-42 33* 12' 44" N Approximate location 81* 43' 51" W* given DU-47 33* 12' 31" N Approximate location 81* 43' 14" W* given H-12 33* 13' 26" N 81* 35' 48" W K-5 33* 13' 02" N Approximate location 81* 39' 57" W* given LA-2 33* 12' 15" N X X X X 81* 44' 26" W LA-3 33* 14' 49" N X X X X 81* 38' 56" W LA-33 33* 12' 27" N X X X X 81* 39' 29" W .__- P G-4 33* 13' 08" N Boring, graphic logs 81* 34' 05" W showing local and well lithologies PH2-2 33' 11' 50" N Approximate location 81* 45' 18" W* given P-5 33* 13' 34" N Approximate location 81* 34' 58" W* given, graphic log P-15 33* 13' 23" N Approximate location 81* 34' 50" W* given P-5R 33* 08' 57" N Depth from composite log, 81* 36' 57" W driller's log of piezo-meters, upper and lower aquiter depths available
- See remarks C-74
TABLE NO. C-1 (SHEET 38A OF 88) INVENWRY OF EXISTING DRILL HO2 AND WATER ELL DATA BARNELL COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL E EVATION GEOLOGIST'S DRILLER 'S SP/ GAMMA / NLMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON P-12R 33' 13' 50" N 381 X 81* 36' 07" W SC-B W-P 4 33' 17' 13" N 301 81' 38' 35" W SCWEC 33* 21' 37" N 160 300 X
#33 W-gl 81* 13' 06" W S WIC 33" 07' 28" N 270 #342-01 81* 19' 56" W XL-5 33' 16' 05" N 441 321 81' 37' 02" W 3-CS 33' 14' 14" N 81* 38' 55" W*
30-P 33' 13' 28" N 605 312 X 81* 34' 47" W 905-91C N 66, 730 608* X E 46, 520 (d) 905-66H N 72, 100 863 303 X X E 62, 190 (d) 90 5-9 5K N 53, 170 607* X E 41, 300 (d)
*See remarks (d) Savannah River Plant (SRP) grid C-75 M M M M M M M M
E E E E E E TABLE NO. C-1 (SHEET 38B OF 88) INVENWRY OF EXISTING DRILL HOLE AND WATER ELL DATA BARNELL COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL MATER WAE R AGENCY NLNIE R I4 CATION REPORT EST IEVEL QUALITY REPORT FEMARKS P-12R 33* 13' 50" N Sample analysis by X-ray 81* 36' 07" W diffraction ** T-B W-P 4 33* 17' 13" N Supplementary well data 81* 38' 35" W available SCWRC 33* 21' 37" N X
#33 W-ql 81* 13' 06" W SCWIC 33' U7' 28" N X #342-01 81* 19' 56" W X L-5 33* 16' 05" N Graphic log 81* 37' 02" W 3-CS 33* 14' 14" N Approximate location 81* 38' 55" W* given 30-P 33' 13' 28" N 81* 34' 47" W 905-91C N 66, 730 Depth from E-log E 46, 520 (d) 90 5-6 6H N 72, 100 X X E 62, 190 (d) 90 5-9 5K N 53, 170 Depth from E-log E 41, 300 (d)
- See remarks
** Not shown on Figure 7-1 (d) Savannah River Plant (SRP) grid C-76
TABLE NO. C-1 (SEEET 39A OF 88) INVENTORY OF EXISTING DRILL HOLE AND KATER ELL DATA HAMPTON COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS E LL EIEVATION GEOLOGIST'S DRILLER'S SP/ GAMMA / N UMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG IE SISTIVITY NEUTRON HAM-1 32' 36' 18" N 1000-1100 81* 14' 52" W HAM-12 32' 45' 14" N R8 50-9 50 112 X 81* 14' 32" W HAM-13 32' 45' 14" N R883 112 X 81* 14' 32" W HAM-18 32' 51' 03" N R870 107 X X Bl* 04' 56" W HAM-20 32* 51' 09" N 900 107 X X 81* 04' 57" W HAM-21 32' 52' 38" N R820 X 81* 06' 42" W HAM-25 32' 55' 32" N 745 81* 11' 11" W HAM-27 32' 55' 40" N 720 135 X 81* 11' 21" W HAM-33 32* 39' 42" N 1008 X X 81* 18' 59" W HAM-34 32* 42' 43" N 822 X X 81* 21' 21" W HAM-38 32* 52' 38" N 1469 105 X 81* 06' 42" W HAM-40 32* 51' 09" N R810 117 81* 04' 57" W HAM-41 32* 51' 49" N R864 100 X 81* 06' 54" W C-77 E E E E E E
M M M M M M M M M M M TABLE NO. C-1 (SHEET 39B OF 88) INVEN'IORY OF EXISTING DRILL HOLE AND WATER NELL %TA HAMPTON COUNTY, SOUTH CAROLINA DATA AVAILABLE WELL CONSTRUCTION HE LL KATER WATER AGE NCY NUMEE R LOCATION RE PORT TEST LEVEL QUALITY REPORT REMARKS HANH1 32' 36' 18" N X 81* 14' 52" W HAM-12 32' 45' 14" N X 81* 14' 32" W HAM-13 32* 45' 14" N X 81* 14' 32" W HAM-18 32' 51' 03" N X Measured depth 673 f t.*
- 81' 04' 56" W HAM-20 32' 51' 09" N X **
81* 04' 57" W HAM-21 32' 52' 38" N X X ** 81* 06' 42" W H AM-2 5 32' 55' 32" N X X 81* 11' 11" W HAM-27 32' 55' 40" N X 81* 11' 21" W HAM-33 32' 39' 42" N X 81' 18' 59" W HAM-34 32' 42' 43" N X 81* 21' 21" W HAM-38 32* 52' 38" N X ** 81* 06' 42" W HAM-40 32' 51' 09" N X ** 81* 04' 57" W liAM-41 32' 51' 49" N X Measured depth 853 f t.** 81* 06' 54" W
** Not shown on Figure 7-1 C-78
TABLE NO. C-1 (SHEET 40 A OF 88) INVENIORY OF EXIS'2ING DRILL HOLE AND WATER WELL DATA HAMPTON COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL E LEVATION GEOLOGIST'S DRI LLE R'S SP/ GAMMA / NUMBER LOCATION DE PTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON HAM - 43 35' 52' 38" N R600* 105 X XX 81* 06' 42" W HAM - 46 32* 53' 07" N 911 X X 81* 04' 57" W HAM - 49 32* 53' 05" N 723 X 81* 00' 11" W HAM - 50 32* 40' 48" N 986 X 81* 11' 20" W HAM - 60 32* 53' 36" N 70 81* 12' 09" W HAM - 61 32* 53' 41" N 70 81* 12' 18" W HAM - 62 32* 54' 15" N 70 81* 13' 35" W HAM - 71 32* 43' 46" N 140 81* 14' 12" W HAM - 72 32* 58' 43" N 880 115 X X X 81* 06' 51" W HAM - 82 32* 51' 09" N 125 81* 12' 23" W HAM - 85 32' 36' 38" N 71 81* 16' 22" W HAM - 90 32' 54' 04" N 537* 105 X X 81* 09' 19" W HAM - 92 32' 45' 31" N 1015 112 X X 81* 14' 46" W
- See remarks C-79
E E E E E - E E E E TABLE NO. C-1 (SHEET 40B OF 88) INVEN"[ORY OF EXISTING DRILL HOLE AND WATER ELL DATA HAMPTON COUNTY, SOUTH CAROLINA LATA AVAILABLE WELL CONSTRUCTION HELL WATER WATER AGENCY NUMIE R LOCATION REPORT TEST IEVE L EPORT QUALITY REMARKS NAM - 43 35' 52' 38" N X X Measured depth - 81* 06' 42" W ?at fe ** HAM - 46 32' 53' 07" N X X X X ** 81* 04' 57" W HAM - 49 32' 53' 05" N X Caliper log ** 81* 00' 11" W HAM - 50 32* 40' 48" N X 81* 11' 20" W HAM - 60 32' 53' 36" N X 81* 12' 09" W HAM - 61 32* 53' 41" N X 81* 12' 18" W HAM - 62 32* 54' 15" N X 81* 13' 35" W HAM - 71 32' 43' 46" N X 81* 14' 12" W HAM - 72 32' 58' 43" N X X ** 81* 06' S1" W HAM - 82 32' 51' 09" N X 81* 12' 23" W HAM - 85 32' 36' 38" N X 81* 16' 22" W HAM - 90 32' 54' 04" N X X Depth from E-log 81* 09' 19" W HAM - 92 32' 45' 31" N X 81* 14' 46" W l
*
- Not shown on Figure 7-1 C-80 l
