ML19011A203
| ML19011A203 | |
| Person / Time | |
|---|---|
| Site: | San Onofre  |
| Issue date: | 12/06/2018 |
| From: | Southern California Edison Co |
| To: | Office of Nuclear Reactor Regulation |
| Shared Package | |
| ML19011A401 | List: |
| References | |
| Download: ML19011A203 (451) | |
Text
{{#Wiki_filter:2.5C APPENDIX 2.5.C SOIL BORINGS A total of 41 onshore borings were drilled to depths ranging from 6 to 987 ft in the plant area of the San Onofre Nuclear Generating Station, Units 2 and 3. In addition, 11 offshore borings and Jet probes were made in the area of circulating water conduits to determine nearsurface seafloor soil conditions. Locations of all onshore borings in relation to the plant facilities are shown on Fig. 2.5.C.1. Locations of offshore borings and jet probes are shown on Figs. 2.5.C.2 and 2.5.C.3. Borings were made by a variety of drilling techniques such as: rotary drilling, bucket auger, hollow-stem auger, jet probing, and vibracore. Both disturbed and intact samples were obtained during drilling by various techniques such as: Standard Penetration Test Method, Modified-California Sampler, Shelby Tubes, and Pitcher Barrel Sampler. In addition to sampling during drilling, a number of intact, hand-carved block samples were obtained for comparison testing to evaluate sample disturbance effects of conventional sampling techniques. Details concerning various investigations, including title and date of original report, number and depth of borings, type of drilling and sampling and PSAR/FSAR sections where the data can be found are summarized in Table 2.S.C.1. Amended: April 2009 TL: E048000
TABLE 2.5.C.1
SUMMARY
OF DRILLING AND SAMPLING No. of Original Report Title and Date Borings Depth Drill Rig Type of Sampling Where Data Reported Range, ft Seismic and Foundation Studies, 4 55-987 Bucket and rotary Pitcher barrel and San Onofre Nuclear Generating Proposed Units 2 and 3, San Onofre Dames & Moore Station Units 2 and 3, Amendment Nuclear Generating Station, 15 Apr 70, underwater sampler No. 1 to PSAR, 31 Aug 70, Dames & Moore Appendix 2B Continuous Seismic Profiling 4 (offshore) 10-22 Jet probe None SONGS Units 2 and 3, Amendment Investigation of the Continental Shelf No. 1 to PSAR 31 Aug 70, off San Onofre, CA 24 Apr 70, Marine Appendix 2B Advisors Inc. Solana Beach, CA Material Property Studies San Onofre 7 30-162 6-in. dia. rotary Modified California SONGS Units 2 and 3, Amendment Nuclear Generating Station March 13, Attachment 3. No. 11 to PSAR 1 Apr 72, 1972 Woodward-McNeill & Assoc. Appendix 2E Stability of Proposed slopes for the 7 40-300 5-in. dia. rotary Modified California SONGS Units 2 and 3, Amendment Proposed units 2 and 3, San Onofre and Pitcher barrel No. 17 to PSAR 18 Apr 73, Nuclear Generating Station, San Onofre sampler Appendix 2H CA, 27 Mar 73, Woodward-McNeill & Associates Dynamic Switchyard Slope stability 13 35-80 5-in. dia. rotary and 6-in. Pitcher barrel, SONGS Units 2 and 3, FSAR confirmation Proposed Units 2 and 3, dia Modified California Appendix 2.5.E shelby tube sampler San Onofre Nuclear Generating Station and continuous San Onofre CA, 18 Oct 74, flight Woodward-McNeill & Associates Offshore Liquefaction Evaluation for 3 (onshore) 40-60 6-in. cont. flight auger Modified California SONGS Units 2 and 5, FSAR the Proposed Units 2 and 3, San Onofre 7 (offshore) 3-7 and 5-in rotary pitcher barrel and Appendix 2.5.A Nuclear Generating Station San Onofre shelby tube sampler CA, 19 Dec 74, Woodward-McNeill & Amended: April 2009 TL: E048000 Associates Final report on Geologic Features at the 7 6-25 Bucket auger None Submitted by letter, J. B. Moore to San Onofre Nuclear Generating Station O. D. Parr Aug. 11, 1977 5 Mar 76, Fugro, Inc. 2.5C-2
San Onofre 2&3 FSAR Updated APPENDIX 2. 5D LABORATORY TESTING AND SOIL PROPERTY EVALUATION Site File Copy Amended: April 2009 TL: E048000 Site File Copy
APPENDIX 2.S.D LABORATORY TESTING AND SOIL PROPERTY EVALUATION A total of 7 separate laboratory investigations were con-ducted for evaluating the soil properties at the San Onofre ~uclear Generating Station Units 2 and 3. Both static and dynamic testing was done to estimate soil parameters to be used in static stability studies and dynamic response and liquefaction analyses. The total number and purpose of the more important tests are summarized in Table 2.S.D.l. Details concerning various inves-tigations including title and date of original report, types of laboratory tests included in each investigation and PSAR/FSAR section reference where data can be found are summarized ln Table 2.S.D.2. 2.5D-l Amended: April 2009 TL: E048000
TABLE 2.5.D.l LABORATORY TEST
SUMMARY
PURPOSE TOTAL NUMBER
=
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Moisture/Density <':I C 138 Grain-Size Analyses
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VI"'::l Chemical Analysis as 1-+ 4
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Thin-section Examination I
- 2 Field Density Insitu Strength/Density 130 Compaction Compaction Characteristics 6
~inimum/:Vlaximum Dens i ty Estimate Relative Density 2 Unconfined Compression Static Strength 22 Triaxial Compression Static Strength 32 V Direct Shear Static Strength i Strain-Controlled Modulus and Damping para-Dynamic Triaxial meters 47 Stress-Controlled Dynamic Triaxial Liquefaction 1.31 2.5D-2 Amended: April 2009 TL: E048000
C" (" C"" San Onofre 2&3 FSAR Updated TABLE 2.5.D.2
SUMMARY
OF LABORATORY INVESTIGATIONS Original Report Title and Date Type of Tests Where Data Reported Seismic and Foundation Moisture/Density, Grain si%e, San Onofre Nucleer Generating Station Studies, Proposed Units Unconf. Compression, Trtaxial Units 2 and 3, Amendment No. I to PSAR 2 and 3, San Onofre Comp .* Direct Shear, Dynamic 31 Aug 7D, AppendiX 2B. Nuclear Generating Triaxial Station, 15 Apr 7D, Damas & Moore Material Property Studies Moisture/Density, Grain Si~e, SONGS Units 2 and 3, Amendment No. 11 San Onofre Nuclear Gen- Unconf, Comp., Field density to PSAR, 1 Apr 72, Appendix 2E, Attach-erating Station, Hax/Min density, Dynamic Triaxial mant 3. Woodward-McNeill & Associates, March 13, 1972 Stability of Proposed Slopes Grain Size, Unconf. Camp., Triaxial SONGS Units 2 and 3, Amendment No. 17 for the Proposed Units 2 and 3, camp. to PSAR, 18 Apr 73, AppendiX 2ft San Onofre Nuclear Generating Station, San Onofre, CA, 27 Mar 73, Woodward-McNeill & Associates Liquefaction Evaluation Report, Compaction, Dynamic Triaxial SONGS Unit$ 2 and 3, FSAR, Appendix 2.5.A Proposed Units 2 and 3, San Onofre Nuclear Generating Station, 22 Jan 74, Woodward-McNeill & Associates Dynamic SWitchyard Slope Hoisture Density, Grain Si%e SONGS Units 2 and 3, FSAR, Appendix 2.5.! Stability Confirlllation, Proposed Sp. Gravity, Unconf. Comp .* Dynamic Units 2 and 3. San Onofre Triaxial Nuclear Generating Station, San Onofre, CA, 18 Oct 74, Woodward-McNetll & Associates 3 Offshore Liquefaction Evaluation Grain Si~e, Field Density, Dynamic SONGS Units 2 and 3, FSAR, Appendix 2.5.A m
- J 0- for the Proposed Units 2 and 3 Triaxial m San Onofre Nuclear Generating 0-
>> Station, San Onofre, CA 19 Dec 74, Woodward-McNeill & ~ Associates I\.l a a(0 Analyses of Properties of Finer- Grain Si:lle, Sp. Gravity, Compaction. Submitted by letter K. P. Baskin
--I Grained Sen Hateo Send, Units 2 Static Triaxial, Dynamic Triaxial to O. O. Parr, November 12, 1976.
r and 3, 31 Dec 74, Woodward-HcNeill m & Associates a .jO>. co a Revision 9 a a 2/93 2.5D-3
San Onofre 2&3 FSAR Updated APPENDIX 2.5E DYNAMIC SWITCHYARD SLOPE STABILITY CONFIRMATION Site File Copy Amended: April 2009 TL: E048000 Site File Copy
DYNAMIC SWITCHYARD SLOPE STABILITY CONFIRMATION PROPOSED UNITS 2 AND 3 SAN ONOFRE GENERATING STATION SAN ONOFRE, CALIFORNIA for Southern California Edison Company P. O. Box 800 Rosemead, California 91770 by WOODWARD-McNEILL & ASSOCIATES Consulting Engineers and Geologists 2.5E-l/2.~E-2 Amended: April 2009 TL: E048000
Los Angeles 18 October 1974 Project No. B469A4 Southern California Edison Company P.O. Box 800 Rosemead, California 91770 Attention: Mr. David H. Johns SUBJECT DYNAMIC SWITCHYARD SLOPE STABILITY CONFIID1ATION PROPOSED UNITS 2 AND 3 SAN ONOFRE GENERATING STATION SAN ONOFRE, CALIFORNIA Gentlemen: In accordance with the prOV1Slons of your Purchase Order No. U0804901, we have completed our analyses of the dynamic stability of the proposed switchyard slopes at the subject site. The attached report transmits the results of our studies. In brief, the results indicate that for DBE loading, the switchyard slopes will be stable, with localized surficial sloughing possible. Also, the analys~s indicate that some lenses of material within the terrace deposit may become over-stressed, however, it is not felt these will contribute to instabili~y as they are not near any slope surface. . If you have any questions or require further information, please contact us at your convenience. Very truly yours, WOODWARD-McNEILL &ASSOCIATES BY~~ Jo n A. arnelC BY~ By~W1LJ~ AnTeW H. Wo rswiC JAB:RLMcN:AMW:ls Attachments 2.5E-3/2.5E-4 Amended: April 2009 TL: E048000
TABLE OF CONTENTS LETTER OF TRANSMITTAL TABLE OF CONTENTS
1.0 INTRODUCTION
1
2.0 DESCRIPTION
OF SLOPE CONSTRUCTION 2 3.0 GEOTECHNICAL CONDITIONS 2 3.1 General Site Conditions 2 3.2 Subsurface Conditions 3 3.2.1 Soil Conditions 3 3.2.2 Gpoundwater conditions 4 4.0 DISCUSSION AND CONCLUSIONS 5 4.1 Soil Properties 5 4.1.1 Dynamic Stpength 5 4.1.2 Dynamic Stiffness and Damping 5 4.2 Groundwater Conditions 6 4.3 Finite-Element Studies 6 4.4 Dynamic Stability Evaluation 7 5.0
SUMMARY
OF CONCLUSIONS 8 FIGURE 1 - SITE PLAN FIGURE 2 - SECTION OF PROPOSED SWITCHYARD SLOPES FIGURE 3 - SONGS UNITS 2 AND 3 SITE, 1928 FIGURE 4 - SONGS UNITS 2 AND 3 SITE, 1972 FIGURE 5 - IN-SITU DYNAMIC STRENGTH ENVELOPES FIGURE 6 - DISTRIBUTION OF TEST RESULTS, DEGREE OF SATURATION ANALYSIS FIGURE 7 - RESULTS OF STABILITY EVALUATION FIGURE 8 - ZONES OF FACTOR OF SAFETY '\..../ 2.5E-5 Amended: April 2009 TL: E048000
TABLE OF CONTENTS APPENDIX A - FIELD INVESTIGATION APPENDIX B - LABORATORY INVESTIGATION APPENDIX C - SOIL PROPERTIES APPENDIX D - FINITE ELEMENT STUDIES APPENDIX E - STABILITY EVALUATION APPENDIX F - REFERENCE GUIDE 2.5E-6 Amended: April 2009 TL: E048000
DYNAMIC SWITCHYARD SLOPE STABILITY CONFIRMATION PROPOSED,UNITS 2 AND 3 SAN ONOFRE GBNERATING STATION SAN ONOFRE, CALIFORNIA
1.0 INTRODUCTION
In accordance with the provisions of our proposal dated 7 Nov 73, Item 1 of Amendment No. 19 to the Preliminary Safety Analysis Report, dated 25 Jul 73, and your Purchase Order No. U080490l, we have conducted a geotechnical investigation and provided consulting services for DBE Switchyard Slope Stability Confirmation, San Onofre Generating Station, Units 2 and 3, San Onofre, California. Previous analyses of the stability of the pro~osed switchyard slopes have been made, and are presented in our report entitled StabiZity of the Proposed SZopes for the Proposed Units 2 and 3~ San Onofre Generating Station~ San Onofre~ CaZifornia~ dated 27 Mar 73. The purposes of the present studies are:
- 1) to supplement previous field investigations in determining the areal degree of saturation of terrace soils,
- 2) to collect and dynamically test selected samples of the critical (weakest) materials encountered during the field investigation, and
- 3) to perform analyses to evaluate dynamic stability of the proposed switchyard slopes.
These studies involved field and laboratory investiga-tions, which are discussed in Appendicies A and B, respectively. Other factual data are presented in the appendicies as follows: Appendix C, Soil Properties; Appendix D, Finite-Element Studies; and Appendix E, Stability Evaluation. Appendix F presents a 2.5E-7 Amended: April 2009 TL: E048000
Page 2 reference guide to aid the reader in locating specific items referenced in Amendment No. 19 to the PSAR. A description of the proposed slope construction is pre-sented in Section 2.0. Geotechnical conditions, interpreted from boring log information, air photos, inspection of site grading operations, and previous studies of the site, are discussed in Section 3.0. A discussion of the significance of these conditions as they relate to the proposed development, and our conclusions, are presented in Section 4.0. A summary of our conclusions is presented in Section 5.0.
2.0 DESCRIPTION
OF SLOPE CONSTRUCTION It is proposed to construct a series of slopes and benches between the proposed SONGS Units 2 and 3 plant grade (elev. 29 ft) and existing Highway 101 (approx. elev. 115 ft) for use as a switchyard. A site plan showing the proposed slopes is presented on Fig. 1.' A cross-section through the proposed switchyard slopes 1S presented on Fig. 2. The slopes will be cut, as reflected by the difference between existing and final grade indicated on Fig. 2. Southern California Edison has indicated that the switchyard structures proposed for construc-tion will be supported on shallow spread footings or drilled pier foundations. Southern California Edison has indicated that switchyard structures, including their foundations, will be designed such that their associated loads will not change the conclusions of the slope stability analyses. 3.0 GEOTECHNICAL CONDITIONS 3.1 General Site Conditions The proposed site for Units 2 and 3 is located adjacent 2.SE-8 Amended: April 2009 TL: E048000
Page 3 to and south of the existing Unit 1, as shown on the Site Plan, Fig. 1. At the present time the switchyard slope area has been graded. The upper slope has been cut to approximately the finished grade. The lower slope h~s been temporarily cut to an inclination of ~:1 (horizontal to vertical) to pro-vide a larger working area for construction. This slope will be cut back to a finished 2:1 grade at a later date. Prior to excavation for the plant site, near-vertical bluffs along the beach rose from sea level to approximately elevation 80 ft. From the top of these" bluffs the natural ground surface rose gently toward the existing Highway 101. Photos showing the topography of the site in 1928 and 1972 are presented as Figs. 3 and 4, respectively. Fills were constructed in the proposed switcnyard area, adjacent to High-way 101, during grading of Unit 1. These fills, which have been removed, prOVided an area for the Unit 1 switchyard and tourist center. 3.2 Subsurface Conditions 3.2.1 Soil Conditions Boring log data (Appendix A), laboratory test re-sults (Appendix B), information from previous studies, and data obtained from inspection of cut slopes excavated on the site, were considered in determining soil condi-tions. A schematic representation of the distribution of soils at the site is included in Fig. 2. As indicated in Fig. 2 the upper portion of the switchyard slope consists of terrace deposit materials. These materials, which extend beneath the surface to 2.5E-9 Amended: April 2009 TL: E048000
Page 4 approximately elevation SO ft, consist of very dense ~ and very stiff soils. The upper portions of the terrace deposit (above approximately elev. 80 ft) are generally clayey sands to silty clays. These materials are under-lain by predominately gravelly sand materials, with occa-sional lenses of clay, silt, and cobbles. The soils which constitute the base of the terrace deposit (approxi-mately elev. SO to 60 ft) are quite variable. In some areas coarse gravel and cobbles are present, while in others silty sand, sandy silt, or silty clay exists. These materials are underlain by the San Mateo Formation, which extends to approximately elev. -850 ft. This for-mation consists of a dense to very dense, well graded sand with apparent cohesion due to efficiency in packing. The borings made during this investigation indicate a slightly different distribution of soils than has been described in the PSAR, however, the dynamic strength of these materials appear to be as high or higher than pre-viously assumed. A discussion of the pertinent soil properties used in the analyses is presented in Section 4.1. 3.2.2 Groundwater Conditions No groundwater was observed in any of the borings made for this study. All boring-log data from previous studies indicate that no free groundwater was present above elev. 5 ft (MLLW Datum). Southern California Edison has indicated that piezometers on the site indicate the ~ groundwater surface is at approximately elev. +S ft *
.2 .5E-IO Amended: April 2009 TL: E048000
Page 5 4.0 DISCUSSION AND CONCLUSIONS ~ 4.1 Soil Properties 4.1.1 Dynamia Strength One of the primary purposes of this study was to define accurately the dynamic strength of the terrace deposit soils. To accomplish this an extensive labora-tory testing program was performed. The details of this program, as well as other tests performed, are presented in Appendix B. In general, the results of the testing program indicate the terrace soils have strengths as high as, or higher than previously assumed. There do appear to be occasional thin lenses of weaker materials in the lower part of the terrace deposit which: 1) appear to be horizontally stratified, 2) are not continuous through the siopes, and 3) are generally less than 3 ft in thick-ness. Our analyses have considered the possibility that weak lenses exist throughout the sandy lower portion of the terrace deposit, as outlined in Appendix E. The interpreted strength curves for this material, as well as the others which are present in the profile, are pre-sented ~n Appendix C. A summary of the interpreted strengths for all materials is presented in Fig. 5 for easy reference. These curves were drawn considering the lower bound of strength data to be defined at +S% strain or 10% total strain, whichever occurred first. 4.1.2 Dynamiq Stiffness and Damping The cyclic triaxial test data were analyzed in order 2.5E-ll Amended: April 2009 TL: E048000
Page 6 to estimate dynamic stiffness and damping properties of the terrace soils, as outlined in Appendix B. These data indicate the sandy portion of the terrace deposit are somewhat stiffer than previously assumed. This change was incorporated in the finite-element model for our studies. These data indicate that the damping assumed for this material during the previous studies was appro: priate, as were the stiffness and damping values for the other soils at the site. The stiffness and damping properties used are presented in Appendix C. 4.2 Groundwater Conditions Analyses were made of the areal degree of saturation of the terrace deposit soils, as outlined in Appendix C. A summary of the analysis of 79 samples is presented in Fig. 6. Figure 6 indicates that: 1) no samples tested were 100% satu-rated; 2) samples with a degree of saturation of greater than 70% were predominantly clayey; and 3) the average degree of saturation is approximately 50%. Southern California Edison has indicated that careful surficial drainage control for the site will be implemented, therefore no significant changes in groundwater conditions are anticipated. 4.3 Finite-Element Studies In order to evaluate dynamic stability, a finite-element model of the slope-foundation system was developed. Static and dynamic computer programs were then used to estimate exist-ing and earthquake-induced stresses throughout the profile. Details of the finite-element studies performed are presented 2.5E-12 Amended: April 2009 TL: E048000 I
Page 7 In Appendix D. The output stresses from the finite-element programs were compared to the dynamic soil strengths (Appen-dix C) in order to evaluate dynamic stability. 4.4 Dynamic Stability Evaluation Analyses were made to determine the number of equivalent equal significant stress applications induced in the soil profile by the DBE to facilitate comparison of induced stress to the dynamic soil strength. Details of these analyses are presented in Appendix E. Analyses were made assuming 1) the most likely soil conditions which exist (based on boring "log data, examination of graded slopes, etc.), and 2) weak lenses are present throughout the iower portion of the terrace de-posit. Based on the results of these analyses it is concluded that, during DBE loading, 1) the overall factor of safety of the switchyard slopes is in excess of 1.0, 2) surficial sloughing to a maximum depth of 5 ft may occur on the upper-most switchyard slope, and 3) overstressed zones may develop in localized portions of the terrace deposit. These zones are shown schematically on Fig. 7. Interpreted factors of safety of each finite element in the slope are presented on Fig. 8 (Factor of Safety is conservatively defined as the ratio of dynamic stress necessary to cause 10% strain for 80 stress applications to the corresponding seismic induced stress as detailed in Appendix E). It is our opinion that the over-stressed zones will not cause instability because there are many stable areas between those which are overstressed and any free surface. Further, the soil strata are essentially 2.5E-13 Amended: April 2009 TL: E048000
Page 8 horizontally stratified with stronger lenses interbedded with weaker ones. The 80 stress applications (consistent with the DBE synthetic time history) used in the present analysis was chosen to demonstrate the stability of the slopes when sub-jected to a very conservative seismic, loading. As a comparison a more realistic number, one consistent with earthquake en-gineering practice for a single severe event (DBE-type), would be on the order of 30 cycles, or less than half the number used in the present analysis. 5.0
SUMMARY
OF, CONCLUSIONS 5.1 In general, the results of the testing program indi-cate the terrace soils have strengths as high as, or higher than previously assumed. 5.2 There appear to be occasional thin lenses of weaker materials in the lower part of the terrace deposit which: 1) are essentially horizontal; 2) are not continuous through the slopes; and, 3) are generally less than 3 ft in thickness. 5.3 Laboratory test results indicate that the dynamic stiffness and 'damping values used in the previous analyses were appropriate for the three primary'site soils (i.e., terrace sands, terrace clays, and San Mateo Sand). The maximum deviation was exhibited by the terrace sands where the modulus was somewhat higher than previously assumed (approximately 12% maximum). 5.4 Extensive laboratory testing indicates that the terrace soils in the subject area are only partially saturated, with an average degree of saturation of approximately 50%. 2.5E-14 Amended: April 2009 TL: E048000
Page 9 5.S Our analyses indicate that during DBE loading: 1) the overall factor of safety of the switchyard slopes is in excess of 1.0; 2) surficial sloughing to a maximum depth of S ft may occur on the uppermost switchyard slope; and 3) over-stressed zones may develop in localized portions of the terrace deposit. It is our opinion that the overstressed zones are unlikely to lead to instability, as discussed in Section 4.4. 2.5E-15/2.5E-16 Amended: April 2009 TL: E048000
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!! Stre~s
>> r-3 r-m III
- J Q.
m (n Cl. (n >> 0 r? "':l ~ ce 1-" I\.l * -i OQ a PI a(0 In
--I r.
m a
.jO>.
co a a a ( ( c
APPENDIX A FIELD INVESTIGATION Between 19 Mar and 2 Apr 74, 13 borings were made at the site for this study. It was originally planned to make 5 to 10 borings of about 100 ft average depth (as described in Amendment No. 19 to the PSAR, p. 1.8 . 2bo). The intent was to have all borings penetrate into the San Mateo Forma-tion. However, at the time of our field investigation grading was in progress, therefore it was not necessary to make borings as deep as planned in order to reach the San Mateo Formation. The locations of these borings, as well as those made during previous studies, are shown on the Site Plan, Fig. 1 Borings were advanced with a 6 in. diameter continuous flight auger drilling rig and a 5 in~ diameter rotary drilling rig using mud. The rotary drilling rig was used for the pur-pose of advancing a Pitcher Barrel Sampler to obtain additional laboratory dynamic test spec imen s . It was determined during the initial phase of rotary drilling that drilling mud did not alter the moisture content of samples, therefore borings were advanced by this method rather than air-drilling techniques, as originally planned. Samples were generally taken at 5 ft intervals with a modified California Sampler, a Pitcher Barrel Sampler, and with Shelby Tubes. In addition, bulk samples were obtained from cuttings removed from the borings. Details of the drilling and sampling program are given on the Key to Boring Logs, Fig. A-I. Boring logs, which are based on examination of 2.5E-Al Amended: April 2009 TL: E048000
Appendix A Page 2 soil samples obtained during drilling, and laboratory test results, are presented on Figs. A-2 through A-l4. In addition to logging and sampling the borings, the slope face was closely examined as it was exposed during grading, and carved block samples were obtained. This procedure was used in lieu of making five test pits (as discussed in Amendment No. 19 to the PSAR, p. 1.8 - 2bo) because more detailed and representative data could be obtained. These data, laboratory test results (Appendix B), air photos, and information generated from previous studies were used to evaluate soil properties and distribution, which are discussed in Appendix C. 2.5E-A2 Amended: April 2009 TL: E048000 I
~
0
... >- U) 0 -~J: :::.e ~ ~
Q. W 0. u; fia:: U- U) (I) U- ::::E~ V J:
~ W
~
- a. en ::JW DESCRIPTION 0-0
(.)z 0::1-
- JZ Z w-W
~
~ 3; ~w o~ a::
-41 Q.