TABLE NO. C-1 (SEEET 41A OF 88) INVENIORY OF EXISTING DRILL HOIE AND WATER ELL DATA HAMPTON COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL ELEVATION GEOLOGIST'S DRI LLE R 'S SP/ GAMMA / N UPBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON HAM - 93 32' 45' 41" N R900 100 X X 81* 12' 30" W HAM - 94 32' 52' 38" N 815 105 X 81* 06' 42" W HAM - 100 32' 46' 23" N 140 81* 16' 23" W HAM - 103 32' 56' 54" N 550 95 81' 02' 04" W HAM - 104 32* 45' 25" N 120 81* 06' 58" W HAM - 110 32' 36' 25" N R1600 60 81* 18' 15" W HAM - 111 32' 38' 20" N R956 74 81* 18' 11" W H AM - 117 32' 38' 02" N R850 75 81' 18' 19" W HAM - 122 32' 39' 49" N 75 81* 19' 30" W HAM - 127 32' 57' 13" N 140 81* 12' 13" W HAM - 130 32' 58' 57" N 120 81' 07' 31" W HAM - 132 32' 40' 29" N 100 81* 09' 40" W HAM - 135 32' 55' 08" N 843 130 X X 81' 11' 14" W HAM - 141 32' 54' 35" N 110 81* 10' 09" W C-81 M M M M M M
- M M M M
M M h t p e d S d K e . R rt A af M s a7 E e9 *
- M7 *
- M YT CR X E NO X X X X X X L P B
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)
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u O 41 50 41 50 40 31 31 31 31 g L i
* * * * ' * ' * * * ' * * '
- F 21 '21* '
- 21 '21 * '
- 21 21 21 38 38 21 38 21 38
'21 38 21 38 3 8 21 2' 38 1 21 38 n 38 38 38 38 38 o
M n w o 0 3 4 0 1 7 2 7 0 2 5 1 h 3 4 0 0 0 1 1 1 2 2 3 3 3 4 s 9 9 1 1 1 1 1 1 1 1 1 1 1 1 M LE LE R t N o M M M M M M M M M M M M M M EMNU A H A H A H A H A H A H A H A H A H i A l A H A H A H A H M
TABLE NO. C-1 (SHEET 43A OF 88) INVENIORY OF EXISTING DRILL HOLE AND WPsTER ELL DATA HAMPTON COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS WE LL ELEVATION GEOLOGIST'S DRILLE R'S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON HAM - 142 32' 50' 34" N 139 81* 13' 21" W HAM - 144 32' 42' 48" N 102 81* 18' 52" W HAM - 147 32' 42' 46" N 114 81* 10' 29" W HAM - 151 32' 52' 20" N 110 81* 08' 01" W H AM - 15 3 32' 51' 42" N 945 X 81* 04' 28" W HAM - 155 32' 58' 39" N 465 110 X X 81* 06' 49" W H AM - 15 6 32' 39' 57" N 505 85 81* 15' 08" W JASPER COUNTY, SOUTH CAROLINA JAS - 102 32' 30' 50" N R210 80 X 81* 00' 10" W JAS - 108 32' 28' 50" N R340 55 3 80* 58' 50" W JAS - 324 32* 32' 39" N R1550 40 81* 10' 09" W
.7AS - 325 32* 35' 18" N 540* 60 X X 81* 12' 41" W
*See remar ks C-83 E E E E E E
m M M M TABLE NO. C-1 (SHEET 42B OF 88) IE'ENTORY OF EXISTING DRILL HOLE AND WARR NELL DATA HAMPTON COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WAE R A2 NCY NUMIER LOCATION PEPORT EST LEVEL QUALITY EPORT REMARXS H AM - 142 32' 50' 34" N X 81* 13' 21" W HAM - 144 32' 42' 48" N X 81* 18' 52" W HAM - 147 32* 42' 46" N X 81* 10' 29" W HAM - l l 32* 52' 20" N X 81* 08' 01" W HAM - 153 J2' 51' 42" N X ** 81* 04' 28" W HAM - 155 32' 58' 39" N X X ** 81* 06' 49" W HAM - 156 32* 39' 57" N X ** 81* 15' 08" W JASFER COUNTY, SOUTH CAROLINA JAS - 102 32* 30' 50" N X X X X ** 81* 00' 10" W JAS - 108 32* 28' 50" N X X X ** 80* 58' 50" W JAS - 324 32' 32' 39" N X ** 81* 10' 09" W JAS - 325 34* 35' 18" N X A Test hole depth 81* 12' 41" W
*
- Not shown on Figure 7-1 C-84
TABLE NO. C-1 (SHEET 43A OF 88) INVENMRY OF EXISTING DRILL HOLE AND WATER % ELL DATA ORAtCEBUBG COUNTY, SOUTH CAROLINA DAT% AVAILABLE SURFACE GEOPHYSICAL LOGS HC LL ELEVATION GEOLOGIST'S DRI LLE R'S SP/ GAMMA / NUMBE R LOCATION DEPTH (FT.) (FT.) LOG LOG RESISTIVITY NEUTRON OBG - 3 33* 29' 44" N 138 300 81* 16' 50" W ORG - 4 33' 29' 53" N R100 - 120 300 81' 16' 49" W O RG - 5 33* 26' 50" N R250 81* 07' 30" W ORG - 11 33' 26' 50" N R100 81* 07' 30" W ORG - 12 33' 26' 50" N 180 81* 07' 30" W O RG - 19 33' 27' 00" N 175 81* 07' 00" W ORG - 20 33' 27' 00" N 195 81* 07' 30" W ORG - 4 5 33' 26' 50" N 162 X X 81' 07' 30" W OBG - 93 33' 28' 24" N 412 300 80' Ol' 07" W ORG - 9 5 33* 26' 49" N 214 240 X XX 81* 07' 25" W O RG - 9 7 33' 26' 52" N 231 X X __ X 81' 07' 31" W ORG - 201 33' 29' 53" N 300 81* 16' 49" W OBG - 204 Norway area, 486 X X South Carolina C-85 m M M
E E E E E E E E E E TABLE NO. C-1 (SHEET 43B OF 88) INVENTORY OF EXISTING DRILL HOLE AND WATER ELL DATA ORANGEBURG COUNTY, SOU'IH CAROLINA DATA AVAILABLE ELL CONSTRUCTION ELL WATER WATE R AT NCY NUMIER LOCATION REPORT TEST LEVE L QUALITY REPORT RE MARKS OE - 3 33* 29' 44" N X X ** 81* 16' 50" W ORG - 4 33* 29' 53" N X X ** Pl* 16' 49" W Om-5 33* 26' 50" N X X X 81* 07' 30" W OIG - 11 33' 26' 50" N X X 81* 07' 30" W OIG - 12 33* 26' 50" N X X 81* 07' 30" W O N - 19 33* 27' 00" N X 81* 07' 00" W OIG - 20 33* 27' 00" N X 81* 07' 30" W OIG - 45 33* 26' 50" N X X X X 8?' 07' 30" W OIG - 93 33* 28' 24" N X ** 80* Ol' 07" W OIC - 95 33' 26' 49" N X X Caliper log Bl* 07' 25" W ON - 97 33' 26' 52" N X X X X 81* 07' 31" W Om - 201 33* 29' 53" N X ** 81* 16' 49" W OHG - 204 Norway area, X X X Electric South Carolina logging data sheet **
** Not shown on Figure 7-1 C-86
TABE NO. C-1 ( SHEET 4 4 A OF 88 ) INVEN'10RY OF EXISTING DRILL HOE AND WATER ELL DATA ORANGEBURG COUNTY, SOUTH CAROLINA DATA AVAILABLE SURFACE GEOPHYSICAL LOGS NE LL E EVATION GEOLOGI3T'S DRILLE R'S SP/ GAMMA / NUMBE R LOCATION DE PTH (PT.) (PT.) LOG LOG RESISTIVITY NEUTRON ORG - 227 33* 27' 06" N 500 X 81* 03' 20" W Om - 228 1.5 mi. NW of 187 200 X intersection of SC-332 & 70 OHG - 230 33* 27' 08" N 480 X 81* 06' 02" W OaG - 245 33* 29' 14" N 300 290 81* 05' 22" W OIC - 249 Off SC-690* 197 SCWRC # Of f SC-690
- 490 X 31V-q2
*See remarks C-87 W E E E E E E E E E
E E E E E E E E E E E E TABLE NO. C-1 (SHEET 44B OF 88) INVENMRY OF EXISTING DRILL HOLE AND WATER ELL DATA ORANGEBUIC COUNTY, SOUTH CAROLINA DATA AVAILABLE ELL ~ CONSTRUCTION ELL WATER WATE R AGENCY NUMIE R IDCATION REPORT TEST LEVE L QUALITY REPORT REMARXS ORG - 227 33' 27' 06" N X Electrical logging 81* 03' 20" W data sheet ** ORG - 228 1.5 mi. NW of X X X ** intersection of SC-332 & 70 O m - 230 33' 27' 08" N X X ** 81* 06' 02" W OIG - 24 5 33' 29' 14" N X ** 81* 05' 22" W OIG - 249 Off SC-690* X X X 0.5 mi. south of the intersection of SC-690 and SC-74** SCWRC 4 Off SC-690* X X X X 0.5 mi. south of the 31V-q2 intersection of SC-690 and SC-74, electrical logging data sheet ** C-88
y -- - _ . ._ I l l m APPENDIX D d CORE LOGS 1 i P i i I
l l l APPENDIX D l This appendix contains the logs from all core holes drilled in this study. The logs from B-33, B-34 and AL-317 are also included. See Chapter 6 for discussion on core drilling methods, Chapter 8 contains the hole h hole correlations. I
GE0L0GIC DRILL L0G v=Tu Eucmc ==Ti= n-T 95io i - i6 v5c-i 0 POSTULATED MILLETT FAULT N 1134867.04 E 679423.71 (GA.) 90 N.A.