Uj
~
C( 0 o~ 0::C( (.)a:: (/)1-
-z )0-w 0 II)
~
~~ ZI- 00 0:: J:
CD
- JU) ::::E(.) 0 0
~
SURFACE ELEVATION
- SK 7 Medium dense . moist , brown SILTY fine-graine d SA~D (SM)
\
- 10
- I *
\1 5-
- I Unifie d Soil Classification----~
~ Measv red Static Water Level
~ Number of Blows Requi red to Advan ce Sampl er One Foot
~--- ---- Tube Sample Locat ion
'---- ----- - Sampl e Number Indic ates Sampl e Tested for Other Prope rties M.A. - Grain -size analy sis S.G. - Speci fic Gravi ty Test C.T. - Cyclic Triax ial Test Notes on Field Inves tigati on
- 1. Borin 8s were advan ced with a 6" diame ter contin uous fligh t auger or a 4 7/B" diame ter rotary drilli ng .rig using mud.
- 2. Sampl es with record ed- blows /ft. (label ed Ml, M2, etc.)
. were obtain ed with ~
Modif ied Calif ornia drive sampl er (2" inside aiame ter) lined with sampl e tubes . Sampl es labele d S11, ST2, etc .....ere obtain ed with Shelb y Tubes (2.713" inside diame ter) hydra ulical ly drive n. Sampl es labele d PI, P2, etc., were obtain ed with a Pitch er Core Barre l Sampl er.
- 3. Class ificat ions are based upon the Unifie d Soil Class ificat ion System , and includ e color , moist ure, and consi stenc y. Field descr iption s have been modif ied- to refle ct resul ts of labor atory analy ses where deemed appro priate .
- 4. NR indic ates no sampl e recov ery.
Project : SO~GS SLOPE STABILITY Job Numbe r: B469A l KEY TO BORING LOGS Fig. A-I 2.5E-A3
DATE OF BOR'G 19 lIar.74 WAT!!:R DEPTH OAT!!: M!ASUR!!:O UMP!,.ES Ca11tornia al\d Shelby Tub~ TYPE OF DRILL. RIG COl\t. Fl1~ht Augar Halo! DIAMETER 6" WEIGHT 01' HAMMER 140 Lbs , FAI,.LI"'G~
.i ..
] wit LS ~.: e . ..
~
w
- ll;; .. z Z 0-s OUCRUITIOH. . 8. .. w w *
. w j ; 0~ ..
~= 8 0 '"
0 SVRFil,CE ELEVA-TIO"': 102' l1ed1um sUff, ""1st. dari< brOVll SA.,.'lll'C CLA'C (CL) (FU1) SF: 1 Vart d....... lIIDist, CUYEY So\ND (SC) with GRAVEY.
~1 62 12.3 119 SG nII\Ct** sil\g CUt COI\Ullt 10- ~ 56
- 7.4 121 SG
- iA xs 78 12.6 12$ SG SK 2 Vary de"..e, u-P, brown SILt"l' SA.'lll (Sl1) wirh G1U.V£L lo- ~4 73 4.9 121 SG
~all$e, d~, light bro"" Ci>..W£LL'C So\ND (Sill
- l'.5 34 1.2 125 SG ST Oann, lIIObt. redd1s11 beD"", SILt"l' $A..W (Sl'll l'.A l
- ~7. llt C1 B
30- Oe"aa to vert da"se. damp, Hght bro.... GltAV£LLt SA.'ID (SII) X6 76 2.9 lOS SG La"s of SIL'l"Y So\ND (Sl1)
',11th COllBL£S to 6" b """.
~7 ~O 6.4 125 SG of Ss:'llly SIL'I: (llL) 40-
)!8
- 5.72 40.
10.6 115 SG uease , d""'P, brown r.R..WtLLY SAND (S;/) vi th COBBLES to 5" 0 (C"able to s"",p1e due to COllllLZS)
~-
- De"u. daep , yano... SA.'lll (SIl)
- 30rtolO of bot:'ng at S7'l ft. de,th (e Iev, 44.$~t.)
60-
~o \later ebse rved in b-orin~ ~o-eo-PfO._Ci:
Job
';ONGS StOr~ S: ..IJHL::Y N"",.,..,.: .l,:
~:::'..) .
LOG OF BORING I ~i .. A-2 WOOOWARO-McNEIL.L. a ASSOCIATES 2.5E-A4 Amended: April 2009 TL: E048000 I
DATE OF BORING ~~ :-<.ar.74 WATER OEPTH DATE MEASURED SAMPLES ~d. Calif. & Shelby Tube TYPE OF DRII.L. RIG ccne , Fl1~ht ~u~er HeL!; DIAMETER 6" WEIGHT OF HAMMER 140 lb s , FALLING~ i ..
- i
....0; ...c ....~ ~
]
.,; ~
~ po
~ po II L~
- I Po
,.: ; po
- >z 0 o
- Z oJ po ..
Z DESCRIPTION
~
uZ !!po Ow o z l;le:
- II l!l * * :118 oJ )- 'I:
Po
- >. 0 0 SURFACE ELEVATION' H2' SI(. M.di.... d~nse , "Ght. b~o"" SILTY SA.'lD (8M) (FILL) 1 0
SI(. lIadiUlll stHf, lI1Oht, darK brQloll\ SA.'IDY CLAY (CL) 2 h Grading SILTY n
- il
. 51<
66
- iedium dense to danae III moist, light oro"" SILTY SAND (SM) with SOlOe GMVEL U.8 114 SG
- 0- 3 Grading darK oro""
- :11ST 23 3.4 120 SG MJ 1
44 J With COBBL~S
)IA 0 7,4 131 SG rr ze:- 114 H 7.8 121 Grading VOl"'; d.nn 6.8 134 sc
- ll.S 93 6.9 140 5G D.nse. IlIOht. reddish ,roW'C1 SILty SA.';\) (Sll) 30- 116 76 3~4 109 SG
* ':.ry dense, daOlI'. brown GRAVELLY SA..'lD (SW) vith COBBW:S to 4"
.. J 94 ~l Lens of SILTY S....';\) (SM) 2.5 113 sc 4Q-lIS 66 4.3 127 sc
- i9
~
9" Very d....se , damp. tan 5IL71 SA.';\) (SM) 30- ST Very dense. !DOht, tan CMnLLY SA..'lD (5;;) .. itn COB8L::S 2
~,
M IT no 10 3.6 SG J1A Caving in COBBLES 60-30ttom of oaring at 6011 ft. de"th (Olley. 51. 5f.e.)
~o vater ooserved in boring 10-0 SO-
*0 90-00-Projetl :
I LOG OF BORING SJ;":~S ::J1..0?~ ~T.A!I:"!:Y FIt-JoO NymOer : 3!...I)~.J.~ 2 A-3 WOODWARD McNEILL a AS SOCIATES 2.5E-A5 Amended: April 2009 TL: E048000
DATE OF BORING n :-Iar.74 W.. TER OlPTH o..n MUSU"EO SAMPLES )lad. Callf. & Shelby 1'lIbe TYPE OF .,jRILL RIG Cons, "', igb,r; ouger HOLl OI.... UER 6" WEIGHT OF HAMMER 140 1bs. FAL~JNG 30 11
.. .. ......~ e ... ....
,.; J
; "-i oj~ !:
..i C':
oj w :I .. ::Iz "z Z
..l OUCIUPTION 8: "w w_
- a. C
~
- a. ,w !! .. ~
* * ~
- II oz
~ <C "lit z ..
~.
- 18 II:
Q '" 0 SURFACE ELeVATION: LL2 r SK O.Q.se, moise, dark br~ C~Y&Y SAND (SC)
-- 1
- -11 36 4.S 113 SG t"T Dense.. moise, lighe brown SILTY S~~ (SX)
SK Gr a d ** eo CLAY~ 5&~ (SC) 2 10- :a 60 U.8 129 SG
- 5K StHf. lII01n, dark bra"" SANDY C~Y (CL)
_ 3
.1I3 46 IT Grading l1ghter brown with Gil.AvtL to 3/4" 8.5 132 SG SK 4
ZOO- )14 38 8.0 129 5G
-~
jj 7.6 132 SG Very dense, moist, brow SILT'! S&'iD (S~) wit!! .0.... GRAVEL 30- ){6 74 b Reddish brown 3.4 103 SC _ Sf\: Very dense, damp a gr.ay GRAVELLY S&'ID (SII) 5 _ !'l7 ~ense. soist, reddi.h brown CLAYEY S&'iD {SC) wit!! GRAVE!; to 1"
~8 7.75 15.9 119 SG ST
- 1 Very d.n.... d_II. gray s,\~ (SP) 40- lIS 95 2~5 103 SG
* ~9 rf%;,0" ~.~erJ dense, damp, yellow S&'lD (511) S~~ ~AT!O FO~~~10N 1. ; 102 SG 30- II
- 10
~" 2.7 105 SG IT Could not ...... ple due to cave-in of GlI.AVi:LLY :oaterial above 6C-SK 6
rc
- 30teom of boring ~t 70 fe. i!.e-pc!l (e Lev
- 0:0 -",at.:- oD8e:ve:d in. ~or;in.8
*2ft. ) ~o- ~o- )C-Projee! : SOllGS S!.JP! ;'MIUTI Joo N.."'lIe. : 3A~Hl LOG OF 'eO~ING F:-:.
A-4
""OOOW<l,i/O l,leNE.LL: a ....
),sSCC,,~,_5 2.5E-A6 Amended: April 2009 TL: E048000
DATE OF eOIUNG ~S ~r. 7~ WATER DEPTH DATI!: MEASURED SAMPLES ~od1fied Caj,,(ornu TYPE OF oRI!,.!,. RIG cene , Fl1~ht Au~er HOLE OIAMETE" 6" WEIGHT OF HAMMER 1:.0 los. FALLING 30"
,.; ~
0,;% ,. ' ;; 0" ....
.. ;It DESC"JPTrON a .. :lz lit
..0:.
..,lIt !! ..
L OZ
- I 0 SURFACE ELEVATION: U2 t
~:;
= 0
- Stif!, dam", broltn SILTY CLAY (ct) \lith GlUVtL
- T
- Grading SA:my xi 25 1--+-------:---':"'"""--::=~_:_:~_::_:-7"":"__::::_::_::::_-"'7":::__-----_I
'0 -
lled1UCll dense, deQl.p, browu SILlY SAm> (SlI) with GRAVEL to It" 6.2 109 SO
-lU 26~+---------------------------_J 5.7 14.6 120 SO Stiff, damp, broltn CUYE'{ S.IND (SC) 20'-llJ 531--1--------------------------------;14.5 13.4 U4 SG Very stHf, d3mp, brown SA.'lDY CUy (eL)
_ ll4 62 17.6 114 5G 30-xs 007~~:;;_,l-+----------------------------- [10" _i Very denso, damp. gray GRAVELLY SAo'ID (S~)
- t-,-oon.o '. "'_,) 108 SG 40- !Ii 86 Vory donn. damp. tan SILTY S....'ID (SM) :.4 124 SG
~
* !IS ~, 2.~ 118 So so-
- 119
~ ..
"0 108 50
** Botto... of boring at nit ft. depth (ele". 60,5ft.)
- water ob'et'led 1n boring
~o ~c-70-eo-JO-prOl1e: : SONGS SLOPE STAlllL.~ Fit.
Jail 11\1"'"': 3469,11 ~OG OF BORING* 4 A-5
'NOOCWARO*MtNEILL EI ,l,SSOCIATES 2.5E-A7 Amended: April 2009 TL: E048000
DATE Of' BORING 27 liar. 74 WATfR DEPTH OAT! MlASUftfO SA.... LES liad. Calif. & Shelby Tube TYPE OF ORIL.L. RIG Cant. flight .~u!e'5' HOLE OIAM!TEIt* 6" WEIGHT 0' HAMMER 140 Ib~ .. 30" FAL.LING
.. ...... eJ &:z1 . . ........
~
~
~
.... ,. .. ~
.... cO: ;;
i "'z z o*
- II" Q
z O£SC'UPTION**
~ s ua c Ii: ," Q
~ u
- II iSz l!: * :i !: :IIQ U C Q ~
SURFACE EL.EVATION: 112'
~d1WIL densCl, d.... I', ten~gra.y GR.A.VELLY SANll (SIo') Uill)
- Stiff, d~, brawn SANDY CLAY (eL)
.0-
*STl 5T2 P GR.A.VEL lens ZG"-
- ST3 Dens... dampt brown CLAYEY So\lltl (SC) 7.9 111 l',A CT SG is'r4 9.7 118 CT F=JDense, damp, brown-gray CLAYEY S&~ (SC) \lith CR.A.VEL GR.WEL to 21:1"
~-
-j:m Dense. damp. gray-bra"" GRAVELLY SA,'lIl (SW) 40-
~T6 Dense, daAlp, tan SA..~ (51') with GRAVEL 12 102 CT
- rr Grad.. to '1ery dense, damp. 3rey-brown SUIT 5..\.~ (5M) llA 5G 00- III
~
P COBllLES to ~"
.~
~ 3.4 121 51; BC- ST IT Grading tan
- [3
~
14.S 104 5G 10- ll4
~ 10.1 llO SG Very dense, damp. yellow tao SA..;~ (SW) Sn..~ llA'rtO ""R.'!AT!ON
- 15
~ 3.3 III SG B~
- 30ttom of ,aria; at 80 ft. de9tn (.. lev , 32ft. )
~o ~ater oDserv.d ~~ ~or1~i
~c-jOO-
~
t LOG* OF' BORING 4-A '""'lacl : SONC:S SLOPE ST.\llILl'r'! .. F;~ JOII N,,"'_: ~.V;'1Al A-6
'!'CO!) "'AFlO 'oIcNE!L._
, a ~SSOC,A T~* S 2.5E-A8 Amended: April 2009 TL: E048000
DATE OF eORI"'G'~ Xu.74 WATER ofPTH OAT! MEASURED SAMPLES Xod1£ied California TYPE OF DRILL RIG Cont. Fl1~ht auge r HOI.E DIAMETER 6" WflGHT 0' HAMMER 14Q lb.. FALLI"'G 30"
... ..... i . .... ......
..<5;" "'. .. ...
~
~ ~
~% ~ ~
- II .. z
..J e, DESCIUPTtOH 0'-
uZ o ~ II:
~
uc z ..
- 0-
- 118 z 0 0 SuRFACE ELEVATIO",' 103" l!IIdiUlO niH. dry. brown SILTY CUY (CLl
*0-
- rnRAvtL to 1'1" 200- 'lery dll1nS8, damp 1 tan-btown euYEY SA.'ID esc: SC b
Xl
~ GlU'm to 3" 15
- i2 9" Very dense. damp, tan SA.'ID (SX-SP) "ith GRAvEL 4.3 12!. sc
'0- :*n 56 sa
~
.. :-,!4 4.3 120 SG 40- l!5 56 6.4 129 SC
~...n se , d"",p. bro"", C:'AYEY SA.\'D (SC) ...tth GRAVEL
\-1 *
- X6 :lR
~- M7
~
** l!8
~ Very dense, damp, yellow S,\,'ID (SII) 2.9 U8 SG
- -19 co 2.1 ics SG
~ Sample disturbed 60- M 10 ~ "
l!
" ~ ~ *.: 124 SG 30tto:o of ~crina at 56'1 ft. deerh (ahv. 36.5ft.)
~lo ..,ater olDSe1'Ved in ~o't"ing eo-j Fi" PrOlffl:
Joll Nu..." r : SONGS SLOPE S1'AS IUn 3~69.~" LOti ~F eCRING 5 , A-7 wOOO.....ARD-MeHEII.L 8 ASSOCIATES 2.5E-A9 Amended: April 2009 TL: E048000
- - - -----~ - - - - -
DATE Of' eORI NG 29 liar. 74 WAn:" DEPTH OAT[ lolUSU"EO SAlolPL[Sllod. Calif.!> Shelby rub .. TYpE OF DRIl.l. RIG Cont. "Plhht ,\ugu HOL[ OIAloltTl!Il 6" W[IGHT 01' HAlollolER 140 lba. I'AI.I.ING~
..... v
..... e .."',.: ... .
)
~ ~
,.; ~
....~ ;: ':z "z ". '"....
OJ z
<5", .. ..
% lI" ooa ...
Q z , Onell/PlIOM uz ", li: II
~* ~ 0" u.
Q ..
!:; :118
~
Q 0 SURFACE ELEVATION: 107 Seitt, damp, brown SA.-rOY CLAY (CL) (F1l1) Ml 54 Dense, da..p. brown CUYE'[ SAND (SC)
- ST lO- 'Oens&t l:IObe, bra..... GRAVELLY SA,-ro (511)
*-~ Den.se, damp, b.-own CLAYEY SAND (SC) 49 12.3 11.7 134 SG ZO--
ST 2
.t'O W P GMV&L eo 2" 2.7 116 SG
--P 30- ~T
- Jen... , damp, tan s",:m (SP)
}'!4 56 2.9 110 SG
- Dense. damp, bra..... (SP-SII) 40- ST GRAV~LLY s~m 4
- ~..s 50
.i)anse. damp. ta.n SILTY fine-grained S....-ro (SM)
Dense., damp, tan 16.7 113 SG GU\'E"~LY Sol.'ID (SiI)
~- l!6
* ~"
~7 lffi 'Jery d~n *** da.""" yellow S....-ro (SOl) SA'! ll.\TF.O FOR."ATION 6C-
- Soteom of bo.-1ng ae 56 fe. depth (dev. Slft.)
~o ~ater observed 1~ ~or1ng
>0-
~o-
~c-00-P'OI.~t JoO Numoer :
- SONGS SLOPE STAB lL l7!
3~,,~oA 1 t LOG OF BeRING 6 I ~~81 ..
;YOCOWARO'~eSEILL a ~SSCC.), 0
-~
" 0 2,5E-AIO
"' ..~ Amended: April 2009 TL: E048000
OAT[ OF BOAING 29 )la~. 74 , WATER O£PTH DATE lit£ASU"EO SAMPl.ES l'!od. Calif. 4 Shelby lube TYPE OF DRILL RIG Conc. Fli~ht Au~er HOl.E DIAMETER 6" WEIGHT OF HAMMER 140 lbs , FALLING 30"
.J .... .. .: .;;z .....
~
w~
.3 DESCRIPTION uz
.. !!o ..z ".. ... ..
- t ..
00 "'z Q ~ w
.:II ,
uo: %
~
Z .. ;liD
~
u 0 0 SURFACE EL.EVATION: 116'
- Stif!. daJllP. dark b~o"" 5A/lDY CUY (ct) (Fill)
M1 SO Very <1ease. damp, brown CUYlY fine-grained SA.'l'O (5C) 2.8 122 SG 10- ST 1 M2 60 9.5 127 5C:: 20- 51 _2 u .o 122 C1: l1A
.~ 14 lJ aa~<1 CLAY 3.3 138 MA SG - SG 30- ST
_3 Den** , damp, gray GRAVnLY SA,o;O (SI/-SP) 9.
~, 2.0 114 SG olO- S1: .4
_!Ms 14 Very danae, dry, tall fine-grained SA.'l'O (SP) 1.4 103 SG
~-ST I"'-T
- 5 ~, C~ad1n~ with coaroe-grained S....'l'O
~ GRAVEl.
2.4 99 SC::
- 30tto.. of borin~ at 66 ft. depth (Ilev. SM e, ),
~o \later obae,..,ed in boring 10-9Q-90-PrOletl : SO~GS SLC?E S1:AaIL!1":' F*.;.
JOb NII"'M<: '~;"" LOG Of' aORING 7 A-9
'ICOOWtlRO'cNEILL a ASSCC.AHS 2.SE-All Amended: April 2009 TL: E048000
DATE OF BORING 2S :iar. 74 WATt It DEPTH OAT! MUSURED SAMP.. ES 2" !loaifiea California TYPE OF DRIl.L RIG Cone. Fligl>e Auger NOl.E DIAMETEIt 6" WEIGHT OF HAMMER 140 1bs. FAl.LING~
........ i ;e :; .. ...
,.;0£ ~ ~
.... ~l; .. z i
c :It DESCRIPTION z
*~ ~
c t 1I o~
~
l!l ~e
- )
- 118 e:
Q c SURfACE ELEVATION: 104
- Seiff, dUlP. bra"" SAl'IDY CLAY (CL)
'0-
!l
- I 61 12.4 130 sa
!l zoo- 2 43 1.4 15.9 1'19 sa
!l D8n5.. , damp, tan GR,\VELLY SA."l'O (SP-SM) 3 4¥.- NR
!l 30-4 42
. 2.0 95 l!A SG
!l P
3 44 CUY has 15 ** 114 sa
)\
Stiff, ""'1se, bro"", S"",-oY CUY (CL) 40- 6 40 12.0 16.3 118 SC
- 11
- ,"er,! d..nse , aamp. un SILTI SA."l'O (SII) 7
~
II
~- a sa
!l
~ 4.6 113 50 3M ~_~1'EO FOEU1ATIO~
9 0" 't'er7 ceus4!:, d..a=.p. white SA."l'O (SII) SN~ r....."' :v"'.....uv~ Bottom of ~oring ae 56~ ft. deoth (el8V. 47.3fe.) 60-
- ~o waC8r obs8rv8a in boring ro-ao-90-100-LOG OF BORfNG 8
~c~:v3 st I1P~ S"!:3~: I~
~
P'O,<lCl ; fi", JOIl Numll ... : ~~6-?".1. foIOCCWARO-1tlcNEIl.L a ASSOC.A A-IO
-"_S I 2.5E-A12 Amended: April 2009 TL: E048000
DATE OF BORING 29 :-tar. 74 WATER DEPTH 1I0NE DATE M(ASURED SAMPl.ES Pitcher BureL ryPE OF DRIl.l. RIG Rotatv .\u.er ~ l!ud HOl.E DIAMETER 6" WEIGHT OF HAMMER FAl.l.ING
..... i.... .; ........
-~
]
~ &;z ",it
"'.: OJ
- II .. =z z z" j DESCIUPTIOM 0'-
.:I
~ i !l ..
0,.
~-: '"
.- .. IE
'1"0 ...ez SURFACE ELEVATION: 104 Fill. COBBLES. eeecre te and CLAY SK 1
H Very stitf, rlamo, dark. ~ro"'l SA.'IDY CLAY (CL) to CLAn:'! SAND (SC) n b IO-
- P3 Brown SA.'ltI (SI1) 13.8 118 CT
- -<.A SG F4 15.8 122 CT SG p~ ll.\
2Q- 15.2 118 CT P6 ~.4 l27 CT SG
- iA P7 11.5 U6 CT SK O.nse. dl!imp, tan GRAVELLY SAND (SP-SW) SG 2 :iA 30-
.S;:
3
- b xe GRAVEL b~o
- SK
- lQ- 4 iPs GRAm
~9
.!p1O O.nse, damp, tan SANDY GRAVEL (GP) 50- IsK (4
!Pu Vu,. dense, damp. l!Il:IIC yellow SA.'ltI (SW) SAN !L\TEO
;O~""TION 60-Botto.. of boring at 59ft. deptll (elev, 45ft.)
)/0 water obnrved i~ ':Ior1n~
70-eo-eo-00-srxsn ':"!
. - LOG PrOleCT :
~ -.. OF BORING l'i4-
';",b I<l~",b<<
~~.~CS ~UPE
- 346':-1l - 9 A-ll WOODWARO-McNEIl.L a ;"SSOC1AT~S 2.5E-Al3 Amended: April 2009 TL: E048000
DATE OF SORI NG 29 liar .14 WATER DEPTH DAU MUSURED $AMPL.ES Pitch.. r Banel TYPE OF DRII.1. RIQ Rotary with l!ud NOL.! DlAMEn" 6" WEIGHT OF HAM"!R FAI.LING v i.... i ..
~
~~ .. I 1l..
Ii: .. ~* i i D!SC ".""ION
- II" o*
uZ
'>z Z
II: Q ::.
- II OX'
! '"0 li!~
- 110
- 0_ <:I SURFACE EL.ElfATION: 98
- As"lutl t e",",cr.. te
- 1'1 n
Stiff. d..-p. brO'lTt SILTY CLAY (CLl dth GRAVEL (FILL) SILTY SAND (SIt) 1'2 Deuse. ooist. dark brown SANDY SIL'!: (lolL) w1ttl or!!""ic root _ted&!
' 0 - I'J h . Very den.e, damp, ~ray CLAYEY SAND (sc) 1'4 Grading brown cr 10.8 121 SG 1'5 MA 20-
- 1'6 Very stiff, damp. 111lht brown S...ND'! CLAY (CL) 11.7 121 <:T SG 8.0 121 MA cr 1'7 ~
SKi ZO.S :27 SG Dense, d&ap~ gray GRAV1lI.LY 5A.'ID (SP-SIl) CT MA Sia SG P :'0 GRAVEL lO-1'8 Den"., duro, brown SA.'iD (sc) '.11th GRAVEL and SOB8LES*
~iO 40- 1'9
- ne
- I'll h Lens of CUY (eL' K4 Very den:le. d...... br...... SA.'iDY GRAVEl. (GP)
]0- 1'12 Very dense. damp, yello" SAND (5") SA.'i }lAna FOR."tATION
- Bottom of .oring at 51~ ft. death (elev. 46.Sft.)
- ~o "eter observed in bor1n~
so-
~O- ~o-90-00-Projscl : ;;O:;GS SLOPE SrABI!.!:"!
I LOG CF BORING SA 1A-12Fit-Joll NII",lIer : 3'::'69-".1 WOODWARO*McNEll.l. a ASSO<:IA. ES 2.5E-A14 Amended: April 2009 TL: E048000 I
DATE OF BORING 28 :iar.74 WATER OEPTH OAT! MEASURED SAMPLES ?itcher Barrel T'lPE OF 0"11.1. RIG Rotar"/ & }Iud HOLE DIAMETER 6" WEIGHT OF HAMMER FAI.I.ING_
..... ~... eJ 1 .. . .....
~
~
~
...i ... ...~
~ &:% ~ ~.
- Ill- Z i 0<11 .. z
. s DESCRIPTION uz
- II ," OZ .:
l!l :J ~~ 20 u SURfACE EI.EVATION, 94
- 0"
'" 0 Very deaoa. damp. dark ~roWII, StLTY SAlID (Sli) '0- PI
- 12.1 118 CI lVI 1'2 SC 14,4 121 CT P3
~
SG
- P4 SI( Very dell5e, damp, brown GRAVELLY SA.'I!> (Sl'-Sl/)
ZO-1 rr C08BL~S
~o-
- to 4"
- R. fU5a1 on COBBLES 40- seeee.. of borillS at 38 fe. depeh (elev. 56fe.)
- lo wacer observed ill borinJ!;
sa-6C-70-60-
~o-00-
-Project , Joll Nu.. o.. : SONGS SLOPE STAB ILt:-'
~469Al 1 LOG OF BORIPJf; ;0 tlA-13 fl4-WOODWARD ""cNEII.I. a ASSOC,AT_" sr" 2.5E-A15 Amended: April 2009 TL: E048000
DATE OF BOAING * '?r H WAT~A OEPTH OAT! MIASUAIEO SAMPl.ES Mod. Calif. & Shelby !"ba TYPE OF DRILL AIG Cant. Flight .....g er HOl.! DIAMETEIII 6" WEIGHT 01" HA"MER 140 Lbs, FALL.ING 30" i e,;~ a .. "z
..J OESCIllIItTlON 0'-
o a u~ 52
~
ao >: Z ..
- I- '"
0 0 SuRFACE ELE....ATIO"" 94 n Medium dane", moist, dark brovu SILTY SAND (SM) n.n.tt
- Ml 39 2.8 l!A
'0- ST Hard, damp, brown SANDt CLAt (CL) CT 13.3 119 1IA
- 1 so
.M2 56 4.!J 112
- n SO lIA ze-- S1 :lR With ORAVEL 2
'1I3 50 1.9 111 SO
~ M4 44 2.8 120 SO
- r--r rr
- \0- M5 Grading vary dans"
* :-foi 50 3.5 124 SO 1IA Grading with COBBLES, caVing Bottom of boring at 35 ft. dapth (alav. 59ft.)
~o ~ater observed in boring 50-60-eo-90--
00-t P'ojact '50:;(;8 ST.\lI tUn FIQ. . JOb NumO.": SLOf~ 3':'6:1Al LOG OF BORING lOA A-14' 2.5E-A16 Amended: April 2009 TL: E048000
APPENDIX B .~ LABORATORY INVESTIGATION B~l Index Tests Laboratory tests were performed on selected samples in order to determine pertinent soil properties. Density, mois-ture content, and specific gravity determinations were made for all drive tube and pi.tcher samples obtained from the borings. Also, unconfined compression tests were performed on a number of specimens. The results of moisture, density, and unconfined compression (static strength) tests are presented on the Logs of Borings (Appendix A) for ease in correlation with the soil profile. The results of specific gravity tests are summarized on Table B-1. The results of grain~size distribution tests are presented on Figs. B-1 through B-9. B-2 Cyclic Triaxial Tests Dynamic testing was performed on pitcher, shelby tube, and carved block samples by stress-controlled cyclic triaxial techniques. Of the two carved block samples obtained, one was not thought homogeneous enough for meaningful dynamic testing. T~e carved block sample test results were not compared with the corresponding Pitcher Sample test results to evaluate possible effects of disturbance during sampling, as originally planned, because slight differences in sample composition made correla-tion difficult. Therefore, for conservatism, no strength in-crease was applied to drive tube sample test results in this evaluation. A total of 28 specimens were tested. A summary of test data is presented on Table B-2. 2.5E-Bl Amended: April 2009 TL: E048000
Appendix B Page 2 Each test specimen was trimmed, placed between platens, encased in a rubber membrane, then subjected to an initial triaxial confining pressure of the same magnitude as the ori-ginal field overburden pressure of the sample (column 4 of Table B-2) and allowed to stabilize prior to testing. The test was performed by cycling a pre-determined increment of deviator stress (at 1 hertz), consistent with post-construction stress conditions, and measuring induced strain and porewater pressure. Samples were tested at field moisture content.* Principal strain of 10% (or +/-S% strain) was considered failure. For tests in which the strain did not reach 10% within a few hundred cycles, the tests were stopped and re-started with a higher deviator stress. The dynamic test results are plotted on Figs. B-lO and B-11 for isotropic and aniso-tropic tests, respectively. Interpreted laboratory strength envelopes are also shown on those figure~. The dynamic tests were also used to estimate modulus and damping characteristics of the terrace soils. For a num-ber of samples, calculations were made of Young's Modulus and hysteretic damping for. the fifth stress cycle of each test. The calculated values, presented on Table B-2, columns 13, 14, and 15, correlated well with assumed modulus and damping values assumed for the previous analysis. However, tests indicate the terrace deposit sands are stiffer than previously
*with the exception of test no. 85, for which the .specimen was inadvertently saturated for 12 hrs.
2.5E-B2 Amended: April 2009 TL: E048000
Appendix B Page 3 assumed. Therefore modulus values were adjusted accordingly for the present analysis. In addition, one large-diameter (4-in.) stress-controlled dynamic test, with 1/3-point and diametral strain measurements, was performed on a sample of the carved block material. This test indicated that the Poisson's Ratio assumed during the previous study was appropriate, and that end effects were negligible (i.e., no correction to platen-to-platen strain mea-surements were required). 2.5E-B3 Amended: April 2009 TL: E048000
TABLE B-1 RESULTS OF SPECIFIC GRAVITY TESTS
( ( c TABLE B-2 SUHNARY OF CYCLIC TRIAXIAL TF.ST nATA CD G) (1) @ G) @ (1) @ @ @ n y f. (\) Dry N f.(\) Otlclll~t['(t IIy~t"r"tic ~1 ra in o'c' (psf) 0,' (ps£) Unified Soil IJcnsity n** IPassl"ll !"d Stress /lxiat Stra in Modl1lu~ 1....'IlTI, i I~J: for (~kll[ati()l1~ Test No. S.~le No. £. pre-test test Classi£lcaHon (per) ~ '200 (!'sf) ~ @ N Cycles (ksO (\) ~illJ(le_ 1.0 2300 1300 S'I 111 O.S 27 12110 250 1.0 1200 24 I.U 81 4/1-Sf3 IlottOlll U.5 I-STl noUOlll 1.0 3400 2500 9-1 III no. M 2100 100 0.5 750 IS 82 10.0 nn 85* 4/1-4 l'oUQIII 1.0 2900 2800 51": 1111 m na 2300 25 m n;t 4/1-Sf4 Middle 1.0 2900 2800 SC 1(19 0.14 43 2750 16 10.0 na no ua 97 10.0 750 2t 0.5
- 98) 4/1-str. Ilott(llll 1.0 5400 5000 SI' 107- 0.5 3 4noo 60
- 99. 9-1'2 Middle 9-1'2 Mi<ldle 1.0 1.0 1400 1400 1000 1000
- JI 9-1 US 118 0.3 0.3 34 34
!l!IO 990 ISO 150 0.61 0.73 S(ilI nn 29 11., ,.,
(I.~ 9!)/I 99B; 9-1'2 Middle 1.0 1400 1000 :JI 118 0.3 . 34 1460 31 10.0 na n,' m 100 9-l'2 Top 1.0 1400 1000 ~I 118 0.3 33 1650 31 ro.o 7& 25 0.4 1300 500 118 0.3 45 500 150 0.2 1162 J7 11.5 101 10-1'1 IlottOlll 1.0 ~I lII-I'J nott... 1.0 1300 500 1JI 118 0.3 45 800 67 0.5 na no un 101/1 500 118 0.3 45 1150 150 6.4 nn na 11., JOIO J 0-1'1 flott... 1.0 1300 9-' 206 14 1.0 1I0 0.2 38 1000 150 0.9 102 10-1'1 Middle 1.0 1300 1000 9-1 N 103 104 10-1'2 IIottOlll
- 10-1'2 .lidd1e 1.0 1.0 1300 1600 1000 1000 9-1 9-1 121 120 0.1 0.1 47 45 1700 1850 75 13 10.0 10.0 ""
192 "" 13 ""
~.4 46 1750 11 10.0 220 19 1.(,
VI 105 10-PZ Top 1.0 1600 1000 91 119 0.1 122 0.25 3S 980 150 0.12 300 26 \.0 t>.:I I 106 Il)1jA 7-STZ BottOlll 7-ST2 IlottOll 1.0 1.0 2600 26110 1000 1000 SC SC 122 0.25 35 1850 475 9.0 m nn
]6 0.4 b:t 2000 1500 CL 118 na na 1380 ISO 0.24 1250 VI 107 9-1'4 BoU... 1.0 118 na
"" 2500 150 0.74 "', n.a 107,.. 9- 1'4 BottOOl 1.0 2000 1500 CI. n~
N 107>> 9-1'4 BottOlll 1.0 2000 1500 CL 118 nil "', 3380 152 10.0 10.0 na 600 na 19 U:1 1.0 9-1'4 Top 1.0 2000 1500 CL 1I7 no m 3700 229 108 4000 20 10.0 2J 3.(, VI 109 9-1'4 MJddie 1.0 2000 1500 CL 122 na na 2~5 2500 lie 122 0.1 45 2200 156 2.5 416 1O 0.1 t>.:I 110 9- 1'5 Bott.,. 1.0 2500 I 9-1'5 Bot_ 1.0 2500 2500 SC 122 0.1 45 4250 I 10.0 n~ na 11:1 110/1. 48 2500 0.4 J20 J2 itA I;;I;l 111 9-1'5 Middle 1.0 2500 2500 lie 127 0.1 ISO 0' 2500 lie 127 0.3 34 3380 2 10.0 na n.1 na 112 9-1'5 Top 1.0 2500 0.35 2000/1000 SW 116 0.1 47 1900 ISO 0.5 1100 22 113 9-1'7 Bottlllli 2.0 3300 1.3
""na SW 116 0.1 47 2900 167 rm 9-P7 IIottOll 2.0 3300 2000/1000 1131\ 47 3000 1 10.0 na no no 1138 9-1'7 Bott"", 2.0 3300 2000/1000 SIt 116 0.1 9-1'7 Middle 3300 2000/1000 CL 117 .015 66 3000 ISO 2.0 11;11 114 2.0
""nn 3500 10.0 no 66 50 2000/1000 CL 117 .01S na 114,.. 9-1'7 Middle 2.0 3300 1500 3000/1500 CL 119 .02 62 2200 150 0.26 nn n~
115 l00\*Sfl Bottm 2.0 m 10A-Sfl IlottOlll 2.0 1500 3000/J5oo CL 119 .02 62 2850 150 0.31 n.1 liSA 3000/1500 a. 119 .02 62 3500 150 0.6 nn no m lISB lO"'-STl BoU,,", 2.0 1500 nn 4500 1.0 n:t USC 116 10A-Sn Bot' M-PS BottOlll 2.0 2.0 1500 2000 3000/1500 400012000 CL SC 119 127
.02 0.1 62 45 3850 ISO 1000 0.9 no ....
11611 9/1-1'5 BottOlll 2.0 2000 4000/2000 sc 127 0.1 45 46SO 1000 1.5 nn n:t 110:1 1250/500 CL 127 .OOS 76 4900 1000 7.5 na na ...a 117 90\-1'6 BoU"", 2.5 2600
- a. 127 .008 76 5900 200 10.0 nn n:t no 2600 1250/500 117,..' 90\-1'6 BoU.,. 2.5 2.5 3000 3250/1500 CL 97 .05 55 6850 J 10.0 "',
118 9"'-P7 BottOll >> 119 9A-P4 Middle 3.0 1600 1500/600 sc 127 0.06 54 1800 1000 0.4 nn nn no nn 3 119A !IA-P4 Middle 3.0 1600 1500/600 SC 127 0.06 54 2420 1000 1.75 m
- J 0-m -Jnadvertently saturated for 12 hours.
0-Test n...be r s followed by A, B. or C are retests. >> Test nu.bers not in sequence as other testing progrA. in prop,ress concurrently. ~ nA .eanS not analyzed, or not te.ted. I\.l a a(0 -I r m a
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c.. "1J Laboratory dynamic test results Isotropic Tests 0 (K~=l.O) terrace deposit materials
~
- 2. LEGEND 0-zc ~
n 1 .If 3 test fT U:l et 0 zG) I. "3
- Test in which 10%
-...d
~~
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\D r- (failure)
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( ( ( c.. 0 ...."l) 0 Laboratory dynamic test results Anisotropic Tests 0-Z Ct" terrace deposit materials LEGEND c: 3 ;;1 2.3. 0- lJ) 1118 ~ Non-failure test la 0 z
- Failure test o:l t;ll 2.2 ... III (10% strain)
-l" I 0' lJ)
U) r-0 Test numbers are shown
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APPENDIX C SOIL PROPERTIES C-1 Generalized Soil Profile Laboratory test results, boring log data, examination of graded slopes, and data from previous studies were analyzed in order to determine a generalized soil profile for use in finite-element analyses. These data indicate the terrace deposit, which constitutes the upper portion of the switch-yard slopes, consists of interbedded, horizontally stratified, dense to very dense sandy soils and stiff clayey soils, with occassional lenses of gravel, silt, and cobbles. The clayey, more fine-grained materials appear to be predominant in the upper portions of the terrace (from approximately elevation 80 to 117 ft). The sandy, more coarse grain materials, which are ipterbedded with the lenses of gravel, silt, clay, and cobbles, generally lie between elevation 50 and 80 ft. This material is underlain by the San Mateo Formation Sand. C-2 Determination of Groundwater Conditions To aid in the determination of groundwater conditions at the site, ,calculations were made of the degree of satura-tion of 79 samples obtained from the borings. A summary plot of these test results is presented on Fig. C-1. These data indicate that 1) no samples tested were 100% saturated, 2) samples with a degree of saturation greater than 70% were predominantly clayey, and 3) the average degree of saturation 2.5E-Cl Amended: April 2009 TL: E048000
Appendix C Page 2 is approximately 50%. This information, consideration of local groundwater hydrology and the fact that no free water was observed *in any borings (above approximately elevation 5 ft), indicates that the terrace deposit soils are par~ially saturated, and that th~y will likely remain so assuming careful surface drainage control is implemented. C-3 Dynamic Strength Determination The laboratory strength tests reported in Appendix B provided the basis for estimating the in-situ strengths of the site soils. Figs. C-2 through C-S present the interpreted in-situ strength curves for the materials which constitute the switchyard slopes. The curves for terrace deposit soils (Figs. C-2, C-3, C-4) represent the" laboratory strength curves reduced by a correction factor of 0.8.* This value is thought to be conservative, because of the very high density of the terrace materials and the fact that they are not saturated. The anisotropic curves shown on Fig. C-4 for local weaker materials were drawn by increasing the isotropic curve an amount proportional to the average anisotropic increase of the other terrace deposit materials tested (shown in Figs. C-2 and C-3). For example, at N=10 stress cycles: For terrace Sands; for a change of K~= 1.0 to 2.0
\J *Correction factor, Cy , defined by Seed & Idriss (1971), ref. 19.
2.5E-C2 Amended: April 2009 TL: E048000
Appendix C Page 3 T cy the corresponding change in O'fc is from 0.72 to 1.33 wh 1C i h 1S
.an .1ncrease 0 f 1. 33 0.72 = 1.85 For terrace clays:
for a change of Kc = 1. a to 2.0 T the corresponding change in cy is from 1.14 to 1.51 O'fc which is an increase of 1.51 = 1.32 1.14
. 1.85 + 1.32 The average increase is = 1.53; therefore, at
, 2 N = 10 cycles, for Kc = 2.0+, the curve was drawn 1.53 times the K~ = 1.0 curve for the local weaker materials in Fig. C~4.
No dynamic strength tests were made on partially saturated samples of the San Mateo Formation Sand, however dynamic tests have been made on saturated samples. Those results are pre-sented in our report entitled Liquefaction EvaZuation for the Proposed Units 2 and 3~ San Onofre Generating Station~ San Onofre~ CaZifornia~ dated 22 Jan 74. Those dynamic strength curves are reproduced on Fig. C-S. They were used for this study for San Mateo Formation dynamic strength. Because the local groundwater conditions minimize the possibility of satura-tion (above elevation 5 ft), use of these data for partially saturated dynamic strength is thought to be very conservative. C-4 Modulus and Damping Values As discussed in Appendix B, dynamic strength test data 2.5E-C3 Amended: April 2009 TL: E048000
Appendix C Page 4 were also used to calculate strain-dependent modulus and damp-ing values, for use in finite-element analyses. The calcu-lations indicate that 1) the sandy terrace deposit soils are slightly stiffer than previously assumed, 2) the stiffnesses previously used for clayey terrace deposit soils are appro-priate, and 3) the damping values previously used for both sandy and clayey terrace soils are appropriate. Plots of the modulus and damping relationships used are given on Figs. C-6 through C-1L C-S Soil Density Moisture and ~ensity determination have been made from
- 1) samples obtained from borings, and 2) field density (sand \-J cone) tests. Based on these data, as well as information from previous studies,* the Net densities given below were use~ for the analyses:
Haterial Ym (pc f) Upper Terrace Deposit 138. (clayey soils) Lower Terrace Deposit 125. (s andy soils) Sand cone tests made in San Mateo Formation Sand indicate an average in-situ dry density of approximately 120 to 125 pcf. Boring log data indicate the moisture content of this material varies from about 2% to 16%. Based on these data, an average
*Ref 21.
2.5E-C4 Amended: April 2009 TL: E048000
Appendix C Page 5 in-situ wet density of 130 pef was estimated. This value was used in the analyses. 2/91 2.SE-C5/2.5E-C6 Revision 7 Amended: April 2009 TL: E048000
20 Predominantly SANDY soils Predominantly 15 CLAYEY soils No. of Samples in Interval 10 5 o o 10 20 30 40 50 60 70 80 90 100 Interval (degree of saturation. %) NOTES:
- 1) 79 "samples analyzed
- 2) Average dep,ree of saturation is 50%
Project: SO~GS SLOPE STABILITY DISTRIBUTION OF TEST RESULTS Fig. J':'lb N~mb.,: S:.69M DEGREE OF SATURATION ANALYSIS C-1 WOOOWARO- McNEILL a ASSOCIA rES 2.5E-C7 Amended: April 2009 TL: E048000
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- 1) Curves for K~.l.O. 1.25, 1.5 are for 2) Curve for K~=2+ is conservative Saturated Tests, presented in Lique- extrapola t ion.
faction Evaluation Report, dated 3) Dashed lines are extrapolated 22 Jan. 74.
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I\.l a a(0 Proj ec t r SONGS SLOPE ST/,BILlTY VARIATION OF SHEAR MODULUS WITH STRAIN FOR CLAYEY TERRACE DEPOSIT SOILS Fig. C-6 r
--I Job Number: B469A3 m
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--I rP"roj ed. :-SONGS SLOPE STABILITY r
m Job Number: B469A3 I VARIATION OF SHEAR MODULUS WITH STRAIN FOR TERRACE DEPOSIT SAND Fig. C-7 a
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Project: SONGS SLOPE STABILITY VARIATION OF SHEAR MOPULUS WITH STRAIN FOR SAN MATEO FORMATION SAND Fig. C-8 Job Number: B469A3 2.5E-C14 Amended: April 2009 TL: E048000
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--I Pro j ec t: SON(;S SLOPE STAB ILITY r
m VAR[ATlON OF DAMPING RATIO WITH STRAIN FOR SANDY TERRACE DEPOSIT SOILS Fig. C-IO a Job Number: B469A3 c
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- J 0-m MAJOR PRINCIPAL STRAIN, , PERCENT 0- I
~ I\.l a a(0 --I r m Project: SONGS SLOPE STABILITY a VARIATION OF DAMPING RATIO WITH STRAIN FOR SAN MATEO FORMATION SAND Fig. C-ll .jO>. co .lob Number: B4h9A3 a a a
APPENDIX D FINITE ELEMENT STUDIES D-l Mesh Construction A finite-element mesh of the proposed switchyard slope configuration was developed with a suitable number of ele-ments to represent the slope-foundation system. Specifically, the mesh, shown on Fig. DR!, was developed to represent the various soil zones and groundwater conditions at the site. The model was then used for stat1c and dynamic analyses, as discussed below. D-2 Static Finite-Element Analysis For estimation of pre-earthquake stress conditions, a gravity turn-on static finite-element computer program was used. This program (LOCKS), developed at the University of California, Berkeley, outputs normal and shear stresses acting on each element in the model' due to the weight of the con-stituent soils and their stiffnesses. The output stresses were then used in the stability evaluation as discussed in Appendix E. D-3 Dynamic Finite-Element Analysis The finite-element computer program (QUAD 4) used to determine dynamic normal and shear stresses induced in each element of the model (by the input base motion) was also de-veloped at the University of California, Berkeley. Details of the computer program are presented in Report No. EERC 73-16, 2.5E-Dl Amended: April 2009 TL: E048000
Appendix D Page 2 entitled QUAD 4~ a Computep Ppogpam fop EvaZuating the Seismic Response of Soil Stpuatupes by VapiabZe Damping Finite-Element Proaedupes, by the College of Engineering of the University of California, Berkeley, dated July 1973. Utilization of this program involved the following pro-cedure:
- 1. The slope-foundation system was divided into a suit-able number of elements to represent the sytem, as outlined in Section D-l. The mesh was extended to a sufficient distance from the s1apes. to minimize the influence of fixed vertical boundaries on the response values in the vicinity of the slope.
- 2. The input base motion (Section D-4) is applied at the bottom of the model and response values through-out the model are computed.
- 3. The computer program for the analyses takes into account the strain dependency of moduli and damping by obtaining new values of these parameters for strain values computed by using initial esti~ated values. The iteration is done for a desired number of cycles to obtain values of moduli and damping (Appendix C) which are compatible with the strains developed in the elements.
- 4. The output from the computer program consists of normal and shear stresses on each element, nodal 2.5E-D2 Amended: April 2009 TL: E048000
-------------------- - ---------- ~~---------------~--------
Appendix D Page 3 point displacements, velocities, and accelerations caused by the given input base motion. The output dynamic stresses were used to evaluate slope stability, as discussed in Appendix E. D-4 Input Base Motion The synthesized acceleration time history of ground motion used for input at the base of the finite-element model is shown on Fig. D-2. This is the same base motion as was used to represent the DBE for the previous dynamic evaluation, and details of its use are presented in that report (Ref. 21). 2.5E-D3/2.5E-D4 Amended: April 2009 TL: E048000
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. Time (sec.)
Time History of DBE Base Motion Input to Finita Element Model Maximum acceleration = O.36g Project: SONGS SLOPE STABILITY SYNTHESIZED DBE BASE MOTION TIME HISTORY Fig. Joh Num;".r: 3:'69AlL D-2 WOODWARD-McNEILL 8 ASSOCIATES 2.5E-D6 Amended: April 2009 TL: E048000
APPENDIX E ~ STABILITY EVALUATION E-I General The previous study made of dynamic slope stability uti-lized assumed values for dynamic strength parameters, $ and c, (friction angle and cohesion) based on correlation with static soil properties and on correlation with dynamic tests of materials from other sites. The dynamic laboratory tests made for the present study facilitated a more accurate deter-mination of the dynamic strengths of the terrace deposit soils. The laboratory test data generated do not facilitate analysis in terms of $ and c however, therefore analyses, were made to determine the number of equivalent significant. stress cycles induced in the soil profile by the DBE, and to compare this to the dynamic soil strength. The basic procedure used for stability evaluation was
- 1) to perform preliminary, very conservative analyses (sum-marized on Table E-1) to size the problem and locate areas of potential instability for furtner consideration, then 2) to more realistically (although still somewhat conservatively) examine the stability of those areas of potential instability.