.... .. ...... ....... . . . . . ........... . . . . . . . . . . . . . . . . . . , .....1 ..........
5-28-82 6-12-82 LAW ENGINEERING Mobil 55 NQ - - 620.0
............i.._, .... ..... _ .. . . . . . . . . . . . . . . . . . . . . . . - - , . . . . . . . . . . . . . .... ,. .........
356.17/57.91 24 3 - 219.0 88.1/131.9 (6-21-82) - N.A. Observation Well K. Wornick
.. :a .i :. . .. . ........ e
- . ; . g .a .
1 3rs ...== ..i
.i : :" : :: :. ::: . . . . . . . .
- 3
- =.
ji .
" l L' 't . g
*= ; E .-
i; . j 8 ........= .
= a u.a . = '. .
- s. ;a . 1 1; . .
a ! '3 1$ a . g d o' G g (Ft.) (Ft.) . Id 1* *
,,o _
0-106.8* -SAND: Moderate reddish E-Z mud. barite. and 2.0 1.4 70s -
>-w~'
brown (10 R 4/6) to Tark yellowish orange bentonite used as (10 YR 6/6). sand (quartz) with clay grading required. out to silt with depth (-60.0') very fine 2.0 1.4 to medium-grained subangular to sub-701 rounded, moderately well graded locally 0-106.8' Poor re-loose, firm in place. covery in this zone partially 1.0 0.5 50s
.-- limits more 5- 0-5.0': Sand and Clay
~
detailed litho-
; logic description.
5.0-15.0': Clay a'nd Silt 0-106.8': Moderate to no loss of cir-
~
15.0-106.8': Loose sand, silt; some thin bedding. culation. 10.0 1.6 16% jo[ , I 15 - E o - -
~
E 5.0 0.7 145 2
~
N' 8 _- 20 - ?
- 5. 0 0.5 101 ;
25 - 2.0 0.5 251 2
~
2.0 0.9 451 2.0 1.2 601 30 ] . 31 - 4.0 0.6 15% 2 M 184 35 -
... ...... ..; ... ... .. ...., m,. . . . . . . ,
. . ... ....: .. .....; . ..,... POSTULATE 0 M1LLETT FAULT V5C-1 Hac e e e.,
I
. . . . . . , . . . . . . . . . . . . . ....... 1 GEOLOGIC DRILL LOG v=1urucaicu==m"'- eSi0 2 .. i e v$c.i
> . . WArca t,. = =5 =
ca r ssu a e
- : a
- 3 rears 3 .
gj ;: * *:
. . a a ...-
j ...<-..--.<*am...a.- ":: ",;",.*;,
- ;a .. : : e== ..
v; :gg
- t. . . . 3. .
ag , . a
- s
. 3 I. . .c-aaac
- .m- . =re.
3e a a a $ = ! ' e' s .' i s l.
* (Ft.)' (Ft.) l 1a 3w .
0-106.8' SAND (cont) W 0-106.8.: Generally 5.0 0.4 81 - - low recovery in loose material assumed to be
- washing out at face of core bit.
40-5.0 0.6 121 45-1.0 0.0 Os 47.0-48.0': l' gradational color change from moderate reddish brown (10 R 4/6) 1.0 0.2 20%
~
to yellowish orange (10 YR 6/6). 1.0 0.5 Sol [ 1.0 0.3 2 [ 48.0-106.8'; Degree of weathering decreasing with depth, 1.0 0.4 4GL w 50-8 u 5.0 0.7 14 2 . 55- . g 2.0 0.0 Os v - E 2 2.0 0.0 01 _ .
~
I.0 0.4 401 60-1.0 1.1 1101 Includes stuh from previous - run. - 1.0 0.6 605 - 3.0 0.0 01 65-5.0 0.9 1 83 n - 5
~
m - w w b IO~ M 5.0 0.0 Os
..* e
?^^ 25' . 6 e m. .
s....t., . . . .,. .. 6.,,...i
...e==....: .. ..,e...: . . .. .. POSTUL AT[D MILLETT FAULT y3c,j HOCF 19 a
95i0 GEOLOGIC DRILL LOG - u numcu -Ti- et-T 3 i6 v5c-i
,> , , W ATrR
- 4 ., enessuar g ...
>> . D o 0 Tr$75
- v
- e,
" i.
a . t ...c='+,-a-- c 6 a * * ac a ,'a-wa, m 6. w. L ..
.-.-==.
j j.;: 3
. . : :a : e.a ac,== --
ta : g :. = t: := : a
. i y j! {{ !, [* 3 , l-lc
- j (rt.) (rt.)
I
.s . ,e 0-106.8': S_Ap_D: (cont) 5.0 3.3 661 -
80 - : 5.0 3.1 621 . 85 - u 5.0 0.5 10% = 2 - m 8 I u - 90 2 90.0-106.8'; Color change from sand to
- fossiliferous calcareous sand; contact
- delineated by presence of calcareous material in sand and clay; clean sharp
- 5. 0 0.9 181 ; horizontal contact
~
w I E Y - 95 - ' II _ _ s 5.0 0.8 161 100 - , I 5.0 0.6 121 I 105-5.0 3.2 64 5 112.2 106 0(:g,..
/ 106.8-185.0*: FOSSittrEROUS CALCAREOUS SA M/ 106.8-186.5'; Mod-
_::: IN. FOSS! LITER 5UTTI'MTSTohE: Yellowish gray erate to total (5 V 8/l) fine-to-medium-grained, typically loss of _Q'NE _ ~ ~i subanquiar to subrounded. circulation.
^
110 - h
-i.'.[h
-w AifY:
5.0 1.0 201 m -2.Nb
= -:Ts.-!
8 _w? .::b._y y .1 ::5
~
ina Il
... ...... ..i .,. .. 6.,..... ..= - 6= ==.
..........a . .,e.... ....... 0STULATE0 MILLETT FAULT VSC-1 H&CF t 9-2
GE0 LOGIC DRILL LOG -u uumc u== = e5w . ie v5c-i es :. . . . . . f = = . = enessuar
- ; ; ; 3 rests S .
~~'==.->
;;;; ',n.n*;,
; ; . i ::
- s .,-
t,
- q
- i
- " - '=-
I 3 1s a a o : w
.' l*
j (Ft.) (Ft.) *
'T:*f . 106.8-185.0': TOSSILIFEROUS CALCARf0V5
-':ff':
' . SAND ~ F055ILIFEROUTITK5Tohr (cont)
Poorly to moderatley sorted. weaTto hard.
-::MS
-::f Je> weathered. (well cemented) numerous large 5.0 1.3 26 1 oyster shells and smaller calcareous shell
-.hj T<M:
fragments 110.0-135.1 fossilifwrous
-?jm .
timestone. 185.0-186.5 moderately hard.
-i:g,ijgij fresn.