These analyses are discussed below. E-2 Stress Cycle Analysis Pr eve.a r thquake stress condi tions were determined by s ta tic I finite element methods (Appendix D). Values of Kc (field 2.5E-El . Amended: April 2009 TL: E048000
Appendix E Page 2 consolidation stress ratio) were calculated for each finite element in order to determine the appropriate dynamic strength curve to use for stability evaluation. Earthquake induced shear stress (Tmax) were taken from the dynamic finite element analysis (Appendix D), divided by initial overburden pressures (Gfc) , and used to determine the number of stress applications (N) required to cause failure (10% strain). The value of N was then compared to the number of stress applications in-duced by the DBE (at a given stress level) to determine the relative stability of each finite element in the slope model. Table E-1 presents a summary of this information for each T element, based on a stress level of :ax in the finite element fc model are shown on Fig. E-1. Review of the data in Table E-1 .\-) shows that even at the maximum stress level (Tma x occurs only once, instantaneously) most elements require over 1000 stress applications to cause failure or overstressing. Previous studies have indicated that the DBE produces approximately 77 significant stress cycles in the free field at a stress level of 65% of T~ax (ref. 22). Because the
. fc present study required the use of a time-history of 22 sec duration to represent the DEE, analyses were made of the num-ber of significant stress cycles produced in the free field for comparative purposes. A pulse spectrum of the shear-stress time history used for this comparison is presented 2.5E-E2 Amended: April 2009 TL: E048000
Appendix E Page 3 on Fig. E-2. The equivalent number of significant stress cycles at the 65% stress level were calculated by the method outlined by Lee and Chan (ref. 10). A summary of this data is presented on Table E-2. These data indicate that the 22 sec. input base motion produces 21 equivalent significant stress cycles at a stress level of 65% of Tmax . Thus, in the free field, 21 cycles for this analysis are equivalent to 77 cycles of the DBE (at 65% Tmax ) . Analysis of elements in the slope portion of the model indicated approximately the same number of equivalent significant stress cycles were produced as in the free field. For each element listed in Table E-l in which failure or overstressing is indicated in less than 50 cycles (at a stress level of T max ) more detailed studies were made. A summary of these data is presented on Table E-1. Analysis was made of the number of equivalent significant stress cycles at the 65% stress level. For example (see Table E-3), for element 255 (location shown on Fig E~l):
.65 Tmax
== 0.33 afc
= 1. 03 Given these data, refer to the dynamic strength curve in Ap-pendix C (Fig. C-4), for the appropriate material, and a value of 150 is read for N. This is the number of cycles (at this 2.5E-E3 Amended: April 2009 TL: E048000
Appendix E Page 4 stress level) which would be required to cause failure or overstressing. Since the DBE will produce no more than about 80 stress cycles, it is assumed that this element will be stable. This analysis was made for each element presented in Table E-3, and the results are summarized schematically on Fig. E~3. Any element for which this analysis indicates failure will occur in less than 80 stress applications has been assumed unstable or overstressed. For the purposes of this study, analyses were made assum-ing that the sandy portion of the terrace deposit could con-tain weaker lenses (with dynamic strengths shown in Appendix C, Fig. C-4) as well as the more representative, stiffer materials (dynamic strength shown in Appendix C, Fig. C-2). The results shown on Fig. E~3 reflect our understanding of the in-situ soil conditions; i.e., weaker lenses are horizontal, and at most only a few feet thick. Calculations were also made of the factor of safety of each element (assuming the most represen-tative soil conditions). These calculations involved a com-parison of the appropriate dynamic shear strength (taken at N = 80 stress applications) to the earthquake-induced shear stress (65% of Tma x , which corresponds to 80 stress applica-tions, as discussed above). The results of this analysis are presented on Fig. E-4. 2.5E-E4 Amended: April 2009 TL: E048000
( c c TABLE E-1 SU~~IARY OF PRELIMINARY STABILITY EVALUATION DATA FOR ALL SLOPE ELEMENTS T Reference N@~ Material , 0'"0 T max T
.si T
(= max) af c Fig. No. for Type Kc (psf) (psf) (stress cycles) Soil Strength Element No. CY fc 0"0 107 San Mateo 1.35 1736 896 .52 120 C-5 108 " 1.38 4196 2030 .48 140 " 112 " 4.53 812 847 1.04 35 " 113 " 1.95 1925 776 .40 350 " 1.50 2808 1458 .52 120 " 114 " 4.20 873 179 .22 1000+ " 120 " N 121 " 1.74 2867 799 .28 " " VI 123 " 4.82 892 234 .26 " " 491 .34 " ft t>1 I 124 " 2.30 1447
.23 "
II t>1 VI 125 u 1.71 3301 761 85 .13 " 11 127 " 4.22 667 128 It 2.68 1423 325 .23 " " 129 " 1.62 2349 484 .21 " " 130 " 1.79 3423 689 .20 " " 131 II 1.42 4492 1067 .24 " " 137 Terrace Sand 4.94 439 69 .16 " C-2 or C-4 138 san Mateo 4.34 738 86 .11 " C-5 139 " 2.22 855 74 .09 u 140 " 2.08 1915 2091 1.09 32 " 1.45 3022 337 .11 1000+ II >> 141 " 1.60 4333 975 .23 II II 3 142 II C-2 or C-4 m
- J 143 Terrace Sand 1.20 269 94 .34 "
0-m 0-144 " 1.92 488 100 .20 II >> San Mateo 1. 70 1195 95 . 08 II C-5 ~ 145 I\.l 146 " 1. 78 1626 255 .16 II II a 270 .12 II II a(0 147 II 1.83 2306
--I 148 II 1.46 2897 755 .26 tI r
.21 "
II m 149 " 1.36 4745 1001 a
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co 150 " 1.44 5214 816 .16 " II a a a NOTE: See Fig. E-1 for locations of elements.
TABLE E-1 (Cont'd) T Tcy Tmax N@ cy Reference Material °0 Tmax (=-) °fc Fig. No. for Element No. Type K' (psf) (psf) 0fc 00 Soil Strength c (stress cycles)
- -- 1000+ C-2 or C-4 ISS Terrace Sand 2.55 464 .09 156 II
- 1. 75 942 102 .10 It II 157 San Mateo 1.47 1533 186 .12 It C-5 158 II 1.48 2085 488 .23 II 159 II 1.49 3153 693 .22 tI II 160 II 1.39 3805 1419 .37 250 "
161 " 1.48 5332 802 .15 1000+ " 166 Terrace Sand 5.83 439 88 .20 II C-2 or C-4 167 II 2.88 971 151 .16 " " 168 II 2.08 1423 645 .45 II II 169 San tvRteo 1.83 2060 344 .17 tI C-5
.N VI 170 Terrace Sand 2.66 1033 311 .30 II C-2 or C-4 t<:I I 171 II 2.09 1634 628 .38 " "
t<:I 0' 172 San Mateo 1.66 2711 1481 .55 110 C-5 173 If 1.65 2708 1053 .39 250 " 174 II 1.47 4034 1515 .38 300 If 175 II
- 1. 38 6247 1440 .23 1000+ II 180 Terrace Sand 5.74 556 152 .27 II C-2 or C-4 181 II 3.70 514 133 .26 If 182 II 2.26 1333 343 .26 " "
183 " 1. 89 1909 814 .43 II II 184 II 1.69 2380 1270 .53 1000+ or 16 II 185 San IIMateo 1.54 3151 637 .20 1000+ C-5 186 1.39 4621 585 .13 " II 192 Terrace sand 5.32 464 66 .14 " C-2 or C-4 193 " 3.26 642 78 .12 II 3 194 II 2.28 1120 202 .18 " " CD
- J 195 II
- 1. 74 1696 448 .29 " "
Q. ~ CD Q. 196 II 1.66 1961 766 .39 "
>> 197 " 1.83 2301 1701 .74 1000+ or 2 " ~ 1.62 2849 2134 .75 "
198 " II I\.l a a(0 199 San Mateo 1.48 3597 1436 .40 230 C-5
--I 200 " 1.35 5066 966 .19 1000+ II
. .14 " C-2 or C-4 r
m 206 Terrace Sand 4.87 376 52 a
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( ( ( TABLE E-l (Cont'd) T N@~ Reference Material , ao Tmax T cy Tmax fc Fig. No~ for Type Kc (psf) (psf) crfc (= (Jo ) (stress cycles) Soil Strength Element No.
-- 1000+ C-2 or C-4 207 Terrace Sand 1.95 671 96 .14 208 " 1.60 398 75 .19 " "
209 " 1.68 1107 205 .19 " " 210 " 1.55 1345 415 .31 " If 211 It 1.49 1768 875 .49 1000+ or 15 " 212 " 1.36 2164 1004 .46 1000+ or 2S " 213 " 1.42 2888 2527 .88 30 or 1 " 214 San Mateo 1.50 3711 1475 .40 230 c-s 215 II 1.38 5432 1671 .31 1000+ It 216 II 1.25 7901 2812 .35 330 If 1000+ C-2 or C-4 N 221 Terrace Sand 1.96 1.10 393 631 109 219
.28
.35 1000+ or 70 "
\.n 222 " 478 .39 850 or 65 "
t=:l I 223 " 1.15 1739 t=:l
-...J 224 It 1.08 1458 933 .64 50 or 1.5 "
225 II 1.17 1985 1279 .64 50 or 1.5 II 226 II 1.25 2239 1598 .68 120 or 1.5 " 227 " 1.27 2861 2741 .96 4 or 0.5 " 228 San Mateo 1.37 3762 976 .26 1000+ C-5 229 " 1.66 4979 2110 .42 230 " 1.29 9057 2584 .29 1000+ II 230 " Terrace Sand 1.12 471 177 .38 1000+ or 60 C-2 or C-4 235 236 " 1.02 667 223 .33 1000+ or 40 " 237 II 1.11 1321 783 .59 90 or 2 " >> 238 " 1.22 613 173 *28 1000+ " 3 CD 239 " 1.09 1365 276 *20 " "
- J Q.
240 " 1.09 1671 996 .60 75 or 2 " 1 or 0.5 " CD Q. 241 " 1.03 2219 2226 1.00 >> 5.5 or 0.5 C-2 or C-4 ~ 242 " 1.00 3122 2449 .78 I\.l a 243 San Mateo 1.06 4506 1354 .30 1000+ C-5 a(0 1.02 6671 2831 .42 60 II 244 " .38 140 " r
--I 245 II 1.00 8450 3201 m
Terrace Sand 1.31 603 614 1.00 4 or 0.5 C-2 or C-4 a 252 a a
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TABLE E-1 (Conttd) T N @ cy Reference Material Tmax Tcy _Tmax O"fc Fig. No. for K' °0 0fc (- (To ) Soil Strength Element No. Type c (psf) (psf) (stress cycles) 254 Terrace Sand 1.05 2441 2331 .95 2 or 0.5 C-2 or C-4 255 It 1.03 3432 1701 .50 110 or 3 II 256 San Mateo 1.14 5121 603 .12 1000+ C-5 257 II 1.17 8164 4474 .54 40 tI 261 Terrace Sand 1.23 614 760 1.24 1 or 0.5 C-2 or C-4 262 " 1.33 1590 1585 1.00 4 or 0.5 " 263 " 1.31 429 203 .47 1000+ or 15 II 264 It 1.14 1014 966 .95 2.5 or 0.5 " 265 " 1.28 1914 1428 .75 70 or 1 " 266 tl 1.29 1702 1805 1.06 2.5 or 0.5 " 20 or 0.5
. 267 1.28 2762 2290 .83 II II IV VI 268 II 1.28 3816 2102 .55 1000+ or 3 "
t:<1 I 269 San Mateo 1.26 5605 2511 .45 150 C-5 tt:l 00 270 tI 1.24 8660 4619 .53 75 It 274 Terrace Clay 3.32 497 1849 3.72 0.5 C-3 275 Terrace Sand 2.20 1347 1397 1.04 1000+ or 1 C-2 or C-4 276 It 1.72 2549 1789 .70 1000+ or 2.5 tI 277 " 1.58 3359 2578 .77 1000+ or 1.5 II 278 tI 1.47 4383 345 .08 1000+ It 279 San Mateo "1.35 6137 2169 .35 400 C-5 280 " 1.27 9172 4352 .47 150 II 284 Terrace Clay 4.48 567 2502 4.40 0.5 C-3 285 " 2.46 1004 1929 1.92 0.5 " 286 Terrace Sand 2.16 1814 1660 .92 1000+ or 1 C-2 or C-4 287 Terrace Clay 5.26 534 410 .77 1000+ C-3
>> 288 " 3.01 1067 2157 2.02 0.5 "
3 CD 289 " 1.76 1855 2019 1.08 1000+ "
- J 0-CD 290 Terrace Sand 1. 74 2985 2217 .74 1000+ or 2 C-2 or C-4 0-291 " 1. 74 2957 2130 .72 1000+ or 2 tI
~ 292 " 1.66 3570 2405 .67 1000+ or 3 "
I\.l a a(0 293 II 1.54 4462 2545 .57 1000+ or 6 " 294 It 1.47 5295 1937 .37 1000+ "
-I r 295 San Mateo 1.36 6947 2165 .31 II C-5 m
a
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C C co a a a (
c c c TARLE E-1 (Con t 'd) ley Reference Material , (J a Tmax Tcy _ Tmax N@- a fc Fig. No. for Element No. Type K (psf) (psf) afc (- 0'0) (stress cycles) Soil Strength c
- -- -- C-5 296 San Mateo 1.27 9853 3888 .39 250 300 Terrace Clay 5.0+ 365 305 .84 1000+ C-3 301 " 5.0+ 518 455 .78 " "
302 II 2.48 1090 379 .35 II II 303 II 1.86. 1973 2084 1.06 II II 304 " 1.52 2767 1873 .68 II II 305 Terrace Sand 1.55 3637 2425 .67 1000+ or 2.5 C-2 or C-4 306- II 1.43 4639 2769 .60 " II 307 II 1.39 5371 2629 .49 1000+ or 10 " 308 II 1.38 6184 2900 .47 1000+ or 15 It 1.31 7799 2642 .34 1000+ C-5
.N I.TI 309 314 San Mateo Terrace Clay 5.0+ 334 417 1.24 II C-3 D:l I 315 II 3.55 622 350 .56 II II D:l I,C 316 II
- 1. 75 1365 437 .32 1t II 317 II 1.64 1665 433 .26 II II 318 II 1.49 2783 1966 .71 " "
319 II 1.37 3192 2100 .66 II 320 Terrace Sand 1.46 4057 2236 .55 1000+ or 5 C-2 or C-4 1.34 4599 2260 .49 1000+ or 10 II 321 " 1.35 5006 2697 .54 1000+ or 4 " 322 II 323 II 1.33 5860 2753 .47 1000+ or 11 " 324 It 1.31 6629 1667 .25 1000+ II 325 San Mateo 1.26 8255 2358 .29 " C-5 330 Terrace Clay 5.0+ 374 126 .34 " C-3 3 m 331 II 1.97 697 284 .41 II II
- J 0-m 332 " 1.67 1124 378 .33 II II 0-333 " 1.37 1614 479 .30 II
~ 334 II 1.32 2313 896 .39 " " I\.l a 335 " 1.24 3356 1383 .41 " " a(0 336 Terrace Sand 1.27 4965 2318 .47 1000+ or 9 C-2 or C-4 r
--I 337 II 1.24 6287 3200 .51 1000+ or 4 II m 338 II 1.24 7039 1504 .21 1000+ "
a
-i>o co 339 San Mateo 1.21 8701. 2592 .30 tI C-5 a
a a
TABLE E-1 (Cont'd) T cy Reference Material , 0"0 T max T ey _Tmax N@-
<1fc Fig. No. for Element No. Type K c (psf) (psf) (ffc (- <10 )
(stress cycles) Soil Strength 344 Terrace Clay 3.12 481 113 . .24 1000+ C-3 345 II 4.26 388 194 .50 " " 346 " 1.16 1258 291 .23 fI II 347 II 1.17 1576 411 .26 " " 348 " 1.15 2558 679 .27 " " 349 " 1.14 3839 1220 .32 II 350 Terrace Sand 1.17 5467 2370 .43 1000+ or 15 C-2 or C-4 351 " 1.17 6733 2788 .41 1000+ or 35 II 352 II 1.18 7385 2630 .36 1000+ or 150 " 358 Terrace Clay 1. 74 547 179 .33 1000+ C-3
. 359 2.33 780 508 .65 "
If II N VI 360 If 1.06 1694 392 .23 " " t':l I 361 If 1.06 2576 1119 .43 " " tr:l t-' 362 11 1.08 3965 1661 .42 " " 0 363 Terrace Sand 1.10 5542 2129 .38 1000+ or 50 C-2 or C-4 371 Terrace Clay 1. 58 665 1096 1.65 0.5 C-3 372 " 1.48 840 989 L18 60 " 373 " L08 1736 1512 .87 250 " 3 m
- J m 0-
~
I\.l a a(0
-I r
m a
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co a a a ( ( (
. Table E-2 Significant Cycle Analysis Songs Switchyard Slope Analysis mc El.emerrt 77
=: 1592 psf r:.: c =: 1.0 San Mateo SAND (Strenp,th data in Appendix C, Fig. C-5)
DATA FROM DATA FROM COMPUTED NOTES SOIL TIME HISTORY STRENGTH
. OF SHEAR STRESS CURVE (FIET,n" INDUCED CYCLIC NO. OF SHEAR STRENGTH .CYCLES WITH PEAKS 1x ()/ IN THIS n...-f An.,
eq (psf) Ufc LEVEL 2093 1.31 T max 1360 0.35
'Lave =
*65tmax
'1.. ref =l~
STRESS LEVEL 1 1840 1.15 2~ ~ 7.5 2 1460 0.92 3 l~ 3 3 1170 0.74 17 2~ 10.2 4 635 0.40 17!:oi 85 0.3 5 SOD 0.31 15~ - For 22 sec. motion, neq = 21 @ 65% 7max (for 80 sec. motion, there were 77 cycles @ .6~max) 80 sec. ....... 77 cycles 22 sec. = 21 cycles 2.5E-Ell Amended: April 2009 TL: E048000
TABLE E-3 SU~~RY OF FINAL STABILITY EVALUATION DATA FOR ELEMENTS WITH INSTABILITY INDICATED AT STRESS LEVEL 1'max (FROM TABLE E-1) Reference (0.65) lmax Fig. No. for Element No. Material °fc Ke' N Soil Strength 112 San Mateo .67 4.53 lOS C-S 140 tI
.71 2.08 92 If 184 Weak Lens .34 1.69 1000+ C-4 197 tI
.48 1.83 400+ II 198 If
.49 1. 62 40 If 211 tI
.32 1.49 1000+ "
212 " .30 1.36 1000+ " 213 " .52 1.42 7 " 213 Terrace Sand .52 1.42 1000+ C-2 224 Weak Lens .42 1.08 15 C-4 225 " .42 1.17 17 II 226 II
.44 1.25 20 tI 227 " .62 1.27 2 "
227 Terrace Sand .62 1. 27 300 C-2 237 Weak Lens .38 1.11 60 C-4 240 tI
.39 1.09 60 II 241 If
.65 1.03 1 "
241 Terrace Sand .65 '1.03 20 C-2 242 " .51 1.00 100 tI 242 Weak Lens .51 1.00 2~ C~4 252 tI
.65 1.31 1~
tI 252 Terrace Sand .65 1.31 350 C-2 253 " .65 1.15 60 " 253 Weak,Lens .65 1.15 1~ C-4 254 tI
.62 1.05 1!;z tI 254 Terrace Sand .62 LOS 40 C-2 255 Weak Lens .33 1.03 150 C-4 257 San Mateo .35 1.17 400 C-S 261 Terrace Sand .81 1.23 18 C-2 261 Weak Lens .81 1.23 1 C-4 262 " .65 1.33 11j "
262 Terrace Sand .65 1.33 400 C-2 263 Weak Lens .31 1.31 1000+ C-4 264 " .62 1.14 1!z 11 264 Terrace Sand .62 1.14 90 C-2 265 Weak Lens .49 1.28 8 C-4 266 Terrace Sand .68 1. 29 150 C-2 266 Weak Lens .68 1.29 1~ C-4 267 tI
.54 1.28 3~ "
267 Terrace Sand .54 1.28 1000+ C-2 2.5E-E12 Amended: April 2009 TL: E048000
TABLE E-3 (Cont'd) Reference (0.65) '[max Fig. '-10. for Element No. Material crfc ~ N Soil Strength 268 \'Jeak Lens .36 1.28 250 C-4 274 Clay 2.42 3.32 ~ C-3 275 Weak Lens .67 2.20 6 C-4 276 " .45 1.72 110 It 277 "
- SO 1.58 20 It 284 Clay 2.90 4.48 ~ C-3 285 " 1.25 2.46 1000+ "
287 " .50 5.26 1000+ " 290 Weak Lens .48 1. 74 100 C-4 291 II
.47 1. 74 110 "
292 " .44 1.66 200 " 293 II
.37 1.54 1000+ "
305 " .44 1.55 110 " 306 " .40 1.43 150 " 307 " .32 1.39 1000+ It 308 " .30 1.38 1000+ " 320 " .36 1.46 1000+ " 321 " .32 1.34 1000+ " 322 323
" .35 1.35 1000+ "
" .31 1.33 1000+ "
336 " .31 1.27 1000+ " 337 " .33 1.24 1000+ " 350 " .28 1.17 1000+ " 351 " .27 1.17 1000+ t1 363 " .25 1.10 1000+ " 2.5E-13!Z.5E-14 Amended: April 2009 TL: E048000
c c ( a0- a., t- ""1j L.. SLOPE PORTION OF FINITE ELI~NENT HODEL c (\l n Scale 1"=40' "3 O*
...... Element Numbers or Given
(\l
.. (J) 0 Z
0:1 C)
~ (J) a-
\D (J)
~ t-'
~ 0
~J 34' ,3o\-.e.
t'1 314 ~I-,J-J'-:r-"..-,. ........---""'-- (J)
>-l 30D ~~I~/
287301 )~~~~~I~360 ~
~
H t-' H 2.74 281- %'I.~I~3'\! 361 I/'\. I"
- =1 206 f~,/2.35 X~~~~~~ 335 3'\9 3E'>2~ ' \ ~
1e,6 IS~ XZ):.
./',,*,;,o\ 1!:fJ:,,,,
~2.'38
.,.(... ~
2.52. Z53 261~ 2.7!t%!J~ 305 f1 336
~_~ n6 2.9~ 306 ~
3S(J 3&3 /1 / \ i 1/ 1/ 1"3. ~~Cll~ 9~~~ 2.4\ 251- 267 ~77 2.93 307323337 3'31 /~
'~~~~~l'1I19.'~~ 2.1~ ~,'I 242. ~338 N 2'55 268 278 2.94 308 352 -....
~'~l~ ',*,~185 ' " 2.1,,\~
_ .". ~fi~Z:Z!% l?:l I H2.. Atir 243 256. 26.9 279 295 309 32:\339\ \ \ \ l?:l lT4 l86 200 2.IS~~.J I"Y I-' --\---'r--
~,= 11'3' 1~~/'l:9 ,~~ ".1... ~4
..... * ~ ":l HH
~~ 107 '75 187 2m I 257 270 I""" 29B 3'0 . \ \ \ \
l{,,, /\-:'0\ 7 \ t'j~ \24~
~t'j
~~ 108 I\tV'~~~32.
lilt. ~h33"", \5 \ . z~
~I~:'l g ~;:(
~~---l---I---I---+--+-+---t---+----\r-I l"l§
"""j..--..-+-----+--+-+-+--+---+--r--_+_
8 ;o::lt'j (Ilt'" I E z ()
>> 1"1 3
m ;=
- J r 0-m Q) 0-
-0 (I) (I)
~
0 I\.l a QIl"l
~ I :!! 1 a(0 !"l I-' oD --I Ih r.
m a
.jO>.
co a a a
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~.
(,-, C'J
~-
LMAX:: 2093 pst 0 100%
........N l =1840 psf
('no LW LEVEL (I ) + MEAN CJ
....... + +
4- 80% Xl/:) ++ u.... _.
+
t/) ._ (2) lMEAN = 1460 psf 0-° +
. 60% ~/J .j" .I-0; w
('yO (3 ,..
++
+ *++ +
+ +
LMEAN = 1170 psf I-- -_ ++ (,/)0 t++4- ..
.. ;t + 40%
+ +
t +
++ +*
V'J (4 )
+ +++++ lMEAN = 635 psf t
.:t +
0 ~
+ +
c + 20%
++ +
++ + +~+ +
+++
(5}.I- $t + 'l:'MEAN:: 500 psf
- = +
+
0
. +
g.- ~. . CO 0*.15 0.30 0.45 0.60 0-75 0*90 PERIOD (SECONDS) Project: PI:LSE SPECTRC'1 Fig. SO~GS SLOPE STABILITY ELEMENT 77 E-2 Job Number: B469M WOOOWARO- McNEIL.L a ASSOCI ATES 2.5E-E16 Amended: April 2009 TL: E048000
( ( (
~
o 0-Z c 3 C7 (J}
~ 0 RESULTS OF SWITCHYARD SLOPE STABILITY EVALUATION
~
Of> (Schematic j;- J' Of) Scale 1"=40')
-o ~
~ G c- "t:l rn c,n l;l:l H
r+ 120 120 H
~
I ['1 Pl t"' r-tv
~
l"l
\J1 t>:I H I
t>:I M (J} H 0 o t--' r: Z Z
...... r- ,...
.-.i (f) ....III III III 0 l't> n
-r:I n c,n 0-3 o-
....e-l;l:l H
iE 0 ::;j
,.r-0 0 t'l
<: Analysis indicates
~
instability (Sft. deep
~
I c:::
~ maxium)
>> E 0-3 3 n H 0 CD
- J Z
PI Z Analysis indicates 0-CD rr slight overstressing --1--40 0-I >> IP ~
- Analysis indicates high D
( /) I\.l a tI) degree of stability. generally gl a(0 0 at least 1000 stress applications t'l~ I _. -I woO required toi i xcause E) fail ure r 1"1 In (see Append i m a
.jO>.
co a a a
c.. -0 0 D'" ""'
~. LEt;ENlJ Z ~
c .. *'.-*-*'zone of F.S.= 0.5 to 0.9 (potential instability) 3 fT U> 0 Z [Jlffi Zone of F.S.= O.H to 1.0 (potential overstressed zone) c;') en tJ:I a-
\C0-VI e-O
~;;)
~1
.:" .. of F.S.= 1.1 to 1.5
~ "l:l 1'1 v.