120 -];10 # 115.0-115.3': Oyster shell. , itng very little
- jg .
5.0 3.3 661 _ 120.1-123.2': Oyster shell. ,( CNC"- _ ..d2 i
. .d q-135.1-135.6': Clay bed.
,Ub:::
125-'.:Q
. 135.6 175.2': Poorly cemented calcareous
_ :::::: sand. g...gj
-y:::. ;
~
?
#$l 10.0 ,h,, 0%
130 y n -.:.:.!y E 2.h. : w .
.,::<.y:
8 ;. y
" - :;::W. l 8
6 k}:
- b.
i::g."
= -
ij9: 135- ;j;ij ig
~.':4.~. i; 5 }N 5.0 2.2 441 -k.%
~
': (:$:
h?$
- M
":-4.3 y#
W
; ?gf
- i.
I 5.0 0.0 01 .e:.:T.;;::
- .y:.::'. ..
_- )M: Includes stut from >revious 1.0 3.7 37% run. :.ij.; n ;.
~
- .i.k w:
-NI M. .
#.t./.: .-
9.0 0.0 01 15y ' .g{ j:ii{::: w: .
~:
M..j$ C
".$h n
_~hk l y.
. . . = .... .. .... .. . .,... POSTIAAIED MILLETT FAULT VSC-1 HIC F 19 3 I
GEOLOGIC DRILL LOG v= m EuCmcu==mG L-T e5w s i6 v5c-i s ..
.. i. . .: .
- .:: :n.::.
.; : :: 3 :: 3. : :.:
.. .i. o..' .,,.
1:
, e.
; ;* a f sj (Ft.) (Ft.) l 1d 1* * ,,
- -. . 106.8-185.0': FosstLIFEROUS CALCAREOUS
,5 ', -[.{!y:.iAND :; - F0531L1F twwd t mtdiuat RBn t) i:: .
5.0 1.4 281 ~
-.....J.
-35.'- :s; ?
'c5 j_ ::,' i 160 -?" - h:)-
- i -l.i:
8 ~ii Y
, i..
5.0 0.0 Os g ,. f:. :Y 165 -
-N-f#-
-;y I 5.0 1.7 341
-;( .n L..A!
?;f.?
4
~h.:::.$.:..
-(I.h 170 -
-$E 5.0 0.9 181 ,,
(M i::.,7.;R s
-?. 9
- b .5-c.
-1:4:
175 - 9.:.W:- 175.2-175.5' Clay bed.
~Yb W .
y f.f.W. . .h..:: a _ . .n e:' 10.0 1.8 181 180_/ . ' :.Tisi' I
- k g
s.,
~
-I. b
?:
-::. : 3
-i: :
..!j
( I 34.0 185 -.i.. 5.h ; :::.
$.--[185.0-186.5':
LIMESTONE : Yellowish grey (5 Y 8/1) some fosstis and shell fragments.
- hard. planar lower contact apparently I 5.0 4.3 861 32.5 186.5
~
186.5-267.2'; CALCAREOUS SILTST05ETMAkQ: Grayish green (5 G 5/2) to dark greenish gray (5 GY 4/1). fresh. 186.5': Little to no loss of circu-lation. I 190_ 5.0 4.7 941 I ... ...... ... ... ... .,. ..i
. . . . . . . . . . ....,....i .... ..
'em .u'
~
POSTULATED MILLETT FAULT VSC 1 Mac r i..a
GEOLOGlC DRllL LOG v=Tu cu=c ==Ti= el-9siO 6 .. i 6 v5c-i !
,, =$ e .. . . WATER .m 4 . .
p
- 3. : ;j PRESSU RE vEsrs
-.*...=:
. : . gl o, ..
. ......... [. .
g ............o...........
;;;;;',n..=2;, }a; . , . . .
- g .
- i. : ; : . ; ; e .4 . n u-. . . .
!; :, 4. - .
1 d '* i!= I. . 1 .' l (Ft.) (Ft.) { 186.5-267.2': CALCAREOUS STLTSTONE (MARL) (cont) Hasnearly horizontal and frequently
- convoluted lamina delineated by small fossil she115/ fragments, calcareous streaks /
- thin beds; weak to hard (tell cemented);
some fractures, asstaned to be mechanical (no polished surfaces: bre.ks approximately horizontal across bedding). 10.0 10.0 1001 200 - 205 - 186.5-267.2': Excel-in
~
lent recovery g
~
throughout. l N 10.0 10.0 1001 7 210 _ l m 1 l 214.2-214.9': Very calcareous, hard. y 215 - 8 -
~
~
l l
=
10.0 10.0 1001 - 220_ e -
~
E m -
~
E 8 : 225 225.9-226.7': Very calcareous. hard. 10.0 10.0 1002 230-
~
~
=
2 - sa ~ 8
-14 235~
....==...=; .........i ..".. ..
.e . . .u . . .. ; .,.... .,,...; ..v .
POSTULATED MILLETT FAULT VSC-1 H&C F 19-a 1 i
I GEOLOGIC DRILL LOG v x Tu n a - C u - - rL - e5,0 2 - 26 v5C.1
.. :. .i :.
...m....
I
- : . :. ..... 3 .
3 =,: 2.,:.
.......................... :::: :n.:..
- t. .. . : :. . . ... .... ....
II $ a a 1 l'
.,,l (Ft.) (Ft.) :
I 1: . g. .
- 186.5-267.2'- CALCARfous SILT 5 TONE (MARL) (cont) n 10.0 10.0 1001 240 -
2 186.5-267.2': Excel-
~
w lent recovery 8 throughout. 245-I I 10.0 10.0 1001 e 250 - 252.3-252.7': Very calcareous. hard. u 2 - 8 g . 255-8
$' I 10.0 10.0 1001 -
260-265-I 1
- CLEAN, APPROXIMATELY HORIZONTAL CONTACT
= 267.7 -
2 267.2-278.7': LIMESTONE: Very light gray (h/8) 267.2-278.7': Slow light olive gray (5 Y 6/1). very fine-grained drilling, no 8 well cemented, hard vuggy. loss of circu-u - lation. 10.0 10.0 1001 27P t M 275-
..........;.................-54
....6.. . a ...... ......i
- VSC-1 Mace so a
I! GEOL 0GIC DRILL L0G v0G1tc tLtCTRiC CtNERATiNG rLANT 95i0 e is v5C i
.. , . WATER Eg. U. .b . . . carssuns .
a g: vests -.v.. .-: 3 [ 3
. . . . . . . . . . . . . . . . . . . . . . ';;;:=:.;,
h.,
. ! 'l :, '
; .s .g 1; . : ; !. 8 =....v.. .-
s 5 ;, 5 . j ;g g. ;5g :s ;s53a . ..u-...'..
$a g . g s , g .- (Ft.) (Ft.] $
1d 1*
- eu' 267.2-278.7: LIMESTONE (cont) Vuggy 267.2-278.7': Slow
- drilling,no loss of circula-tion.
GRADATIONAL CONTACT
-59.7 e. 278.7-295.8': FOSSILIFEROUS CALCAREOUS 278.7-295.8 Slow 10.0 10.0 1001 280 - ..V SANDSTONE: Very light grey (N/8) to light drilling.201 P T. olive grey (5 Y 6/1) very fine-grained well loss of circula-
'f to moderately well cemented. many shells and tion.
p' shell fragmPnts; vuggy 286.5-287.3'. Y
- g
- M x;
.+
n, 285 - 4+. o W; z g-E
~
w - O 4, . b b' jf-v n. 10.0 4.6 461 290 -'xv ' [fv.
-4 v
nz
- .w-4 Lp 9
2952 # GRADATIONAL CONTACT 76.8 795.8-.$* W , , 8 2 0ifi (5 GY 4/1)Tgreenish black (5 GY 2/1). drill rate, high
/r
- _d!#. coarse-9 rained, loose. poorly cemented, loss of circula-
_W.E moderatley calcareous. tion. pf.GF 250 gallons of drill mud lost
-. ':g.s,'P i to formation.
10.0 5.6 561 300 -3if:iE I b.
-P liin .i. .
L ..:
.f.
M- ..d 305.1 305.2' Locally well cemented bed h):;#$
! (sandstone) 5 [ ink.
= .;; w.
fff.::
-( 4_
-.. i$
10.0 3.7 373 310 .
-9$i5 M:i.
n:. _,);;.
-_Eg ~
GRADATIONAL CONTACT
-- (f 0 ,/ 314.8-324.8':
. 314.8-324.8': Slow FOSSILIFEROUS CALIARtuud drill rate.
-95.8 -
SANDSTONE
.....uv....=i .v. .-. .,vv... .".
....==....i .. .,....: . . ..... POSTULATtD MILLETT FAULT VSC-1 nacr so a
1 GEOL 0GIC DRILL L0G v='-cmc === t- esia ,-i. vsC-i
.m.
. . i .i :.
. . 1
.a .
.. a i .
- 5? *3 . ;; :* I
- ; e .g
- q
- 1. "
; 5 . 1
!Ig a
I: a a . 1 I
- I* (Ft.) (Ft.) * '
I i Id 1* *
-'D - gle 314.8-324.8': FOSSILIFEROUS CALCAREOUS
-4;f .- SANOSTONE (cont) very light gray (N/8) to TTi
[-- wekht olive (5 Y 6/1), 1-to-moderately wellvery fine-grained. cemented,suny shell i
- bE and shell fragments.
t 10.0 5.1 511 N' 320 - g a
-e
- . .,o
+;,
t ,. 8 324.p CLEAN CONTACT
-105.8 325~
?:y.-
l.:'jj 324.8-366.4': $ANO: Grayish yellow (5 Y 8/4) 324.8-366.4': Fast to dusky yeTT5w (5 Y 6/4), coarse grained, drill rate. High 8 loose, poorly cemented, moderatley clean, loss of circula-w !.f:t - non-calcareous. tion. 8 -ff'k., - 100 gallons of u -; :0K:
, drill mud per
!E:$Y;T 10 ft core run.
.1 10.0 0.8 81 330 ~i:?.-. '
-j?.'d-
-::s
- Ui::
-i.is??:
!!?$.h'.
y - i "5:$.y::!. h.:). c }!:;9.
- T.
I
-j:
5
-kili-
-);y.::h.
10.0 2.1 211 -sD 340 -g.g
-2
-:l: s
[(ff:5-5
-:a: .
sY 3452f(fig:p l 2 -i; '
..i 8 s E -:!
S -
-}~
~2 10.0 0.5 51 350 -?:
~Ni:l I
-9:c, 8w
~
au --src
.....u......; ... ... ., ..., erv . -- . . . . . . .
. . ..==...=; ...... ..; . . .,... POSTULATED MILLETT FAULT Yst.1 H&CF 9 9-a
l l GEOL 0GlC DRILL L0G vxtu mc1Ricu - ru1 eSi0 i0 i6 vsc-> l r ,, e..s :. a m.. l
=: = :..
. 3 .
- p. : :. .; c ::
. = .
i 1 ........ ..
- 4. *.,i a.
- a. , : . a .. ..
II 8
. {
,8.! 3 : ' d
{' i (r.t) (ft.)
- 324.8-366.4*; SAND: (cont) Graytsh yellow
-iJb 'pF- 324.8-366.4'. Fast
- (5 Y 8/4) Io Husky yellow (5 Y 6/4), drill rate. High
......; coarse-grained loose, poorly cemented. Ioss of circula-wire. moderatley clean, non-calcareous. tion.
-?i.@i 100 ga11ons drill mud per 10 f t Core run.
10.0 0.0 Os 360 -..l:g,(
- v:;;
/
~??E-
-.i.Wi!i 365.4-367.4 Sand and clay.
365 -a.
-::f.:p. .
2.0' GRADATIONAL CONTACT 147.4 366dE--
- 366.4-423.4': SANDY CtAY Multi- 366.4-423.4': Mod-
- . colored; very pale orange (10 YR 8/2) to erste dell) rate.
- pale red, purple (5 RP 6/2) to greytsh red No loss of circu-purple (5 RP 4/2); locally highly mottled, lation.
7.0 3.4 491 - nisnerous oxidized zones and stringers.
- massive, firm, generally long core lengths.
370- Unit varies slightly in percentage of 2 -
. constituents; and to a greater degree in weathering. Some red purple beds hard.
~
E - 366.4-378.7': Lighter (kaolin) clay 3.0 0.0 01 ~
. moderatley friable, no caidized zone
_ apparent. w
'c1 375" ~
378.7-412.5' Red purple oxidized zone.
'l 7
10.0 10.0 101 38h E i ! ,~ . 385- . 10.0 4.8 481 7 39 [ ). w i g - 1
.a. -ti- E - ^ .......
t.......... ... ......... e.........a.. .....i . ...... Hl
' C .r 9 9 a
I GEOLOGIC DRILL LOG
- ,cn v=m mCmC u== Ptm e5w n o. a v5C-i
. i. .s :.
I
... : . . . .. . e ,,n e,s,s u,n c . . . . . . . .
- . " .. 5 :' ':
- =.. .
. i; : ! !. ..a...... .-
; . I ::
1 ;. ; i .g :4 1! I : I 5 : : ' i (Ft.) (rt.) . . 1s :* . U6 - 366.4-423.4* SANDY CLAY (cont) 66.6 m-5.0 10.2 2041 Rec. stub f prei inus run. -
, p p g recovery through-
- h. out as driller g -
- adjusts to u - thinner viscosity I
4007 4 5.0 4.8 %1 5 I 405 - I 2 g m 1. I 10.0 10.0 1005
%W 8 410 2 412.8: Polished surface.
;. , 413.9: Polished surface.
~
414.3: Polished surface. 415.0-415.3': Highly oxidized zone. w 415[X 416.3: Polished surface. E
't
\ 417.0-423.4': Polished surface zone E 4 7.1. 417.6. 419.9-240.2. 421.0, 421.9
_ 423.5 10.0 10.0 1001 - I 420 _
-204.4 423iL __ LOWER CONTACT DIP 200-300 Color change not in
.n lamina, possible
- c.: 423.4-477.1': CARBONACE0uS CLAY: Dark change in depositional 8 gray (N/3), weak to moderately hard, fine l
425 " -:--E env. (i.e. reducing l- w *JJ- to very fine sand and slit. thinly bedded, env.) 8 E6 occasionally micaceous, trace thin beds of I " - (-24 pyrite, occasional subrounded quart 2 grains. _-: move in low density, porous rock 5. non-cal-careous. {:~:;f
~ .
AYi 2 a** 10.C 10.C 1005 4 30 - f{ FZ-Ei E_-5 I C&: F2 E{
- 29. :-
-216 435 ~C-25
... ..u. . ..t e.. .. 6.. ....s .. a.'.**..
. . ....... .. .......; e . .. .. POSTULATED MILLETT FAULT V5C-1 eeacr t o-a
g GEOL 0GIC DRILL L0G v0c1t< <trc1 ic ct <aAri c PtA 1 95i0 i2 ie v5c->
.s .:.. - .
...m.,.,..
- r. .
.s e.. ..g ,., .
e a .: :
... n, 3 ., , g ; .. s ,- ;. .
g (Ft.) (Ft.) . Id 1*
- ___ nie
.m -
-r:: 423 4 477.1': @ BONACEOUS CLAY: (cont)
~~:.
{!*Ej High Angle Polished Surfaces:
-: ;- 425.2-425.4'
-I:'
~4E 427.4-427.6' 10'0 7*7 771 440 - PJ-~
3r: 444.7-444.8' 423.4-477.1*: cen-
--- .O. erally fast delli
- 453.7-453.8' rates and high
_:. - core recovery
- -+ :. 457.7-457.8' throughout.
E -E ~r3
- 466.7 w '.
E P~- 469.0 445 --[-29
-T-E4 469.4
-?: -
-C3 469.8-470.1'
-7.: ---
10.0 10.0 1001 450 -; ~
-~;; .
?::.
F.
-7_._
w O 455 - r ' 9. 8 u m o m w 8 - u -: -:
.::a
~~~.
10'0 10'0 100% 460- .~ ~# 461.3-464.4': Silty sandstone. coarse-
+ 2#:{
.[:f grained, subangular, stiff. moderately
.r;.g.{ weathered.
-.-: .a .
~:.::
-:,3J.,
467.4-468.0': Joint - nearly horizontal.
-' ;. no movement indentified. possibly mech-
-::J anical.
465--
-:p_Z#. 470.1-477.1'. Zone of broken silt / clay.
.2
-[ ]. _ .
10.0 8.7 87%
- 470-[-I 8 -::-
w .~:.- 5
-.-:; C-
-~::.
~
. ?% $]5 '5* ~-
... ....,. ... . ............ .. =**.a*-
....==...=;....ve-..: ...,... P051ULATED MILLETT FAULT v5C-1 eaccv so a
GEOLOGIC DRILL LOG v=ra cu = C - r - raht 95io i3 ie vsc-i ei . . ...e.