H
~ ESJ Zone of F.S.- l.~ to ~.O
.-.r-H
~ r:::l Zone of F.S * . 2.0 U
tv
\Jl or; I
[I' ~. t-' N 00 o ,td. 29 ft
- G r'1 (Jl o
'"<l
;l.-
n
~
o
- E :lCl 0
o"rj Scale 1" = 40' 0 Pig. 7 for interpreted results)
~ 'u>
)-
(S~e
~ "rj I :-<l
...s::
o-l
.~
z Dvnamic Stress at 10% strain for RO stresS applications
~ 10'.5.
>> r 6jZ uf Seismic Induced Stress 3 r CD
- J S-Q.
CD ~ Q. U) U) 0 ~ n 10- tTl I TI I\.l -i a +~ .0 a(0 rtl
<J) --I r
m c a
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co (, a a a (
APPENDIX F REFERENCE GUIDE This appendix presents a reference guide to aid the reader in locating specific items referenced on pages 1.8 - 2bn and 1.8 - 2bo of Amendment No. 19 to the PSAR. This data is pre-sented below, in the order referenced therein. Where to Look Item in this Report
- 1) Drilling Appendix A
- 2) Sampling Appendix A
- 3) Evaluation of possible disturbance Appendix B during sampling Section B-2
- 4) Density, moisture content, and Appendix B specific gravity tests Section B-1
- 5) Classification tests Appendix B Section B-1
- 6) Dynamic strength tests Appendix B Section B-2
- 7) Static strength tests Appendix B Section B-1
- 8) Dynamic strength parameters Appendix C Section C-3
- 9) Damping and modulus values Appendix C Section C-4
- 10) Evaluation of end effects on Appendix B dynamic test results Section B-2
- 11) Evaluation of stability Appendix E
- 12) Finite element mesh Appendix D Section D*l l.3) Analysis of two soil distributions Appendix E Section E-2
- 14) Adjustment of stiffness and damping Appendix D for strain compatibility Section D-3 Z.5E-Fl/Z.5E-FZ Amended: April 2009 TL: E048000
REFERENCES
- 1. Clough, R. W. and Chopra, A. A. (1966) "Ba r t hquake Stress Analysis in Earth Dams," Journal of the Engineering Mechanics Division, ASCE, Vol. 92, No. EM2, Proc.
Paper 4793, April, pp. 197-212.
- 2. Duncan, J. M. and Chang, C. Y. (1970) "Nonlinear Analysis of Stress and Strain in Soils," Journal of the Soil Mechanics and Foundations Division, ASCE, Vol. 96, No. SMS, September.
- 3. "Elastic and Damping Properties, Laydown Area, San Onofre Nuclear Generating Station," Report by Woodward-McNeill &Associates, dated 14 Oct 71.
- 4. Hardin, B. O. and Drnevich, V. P. (1972) "Shear Modulus and Damping" in Soils: Design Equations and Curves,"
Journal of the Soil Mechanics and Foundation Division, ASCE, Vol. 98, No. SM7, Proc. Paper 9006, July, pp. 667-692. S. Idriss, I. M. and Seed, H. B. (1967) "Response of Earth Banks During Earthquakes," Journal of the Soil Mechanics and Foundations Division, ASCE, Vol. 93, No. SM3, May, pp. 61-82.
- 6. Idriss, I. M., Dezfu1ian, H. and Seed, H. B. (1969) "Com-puter Programs for Evaluating the Seismic Response of Soil Deposits with Non-Linear Characteristics Using Equivalent Linear Procedures,f1 Research Report, Geo-technical Engineering, University of California, Berkeley.
- 7. Idriss, T. M. and Seed, H. B. (1972) "Se i smi c Response by Variable Damping Finite Elements," Journal of the Soil Mechanics and Foundations Division, ASCE, Vol. 98,
)[0. 5M3, ~1arch.
- 8. Idriss, 1. M., Lysmer,'J., Hwang, R. and Seed, H. B. (1972)
"Computer Programs for Evaluating the Seismic Response of Soil Structures by Variahte Damping Finite Elements,"
Report, Earthquake Engineering Research Center, Uni-versity of California, Berkeley, August.
- 9. Ku l hawy , F. H., Duncan, J. M. and Seed, H. B. (1969) "Finite Element Analyses of Stresses and Movements in Embank-ments During Construction," Report No. TE 69-4, Office of Research Services, University of California, Berkeley.
2.5E-F3 Amended: April 2009 TL: E048000
- 10. Lee, K. L., and Chan , K. (1972 ) "Number of Equi valen t Sign ifica nt Cycl es," Univ ersit y of Cali forn ia, Los Ange les.
- 11. Lysm er, J., Seed , H. B., and Schn abel, P. B. (1970 )
"Infl uenc e of Base Rock Cha racte risti cs on Resp onse ," Earth quak e Engi neeri ng Rese arch Grou Cent nd Repo rt No. EERC 70-7 , Univ ersit y of Cali forn ia, er Berk eley, November.
- 12. Newmark, N. M. and Hall , W. J., (1969 ) "Seis mic Desi gn Crit eria for Nucl ear Reac tor Faci litie s," Proc eedin gs, 3rd World Conf erenc e on Earth quak e Engi neer ing, Vol. II, Sant iago , Chil e.
- 13. Newmark, N. M., and Rose nblu eth, E. (1971 ) "Fun dame ntals of Earth quak e Engi neer ing," Pren tice Hall .
- 14. Schn abel, P., Seed , H. B. and Lysm er, J. (1971 ) "Modi-ficat ion of Seism ograp h Reco rds for Effe cts of Loca l Soil Cond ition s,tl Earth quak e Engi neeri ng Rese arch Cent er, Univ ersit y of Cali forn ia, Berk eley, Dece mber .
- 15. Seed , H. B. and Ld ri s s , 1. M. (1970 ) "Soi l !'1oduli and Damping Fact ors for Dynamic Resp onse Anal yses ,"
Earth quak e Engi neeri ng Re3e arch Cent er, Repo rt No. EERC 70-1 0, Univ ersit y of Cali forn ia, Berk eley,. Dece mber .
- 16. Seed , H. B. and Idris s, I. M. (1969 ) "Rock Moti on Acce erogr ams for High Magn itude Earth quak es," Earth - l*
quak e Engi neeri ng Rese arch Cent er, Repo rt No. EERC 69-7 , Univ ersit y of Cali forn ia, Berk eley, Apri l. 17 Seed , H. B~, Idris s, I. M. and Kief er, F. W. (1969 )
"Cha racte risti cs of Rock Moti ons Durin g Earth Jour nal of the Soil Mech anics and Foun datio ns quak Divi -
es," sion , AScB, Vol. 95, No. SM5, Septe mber .
- 18. Seed , H. B. and Idris s, I. M. (1972 ) "Det ermi natio n of Equi valen t Unifo rm Stre sses durin g Earth quak es,"
Tech nical Note , To be subm itted to ASCE for poss publ icati on in the Jour nal of Soil ~1echanics and ible Foun datio ns Divi sion .
- 19. Seed , H. B. and Idris s, It H. (1970 ) "A Simp lifie d Pro-cedu re for Eval uatin g Soil Liqu efact ion Pote ntia l,"
Earth quak e Engi neeri ng Rese arch Cent er, Repo rt No. EERC 70-9 , Univ ersit y of Cali forn ia, Berk eley, November. 2.5E-F4 Amended: April 2009 TL: E048000
- 20. "Seismic and Foundation Studies, Proposed Units 2 and 3, San Onofre Nuclear Generating Station, San Onofre, California," Report by Dames &Moore, dated April 15, 1970.
- 21. "Stability of Proposed Slopes for the Proposed Uni ts 2 and
- 3) San Onofre Generating Station, San Onofre) California)"
Report by Woodward-~fcNeill & Associates) dated 27 Mar 74.
- 22. "Liquefaction Evaluation for the Proposed. Units 2 and 3)
San Onofre Nuclear Generating Station, San Onofre) California," Report by Woodward-McNeill &Associates) dated 22 Jan 74. 2.5E-F5 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5F GEOLOGIC REPORT ON THE AREA ADJACENT TO THE SAN ONOFRE NUCLEAR GENERATING STATION NORTHWESTERN SAN DIEGO COUNTY J CALIFORNIA Site File Copy Amended: April 2009 TL: E048000
GEOLOGIC REPORT ON THE AREA ADJACENT TO THE SAN ONOFRE NUCLEAR GENERATING STATION NORTHWESTERN SAN DIEGO COUNTY, CALIFORNIA by Perry L. Ehlig 1560 Via del Rey South Pasadena, California 91030 for Southern California Edison Company 2244 Walnut Grove Avenue Rosemead, California 91770 September 31, 1977 Amended: April 2009 TL: E048000
~~-~... -"T""~-~.~_.- - - - - - - - - - - ~ ~ - - - - - - - - - - - - - - - - TABLE OF CONTENTS PAGE INTRODUCTION 1 GEOLOGY 2 REGIONAL GEOLOGIC AND PHYSIOGRAPHIC SETTING 2 LOCAL GEOLOGIC AND PHYSIOGRAPHIC SETTING 4 STRATIGRAPHY 8 DESCRIPTION AND ORIGIN OF FORMATIONS 8 LA JOLLA GROUP 8 SAN ONOFRE BRECCIA 8 MONTEREY FORMATION 13 CAPISTRANO FORMATION 20 SAN MATEO FORMATION 21 MARINE TERRACES AND ASSOCIATED DEPOSITS 23 GEOLOGIC STRUCTURE 29 CRISTIANITOS FAULT 29 FAULT "E" AND RELATED FAULTS 32
SUMMARY
OF THE GEOLOGIC HISTORY 34 CONCLUSIONS 36 REFERENCES CITED 38 TABLE I i Amended: April 2009 TL: E048000
ILLUSTRATIONS FIGURE 1- Location Map
- 2. Forest Beds
- 3. Fossil Locations
- 4. Reverse Drag Features
- 5. Geologic Maps Sheet 1 of 3
- 6. Geologic Map 'Sheet 2 of 3 7* Geologic Map Sheet 3 of 3
- 8. Geologic Sections A-A I " D-D I , F-FI
- 9. Geologic Sections E-E I, G-G'
- 10. Columnar Section it Amended: April 2009 TL: E048000
INTRODUCTION This report, prepared at the request of Southern California Edison Company, is based on the study of a 60 square kilometer area extending from San Mateo Canyon on the northwest to Las Pulgas Canyon on the southeast and from the coast to the east side of the San Onofre Mountains. The San Onofre Nuclear Generating Station is in the northwestern corner of the subject area. This report is based on:
- 1. Twenty two days (44 man days) of geologic 'mapping and field stUdy by Perry Ehlig and his field assistant, Thomas Farley, during the period between July 17 and September 6, 1977;
- 2. the study of ~wo sets of aerial photographs provided by Southern California Edison Company;
- 3. the review of published and unpublished reports on the geology of the area including pertinent parts of an earlier report on Units 2 and 3 of the San Onofre Gene-rating Station and a,report prepared for Los Angeles Department of Water and Power (1971).
- 4. discussions with staff geologists and consultants of Southern California Edison Company who are associated with the geologic investigation for Units 2 and 3 of the San Onofre Nuclpsr Generating Station; and
- 5. prior knowleage of the regional geology and a review of literature pertaining to it.
1 Amended: April 2009 TL: E048000
GEOLOGY REGIONAL GEOLOGIC AND PHYSIOGRAPHIC SETTING The area surrounding the San Onofre Nuclear Generating Station 1S in the southwestern part of the Peninsular Range Province of southern California. The main body of the province consists of ranges with a northwest-trending structural grain. Relief within and between ranges is due largely to differential ero~ion super-imposed on broad regional uplift and warping. Differential uplift by faulting has occurred along branches of the Elsinore and San Jacinto faults and along the eastern margin of the province. (See FSAR Figure 2.5-6) Basement rocks are exposed over much of the province. They include remnants of a thick sequence of Triassic and Jurassic sedimentary and volcanic rocks interspersed between Cretaceous batholithic rocks of granitic to gabbroic composition. The Mesozoic basement rocks are unconformably overlain by Upper Cretaceous and younger sedimentary strata in coastal areas and in the Los Angeles Basin, a structural depression that occupies the northwestern corner of the Peninsular ~ange Province. The basement terrane of the Peninsular Ranges probably terminates at or near the northwest-trending South Coa~t Offshore Fault Zone which is about 5 miles offshore from San Onofre (see Figure 1). All observed basement rock to the west of the fault zone consists of Catalina Schist and ass:ciated rocks. This western basement 1s Amended: April 2009 TL: E048000
considered to be derived from a Franciscan assemblage of sedimen-tary and volcanic rocks that were deposited on oceanic crust and subsequently metamorphosed at great depth within a late Mesozoic subduction zone (Platt, 1975). From the perspective of global tectonics, the Peninsular Range Province became a relatively rigid part of the North American continental plate following emplacement of Cretaceous batholithic rocks. Between the Cretaceous and Early Miocene the province appears to have been stable exoept for gentle westward tilting accompanied by erosion on the east and sedimentation on the west. During this time, interaction between the Farallon and North American plates was taking plaoe to the west. Plate reconstructions in combination with data from land based geology suggest large magnitude right slip ooourred along northwest-trending transform faults within the Continental Borderland during the Miocene. Commencing about Q.5 million years ago during Early Pliocene and continuing to the present, motion between the Pacific and North Amerioan plates has taken place primarily by spreading Amended: April 2009 TL: E048000
in the Gulf of California and right slip along the San Andreas fault and its branches (Atwater and Molnar, .1973). As a result of this, Baja California and the Peninsular Ranges have been detached from the North American plate and become part of the Pacific plate. During the Pleistocene and Holocene the Peninsular Ranges have been uplifted and warped, probably as a result of interaction between the Pacific and North American plates. Much of the Quaternary deformation within the northern part of the Peninsular Ranges appears to be due to interplate compression along the bend in the San Andreas fault' which extends from the northern end of the Salton Trough to the southern end of the Coast Range~. LOCAL GEOLOGIC AND PHYSIOGRAPHIC SETTING Within the coastal area adjacent to the San Onofre Nuclear Gene-rvting Station there is a pronounced change in the bedrock geology across the north-northwest-trending Cristlanitos fault. The area east of the fault belongs to a large, essentially intact structur b~ock which extends from the Elsinore fault to the coast and 'lcluc; ,~e "ar t a Ana, Elsinore, San ta ;'lorgariti. and San Harcos Mountains along with ranges further to the southeast (see Figure 1). The area west of the fault 1s part of the Capistrano Embayment, a northward-trending structural trough of Late Miocene and Early Pliocene age which interconnects with the Los Angeles Basin. The structural block east of the Cristianitos fault has basement rock exposed over most of its surface. About 6 miles inland from the coast the bosement terrane is unconformably overlain by a thick Amended: April 2009 TL: E048000
sequence of sedimentary rocks which dip southwestward toward the coast. The lower part of the sequence is Upper Cretaceous to Eocene in age and consists mainly of quartzofeldspathic sandstone derived from erosion of basement terrane to the northeast. Only the upper part .of the Eocene La Jolla Group was observed during this investigation. Two to four miles inland from the coast, Eocene strata are overlapped by the Lower to Early Middle Miocene San Onofre Breccia. The breccia has an average dip of about 35 degrees toward the south-west and a maximum exposed thickness of nearly 4600 feet. It consists of coarse schist debris which was deposited on alluvial fans emanating from a mountainous area southwest of the present coast. Because of its resistance to weathering and erosion, the breccia forms the San Onofre Mountains, a prominant northwest-trending ridge extending from Oce~nside to San Clemente along the landward side of the coastal terrace. The Middle to Early Upper Miocene marine Monterey Formation unconformably overlies the San Onofre breccia and generally dips toward the southwest at low to moderate angles. It was deposited by a sea transgressing from the southwest (the direction from which the San Onofre breccia was derived) and includes a basalt conglomerate and sandstone member derived from ero~ion of the breccia. The bulk of the Monterey Formation consists of thin bedded siltstone, shale and sandstone in the northern part of the area and massive sandstone in the southern part. The Monterey Formation is the yout~est bedrock formation present in the study area to the east of the Cristianitos fault. Amended: April 2009 TL: E048000
To the west of the Cristianitos fault is the Capistrano Embayment, a relatively flat-bottomed structural trough trending about north 10 degrees west. The trough was a marine embayment during the Late Miocene and Pliocene but has subsequently been uplifted relative to sea level and is marked by hilly terrain. It is about 3.5 miles wide near the coast and gradually narrows toward the north. The San Onofre breccia and the Monterey Formation are exposed near its margins. Siltstone and sandstone of the Upper Miocene to Lower Pliocene marine Capistrano Formation constitute exposed bedrock within th~ interior of the trough. The Capistrano Formation has been gently folded in an irregular pattern. The formation is locally capped by subhorizontal siltstone and sandstone of the Upper Pliocene marine Niguel Formation. Sandstone of the Upper Miocene to Lower Pliocene San Mateo Formation crops out adjacent to the Cristianitos fault near the coast and underlies the San Onofre Nuclear Generating Station. Pleistocene marine terraces are well developed along this part of the southern California coast. The lowest terrace has an average width of about one half mile and is continuous except where inter-rupted by 1. dor drainage courses. It is mantled by marine and non-marine deposits. Numerous higher terraces are present on the southwest flank of the San Onofre Mountains. The highest terrace mantled by beach gravel is at 1,275 feet above sea level. Higher benches of probable marine origin but lacking marine deposits occur as high as 1,500 feet ahove sea level. The highest terraces may be Pliocene in age. River terraces are present in inland areas but were not encountered during this study except locally adjacent to Las Pulgas, San Onofre and San Mateo Canyons. Amended: April 2009 TL: E048000
The Cristianitos fault is the only major fault in the area. It has an average strike of north 18 degr~es west and dips steeply toward the west. Normal dip-slip displacement occurred along the Cristianitos fault in association with development and deepening of the Capistrano Embayment during the Late Miocene and Early Pliocene. The fault has not moved since formation of the lowest marine terrace and has probably been inactive since the Pliocene. Minor faults are present in many places within the San Onofre breccia but are not generally traceable beyond individual outcrops. Four faults'have been mapped because they displace the unconformity between the Monterey Formation and the San Onofre breccia. All four are subparallel to the Cristianitos fault but three have a reverse sense of displacement opposite to that of the Cristianitos. None appear to have been active during the Late Pleistocene or Holocene. Amended: April 2009 TL: E048000
STRATIGRAPHY DESCRIPTION AND ORIGIN OF FORMATIONS La Jolla Group Medium to thick bedded friable sandstone composed of quartz, feld-spar and biotite underlies the San Onofre breccia along the north flank of the San Onofre Mountains. In most places the sandstone is covered by soil or slope debris. During our limited examination of the sandstone we found no fossils. Since it has previously been mapped as part of the Eocene La Jolla Group (Moyle, 1973), we have designated it as such on the leologic map (Figures 5, 6 and 7). Sandstone similar to that described above underlies the San Onofre breccia on the ridge between San Onofre and San Mateo Creeks. We designate it as Eocene La Jolla Group on the geologic map although part of it was previously mapped as the Monterey "Formation (Moyle, 1973). It is clearly not part of the Monterey Formation as used in this report and it may belong to the Lower Miocene Topanga or Vaqueros Formations. These units were not differentiated from the underlying La Jolla Group during this study. Sdn Onofre Breccia The San Onofre breccia of this area has previously been described by Woodford (1925) and Stuart (1975). Most of the formation is a repetitious sequence of coarse, poorly sorted and irregularly bedded breccia containing sedimentary structures typical of alluvial fan deposits. Clasts within the breccia are angular to .'-...../. Amended: April 2009 TL: E048000
subangular and are exclusively of metamorphic rock types character-istic of the Catalln~ Schist and other basement rocks associated with it. Common clast types include: blue-gray glaucophane schist varying from very fine grained schist to schist with abundant epidote crystals as much as 1.5 inches long; gray-green schist composed of variable amounts of chlorite, actinolite, epidote and albite; dark gray muscovite-albite schist; quartz schist derived from chert and containing such minerals as riebeckite, muscovite, manganiferous garnet and piedmontite; milky-white vein quartz; dark colored amphi-bolite and garnet amphibolite; metagabbro and metaserpentinite. Most clasts fall within the size from granules to small boulders but clasts 3 to 6 feet long are present in many places and the largest observed clast is 43 feet long. The coarseness of the San Onofre breccia increases from south to \-/ north along the San Onofre Mountains and from the base upward with-in the lower part of the .formation. Relatively fine grained sedi-ments representing distal fan deposits are common near the base of the formation throughout the area. Between Horno and Las Pulgas Canyons they comprise the lower 330 feet of the formation and con-sist of interbedded granule to pebble breccia, sandstone and sandy mudstone varying from light brown to reddish brown in color. Bedding planes tend to be parallel to each other and are commonly well developed in sandstone *. Sandy mudstone beds representing old solI horizons are internally massive and grade from brown near the base to red-brown at the top. The middle and upper parts of the formation appear to represent rapid accumulation on a relatively steeply sloping alluvial fan.
/
Amended: April 2009 TL: E048000
The most abundant lithology is breccia with clasts ranging from pebbles to small boulders 1n size and showing clast to clast support. Tabular schist clasts within the breccia tend to have their broad surfaces in subparallel alignment. Clast imbrication is common and characteristically indicates sediment transport from the southwest to the northeast. The matrix between clasts consists of granule- to silt-sized particles derived from mechanical abrasion of the clasts. The fine grained part of the matrix is rich in chlorite and muscovite. Interspersed between breccia beds are thin discontinuous beds of sandstone. The sandstone has the same comp~ sition as the matrix of the breccia. Bedding varies considerably in orientation from place to place within individual sandstone beds as well as from one sandstone bed to the next. When seen in fresh exposures, the material forming the sandstone and the matrix of the breccia is greenish gray in color and appears to have experienced little weathering prior ti deposition. The red coloration seen in many places along the south flank of the San Onofre Mountains is a surficial weathering feature caused" by prolonged exposure during the Quaternary. Coarse, internally massive beds of probable mudflow origin are fairly common within the middle and upper parts of the formation. Clasts generally show little preferred orientation and are enclosed within a greenish gray, muddy matrix having essentially the same composition as the clasts. In several places there are thick massive units interpreted to be avalanche deposits. The individual units are typically monolith- ,~ Amended: April 2009 TL: E048000
ologic and consist of tightly packed angular fragments of highly variable size. Tuff beds and tuffaceous sediments occur in a few places. Most are composed of fine grained ash and alteration products derived from ash. The only tuff bed which was traced more than a hundred feet occurs in the highest exposed part of the formation directly northeast of the landward edge of the lowest marine terrace be-tween map grid locations 20,500 feet southeast and 33,800 feet southeast. The tuff is exposed at 9 locations distributed over a distance of 2.5 miles as shown on the geologic map. The main part of the tuff consists of fairly well sorted, closely pack~d, cream-colored pumice lapilli. The most southeasterly exposure is estimated to be about 16 feet thick, lacks visible bedding and contains angular fragments as much as 2.5 inches long of a dense black volcanic rock scattered among the pumice lapilli. It is interpreted to be an airfall deposit at this location and is probably quite close to the vent. In the northwestern exposures part of the tuff was transported by water as shown by bedding. The tuff 1s important because all 9 exposures are in linear align-ment parallel to the strike of bedding in the San Onofre breccia. This indicates a lack of significant cross-cutting faults within the 2.5 miles interval 1n which the exposures occur. The San Onofre breccia has a maximum exposed thickness of about 4900 feet as shown by cross sections E-Et (Figure 9 of this report). The thickness shown may vary by several percent because of uncertainty concerning the mean dip of bedding and because of pos-Amended: April 2009 TL: E048000
sible repetition of strata by minor faults. The exposed thickness 1s greatest in the vicinity of San Onofre Mountain and this south-ward due to original lensing in this direction and thins northward \-/ due to unconformable overlapping by the Monterey Formation. The entire thickness is of nonmarine alluvial fan origin. Stuart (1975) refers to the presence of marine fossils within the San Onofre breccia of this area; however, the strata which contain marine fossils are assigned to the Monterey Formation in this study. The San Onofre breccia is of Late Lower to Early Middle Miocene age as shown by its stratigraphic position. The age of the strata immediately underlying it is not known within this area. The lower part of the Monterey Formation which unconformably over-lies the San Onofre breccia in this area contains abundant fossils of Middle Miocene age. -The San Onofre breccia is a product of tectonic activity within the nearshore part of the Continental Borderland. It was derived from a landmass southwest of the present coast as shown by paleocurrent directions derived from clast imbrication and by the fact that clast types are characteristic of Catalina Schist terrane which is only known to occur to the west of the present coast. (see Stuart, 1975, for greater detail). The coarseness and thickness of the breccia is characteristic of accumulation along a fault scarp adjoining a subsiding basin. The source area must maintain high relief in order to deliver coarse debris while at the same time the crust beneath the alluvial fan must be subsiding in order to allow thick deposits to accumulate. It should be noted that although the San Onofre Amended: April 2009 TL: E048000
breccia has been referred to as an alluvial fan deposit, it actually represents a coalescence of fans derived from several drainage sys-tems emanating from a relatively linear range front. This is shown 'by the fact that the types of clasts present and their relative abundances vary along the trend of the range and by the fact that paleocurrect directions are subparallel along the trend of the range rather than being arranged 1n a fan shape. Deposits interpreted to be of avalanche origin and some of the very coarse debris, including a block 43 by 27 by 19 feet and another 38 by 27 by 13 feet, may have originated by landsliding from a steep mountain front or escarpment. Monterey Formation In the coastal area southeast of the Cristianltos fault the non-marine San Onofre breccia is unconformably overlain by marine strata which vary in their gross lithology both laterally, parallel to the trend of bedding, as well as stratigraphically upward perpendicular to bedding. This has led to uncertainty concerning the assignment of formation names and has resulted in conflicting assignments among prior geologic reports on the area. The problem has been resolved by the dating of microfossil assemblages from 14 widely scattered localities within the area between the Cristianitos fault and Las Pulgas Canyon (Figure 3). All of the microfossil assemblages are of Middle to Early Upper Miocene age (Table 1). Marine strata of this age are traditionally assigned to the Monterey Formation in coastal areas of California and are so assigned in this report. (Anderson, Warren, 1977, Appendix A) Amended: April 2009 TL: E048000
In the area of the Capistrano Embayment to the west of the Cristianitos fault, Woodford (1925, p. 216-217) established the \-I Capistrano Formation to include Upper Miocene and Lower Pliocene marine shale and sandstone which conformably overlie shale of the Monterey Formation but are lithologioally different from it. Although the two formations are different in their gross appearanoe, they contain overlapping lithologies such as diatomaoeous shale. This causes uncertainty concerning placement of the oontact between the two formations. Our formational assignments are consistent with those of Blanc and Cleveland (1968) who have mapped the contact in the area north of San Clemente. It should be recognized that the Capistrano Formation is a local name. Had it not been established, the Upper Miocene strata included within it would either be referred to as part of the Monterey Formation or the Puente Formation, a looal formational name used to the northwest of this area. The base of the Monterey Formation is exposed in several places near the northwest end of the San Onofre Mountains. The base is concealed beneath deposits mantling the lowest marine terrace in most of the area southeast of the Cristianitos fault and lies at depth beneath the Monterey and younger formations in the area west of the Cristianitos fault. The basal part of the formation consists of conglomerate and coarse grained sandstone derived from erosion of the San Onofre Breccia. These basal deposits are as much as 160 feet thick in the area upslope from the lowest marine terrace between map grid locations 6,000 and 12,000 feet southeast. A series of small sand and gravel '~ borrow pits have been excavated in the basal member adjacent to the Amended: April 2009 TL: E048000
old highway in this area and provide good exposures. The basal member can be distinguished from the underlying San Onofre breccia by (1) better sorting of clasts ~nd an absence of clasts larger than cobbles, (2) the presence of better rounded clasts, (3) the absence of silt and clay from the matrix of the sandstone and conglomerate, (4) the local occurrence of shells, particularly oyster and pectin shells, and (5) the presence of light colored calcareous material filling the spaces between clasts in some beds. The basal member was previously mapped as part of the San Onofre breccia by Woodford (1925) and Stuart (1975). However, the two formations are separated by an angular unconformity and represent very different depositional environments. The San Onofre breccia was deposited by an alluvial fan emanating from the southwest whereas the Monterey Formation was deposited by a sea encroaching from the southwest. In the area described above there 1s a buttress unconformity between the Monterey Formation and the San Onofre breccia as illustrated in Figure 2. The relationships are best seen in the vicinity of a flat-topped ridge near map grid location 9000 feet southeast, 4,500 feet northeast. Bedding within the San Onofre breccia has an average dip of about 37 degrees to the southwest in this area. The uncon-formity dips about 30 degrees to the southwest as shown by its outcrop pattern. A resistant calcareous conglomerate unit, 10 feet thick, underlies and structurally controls the crest of the flat-topped ridge. The conglomerate unit dips 12 degrees toward the southwest and converges with the unconformity at its uphill end. The conglomerate unit 1s made up of a series of foreset beds which Amended: April 2009 TL: E048000
dip about 40 degrees toward the southwest and represent a seaward prograding of beach derived material, perhaps following deep scour by a severe storm. A good view of these relationships can be \-J obtained by taking the powerline road to the crest of the ridge southeast of the site. Similar relationships are present elsewhere in this general area. The buttress unconformity may represent deposition of sediment against a submerged and erosionally flattened wave cut cliff. To the north-northwest of the above location, the thickness of the basal sandstone and conglomerate member decreases and bedding within it becomes subparallel to the underlying unconformity. Both dip gently toward the southwest at an angle of about 25 degrees less than the dip of the underlying San Onofre breccia. This probably reflects transgression of the Monterey sea across a subhorizontal erosion surface cut across breccia dipping 25 degrees to the southwest. On the ridge between San Onofre and San Mateo Canyons, the base of" the Monterey Formation overlaps the base of the San Onofre breccia and rests upon the underlying Eocene sandstone. In part of this area the ~asal sandstone and conglomerate member 1s no more than 3 feet thick. Diatomaceous and calcareous shale are directly above the unconformity. From the Cristianitos fault southeastward to Las Pulgas Canyon, the Monterey Formation is well exposed in the lower part of the sea cliffs and in the mouths of canyons in areas not affected by land-slides. The exposed beds occupy a relatively thin stratigraphic interval .which is probably 100 to 150 feet above the base of the Amended: April 2009 TL: E048000
Monterey Formation in most places (see cross sections CC', DD' and EE' Figures 8 & 9). The lithology of the Monterey Formati6n under-goes lateral facies changes along this segment of the coast. Close to the Cristianitos fault the exposed strata consist of dark brown to greenish gray thin bedded siltstone and clayey siltstone with thin tuff beds scattered through the section, near grid location 13,500 southeast exposed strata consist of interbedded clayey siltstone and fine grained arkosic sandstone rich in biotite. Southeast of grid location 18,000 feet southeast the exposed strata consist mainly of coarse grained arkosic sandstone. From grid location 28,000 feet southeast to Las Pulgas Canyon the exposed strata are almost entirely m~ssive coarse grained arkosic sandstone. This change in lithology is due to lateral changes in the depositional environment. The massive sandstone along the southeastern part was probably deposited by grain flow near the head of a submarine fan. Thin bedding siltstone near the Cristianitos fault probably represents pelagic sediments deposited on a flat-bottomed ocean floor. Strata exposed in between the two areas probably represent the zone of interfingering between fan derived sediment and pelagic sediments. South of the area shown on the Geologic Map, the arkosic sandstone 1s exposed along the coast near Las Pulgas Canyon may have been transported down a submarine channel which had approximately the same location as Las Pulgas Canyon. The Monterey Formation exposed on the west side of Las Pulgas Canyon at fossil locality 27B-1 (see Table I) (map grid SE38ij20 ft., NE 11360 ft.) consists of very thin beds of fine grained biotite-rich arkosic sandstone Amended: April 2009 TL: E048000
separated by diatomite partings. One of the beds contains a mat of fish fossils. This sequence of strata which has an exposed thickness of about 16 feet is truncated on the southeast by massive coarse grained arkosic sandstone. The contact between the two is steeply inclined but irregular and clearly of sedimentary origin. Only massive arkosic sandstone is exposed across the entire hillside to the southeast. Based on the above relationships, the sandstone appears to be backfill within a submarine channel. The upper part of the Monterey Formation 1s exposed to the west of (:' the Cristianitos fault between San Onofre and San Mateo' Canyons. It consists of thin bedded diatomaceous siltstone and clayey silt-stone with thin ash beds present at fossil locality 57B-2. Fossil localities are shown on Figure 3 and data pertaining to them are summarized in Table 1. Microfossil assemblages were analyzed by Anderson, Warren and Associates, Inc., (1977, Appendix A) from 14 localities within the Monterey Formation to the east of the Cristianitos Fault and from 4 localities in the Monterey Formation and 2 localities within the lower part of the Capistrano Formation to the west of the Cristianitos fault. The microfossil data indicate most of the Monterey Formation east of the Cristianitos fault belongs to the Luisian Stage of the Middle Miocene. This is equivalent to an absolute age of .14 + 1 million years according to correlation charts currently in use. (Anderson, Warren and Assoc., 1977, Appendix A.) Microfossils from 3 localities east of the fault belong to the Lower Mohnian Stage of the Early Upper Miocene. This equates to 13 Z 1 million Amended: April 2009 TL: E048000
years according to Anderson, Warren and Assoc., (1977, Appendix A). An additional locality east of the fault gives a less diagnostic age of probable Upper Miocene. Of the four microfossil localities in the Monterey Formation to the west of the Cristianitos fault three indicate a Late Miocene age and one indicates a Middle Miocene age. The strata at locality 49A-l, which yields a Middle Miocene age, are strongly deformed and have probably been dragged upward along the Cristianitos fault. Microfossils from locality 49C-1 belong to the Upper Mohnian Stage of the Upper Miocene and are equivalent to an absolute age of be. tween 9 and 12 million years. This locality is several feet below the base of the San Mateo Formation and represents the youngest part of the Monterey Formation in this area. The Monterey Formation was deposited during a period of relatively rapid subsidence (or rise in sea level). Part of the basal sand-stone and conglomerate were deposited within the surf zone and con-tain shallow water oyster and pectin shells. Yet the diagnostic microfossil assemblages indicate bathyal depths of 600 to 1200 feet. Localities 49C-2 and 58A-l are within a few feet of the base of the Monterey Formation yet both indicate middle bathyal depths during the Luisian Stage. As a result of the relatively rapid increase in water depth, the near shore topography was probably fairly rugged during deposition of the lower part of the Monterey. This is probably the reason for the relatively abrupt lateral and verti-cal changes in the lithology of the Monterey Formation in this area. Amended: April'.2009 TL: E048000
Capistrano Formation The Capistrano Formation occurs within the Capistrano Embayment where it overlies the Monterey Formation with apparent conformity. Only a few exposures of this formation were observed along the west side of San Mateo Canyon during the present investigation. The exposed strata consist of interbedded siltstone, mudstone and fine grained biotite-rich arkosic sandstone. Diatomaceous silt-stone occurs with the above lithologies at fossil localities 57D-1 and 57D-2, to the north of the Geologic Map area. The transition between the Capistrano Formation and underlying Monterey Formation is exposed in section 27 (T.8S.R.7W.) directly northwest of the study area. Here, the upper part of the Monterey Formation consists of thinly interbedded diatomaceous siltstone and clayey siltstone. The basal part of the overlying Capistrano Formation consists of in~erbedded mudstone, clayey siltstone and fine grained biotite-rich sandstone. This grades upward into a more thickly bedded sequence dominated by fine to medium grained sandstone rich in biotite. The Capistrano Formatton 1s of Late Miocene and Early Pliocene age as determined from foraminifera by White (1956). Locali~ies 57D-1 and 570-2 on the west side of San Mateo Creek yielded microfossils indicating a probable Late Miocene age. The stUdy by White (1956) indicates much of the Capistrano Formation was deposited' at bathyal depths of 600 to 12,000 feet. Amended: April 2009 TL: E048000
San Mateo Formation The San Mateo Formation forms the bedrock beneath the San Onofre Nuclear Generating Station and is well exposed in the sea oliffs adjaoent to the station. Strata speoifioally designated as belonging to the San Mateo Formation orop out 1n a relatively small triangular area bounded by the Cristianitos fault on the east, by the ooast on the southwest and, on the north, by a line trending south 70 degrees west from where the Cristianitos -fault orosses San Mateo Creek. Within the area oovered by the geologic map, the San Mateo Formation is primarily oomposed of massive, ooarse grained, light yellow-brown to light gray arkosic sandstone. Disoernible bedding is rare in most exposures. Lenses of pebble-oobble oonglomerate ooour in a few plaoes. Clasts within the conglomerate are rounded and include voloanio and granitio rocks along with rooks reworked from the San Onofre brecoia. The upper part of the formation contains broad open oross beds in exposures north of Basilone Road about 1/2 mile east of the Camp Pendleton entranoe. The San Mateo Formation is only slightly deformed exoept in areas olose to the Cristianitos fault. In areas where bedding 1s pre-sent, it oommonly varies in orientation due to initial deposition on sloping surfaoes. The maximum thiokness of the San Mateo Formation within its outorop area 1s estimated to be less than 1000 feet. The formation extends from the surfaoe to a depth of 900 feet beneath San Onofre Nuclear Generating Station (FSAR Section 2.5.~.2.1.3). Since bedding is Amended: April 2009 TL: E048000
gently inclined the vertical thickness should be close to the true stratigraphic thickness in this area. The San Mateo Formation appears to be entirely of marine origin. The massive coarse grained sandstone comprising the lower part of the formation near the Cristianitos fault was probably transported by grain flow and could have been deposited within a wide range of water depths. Broadly cross bedded sandstone in the upper part of the formation might also have formed in a wide range of depths but by current action. The sand within the formation was probably transported into this area by the ancestral drainage systems to San Onofre and San Mateo Creeks. The formation probably represents the backfilling of a submarine channel which extended from the mouths of the two creeks. Localization of the formation to this area may have been due to the creation of a structural trough along the down thrown side of the Cristianitos fault. Channels might also have been eroded by sediment being transported from the Capistrano Embayment into a deeper open-ocean basin to the southwest. The San Mateo Formation has not yielded fossils or other material suitable for dating. Stratigraphic relationships bracket its age as between Early Late Miocene and Late Pleistocene. Its age is generally interpreted to be younger than the Capistrano Formation because it overlies the Capistrano Formation in the area west of San Mateo Creek. However, exposures of the San Mateo Formation in the cliffs along San Clemente State Beach have been examined and it is believed they represent turbidite deposition within a submarine channel within the Capistrano Formation. The San Mateo Formation is well bedded in this area, and displays the Bouma (1962) Amended: April 2009 TL: E048000
sequences of turbidite structures. Very similar deposits occur as channel backfills within the Capistrano Formation near Dana Point and are described by Bartow (1966) and Piper and Normark (1971). Therefore, the San Mateo Formation is probably a facies of the Capistrano Formation. The lower part of the San Mateo Formation might be Late Miocene in age and could have been deposited synchronous with the lower part of the Capistrano Formation. The upper part of the San Mateo formation is probably Early Pliocene in age where it rests against the Capistrano Formation at San Clemente State Beach. Marine Terraces and Associated Deposits The seaward flank of the San Onofre Mountains contains a remarkable number of marine terraces consisting of wave cut benches which are in part mantled by marine and non-marine deposits. The lowest terrace forms the coastal plane and is essentially intact. Terraces above an elevation of about 450 feet are only locally well preserved due to the combined effects of undercutting of higher terraces dur-ing formation of lower terraces and SUbsequent erosion associated with downcutting of canyons. Deposits on terraces above the eleva-tion of 450 feet are limited to beach gravel and fine grained sediments filling in around the gravel. Much of the gravel is concentrated in beach bars which are 1n linear alignment from one terrace to the next. The highest occurrence of beach gravel is at an elevation of 1275 feet. Remnants of what appear to be wave cut benches extend to an elevation of about 1550 feet. The crest of the mountains is marked by a gently sloping erosion sur-face which is probably of non-marine origin. Amended: April 2009 TL: E048000
Marine terraces are not shown as such on the geologic map; only the terrace deposits are shown. Deposits designated as marine in origin consist mainly of pebble-cobble gravel on all but the lower terraces. \-I Beach gravel is easy to distinguish from gravel derived directly from the San Onofre breccia because it is well rounded and is domi-nantly composed of rock types not found in the San Onofre breccia. The most abundant rocks are volcanic in origin. They probably came from outcrops of the Jurassic Santiago Peak Volcanics in the Santa Margarita Mountains and were transported to the coast by San Mateo, San Onofre and Horno Creeks. Granitic rocks make up a small part of the beach gravel. Their principal source appears to have been Horno Canyon since they are considerablely more abundant to the southeast of it than to the northwest. Beach drift was from northwest to southeast (as it is today) as shown by the symmetry of scallops in the old shorelines. A moderate amount of the beach gravel is derived ~ by reworking of olasts from the San Onofre breocia. Unlike the angular to subangular olasts in the breccia, it is well rounded and, in the case of quartz-rich clasts, typically shows percussion
~
marks from having been tossed in the surf. Beach armor is common at the base of beach gravel depo s I ts and the upper surf zone dovns Icre from the beach. The armor con:Lsts of boulders derived from the San Onofre brecoia whioh were too large to be transported by the surf. They show rounding and sculpturing from abrasion by sediment being moved by the surf. Marine terraces are generally assumed to be Pleistocene in age and to relate to glacially induced changes in sea level. In areas such as this where terraces occur at high elevations, the terraces Amended: April 2009 TL: E048000
are assumed to have been uplifted by tectonic processes. If the above assumptions are applied to the San Onofre area, questions concerning the tectonic stability of the area must be considered. Data collected during this study, indicate the marine terraces in this area represent a gradual recession of sea level since Lower Pliocene and is a feature which affects the entire region, not just the San Onofre Mountains. Evidence for this conclusion are developed below. The first question 1s whether the observed terraces are essentially a regressional sequence with the oldest at the top and the young~ est at the bottom. With one minor exception, the t err-aces appear to be a recessional sequence. Terraces undoubtedly formed during eustatic low stands in sea level but were later reworked when the bench was reoccupied by the long-term lowering of sea level. This conclusion is supported by the following three lines of evidence. First, there should be an overlapping of terrace deposits if higher terraces are younger than lower ones. Only one example of this has been observed and it only involves an increase of about 30 feet in terrace level. This example is exposed in the canyon opposite grid location 29,500 feet southeast. The base of the lower terrace is at elevation 370 feet and the base of the overlapping terrace is at an elevation between 400 and 405 feet. The head of the higher terrace is no more than a few tens of feet further inland than the head of the lower terrace. In the case of the higher terraces, only gravel deposits are present but they are concentrated in bars with a relatively clean wave cut bench downslope from each bar. Had higher terraces formed after lower ones, debris transported down slope during formation of the higher terraces should have Amended: April 2009 TL: E048000
been deposited over the lower terrace. Even if later erosion removed all fine grained material, a layer of lag gravel should blanket the lower terrace. Such deposits have not been observed. A second reason for believing the terraces were formed by a long term lowering of sea level 1s that in many places the higher ter-races have been removed by undercutting during formation of lower terraces. The position of the higher terraces is occupied by a faceted ridge representing the remants of a wave cut cliff of a lower terrace. Had the higher terraces formed after lower ones, they should be marked by continuous w~ve cut benches which truncute the top of the wave cut cliff at the head of the lower terrace. The third reason relates to the occurrence of volcanic-clasts in the terrace gravel. The nearest source for the gravel is the Santa Margarita Mountains, a minimum of 4 miles to the northeast. The area northeast of the San Onofre Mountains is presently occu-pied by the broad deep valleys of San Mateo, San Onofre and Horno Creeks. These valleys could not have been eroded below the level of the marine terraces at the time the terrace~ formed. Had they been de s ner they wouL:' have been unable to deli ver the gravel which occurs on the terraces. The above valleys do contain river ter-races indicating oscillations in base level but the oscillations are small compared to the total relief within the valley. The higher terraces on San Onofre Mountain are probably Pliocene in age and probably correspond to a decline 1n sea level near the close of deposition of the Capistrano Formation. As explain-ed 1n the discussion of the Cristianitos fault, the Capistrano Amended: April 2009 TL: E048000
Formation was deposited in 2000 to 4000 feet of water. During its deposition the marine strand line was along the base of an upland \.-i er cs'I on surface which extends across the Peninsular Ranges to the north and northeast of this area. A decline 1n sea level occurred in late Pliocene time. The Upper Pliocene Miguel Formationl which caps the Capistrano Formation at elevations between about 400 and 700 feet above sea level in the Capistrano Embayment, is of shallow marine origin. It reflects a recession in sea level. There is no evidence of younger marine terrace deposits overlying the Niguel Formation in inland areas. Had sea level risen during the Pleis-tocene to create the terraces on the San Onofre Mountains, there should be a record of this rise in the form of Pleistocene marine deposits in low lying inland areas, such as around El Toro. Pleis-tocene marine deposits are not known to occur in these areas. High level marine terraces are known in other areas of southern California. Marine terrace deposits cap the crest of the San Joaquin Hills to th~ northwest of this area at an elevation of 1000 feet. They occur up to about 1300 feet in the Palos Verdes Hills. The terraces are referred to as Pleistocene but none of the high level terraces have been dated. All of the area surrounding. the Los Angeles basin was occupied by deep water during Early Plio-cene. The high level terraces may reflect the recession of the Early Pliocene sea. The marine terraces within the study area show no evidence of major deformation since their formation. Data are inadequate to determine if there has been small scale deformation. In the case '~ of the lowest marine terrace, the elevation of its base varies Amended: April 2009 TL: E048000
regionally in exposures along the coast. However, this probably reflects the extent to which the wave cut bench has been removed by erosion. The elevation along the head of the lower 100 to 200 foot present day terrace varies from place to place also but this reflects vari-ation in the thickness of deposits overlying the marine platform. Elevations are high in areas where minor drainage systems have deposited alluvial fans across the terrace surface. Elevations are low adjacent *to major drainage systems, such as Las Pulgas Canyon where channels are adjusted to modern sea level. Amended: April 2009 TL: E048000
GEOLOGIC STRUCTURE Cristianitos Fault The Cristianltos fault crosses the coast .9 miles southeast of San Onofre Nuclear Generating Station. Here, it 1s well exposed in the sea cliff. The fault plane has an average strike of about north 32 degrees east and an average dip of 58 degrees to the southwest. Well developed slickensides trend subparallel to the dip. Sand-stone of the San Mateo Formation forms the west wall of the fault and thin bedded siltstone of the Monterey Formation forms the east wall. These relationships indicate the Cristlanitos fault is a normal dip-slip fault with the west side down. At the outcrop of the Crlstlanitos fault in the bluffs at San Ono-fre State Beach, terrace deposits overlie bedrock at an elevation of about 55 feet above sea level. About 3 feet of marine gravel occurs at the base of these deposits and is overlain by 39 feet of nonmarine material. The terrace deposits extend directly across the fault without being offset; thus, dating the most recent dis-placement as older than the terrace deposits. There is no evidence indicating Quaternary offset along the Cristianitos fault within the area studied. In the sea cliff exposures to the northwest or the Cristianitos fault, beds within the San Mateo Formation are arched into a broad anticline and cut by numerous small faults as illustrated in Figure
- 4. These features are typical of "reverse drag" -along normal fault as described by Hamblin (1965). They probably result from a flat-tening of the dip of the Cristianitos fault at depth beneath this area.
Amended: April 2009 TL: E048000
The Cristianitos fault is concealed benepth the coastal continental terrace for about one half mile. North of the terrace, the fault trends directly north for .9 miles and then bends westward where it disappears beneath nonmarine terrace deposits. Along this segment of the fault the unconformity bet~een the Monterey Formation and San Onofre Breccia is essentially at ground elevation on th~ east side
. .;~ It. ,
of the fault and the San Mateo Formation is on the west side. The San Mateo Formation shows normal drag with bedding dipping more steeply toward the west in beds close to the fault than in those a short distance away. Secondary faults occur subparallel to the main fault within the San Mateo Formation; however, we did not find two separate throughgoing fault traces. From the east side of San Onofre Canyon to San Mateo Canyon, the Cristianitos fault has an average trend of about north 25 degrees west. The change in trend from that present further south appears to have no special significance. It is common for normal faults to have bends in them as original features, for example, see Hamblin (1965) Figure 1. The dip of the fault in this area is p~obably steep but exposures suitable for measuring the dip are lacking. The unconforMity at the base of the Monterey Formation 1s within 165 feet of the ground surface on the north side of the fault with-in most of this area and the contact between the San Mateo Formation and the Monterey Formation is within 165 feet of the ground surface in most areas along the south side of the fault. Thus, the strati-graphic separation along the fault is apprOXimately equal to the stratigraphic thickness of the Monterey Formation, or about 855 feet Amended: April 2009 TL: E048000 I
based on the thickness of the Monterey Formation penetrated in an oil well drilled 2.5 miles to the northwest (Humble Oil and Refining Co., Visbeek No.1.). This offset is somewhat less than would be obtained by projecting stratigraphic horizons into the fault from a short distance away because strata are dragged upward along the west side of the fault. The gentle east dips in the San Onofre breccia on the north side of San Onofre Canyon are an anomalous feature. They may be due to backward rotation along an arcuate slip surface within soft sand-stone beneath the breccia. The mode of failure would be like th~t of an arcuate landslide except that the toe of the failure plane would terminate at depth against the Cristlanitos fault and movement of the block would be associated with fault movement. Activity along the Cristianitos fault probably occurred primarily during late Miocene and Early Pliocene in association with sub-sidence 1n the Capistra~o Embayment. The embayment appears to have formed by crustal extension in an east-west direction and its subsidence was accompanied by deposition of the Capistrano Formation. Paleontologic data from surface samples collected a few hundred feet above present sea level indicate water depths increased during accumulation of the Capistrano Formation. Water depths were between 2,000 and 3,000 feet during the Late Miocene and 2,000 to 4,000 feet furing the Early Pliocene (White, 1956). Such water depths would not have been possible without down-dropping the Capistrano Embayment relative to the Peninsular Ranges to the east. OtherWise, the sea would have extended across the top of an old, somewhat deformed, erosion surface that presently lies at an eleva-Amended: April 2009 TL: E048000
tion between 2,000 and 3,500 feet above sea level within the inter-ior of the mountains. Within the headwaters of San Mateo Creek remnants of a once extensive lava field cap the erosion surface. The lava flows have been dated at 8.3 ~ 0.5 million years (Hawkins, 1970). This age is within the Late Miocene. Since the lava flows were deposited on a land surface, the sea could not have extended to the elevation of the flows. Fault "E" and Related Faults Minor faults are fairly common within the San Onofre Breccia. In most places they cannot be traced because of inadequate exposures and repetitious lithology. An exception occurs in the northwestern part of the San Onofre Mountains where remnants of the Monterey Formation overlie the San Onofre Breccia. The contrast between the lithologies of the two formations makes it possible to trace faults which offset the contact between them. Four such faults have been recognized. The largest of the four, referred to as the fault E on the geologic map, offsets the base of the Monterey Formation about 330 feet vertically with the north side down. The fault is not exposed but can be located within a few feet in areas where it brings the two formations in contact. The fault has been projected across areas where only breccia is present. Along the northwestern part of the fault, as shown on the map, the projection was done to link up known fault segments where the,Monterey Formation has been downfaulted against breccia. Amended: April 2009 TL: E048000
Two faults with displacements similar to the fault E occur to the northeast of the fault E. Neither of the faults is exposed. In both cases a fault has been shown on the map beoause the basal part of the Monterey Formation has been juxtaposed against breccia. The fourth fault, referred to as the fault F on the map, (Area 4), has a dip slip separation of about 26 feet with the west side down. The fault surfaoe 1s well exposed in a small quarry adjacent to the old highway. It strikes about north 15 degrees west .and dips about 78 degrees southwest. where exposed in the quarry. Striations occur in more than one direotion on the fault surface but steeply inclined striations predominate. None of the above faults shows evidenoe of Quaternary aotivity. The only places where there is physiographic expression along these faults is where erosion has worn down the softer Monterey Formation more than the breccia. It should be noted that the fault E and the other two faults which down drop Monterey Formation on their north-east sides must have been active before erosion stripped the Monterey Formation from the main part of the mountainside in this area, otherwise there would have been no Monterey Formation to down drop. The only reason the Monterey Formation is still present is because it was down faulted while the Monterey Formation still covered the breccia and has subsequently been protected by brecoia from erosion. Remnants of a marine terraoe mantle the San Onofre breccia between elevation 800 and 900 feet along the ridge orest from the center of the fault E. Since this terraoe rests on breocia, it postdates removal of the Monterey Formation from the southside of the fault and therefore postdates down faulting of the Amended: April 2009 TL: E048000
Monterey. On the south end of fault E the remnants of a marine terrace appear to extend across the fault at an elevation of 350 feet. Bulldozing has disturbed the ground surface in this area and leaves doubt concerning whether the terrace is intact. Faulting within the San Onofre breccia and overlying Monterey For-mation might be due to several causes. Much of the minor faulting within the breccia is probably related to folding of the breccia into its present orientation. The breccia lacks well developed bed-ding planes that can act as flexural slip surfaces during folding. As a result, ,it acts as a brittle substance and accommodates bending by adjustments along small faults. The northerly trend of the four faults described above suggests they may be related to the Cristianitos fault or to a system of faults in the San Joaquin Hills to the west of the Capistrano Embayment. The San Joaquin Hills contain numerous north to north-west trending faults which cut Lower and Middle Miocene formations. Many of the faults have Miocene volcanic dikes intruded along them. Thus, at least part of the faults, if not all of them, are Miocene in age.