- i. ff;,r- : .... . .
- ! i : :. ::;: . ......
- : ; ............................ ::::: =:. .
i:: 3 :: ;;
- 3r n : :- i .........
. . i
- . ., i
*! 3 : 8 h
{* a (Ft.) (Ft.) I--E" 423.4-477.!' CARB0hACE005 CLAY: (cont)
~::
E{
-?58.1 L77.1-Ft
- 477.1-570.2*. SANDY CLAY: Multi-colored; 477.1-570.2' Slow light gray'-{Ti7T toTnedium light gray (N6) drill rate used grading into grayish red purple (5 RP 4/2) and very thin mud and pale reddish bmwn (10 R 5/4) to to recover sandy moderate reddish brown (10 R 5/4) con-10.0 5.2 525 clay.
480" > tinuing back into light gray (N7); and E _ light bluf sh gray (5 B 7/1); generally sandy clay with occasional alternating g beds (thin to thick) of sand or clay; w , sands are mediwn to coarse-grained, sub g angular to subrounded, hard, moderately I u j fresh; clays are very fine, fresh to
/ moderately weathered, soft to hard.
485
/ 477.1-485.0': Clay with some carbonaceous
_ stitstone inclusions near contact 2/- 485.0-486.0': Sandy clay. fresh. 486.0-515.4' Sandy clay, weathered. 10.0 3.1 315 490 - V
..,t
~V y 2 /-
8 4% -/ N : , I 5.5 0.6 III
~7 500.0-505.0': Loss O E~ assumed to be
~
x ~ wash out in a 2 zone of increased w [- sand. 4.5 0.0 Os 3 , I
/ 505.0: Wire line 505 - /j ,jtsnped off pulley
/'
and was realigned
/
~/..
10.0 9.5 951 ; [' A I I .....u....;
. . ........s
......... w..;
N
- POSTULATEO MILLETT FAULT V5C-1 MdbC F 19 a
GEOL 0GIC DRlLL L0G
.1ucuC1,1Cm m;,m1
,5io i4 .. i S
.5C.1 l
ei :. - ,em
- b. : : : ; : ff;r, - : .... . .
.........:=...
a.
;a 5 .
- u:.
1 g; n I s .,- :4
";5
- i -
3j j a g g * '
. ;. i (Ft.) (Ft.)
- Id 1*
- eu"'
477.1-570.2': SANDY CLAY (cont) i 515.4-535.4': Sandy clay (coarse sand), fresh, _ 515.4-544.7': Color 0.0 7.1 7M _ change not in 520 - lithology; pos-sible change in depositional environment. 525 _ 10.0 0.0 01 530 - 535 - 535.4-544.7': Sandy clay, mottled, 535.0: Wire line 5 weathered. jumped off boom w pulley and was 8 a' realioned. u g _ fi _ 10.0 8.6 861 540 g
~
544.7-566.2'. Clay, kaolinite. very light _ gray to tarker reds, no sand. 545 - . 10.0 10.0 1001 550 - c -
=
1 E - l s u \ Y
-336 45_ ~ r _
- e. . . . u. . . .; ... ...... ..... .a= . . . . . . E o.........;.........; ....... POSTULATED MILLETT FAULT V50-1
. enc r is.:
GEOL 0GIC DRILL L0G v=1a ructuc aN=1- em1 95io i5 i6 .Sc.,
.i :.
e
.. :. . , : .a : . . . .. . . . . . . . . . .
- . i
- .. :. : ., . . . . . . . . . . . . . . . . . . . . . . ::::: =.
- L' .
i; .
! !* ...a....a ...
- 1. 5 - 1 :; ; s .g :.
1I I I 1 ! ' s **
- I
$ i (Ft.) (Ft.)
1d 1* *
> 477.1-570.2': SANDY CLAY (cont)
E I a. 10.0 7.8 781 g ' - 3 560 - W,-
./
565 566.2-570.2': Sandy clay mottled. _ weathered. u_ I
-r lu.0 9.9 991 351.T 570 -h 570.2p~ ._.. _ _570.2-620.0': SAND: Light gray (N7) to dark 570.2-620.0': Very y -f gray (N3).~sIIt and/or clay matria, some slow drill rate a and thin mud
-:i ,:. .s,< dark minerals and mica. medium-to coarse-g -. . . ' ' ' ' " grained. subangular to subrounded. used to recover
=
"$ generally well graded, clean: non- sand.
g :g;)g calcareous, weak to very weak. 8 _ I W 575 -:( g -.:: , N ::: I a 10.0 4.0 401 ' I 580
$.22:
-yTj 5 :E{
I
- :;,, sic.
_3::: 585 -
.l7 g.:
I 3 50$-
-::::.r.- ::n.;;
*r 10.0 7.8 783 g Ijlr;;;;
g ..:. O
- 1 g - -
o -
" q el I .....u,...;
.........4 1
-31L 595
,05TULATED MILLtTT FAULY VSC-1 M dbCF 19 a
. . . . . . . . . . . . . . . . . . . . . a 5
GEOL 0GIC DRILL L0G .0Gru tuCm0 uoriNG PUNT 95io i6 i6 v5c.i
.s :. . . ..Tra
.. enessunc g; ;. ; "
*
- vests 3
..'.* = .i : :: :': . .
e ....................... ;^;;; ";;;*;,
}! ?
'! :' 3 i; : .
! 8 c.a..c' . ..
}.:: }:
3 ! .j :i * ***"'"*"'*-
- n. . I "
15 s 8 a 5 1 ! e' i (Ft.) (Ft.) '
.d :" *
~,,, 1m~
. ..:. 570.2-620 n':5AND A (cont)
., :::5.t
-f 10.0 10.0 100% -'
a . [ 600ji' '
$ -?O.Y:_
- -:i&'9:.
-'c.. - :::3i.
_-. $. h..) 605 -$ji
-,.y -
$:::4
- hib
-4::::.
10.0 4.9 491
-iiiiiiii:
610 -/l.?iiii '
-:::ll:.k]
~
L.J
-{ .N.1 8
v
=
= -i.:. i h 5 .:
s' _ 8 -:- 615_:i
~.5 ,
5.0 4.8 961 -.{
~
- ,jNs
- [ 2
-401 620 TOTAL DEPTH - 620.0'
~
CONDITIONED BORING IN PREPARATION FOR _ u 0 PHYSICAL LOGGINC. INSTALLED OBSERiATION WELL. g
... . 6.,. ..; .,. ... .,ww..; '. ..s....
. . . . . . . . . . .........a . . . ... POSTULATED MILLETT FAULT VSC-1 H&CF I S-2
....e., . . . . . . . . . , = . . .6....
GEOLOGIC DRILL LOG v=TtE m CTRiC u - m G P - e5io i- ie v5C-2
.... . ... .,.. .6..om.... .e.....
Postulated Millett f ault N 1141512.71 E 673492.62 900 I NA
...ua com et s ve o ..66e. .. 66 =ame ano wooe6 mote o.as ev e n ev n e s a te,.3 = o c a te,.3 ve,at os e, 5/26/82 6/11/82 Law Engineering / Ivy Mobil Drill NQ - - 600.0 coas e scovea, te,.,4 come eene, 6e. e t. vo, o, ca.. omov== e s. esevase6.e=ov==..,ma ese,=,s6.,oeornoen
- - 201.7 See Observation Well -
..=ese ma === = me = vie 66 c . .... s e e , .. no6 e : ....,6ame,- 6... ev:
See Observation well Ron Wood (Geologist G.P.C.) (K. Wornick) I ll gj ! 35
- a =
- E*
o
**e I
*s e
a
*a
,3 ,* ,: ; ,5
*^TE" pnessuns TESTS
. , etevano=
l e v e {e
* *
- c a *,'a= a ae c 6 a m' 'c a *a a**** *":
I's"', $'l ta g
;a ; = ts
=v .
3a o g ! c=aaac'sa **
*; s a a 'u'a* . "' c-I ;
o t s I5g :4 : e= , e , e s .
** = * *
{e {$ g a (Ft.) (Ft.)
~
0-2.2': BLOW SAND 0.0-8.5': Split
- spoon samples.
I 2.0 0.2 201 y99,5
.2 :
-3@:
,.1:
9.?ff 2.2-6.0*: SAND: Dark yellowish orange (10 YRT/ii) fine grained, slightly clayey, silty. 1 ose to firm. p 2. 0 2.0 1001 hhih. . 5-$.v.: . . 2.0 1.5 751 -9:5 6.0-6.5': High re-6.0 j--- s m ance u pu W ng 0.5 0.5 100s Y' 6.0-24.0': CLAY: Dusky red (5 R 3/6) slightly spH t spoon. I 1.0 1.0 1.0 0.4 100% 40%
;/
silty, sandy, n mottled, stiff to very stiff. 8.5': 5/26/82 Stopped sampling. 8.5-15.0*- : NQ wire I 10 .- jgn,~ 4.0 2.5 631 - 0.0-15. 0' : Reamed 6" d. l t
?
2.5 0.0 C1
\
0.2 0.2 5 - 15.0-15.2': Split I iu
= 15 - spoon resistance TRX du, coring A 0.2/0.2.
4.0 0.0 01 2 15.2-30.0': Cored NQ j WL. 19.2-25.(f : Poor re-covery because inner 20 - barrel did not lock 21.0-24.0 *: Clay; blue white (5 8 9/1) and pale red purple (5 RP 6/2). Slightly I E 5.8 0.4 7% silty.
*177.7 24 - . _ , .
- - AP_PR_0x!
--- MATE _C_ON_T A_CT_ _ _ - ,. . _ _ _ _ _ _ _ - - - -- 24.0*: Orill mud 25j 24.0-152.0 * : SAND: Very pale orange (10 VR 8/2) showed sand.
;.[N: 93.. to moderately orange pink (5 YR 8/4) to
_9' dark yellowish orange (10 YR 6/6) slightly silty, fine grained, very dense, thin _y. bedding delineated by color , 5.0 0.0 01 _f l 30.0-48.0': Oriving l 30 - i. ., 2 7/8" split spoon. l 2.0 1.8 901 _
ikh 32.0 34.0*: 18 5/2'
,@ used sand trap, did
. not work.
I E 2.0 0.0 2.0 1.6 40% 80% _7.1 34.0-35.0 Gravel, silt. sand I 6.,. e,..=e6.,,w.ei
- o. .e==....i .. .,c e. o.o,=== POSTUL ATED MILLETT FAULT VSC-2 Macr es.
GEOL 0GIC DRILL L0G .0cmuc1,1c cm ,1-,u 1 95i0 2 -ie YSc., e . .n
* .s .: :. .a .
E s.
- : ; ; 3.. . , 3
- e .n e.s,s,u s nc .
o .,. . . . . . . . . ; g ........ . . . . . . . . . . . .
- o. , :, ,, ., .. ,= .
- s. *., , :: : .
1: a=, .s :. 1 ! 8 ' 4 :* g (Ft.) (Ft.) :
*
- ug, 35 2.0 24.0-152.0': SAND (cont): very pale orange 32.0-34.0 ': Gravel; 1.6 801 -
(10 YR 8/2Tto moderately orange (5 YR 5/4) well rounded. 2 mm to dark yellowish orange (10 YR 6/6), to 2 cr. 5.R.R.R. 2.0 1.4 70%
- silty, fine grained, thin to medium bedded.
delineated by color, dense to very dense. 2.0 1.4 705 Rim 40 - ! 2.0 1.0 501 - g M
~
- c;;4 42.0':5/27/82 Stopped
.,a.. . -. . ..:,
sampling. 2.0 1.1 55% 2.0 1.3 65% 45 fi
-i:.
2.0 1.3 65% 4 -
-': ::;p 48.0-600.0';
Total depth NQ WL. 3.0 0.0 01 -i:. ... 50 -ii@ s. 0.7 2.0 351 "I# = 53.0' : Dark yellowish orange (10 YR 6/6)
,. silty, fine-to medium-grained, dense to 2.0 1.0 50s , very dense, some slightly clayey lenses.
E - i 55.0-80.0': Sand in 55 - .y return drill mud. [ 3.0 0.0 01 [f.
.,I}
2.0 0.0 Os ..A
- u. -:.-
g 60 -'j 3.0 0.0 01 ~i[ l 2.0 0.0 01 W 65--H 3:
- a 3.0 0.0 01 -:::
[.:.' Pale orange (10 YR 8/4) to dark-yellowish-orange (10 YR 6/6), slightly silty, fine-to medium-grained, dense to very dense. 2.0 0.0 Ot - 70-'-;- 2.0 0.0 0% : l
-.\
3.0 0.0 C1 -? e . ........ .. .......; . . .. .. POSTULATE 0 MILLETT FAULT V5c-2 Mrcr s. a
GEOLOGIC ORILL LOG .-1u tuam mt== -T 95iO 3 - ie vsc-2
.. ei : =. . . i ....a enessuns
=
= =
3 : vezvs 3 .
=='=.==' ==
3
,= :, ;} . . = 6 v a v'.-
[ r j = = .c a ' 'a= a == < t a . .'- c a * a "U* * .0'.*l. gs : ; a
; .. . g 2; : !.
, eaaaaev== e-
=a'u'aa. = re.
.= :. s. c.:sc 5 . *= .!3 .
3
. ., . . . ; e (rt.) (rt.) =
I
.. s 3 . . . .
,,;,, ,e 24.0-152.0'; SAND: (cont)
_~
*4 3.0 0.0 01 -
-y' '
2.0 0.0 0 -25 80 -, :, 2.0 0.4 201 3.0 0.6 20% h,:Jt.5
.:r . . 48.0-105.0': Made list 85 'X5;:' of drilling variables (i.e.. RPM's water
- 2. 0 0.0 02 -!.! pressure, down pres-sure, water opening
-.. at end of inner
-:i barrel, drill mud.
etc.) and tried 3.0 0.0 0% - 3 combinations of these
~c on short 2.0-3.0'
.: . irs runs to recover sand.
90 [.:i: ::i 2.0 0.0 01 -1 E ~ O -..!. E 3.0 0.0 0% [ [ 8 - g 95 -:! . 8 -f: 2.0 0.0 0% '7
-l:: .
- 3. 0 0.0 0% 2.kU
-Mk;;
100 - 'f 2.0 0.0 01 ?- 3.0 0.0
~
Os 105 ::.
]:[ 106.0': Medium-grained, clean (sugar)
I 5.0 0.6 121 loose to firm.
.(S.:!!
110 -6:
~
t 5.0 0.0 01 -
?.
3
~
m
~~~
... ..s.,. ... ... te,,ves:
POSTULATE 0 MILLETT FAULT VSC-2
..........:.....c...: .. . ...
nacr so a
GEOLOGIC DRILL LOG voc1u tuam u=ma -1 Ss>0 . .. i 6 v5C-2
-,r.
.. n. . ..
. =
enessuna
.. a e
- ;e
; I 3 vaars 3 .
- . = . .a i
$ . t.w a re m w .. .c . erve.= a n . e ta ..ee sc a te. ' " , ' ' , ' , ' ,' ' ,
- j e , .!
ge
- I . g' *w ;* 5 ,'-3 3J . I l !. e C **C
= * "ma.'.'* .
. , ; ,s.
, *=
!> . ='C
$$ $ e 1 ! s E l (Ft.) (Ft.) e 1[ d 1*
- ii,w w
24.0-152.0': SAND (Cont) 5.0 0.0 01 2):, _
-Sa:-
120 -,.: 5.0 0.0 0%
- l.:.:.i.i 125 _
5.0 0.8 161 u 1302':': very pale orange (10 VR 6/2), clayey (kaolonite) fine-to medium-gratned, dense to very dense. y -t:. 5.0 0.0 01 m 3 . 5 -0:i$ g m -3,- E ~ 8 _~%. ,.' ' z I?5.0-140.0': Yellow green (5 G 6/4), 135.0-140.0': Appron-US.~ - sandy clayey silt; medium bedded with imately 0.5' core alternate silt and sand zones, very stiff fell in hole as bar-
..'- to hard. rel was pulled from 5.0 1.3 26%
over hole. 140 -':
~j ti
-?:
5.0 0.0 01 ~[ ' 145 Olive brown (5 Y 4/6) to licht olive (0 V 5/4), -
. silty, sandy, clay; some shell fragments,
_ slightly calcareous, very stiff to hard. 5.0 1.3 261 h
~
150-d [" !.f$
~
49.7 152_ CONTACT UNCERTAIN ( i 1.0') 5.0 1.3 261 152.0-233.8: CALCAREOUS $1LT5 TONE (MARL):
~
... . s.,. ..; .,... 6.. ....; .a's
,s5 4 . 6e ..