SUMMARY
OF THE GEOLOGIC HISTORY The coastal area adjacent to the San Onofre Nuclear Generating Station was tectonically very active during the Miocene and Lower Pliocene. Near the beginning of the Middle Miocene, the San Onofre Breccia was deposited on coalescing alluvial fans emanating from an uplifted Catalina Schist terrace located southwest of the present coast. The breccia appears to have accumulated very rapidly within \~ Amended: April 2009 TL: E048000
a subsiding basin. During the early part of Middle Miocene, the breccia was tilted southwestward and partially eroded. About the same time the sea transgressed from the southwest deposit-ing the Middle Miocene Monterey Formation on the breccia. Sub-mergence appears to have occurred rapidly. The basal part of the Monterey Formation contains beach deposits yet less than 330 feet above the base faunal assemblages indicate middle bathyal depths. The Capistrano Embayment deve'l.oped during the Late Miocene and Early Pliocene. Dip slip displacement along the Cristianltos fault allowed the embayment to become a deep marine trough while' the Peninsular Ranges to the east remained above sea level. Since late Pliocene, the area has been uplifted gradually above sea level, but otherwise appears to have been tectonically stable. Topographic features in the area are products of differential erosion rather than tectonic activity. The San Onofre Mountains stand high, because they are composed of breccia, which is highly resistant to weathering and erosion. Formations on either side of the breccia have been eroded away from flank of the mountains since Late Pliocene. The marine terraces on the southwest face of the San Onofre Mountains appear to record a gradual decline of sea level since Late Pliocene. So far as can be determined, the terraces are undeformed. The lowest terrace is continuous along the coast except where interrupted by major drainage systems. The lowest terrace extends across -the Cristianitos fault with no sign of displacement. Amended: April 2009 TL: E048000
CONCLUSIONS
- 1. The coastal area adjacent to the San Onofre Nuclear Generating Station appears to have been tectonically stable since Late Pliocene except for regional uplift relative to sea level.
- 2. The north-northwest-trending Cristianitos fault 1s the only major fault within the 'area. It is a normal dip slip fault with the west side down about 900 feet in the ar~a between San Onofre and San Mateo Canyons. The fault has not moved since formation of the lowest marine terrace (about 120,000 years ago) and may have been inactive since Late Pliocene.
The youngest formation known to be cut by .the Cristianitos fault 1s the San Mateo Formation. Although the San Mateo Formation was previously considered to be younger than the Capistrano Formation, our study indicates it is a submarine channel backfill within the Capistrano Formation and is of Late Miocene to Early Pliocene age.
- 3. Four minor faults, inclUding those referred to as the "E" and "F" faults have been mapped on the northwest flank of the San Onofre 'Mountains to the east of the Cristianitos fault. Each of these fdults down drops Monterey Formation against San Onofre breccia. None of these faults shows evidence of Quaternary displacement. Three of the faults have Monterey Formation down dropped on their uphill (northeast) ~ides.
The Monterey Formation has subsequently been stripped from the downhill side of the faults. The stripping occurred prior to the formation of a marine terrace at an elevation between Amended: April 2009 TL: E048000 I
800 and 900 feet above sea level. The terrace is probably of Late Pliocene age. Therefore, the faulting is probably of" Late Pliocene or earlier age.
- 4. No significant faults, other than those noted above, have been recognized within the area between the coast and the San Onofre Mountains from the Cristianitos southeastward to Las Pulgas "
Canyon. There is continuity in the geologic structure between the San Onofre Mountains and the coast as shown by geologic cross sections CC', DO' and EE'. Variations in the lithology of the Monterey Formation in exposures along the coast is due" to lateral facies changes rather than structural complications.
- 5. A distinctive tuff bed within the San Onofre breccia crops out in nine places over 2.5 miles extending on either side of Horno Canyon directly upslope from the lower marine terrace. All of the. outcrops are 1n linear alignment, thus indicating an absence of significant cross faults in this area.
- 6. Marine terraces are well developed along the southwest flank of the San Onofre Mountains below an elevation of about 1500 feet above sea level. These terraces appear to reflect emergence of the coastal area following deep submergence during the Late Miocene and Early Pliocene. Terraces above an elevation of about 1500 feet are likely to be of Late Pliocene age. The terraces do not appear to be deformed or tilted.
Amended: April 2009 TL: E048000
REFERENCES CITED
- 1. Anderson, Warren and Associates, 1977, Appendix A
- 2. Atwater, T., and Molnar, P., 1973, Relative motion of the Pacific and North American plates deduced from the sea-floor spreading in the Atlantic, Indian, and South Pacific Oceans:
Stanford University Publ, v. XIII, p. 136-148.
- 3. Bartow, J. A., 1966, Deep submarine fan in Upper Miocene, Orange County, California, Jour. Sed. Petrology, v. 36,
- p. 700-705.
- 4. Blanc, R.' P., and Cleveland, G. B., 1968, Natural slope sta~ility as related to geology, San Clemente area, Orange and San Diego Counties, California: Calif. Div. of Mines and Geology, Spec. Rpt. 98, 19 pp.
- 5. Bouma, A. H., 1962, Sedimentology of some Flysch Deposits.
Amsterdam, Elsevier, 168 pp.
- 6. Hamblin, W. K., 1965, Origin of "reverse drag" on the downthrowri side of normal faults: Geol. Soc. America Bull" v. 76, p , 1 I .j 5-11 f ij
- 7. Hawkins, James W., 1970, Petrology and possible tectonic significanoe of late Cenozoio voloanio rooks, Southern California and Baja California: Geol. Soc. America Bull.,
- v. 81, p. 3323-3338.
- 8. Humble Oil and Refining Co., 1959, Well number 1, Visbeek Ranch.
Amended: April 2009 TL: E048000
- 9. Los Angeles Dept. Water and Power, 1971, Preliminary geologic report of the coastal central portion of Camp Pendleton M~rine Base, San Diego County, California, 20 pgs., Appendix A and B.
- 10. Middleton, G. V., and Hampton, M. A., 1976, Subaqueous Sediment Transport and Deposition by Sediment Gravity Flows, IN Stanley, D. J., and Swift, D. J. P., eds., 1976. Marine Sediment Transport and Environmental Management. New York, John Wiley Sons, p. 197-219.
- 11. Moyle, W. R., 1973, Geologic map of western part of Camp Pendleton, southern California, U.S.G.S. open-file map.
- 12. Piper, J. W., and Normark, W. R., 1971, Re-examination of a Miocene deep-sea fan and fan-valley, Southern California:
Geol. Soc. America Bull., b. 82, p. 1823-1830.
- 13. Platt, J. P. 1975, Metamorphic and deformational processes in the Franciscan Complex, California: some insights from the Catalina Schist Terrane: Geol. Soc. America Bull., v. 86, p* 1337-1347.
- 14. Southern California Edison Company, 1976, San Onofre Nuclear Generating Station, Units 2 and 3, Final Safety Analysis Report.
- 15. Stuart, C. J., 1975a, The source terrain of the San Onofre Breccia, Southern California: Geol. Soc. America Abstract with Programs (Cordilleran Sec.>, v. 7, no. 3, p. 379.
\.J Amended: April 2009 TL: E048000
- 16. Vedder, J. G. f Yerkes, R. F. f and Schoeihamer, J. E., 1951, Geologic Map of the San Joaquin Hills - San Juan Capistrano \-)
Area, Orange County, California: U.S. Geological Survey Oil and Gas lnv. Map OM 193.
- 17. White, William R., 1956, Pliocene and Miocene foraminifera from the Capistrano Formation, Orange County, California:
Jour. of Paleontology, v. 30, p. 237-260.
- 18. Woodford, A.D., 1925, The San Onofre Breccia its nature and origin: Univ. of Calif. Pubs. 1n Geology, v. 15, p. 159-280.
Amended: April 2009 TL: E048000
TABLE 1 ,.J
SUMMARY
OF PALEONTOLOGIC H (f) DATA (f)
'0 0 l::...
§j~
- .etu Z H
- E: (f)
(f) ,.J
- (f) H 0
- :; (f) 0 (f) en ~ ~ 0
< u
~
~
NORTH PACIFIC U H <
'~"'
,.J ,.J SAMPLE FORMATION AGE STAGE DIATOM ZONE ENVIRONMENT 0 <t H COORDINATES (in feet)*
\:1.< u (f)
~P GRID LOCATION (in ft.)
20D-1 Tm Prob. Early Late Mioc. Early Mohnian 17-20 ---- Ix X X X N420,670 E1,633,230 SE 37,100' NE 8,800' 26B-1 Tm Prob. Late Miocene Mohnian 14-20 Outer Neritic-Bathyal X Ix X X X N421,540 E1,621,100 SE 27,800' NE 850' 26B-2 Qm Quaternary --- --- ---- I X N424,265 E1,6l8,835 SE 24,260* NE 1,170' 26C-1 Tm Middle Miocene Relizian-Luisian --- Outer Neritic-Bathyal X N428,580 E1,6l5,030 SE 18,505' NE 1,560' 26C-2 Qm Quaternary --- --- ---- N425,640 E1,617,710 SE 22,480' NE 1,360' X 26C-3 Qm Quaternary ---- X N425,500 E1,617,850 SE 22,665' NE 1,360' 27B-l Tm Prob. Early Late Mioc. Early Mohnian 17-20 Outer Neritic-Bathyal X X X X X N421,550 E1,636,000 SE 38,420' NEl1,360' 33B-1 'I'm Early Middle Mioc. Probable Luisian Middle to Lower Bathyal X X* N431,980 El,6l1,650 SE 13,675' NE 1,605' 33D-1 Tm Early Middle Mioc. Luisian 20-23 Middle to Lower Bathyal X X* x* X X X X N435,620 E1,607,110 SE 7,870' NE 1,000' 33D-2 Tm Middle Miocene Luisian 20-23 Middle Bathyal X X X X X N435,360 El,607,400 SE 8,250' NE 1,025' 33D-3 Tm X N435,840 E1,610,200 SE 9,880' NE 3,340' 33D-4 Tm Barren --- --- ---- X N436,370 El,608,820 SE 8,560' NE 2,750' 4lA-l Tm Barren --- --- ---- N437,730 E1,604,820 SE 4,750' NE 900' 4lA-2 TID Barren --- --- ---- X N440,370 El,605,540 SE 3,370' NE 3,270' 4lA-3 Middle Miocene Probab1 Luisian 20-23 ----
"'~
'I'm X" X X X X N440,385 El,605,190 SE 3,100' NE 3,075' 4lA-4 Tm Prob. Early Late Mioc. Early Mohnian 17-20 Outer Neritic-Bathyal X rx X X X N437,190 E1,605,660 SE 5,720' NE 1,075' 41B-1 TIn Middle Miocene Probable Luisian 20-23 ---- IX* X X X X X N438,7l0 E1,606,080 SE 4,950' NE 2,480' 41B-2 TIn Middle Miocene Luisian 20-23 ---- IX X X X N438,940 El,609,180 SE 6,990 1 NE 4,805' 41C-l TIn Middle Miocene Probable Luisian 20-23 ---- Ix* X X X X N441,930 E1,605,120 SE 1,950' NE 4,080' 41C-2 TIn ---- X N444,910 El,605,460 SE 140' NE 6,480' 49A-1 TIn Early Middle Mioc. Luisian 20-23 Probable Middle" Bathyal X X X X X X N447,240 E1,602,965 NW 3,325' NE 6,330' 49C-1 TIn Late Miocene Late Mohnian 13-16 ---- X X X X N451,500 E1,602,140 NW 6,870' NE 8,710' 49C-2 'I'm Prob. Early Mid. Mioc. Luisian 20-23 Middle Bathyal X X X X X X N452,020 E1,602,940 NW 6,690' NE 9,720' 57B-l Tm Late Miocene Mohnian 15-18 ---- Ix X X X N454,685 E1,599,180 NW 11,270' NE 8,900' 57B-2 Tm Late Miocene Mohnian 15-20 ---- IX N454,935 El,599,190 NW 11,470' NE 9,100' X X X 57D-l Tc !Frob. Late Miocene --- ---- X X X X N458,250 E1,595,195 NW 16,660' NE 8,650' 57D-2 58A-l Tc ~rob. Late Miocene --- --- ---- X X X X N458,565 E1,596,020 NW 16,330' NE 9,510' Tm ~ar1y Middle Mioc. Luisian 20-23 Middle Bathyal X X* X X N454,790 E1,601,840 NW 9,530' NE10,890' X X 502/3 1,2 Tsm Barren --- ---- X N439,800 E1,602,450 S02/3 3,4 Tsm Barren --- --- ---- N437,560 E1,604,700 Note - Prob.= ,
Probable ! co bOo
. *Ca1ifornia Grid Zone 6 M:ioc.=Miocene *...l d (f.J
~11 the above ages are I
$-I co 1+-1 ~
a0 (f.J "Provincial" *These samples have nearly !I ......0 0 *...l 0"0 identical siliceous micro- *...l "0
+oJ *...l *...l co ...... $-I fossil assemblages , p:::co *...l *...l ..0
*These samples h ave ne a rly . Q (f) ~
identia1 nannofossil (calca*.) assemblages i Amended: April 2009 TL: E048000
San Onfore 2&3 FSAR Updated APPENDIX 2. ~G GENERALIZED SUB-SURFACE GEOLOGICAL AND GEOPHYSICAL STUDY CAPISTRANO AREA
\...../- ORANGE COUNTY, CALIFORNIA
.NOVEMBER 1975 Site File Copy Amended: April 2009 TL: E048000
JACK C. WEST OON8tlLTlNG PBTltOLBUJI GEOLOGIST B3SO LoI CoJotelJ Drive Buena Park. Callfomia 90621 Telephone (714) 523-9MO GENERALIZED SUB-SURFACE GEOLOGICAL AND GEOPHYSICAL STUDY CAPISTRANO AREA ORANGE COUNTY, CALIFOlUIIA NOVEMBER 1975 Amended: April 2009 TL: E048000
ILLUSTRATIONS EXHIBIT A - GEOPHYSICAL LOCATION MAP EXHIEIT B - CONTOUR MAP STRUCTURE SECTIONS
- 1. A-B 4. F-G
- 2. C-B 5. B-G
- 3. D-E i
Amended: April 2009 TL: E048000
INTRODUCTION This study has been conducted for the Southern Cali£ornia Edison Company to investigate and acquire certain basic geophysical and geologic well data held by various oil companies, and to prepare a sub-surface contour map with appropriate geologic structure sections in the vicinity of the Capistrano embayment with emphasis on the area adjacent to the Cristianitos Fault. The purpose of this study is to prOVide more information that would aid toward understanding of recent seismic ~ctivity as it might relate to any geologic structure in the area. REGIONAL GEOLOGIC SETTING In general, this area of study, covering about 350 square miles, lies in a synclinal area between a large structurally complicated uplift, the San Joaquin Hills, on the west, and a much larger uplift, the Santa Ana Mountains, to the north and east. Within the central part of the area of study lies the Capistrano em-bayment (relating to the local distribution of Middle and Late Miocene sediments) along which trends the Cristianitos Fault in an apprOXimate N 5-20 0 Wdirection. The Pacific Ocean lies to the south. 1 Amended: April 2009 TL: E048000
Page 2 GEOPHYSICAL DATA An extensive search for geophysical data among oil companies' has been conducted. The results of this investigation are shown on Exhibit A, which illustrates the source, kind, and location of geophysical data. The area of gravity and air magnetic coverage is shown in an insert in the lower part of the map. Shell seismic work 1s available by purchase only through the Geophysical Trade Service in Houston. A few records from one Shell line were examined. The data appeared very poor. Considerable effort was made to acquire Exxon's (Humble) seismic data by trade and/or purchase. It was found that Exxon had lost their records on lines D 64, 65" and 66, and they have no interest in selling or trading their lines D 62 or D 63. standard Oil seismic is all available for purchase through Geodata'in Denver. This'data was briefly examined in Standard OillS San Pranoisco offioe. It is old work, and Standard had processed only one line (No. N-147) through modern computers. Useable data is present on this line, but its location is several miles trom the Cr1atianitos Fault, and accordingly, it is of little or no value toward the purpose of this report. At this time the following geophysical surveys have been acquired, by trade. They have been turned over to Dr. Shawn Biehler, University of California at Riverside, for further study $1) (1) Dr. Biehler's evaluation of these surveys is included in Enclosure 4 of this report. Amended: April 2009 TL: E048000
Geophysical Data (cont.) Page 3
- 1. Standard Oil Gravity Data (820 Gravity Stations)
Preliminary examination of this work suggests a general confirmation of the geologic interpre-tation'as presented below.(2)
- 2. Gulf Oil Air Magnetic Data (2,lOO line miles)
Preliminary examination of this work, also in general, confirms the geologic interpretation as presented below.(2)
- 3. Mobil Oil Seismic Line Initial negotations of trade for this line set forth nine miles of line along the Ortega High-way (Highway 74) where the westward one mile extended west one mile of the surface trace of the Cristianitos Fault and eastward one mile of the line ended close to the contact of the Cretaceous sediments with the Basement Complex.
However, it has been later ascertained that the useable data, which is sparse, includes only seven miles, excluding 'one mile on each end of the line. ~ The contractor for this line was GSI (Geophysical Service Incorporated), ana the line was run in 1971. The energy source was VIBROSEIS, which involves a surface Itthumper", in oontrast to setting ott a charge in a shallow (50 - loot), shot hole, thereby recording sound energy retlected back to surface seismometers from the various formations *
.Although the data from this line is meager, initial examination appears to confirm the present sub-surface geologic interpretation.
(2) Final examination of this work is included in Enclosure 4. Amended: April 2009 TL: E048000
Geophysioal Data (cont.) Page 4 In addition to the above geophysical trades, a Standard Oil seismic line, N-152, which crosses the Cr1stianitos Fault, was purchased. This line was shot in 1954. Western Geo-physioal was the contractor. The records have recently "been re-processed in Houston by Western using modern methods-- resulting in a non-migrated record section. The data is poor, but helps to confirm the general geologic interpre-tation. Western attempted to apply migration to this section by modern methods, but due to steep dips and refractions their efforts were unsuccessful. GEOLOGIC DATA The geologic*interpretation'as set forth by illustrations (structure sections and map) acoompanying this report is based upon pubiished surface geology and proprietary sub-surfaoe oil well and core hole data. The source of the oil well and core hole data consists of various major and inde-pendent oil companies who have released the information to the writer and to other individuals who. have in turn passed the *information on to the writer. Much of this data was obtained prior to commencement of this particular study for other purposes, but that part has been used to complete this current study*. More speoifically, the geologic sub-surface well data consists of the follOWing items where either all or part of this list for anyone oil well or core hole is present in the basic files used for this report. Amended: April 2009 TL: E048000
Geologic Data (cant.) Page 5
- 1. Electrical Surveys This includes a variety of logs such a$ the electric log, sonic or density log, micro-log, or d1pmeter.
- 2. Well HistorY In addition to the chronological events involved in drilling a well, this generally includes such inform-ation as the description of cores and side wall samples taken tram the bore hole, and results of formation tests.
- 3. Paleontological Data This may be mentioned in the well history as a form-ation contact point based upon the operator's paleo-ntological report or it may be the actual paleonto-logical report by the operator's paleontologist.
~ AlSO, the da~a may have been acquired in~ep~ndently trom sources other than the operator of the particular well.
- 4. Mud Loge These logs show lithology, drilling rates, oil and gas shOWings and other miscellaneous information helpful toward evaluation of the rocks penetrated by the bore hole.
- 5. Cable Tool Logs These are confined to old wells when modern technical methods of evaluation of bore holes had not been developed. They are usually a description of the lithology encountered and desoribed by the driller.
Amended: April 2009 TL: E048000
Geologic Data (cont.) Page 6 Various data pertaining to one or more ot the above kinds have been obtained from 118 wells (abandoned oil wells or core holes) w~1ch include all of the wells pertinent to ,the area of study. GEOLOGIC INTERPRETATION Five structure sections and a sub-surface contour map were prepared to illustrate the general sub-surfaoe geology. These have been included as Exhibit B, and Structure Sections A-B, C-B, D-E, F-G, and H-G. A discussion of each of these illustrations follows: EXHIBIT B ,- Generalized Contours on Base of Tertian or Top 01 Cretaceous Th;s map is designated "generalized" due to the large area contoured and the fact that only twenty one control points from wells that reaohed the Cretaceous are present. Due to the lack of paleontological data, some of these po~ts are interpretative. Estimated points from five additional holes were also used. This' horizon was chosen as best for depicting the regional structure at depth. The map is further supported by surface geology and thickness estimates of the younger formations overlying the Cretaceous. Shown on the eastward portion ot this map are the areas where Oretaceous sediments and the Basement Complex are exposed at the surface forming the western slope of the Santa Ana Mountains. -The surface contaot between the Amended: April 2009 TL: E048000
Geol ogic Inter preta tion (con t.) Page 7 over lying Tert iary sedim ents and the Oreta ceou s is a faul t cont act over most of the outcr op area . The faul t is calle d the Miss ion Viejo Faul t and the youn gest rock s cut by the faul t are Eocene in age. Moving westward on the map the conto urs show a gene ral bowing struc ture that plung es to the south west . These conto urs are inte r-rupte d by a large normal faul t, the Cr1s tiani tos Faul t, which has a "dow n-to- the-w est" movement, trend ing in a N 50 - 20 0 Wdir ectio n throu gh the cent ral part of the' mapped area . Imme diate ly westward of the Cris tiani tos Faul t Zone, the struc ture at Creta ceou s depth is homo clina l to the west --exc ept in the south cent ral part ot the map (cen tral part of T 8 S - R 7 W)w here a fault ed anti clin al struc ture west of the Cris t1an itos Faul t
,~a prese nt." A mino r amount 9f oil (non- comm ercia l) has been recov ered from three abandoned oil well s on this struc ture tram sands at Creta ceou s age.
The oil is trapp ed partl y by strat igrap hy With in the Oreta ceou s beds , partl y by the fault ed anti clin al struc ture and partl y by the Cris tiani tos Faul t. The cent ral struc ture of the mapped area cons ists of a regio nal sync line which is bifur cated in the north - west ern part of the map by a sout herly plung ing fault ed antic line that culm inate s in a loca l area in T 5 S, R 8 W, where Creta ceou s rock s looa lly crop out. This antic line is apprOXimately on trend with the fault ed antic linal struc ture ment ioned abov e. The regio nal sync line plung es to the south east and to the north west in areaS With in the east cent ral part of T 7 S, R 8 W, resu lting in a low basin al struc ture abou t a mile north - west of the Janu ary 1975 ea~thquake epio ente rs. Amended: April 2009 TL: E048000
Geologic Interpretation (cont.) Page 8 The eastern flank of the San Joaquin Hills is in the area between Highway 5 and the shoreline, within the southwestern po~tion of the map. !he general struc-ture at Cretaceous depth in this area is a faulted northeast dipping homQoline, which terminates at the regional syncline axis disoussed above. The Shady Canyon Fault is an old prominent and large fault that is exposed at the surface in the San Joaquin
. Hills. This fault oan be traoed on the surface into the most western part of the mapped area where it is oovered at the surface by beds of Upper Miooene and Pliooene Age. Due to the apparent magnitude of it's displacement (4,OOO+/- feet) it is interpreted as oon-tinuing to the southeast as shown. No well data at Cretaceous depth to support this interpretation is present.