.. ........ ..e.,em..; .....e." POSTULATE 0 MILLETT FAULT V5C-2 MOCF 19 a
l GEOLOGIC DRILL LOG v=rutuc=ca -ti = = i eSi0
. = . . . . .
5 ie vsc-2 a. t a .5 :.. a waver PR ESSU R E g
- :* 3 3: 1E31s 3 .
......=>
;8 *: ;" .. .c = *r= = a a. c 6. .. .c a r... O" l*,;"l*g, is ;;o
$ *" ,, . . . t. v a v e..
{ t te la , . . a 3 . : 3 !< !. a.aev.. ..
=.6u=..
ae :: s = a ." eic
** ' :4. s a> = .v..
- El (Ft.) (Ft.)
I 18 a j a 1 . Id E" u.
, ice 152.0-233.8': CALCAREOUS SILTSTONE (MARJL :(cont) 155.0': 5/29/82
~
Dark greenish gray (5 GV 4/1), calcareous. Stopped coring. slightly sandy, clayey, numerous shell
, # fragments, hard to very hard, thin to
_ l medium bedded to finely bedded.
~
l 10.0 1.8 181 " 16h 3 s - m I 8 .~ 16 5.0 6.5 1 30% I 170-5.0 3.8 76%
~
v - g 17 t175.0': Slight gradational change. I w - 5 E! 10.0 10.7 1071 8 180-1
- \
- i 185- l I
2 Limestone: Moderately hard, light gray (N7)
- fine-grained lenses at 191.8 to 192.2.193.4- I 194.4.1%.3 to 196.7.197.7 to 198.1.199.1 to 199.3. 200.0 to 200.1. 204.6 to 205.0 l 205.3 to 205.5.
10.0 9.2 921 1 w - 8 I
.es .
...........=....,ca..;
.....uv.. ; .,. .. 6., , ...
.. ,,=.. POSTULATED MILLETT FAULT .,,,,,,,'gy3 R .c . ..a
GEOLOGIC DRILL LOG v= u m c m c == = = " ca ' esio . .. i . vsc.2
- i : :i .. ...
o: 3 3 i ; ! ; : i. !! !a. !;. i.; fffft-I
' 3 13 s -
a 5 : s !'
- i (Ft.) (Ft.) -
I' 1*
- 5.7 tes 152.0-233.8': CALCAREOUS 51LTSTONE (MARM(cont) 10.0 10.0 1011 [
= 2* :, l
~
E' 8 l
] +
2 205 -
' Polished surface 209.8 9 500 10.0 10.6 1063 210 e -
w w - g 8 215 -
~
g 215.8': Gradational change from grayish E v _ yettow green (5 Gv 7/a) to paie oisve (10 Y 6/2), slightly sandy. clayey. cal-
,, , careous. hard to very hard. some shell frag-
_ j ments. 10.0 2.7 271 220 225 -
~
l 2 I l
- I l
10.0 10.1 1011 239 _- !
~ -
E>
- I m
E>
-12.1 233.E Di
.......,. ..; e,. ...... ...i .
POSTULATED LIMTT FAULT
\stinctsharpcontact.
e......... ......... ... ... VSC-2 I HGC F 9 9-3
GE0 LOGIC DRILL LOG v=tutucmc===>=rt- 25m 2->6 V5c 2
.. 5 .. . . warra l
.. .a .5
. ; .; ,o r,.,.,u,a r
- i : ;. : :: :: : : ; . . . . . . . . . . . . . . . . . . . . . . ::::: n;;:;
;i . ; ? '; . .. : ;; . i ; 3 s .g-
- q i!;
; = ~ ~ * " * -
.h !. *
! 8 (Ft.) ( Ft,. )
, 4
- 34. 3 236 233.8-236.0'. LIMESTONE: White (N9) to s medium blutsn gray (5 8 5/1).
bioclastic, calcareous. soft to morterately ha.M. 10.0 1.1 111 l m.T RT w rpT m 236.0-256.5*. LIMESTONE: Grayish yellow green (5 GY 7/2), fossiliferous, sandy, sof t to moderately hard. becoming sandter and less cemented with depth. I 245 10.0 0.0 0% - 250 g . - 8 ~ - g 5 y 255 " 8 :
-54'8 256.5.
5.0 3.6 72 % _.)H?: 256.5-316.0 ': SAND: Pale olive (10 Y 6/2) clean I
'C non-calcareTus. fine-to medits.-grained.
loose to firm. ii . :
- &.s. G c$ 260.0: 5/30/82 26d O !!n Stopped coring
![N$.
?.
0.0 Ifk 5.0 0% -ff!!:0 I
~
- .c::.
265 : : f.' Olive gray (5 Y 4/1), fine-grained, slightly silty, carbonaceous. 265.9-270.0': Small amount of material caught by core I 5.0 0.0 0%
)W.".
UI.b0 catcher. I ~ 270 .?-
- )
.N
-;!l9::.,. Grayish olive (10 Y 4/2), fine-grained, slightly 5.0 1.0 20% -: .c.t silty, dense to very dense.
-:I !!s
, ,e ,
,gs , m , , ,, ,
.......... ..... ... . ...... VSC-2 Hacr is a
v==arcmcu==" = " 's'o a- a GEOLOGIC DRILL LOG vsc-2 warra
.5 .. ...*
t . r, . - . - arssuar g: ; ; ......=>
$ g" vr3rs I, - ,
gl * *
- 2, ;. . . . . v a r e.= l .
j =..<aw'.=aa. e 6 a . .. ee * * *= = U!*
- l'!",i',l, g
ta a. .
;a . i *; ; g .4 :, .a !.
l
. =aew =*. **c.
15 .'-
.~
11 d o' ;* a!l>
'2 2 vs 256.5-316.0': 5ANO: (cont) Dark greentsh gray (5 GV 4/1), non-calcareous, clayey, fine to medium gratned, fim, dense.
5.0 0.0 01
~!UI@.)
e, - !'.h w - s< M 280 -[: Il _ 8 5.0 0.0 Of , _i! 285 .~ 285.0-290.0': Sand
~
.'. caught behind core catcher (fine-to 3
[(dg[[[ medium-grained sand). 5.0 0.0 01 g 290 -6 w -79. %: 4 8
- 2 X..;f:
o _
- 5.0 1.5 301 '::
_3.S$S.i _x 295- .<.. 295.0: Sand return-
. .!!/U ing in drill mud.
_ W@; added barite to E-Z
. :. mud.
5.0 0.0 01 m '
- -'f?- 275.0-310.0': Sand fii? _9 in drill mud.
$ _~,f NE u :::
.?;
300_
~;.
~l .'
5.0 0.0 01 ~_}' .,.3. .. , Medium gratned, clean. 305.0-310.0*: Sample 305N: taken from rods i-
~I- tended in 80' from
~'fs:j bottom of hole at 5.0 0.0 01 _
. 310.0*
~.
~_
-.: e 31 0 - .
-a
- Medium-grained, clean.
5.0 0.0 01 -.. .fei 115~
....eu,.....; .,......,vv..; ' "***"*-
....==...=6 e. e.ve...: ...,=.= POSTULATED MILLETT FAULT v5C-2 Mccr s. a
GEOLOGIC ORlLL LOG v = m t u c m c u = T = Pla T 95i0 9 i. v5c- 2
- . i :. . . .
.. m. . . .
I .:
- : :. : ;: s : .e.... ! .
- .:: ==.;
e :: .< g . . . . . . . . . . . . . . . . . . . . . .
.I:
t.
- t .: n.
- . ; 'wa* . . . * .
t g.
- g: :
j* 3 g I j (Ft.) (Ft.) .
~
256.5-316.0': M (cont) 305.0-310.0*:(cont)
-114.3 316 Rid broke attempting
- 316.0 319.4' SILT: Very Itght grey (N8). to pull rods. 5/31/82 sedium Itght gray (ks). vedium gratned.
I 5.0 2.8 56g 117.7 319. 4~ pyrite /marcasite along streaked areas. 310.0: 6/2/82 Rig re-paired, washed back to bottom of hole 310.0' 316.0: Wer in. 319.4-354.0': ct M Blaish white (5 8 9.1) to I 320 - dfcated clay at this very lightTray (N8). mottled. dark reddish depth. brown (10 R 3/4) to dark yellowish orange (10 YR 6/6) and pale purple (5 RP 7/2) to 316.0 319.4 Several 5.0 3.1 62% grayish red purple ($ RP 4/2) slightly P'II5h'd #8C}}