Some of the additional faulting at Cretaoeous depth is based upon surfaoe mapping, partioularly in the vioinity immediately west of the Cristianitos Pault. Worthy of note is that the direotion of faulting tends to merge into and paralle~ the strike ot the Cristianitos Fault in the southern part of the mapped area. CRISTIANITOS FAULT This fault extends southeasterly from the southeast part of T 5 S - R 8 Wa distanoe of about 24 miles to a point about 3/4 mile east of the San Onofre Nuclear Generating Plant, and then oontinues south-easterly a few miles offshore. Over the distance Amended: April 2009 TL: E048000
Geologic Interpretation (cant.) Page 9 \ ****..J onshore the well control is sparse for mapping this fault in the Bub-surface where it intersects the base of the Tertiary and/or the top of the Cretaceous. Actually, there are only three abandoned exploratory holes (wells) that have penetrated the fault. These are as follows:
- 1. ERA Oil Company "Glenn Ranch" No.2-I, Section 8, T 6 S, R 7 w.
- 2. Exxon (Humble) "O'Neill Estate" No. C-l, Section 15, T 8 S, R 7 w.
- 3. Texas "O'Heill Estate" No.1-I, Section 22, T 8 S, R 7 w.
However, other factors that support the general position of the fault at Cretaceous depth are--
- 1. The surface trace of the fault where the fault has been ~apped by others cited in references noted on the accompanying structure sections and map.
- 2. Information from exploratory holes within approx-imately one-half mile on either side of the fault.
These holes are ten in number and they aid in map-ping the fault.
- 3. Geophysical data.
In the few oases where wells have penetrated the fault the apparent dip of the fault from the surface trace to the point in the well varies between 60 and 70 Amended: April 2009 TL: E048000
Geologic Interpretation (cont.) Page 10 degrees. There is little or no control at depth except the proximity of some of the non-faulted deeper holes within one-half mile of the fault suggests that the dip may steepen at depth. The accompanying structure sections show the fault zone to steepen, in general, to 750 - 80 0 westward in' the deeper part of the sedimentary column. The fault is complicated by en-echelon slivers and branches forming a fault zone which at the surface is in places as wide as 2,000 feet. The largest branch, in the vicinity of Sections 4, 9, and 10 of T 8 S - R 7 W, and Sections 28 and 33 of T 7 s, R 7 W, has been called the Forster Br~ch by others, and it is separated horizontally on the surface from the main branch by as much as 5,500 feet.
,The displaoement on the Cristianitos Fault appears to be essentially vertical and it is' "down-to-the-west."
The amount of vertical separation is variable but appears to decrease at the north end and the south end (near San Onofre) with the greatest displacement in the central part of its length onshore. The greatest vertical separation is between 3,500 and 4,000 feet in the area of Sections 20, 21, 28, and 29, T 7 s, R 7 W, where the north end of the Forster Branch merges with the Cristian1tos Fault. In the central part of T 8 S, R 7 W, wher~ a faulted anti-clinal structure is present west of the Cr1stianitos Fault, the vertical separation reaches a maximum of about 2,500 feet. It decreases to about 1,700 feet where Highway 74 (Ortega Highway) crosses the fault. Amended: April 2009 TL: E048000
Geolo~ic Interpretation (cant.) Page 11 This decrease is associated with additional "down-to-the west" displacement on the Forster Branch. The estimates of the amount of displacement on the fault are generally supported by the contours on top of the Cretaceous on either side. However, due to lack of additional sub-surface control, the amount of displacement over its entire length is approximate. STRUCTURE SECTIONS - A-B, C-B, D-E. F-G, and H-G The general stratigraphy of the area covered by this study is demonstrated by the above structure sections. For the most part the sections are self-explanatory. This report does not include a description of the various formations since they have 'been defined and discussed by authors of surface geology as cited on the sections. Although th~se sections do not pass throu~h all sub-surface well control, the more import-ant holes are included. The main purpose of the sections is to illustrate the interpretation of the Cristianitos Fault Zone at depth and to define the sedimentary column. Sections A-B and C-B are more regional and aid in the definition of the geologic setting. Sections D-E and particularly F-G and H-G show specific data that support the amount of dis-placement of the Cristianitos Fault at those locations. It can be readily seen that information at depth is sparse and that the geology at depth is thereby Amended: April 2009 TL: E048000
Geologic Interpretation (cont.) Page 12 highly interpretative. However, formation thick-nesses have been studied and applied to the various sections to maintain a continuity of thickening and thinning based upon electric log correlation, age determination by paleontological data, and isopachs ot local member and formation units. Where available, reduced electric log curves and dipmeter are plotted to aid in the final inter-pretation. CONCLUSION An investigation of existing geophysical work within the area of study has been made and recorded on Exhibit A of this report. Examination by the writer indicates that the geophysical data that has been gathered confirms the geolo~ic interpretation as illustrated in the acoompanying Exhibits. Further geo~ physioal stUdy by Dr. Shawn Biehler is in progress. (3) The' Cristianitos Fault is a normal fault whioh dips between 600 and 75 0 to the west with essentially only vertical displaoement "down-to-the-west. tI The ,greatest vert~cal separation occurs in the vicinity of the central part of its onshore length. where it varies between ~,700 and 4,000 feet. The shallower'dip of the fault appears to be at or near the surface with steeper dip at depth. The fault is complicated by fault'slivers en-eohelon to the main trace and by other faults at angles to and merging into the,main trace. No significant movement along the Cristianitoa Fault appears to have occurred since Late Pliocene time. (3) This study has been completed and is reported in Enclosure 4. Amended: April 2009 TL: E048000
Conc lusio n (con t.) Page 13 This study does not indic ate that the sourc e of the two epic ente rs plott ed with in the south one- half of Sect ion 25, T 7 S, R 8 W, is from any movement on the Cris tiani tos Faul t. In fact , there is no subs tanti al evide nce that any struc ture as inter prete d by this study is comp atibl e with these epi-cent ers exce pt that thei r loca tion is in a gene ral way coin ciden t with the lowe st part of the Capi stran o Basi n. Acco rding ly, one expl anati on of the sourc e of the epic ente rs may be diffe rent ial settl ing with in the basin . C. West Amended: April 2009 TL: E048000
Page 14 SELECTED REFERENCES
- 1. ALLISON, E. C. 1970- Basement Rocks of the Northern ~anta Ana Mountains: AAPG-SEPM-SEG-Pacific Section, Southeastern Rim of The Los Angeles Basin, Orange County, California-Newport Lagoon-San JoaqUin Hills-Santa Ana Mountains, Geologic Guidebook for Mareh 1970 Field Trip, p. 33-36
- 2. ALMGREN, A. A. 1973- Upper Cretaceous Foraminifera in California: Soc. Eeon. Paleontologists and Mineralogists, Pacific Section, Cretaceous Stratigraphy of The Santa Monica and Simi Hills, Guidebook for Fall Field Trip, p. 31-44
- 3. BLANC, R. P. and 1968- Natural Slope Stability as Related to CLEVELAND, G. B. Geology, San Clemente Area, Orange and San Diego Counties, California: Calif.
Div. of Mines & Geology, Special Report 98
- 4. EDGINGTON, W. J. 1974- Geology of The Dana Point Quadrangle,
.v Orange .County " Oal:i.fornia: Calif. Div. of Mines & Geology, Special Report 109
- 5. FI:b'E, D. L. 1974- Geology ot The South Half of The El Toro Quadrangle, Orange County, California:
Cali!. Div. of Mines & Geology, Special Report 110
- 6. GOODBAN. F. R. 1958- San Clemente Oil Field: A Guide to The Geology and Oil Fields of The Los An~eles and Ventura Regious: Pacific Section of American Association of Petroleum Geologists, p. 145-148
- 7. INGLE, Jr., J. C. 1971- Paleocologic and Paleobathymetric History of The Late Miocene-Pliocene Capistrano Formation, Dana Point Area, Orange County, California: Soo. Econ. Paleontologists and Mineralogists, Pacifio Section, Geologic GUidebook, Newport Lagoon to San Clemente, Ca., Coastal Exposures of Miocene and Early Pliooene Rocks, Octobe~
1971 Field Trip, p. 71-86
- 8. KLEME, D. H. and 1973- Geology of The Upper Aliso Creek Area:
FIFE, D. L. South Coast Geological Society, Guide-
'~. book to The Tertiary Geology of ED.:3terll Orange and Los Angeles Counties, Calif-ornia p. 41-46 '
Amended: April 2009 TL: E048000
Selected References (cont.) Page 15'
- 9. LANG, H. R. 1972- San Clemente Oil Field: California Summary of Operations, Division of Oil and Gas Volume 58 No.1, p. 51-56
- 10. MORTON, P. K. 1970- Geology'of the NE 1/4 and NW 1/4 Ca~ada Gobernadora Quadrangle, Orange County, California: Calif. Div. of Mines &
G~ologyt Preliminary Report 10
- 11. MORTON, P. K. 1972- Reconnaissance Geology of the Northeast portion of the San Clemente Quadrangle, Orange County, California: Calif. Div.
of Mines & Geology, Unpublished Map
- 12. MORTON, P. K. 1973- Geo-Environmenta1 Maps, Orange County, MILLER, R. V. California: Calif. Div. of Mines &
Fife, D. L. Geology, Preliminary Report 15
- 13. MORTON, P. K. 1974- Geology and Engineering Geologic Aspects of The South Half of The Canada Gober-nadora Quadrangle, Orange County, Ca:
Calif. Div. of Mines & Geology, Special Report III
- 14. MORTON, P. K. 1974- Geology and Engineering Geologic Aspects EDGINGTON, W. J. of the San Juan* Capistrano Quadrangle, FIFE, D. L. Orange County, California: Calif. Div.
of Mines & Geology, Special Report 112
- 15. MOYLE, Jr., w*. R.1973- Geologic Map of Eastern Part of Camp Pendleton, Southern California: U. S.
Geological Survey Open ,File Map 1 & 2
- 16. ~DDER, J. G. 1959- Geologic Map of The San JoaqUin HillS, YERKES, R. F. San Juan Capistrano Area, Orange County, SCHOELLHAMER, J.E. California: U. S. Geological Survey Oil and GaB Investigations Map OM 193
- 17. VEDDER, J. G. 1970- Summary of Geology of The San Joaquin Hills: AAPG-SEPM-SEG-Pacific Section, Geologic Guidebook. Southeastern Rim of The Los Angeles Basin, Orange County.
Oalifornia-Newport Lagoon-San Joaquin Hills-Santa Ana Mountains, March 1970 Field Trip. p. 15-19
- 18. VEDDER, J. G. 1971- The San Onofre Brec,cia in The San J oa quf.n Hilla: Soc. Econ. Paleontologists and Mineralogists, Pacific ~ection, Geologic GUidebook, Newport Lagoon to San Clemente, Ca., Ooasta1 Exposures of Miocene and Early Pliocene Rocks, October 1971 Field Trip, p. 12-21 Amended: April 2009 TL: E048000
Selected References (oont.) Page 16
- 19. WEBER,Jr., F.R. 1958- Geology and Mineral Resources of San 1959 Diego County, Oalifornia: Calif. Div.
ot Mines & Geology, County Report 3
- 20. WHITE, W. R. 1971- Biostratigraphy of The Capistrano Form-ation, Dand Point, California: Soc. Eeon, Paleontologists and Mineralogists, Pacifi0 Section, Geologic GUidebook, Newport Lagoon to San Clemente, Ca., Coastal Exposures of Miocene and Early Pliocene Rooks, October 1971 Field Trip, p. 12-21
- 21. WOODFORD, A. O. 1925- The San Onofre Breccia; its nature and origin: Univ. Calif. Publications, Dept.
of Geological Sciences, v. 15, No.7,
- p. 159-280
- 22. WOODFORD, A.O. 1954- Geology of The Los Angeles Basin: Calif.
SCHOELLHAMER,J.E. Div. of Mines Bulletin 170, Geology of VEDDER, J.G. Southern California, Chapet II, Geology YERKES, R. F. of The Natural Resources, p. 65-81 Amended: April 2009 TL: E048000
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San Onofre 2&3 FSAR Updated APPENDIX 2.5H SUPPLEMENT TO THE GENERALIZED SUB-SURFACE GEOLOGICAL AND GEOPHYSICAL STUDY CAPISTRANO AREA
. ORANGE COUNTY, CALIFORNIA JANUARY 1979 Site File Copy Amended: April 2009 TL: E048000
JACK C. WEST CONSUlTING PETROLEUM GEOLOGIST 515 West Commonwealth Ave., Suite 206 Fullerton, California 92632 Telephone (714) '25-;;66 SUPPLE~mNT TO THE GENERALIZED SUB-SURFACE GEOLOGICAL AND GEOPHYSICAL STUDY CAPISTRANO AREA ORANGE COUNTY, CALIFORNIA NOVEMBER 1975 JANUARY 1979 Amended: April 2009 TL: E048000
--.;~~,-
CONTENTS PAGE I INTRODUCTION 1 II DISCUSSION OF ILLUSTRATIONS 2 - 14 A Exhibit A-1
- 1. General Comments 2 - 3
- 2. General Structure 4
- 3. Faulting-Response to part (e) 4 - 7 NRC Question 361.35 B Exhibit B 7 - 9 C Structure Sections 9 - 11 D Annotated Onshore Reflection 11 Profiles-Response to part (c)
NRC Question 361.35 E Well Data-Response to part (d) 14 NRC Question 361.35 III Conclusion 14 IV Selected References 15 ILLUSTRATIONS Exhibit A-1 Monterey Countour Map Exhibit B Cretaceous Contour Map-Revised Structure Sections
- 1. A-B Revised
- 2. C-B Revised and extende~ offshore 3 . D-E Revised
- 4. H-G Extended offshore
- 5. I-J
- 6. K-L Annotated Onshore Seismic Reflection Profiles
- 1. Line No. 152
- 2. Vibroseis Line No. 8
- 3. Line No. 147
- 4. Line No. 160 1
Amended: April 2009 TL: E048000
INTRODUCTION In partial response to NRC question 361.35 regarding the Capistrano Embayment, this report was prepared to supplement and revise my November 1975 report "Generalized Sub-Surface Geological and Geophysical study, Capistrano Area, Orange County, California" (6). ~e present report centers on interpretations of the relationship between onshore and offshore geologic structure in the vicinity of the San Onofre Site. The illustrations included in this report are based upon newly acquired onshore seismic data, recent. geolo.gic suzrace mappang, formerly acquired offshore seismic data (2), and re-examination of all former surface geology and all avail~ble onshore and offshore well data. A general discussion of the illustrations follow in order to demonstrate the bases ot interpretation, but in partic-ular, this report addresses response to parts (0), (d), and (e) of the above NRC question. 1 Amended: April 2009 TL: E048000
Page 2 DISCUSSION OF ILLUSTRATIONS EXHIBI~ A-l - Generalized Contours Near ~op of Monterey Formation General Oomments To present a comprehendable picture that reflects relatively late tectonics involving an area partly covered by water, a regional sub-surface contour map, based upon the most shallow and youngest information, is necessary. After reviewing horizons within the Capistrano Embay-ment, the top of the Monterey Formation was selected as ~he bes~ and most shallow horizon that could be mapped onshore and offshore. The contact of the top of the Monterey onshore outcrop, as mapped by surface workers (1) is shown on this exhibit. Microfaunal data indicate beds near this contact ran~e in age from the lower part of the Upper lVlohnian to Lower Mohnian. Sub-surface control on this horizon is pro-vided by wells (microfauna1 and electric log data) and seismic profiles. Where applicable, contouring of this horizon has been guided by folds observed in outcrop. Western Geophysical's seismic nBtt horizon (2), which is a "time maplt was used to compile the offshore part of this map. Time "picks" on Western's map have been converted to depth using Westernrs velocities. An area of "no data" exists between the most landw~d offshore seismic shot points and the shoreline. However, information from lVlobil "San Clemente I' No. 1 core hole, depth values from the seismic profiles, and extrapolition of on-shore surface and well data to the offshore area--indicate that Westernts seismic "B" horizon is apprOXimately eqUivalent Amended: April 2009 TL: E048000
EXHIBIT A-l (cant.) Page 3 to the top of the Monterey as contoured onshore. In my opinion, the accuracy of the onshore and offshore contours being equivalent is within ,200 feet in elevation of each other. A faulted anticline is interpreted to lie within the "no data" area mentioned above because of the southwest dip of seismic reflectors and the northeast dip of beds exposed along the shoreline. The dip of onshore beds de-creases southeasterly along the shore and becomes nearly horizontal at the San Onofre Site. Quaternary deposits cover most of the older sediments, and surface dip data is qUite sparse in the San Mateo Point--San Onofre area. My structural interpretation ot the offshore area is apprOXimately th~ same as Westernts with the exception of \.J the fault near the Mobil "San Clemente" No. 1 core hole. IN'estern, on their "time" map of the ":B" horizon, has inter-preted a tault southwest ot the core hole. I agree that minor faulting may be present southwest of this hole. However, considering the age of the formation (Lower Mohnian) near the sea floor at this location together with the, seismic data on Line No. 123, I interpret the main ana significant fault to be northeast ot the core hole as shown on this exhibit. Evidence of this fault lies between shot points 87 and 99 where:
- 1. An offset ot reflections appear along the axis of a SYncline, and
- 2. The bottom of the syncline has no reflections that flatten as they normally do.
In addition" spurious events (possibly reflected refractions), that could have been generated by this faUlt, occur between shot points 123 and 99 (see Struct~re Section K-L). Amended: April 2009 TL: E048000
Page 4 GEUERAL STRUCTURE From the El Taro area to San Juan Capistrano the overall structural setting at the Capistrano Embayment is a north-south synclinal basin interrupted by some west to northwest trending arches and some minor northwest trending faults. From San Juan Capistrano southward into the offshore area the synclinal basin becomes a series of northwest trending folds and faults nearly parallel to the shore line. Farther to the southeast and southwest the dominant structure is a more homoclinal. dipping southwestward. The South Coast Offshore fault zone comprises the major fault structure offshore. FAULTING - Response to part (e) NRO question 361.35 Faults that more or less bound the Capistrano Embayment, or are exposed in outcrop outside the Embayment, are the Cristianitos fault on the east and the many faults of the San JoaqUin Hills on the west. Faults cutting the Monterey Formation interior to the embayment are relatively rare, but several are shown in Exhibit A-l generally south of San Juan Capistrano. The more important of these are discussed below. For discussion purposes three new fault names are introduced; these are, from east to west, the "Carr"', ltVaci~derotf, and "Offshore Dana Point .. faults. Evidence for the "Carr" fault includes surfae:e" mapping (3), (4), and (5), and sub-surface contour spacing based on closest well control. The fault strikes north-northwest and dips steeply southwes~. Its vertical displacement is down to the southwest (see structure Section C-B). Its. trace is obscured on the surface over one mile onshore from the shoreline. However, the shoreward extremities of seismic Amended: April 2009 TL: E048000
FAULTING (cant.) Page 5 lines No. 108 and No. 125 have evidence of faulting with "down-to-the-southwest" displacement. This displacement may possibly be the offshore extension of the "Carr ll fault.* At one* local area near the onshore surface trace of this fault a thin veneer of Niguel Formation has been mapped showing possible disturbance by this fault (4). The age of the Niguel Formation is probably Late Pliocene (5). Although we find that, in general, the Niguel Formation in the Capis-trano Embayment is relatively undisturbed, this possible evidence suggests that the latest movement on the "Carr" fault may have been during the Late Pliocene. Evidence for the "Vaciadero n fault consists of sub-surface contouring based on local well control (dipmeter, paleontological, and electric log data). The fault plane' is not exposed at the surface and is, therefore, believed to be older than t,he If Carr II fault. Its apparent direction of displacement, although larger, is the same as the "Carr't (see Structure Section C-B). Evidence of its strike is lacking. Its strike has been assumed to be similar to the IICarr" fault. Evidence for the ItOffshore Dana Point U fault consists of the low structural position of the seismic "B" horizon (approximate eqUivalent to the top of the Monterey) near th~ intersection of seismic lines No. 110 and No. 129 com-pared to the older surface rocks (San Onofre Breccia) cropping out at Dana Point. This suggests considerable vertical move-ment, down to the south (see structure Section C-B). Evidence of "offset" of seismic reflections near the intersection of Amended: April 2009 TL: E048000
FAULTING (cont.) Page 6 line No. 110 and line No. 127 (SP 40), where a down-to-the-southwest displacement is indicated, is interpreted as the southeast extension of the "Offshore Dana Point" fault. If this fault is part of the Laguna Canyon fault zone onshore, as suggested by its alignment, and the two faults are contemporaneous, then the last movement of the "Offshore Dana Point" fault is probably no later than Upper I1.iocene. The Dana Point fault has been mapped at the ground surface (1). Its dominant displacement appears to be ver-tical and down to the northeast, resulting in a horst block in the Dana Point area. Latest movement on this fault was also probably during the Upper Miocene. The South Coast Offshore fault has been interpreted as a zone of faulting including displacements that are down to the southwest and down to the northeast. In occassional areas possible lateral displacement has been interpreted. Horst blocks within the fault zone have resulted from this variable direction of displacement. The' fault zone also varies considerably in width (see Western's Horizon C map (2) ). In addition, different age of movement has been involved since only older beds are disturbed in certain areas along the' fault zone (see Structure Sections C-B. H-G. and I-J). Only that part of the South Coast Offshore fault zone nearest the shore is seen at the seismic "BIf horizon (near top Monterey). Evidence for this part of the fault zone is seen on seismic line No. 127, where labeled the "South Coast Offshore Fault", and on alignment toward the south-east, on seismic lines Nos. W-IO, 145, WS 70-18, and 123. Amended: April 2009 TL: E048000
FAULTING (cont.) Page 7 However, the fault does not continuously displace this horizon although older beds may be disturbed. For exam;le, the fault does not displace seismic horizon liB" on seismic lines Nos. 129 or 125. Some lateral movement (possibly 2500 feet) is suggested by offset contours near the intersection of seismic lines Nos. 145 and WS 70-18. The Cristianitos fault appears to die out southerly at Monterey depth. However, along the projection of the Cris-tianitos fault, evidence of faulting of older beds can be observed on seismic line No. 106 (see Structure Section K-L) . Considerable minor faulting based on surface mapping (1) is shown in the central part of T8S, R7W, where Monterey crops out. Due to the lack of significant displacement of the, top of the Monterey contact in outcrop, these faults are considered minor. At Monterey depth at more basinward positions the contour~ accordingly show minor to no displace-ment on these faults. Since the Niguel Formation, located farther north and west within the Capistrano Embayment has had relatively little fault disturbance, it is believed that movement on these faults in this area prob~bly ceased during the Late Pliocene. EXHIBIT B - Contours on TOP'of Cretaceous (Revised) This exhibit, when formerly submitted under reference (6), was intended basically to demonstrate the Cristianitos fault at Cretaceous depth and its relationship to the January 1975 earthqUakes. The revised map, insofar as available data permits, Amended: April 2009 TL: E048000
EXHIBIT B (cant.) Page a represents a better and more accurate regional interpre-tation of the area av Cretaceous depth because of newly acquired data and further study of faults in conjunction with the construction of the Monterey map, Exhibit A-l. Most of the revisions of this map are confined to the southwestern portion from the Dana Point--San Clemente area northward into the northern part of T7S, RaW. Newly acqUired seismic data, specifically line No. 147 (discussed further below), contains information that supports the presence of a SYncline, an antioline, and possibly, the Shady Canyon fault. The location of this line is plotted on this map and the interpretation of the structure at Cretaceous depth has been revised as shown by the contours *
. T~e position of th~ Shady. Canyon fault has been revised
'to coriform with its interp~eted location~on line No. 147; that is, it is now shown about 1,000 teet northeast from its former location in the Vicinity of line No. 147, but otherwise remains as shown on the original map. The po~sible extension of the Shady Canyon fault south-east from the location of line No. 147 is based on Cretaceous well points to the east and estimates of Cretaceous depths west of the fault. More specifically, the Cretaceous depth,- 5,360 feet at Roy Gill Krum No.1, Section 7, TaS, R7W, is regionally fairly shallow. There are no deep holes sout~east of the Shady Canyon fault except Roy Gill Forster No.1, Section 13, T8S, R8W. This hole did not reaoh the Cretaceous, but it 1s estimated at-7,OOO feet. I interpret this large d:ifferet:lce of Cretaceous elevations be'CWeen the. above holes to be due to fault1ng--partly by the lfCarr" fault (discussed above) and partly by the Shady Canyon fault (see Structure Section C-B). Amended: April 2009 TL: E048000
EXHI3I:f B Page 9 The direction and' length of the "Carr" and nVaciadero" faults at Cretaceous depth have been changed to conform with the Monterey map where their displacement, direction, and length have been discussed above. These faults were not named in the original 1975 report but they can be identi-fied on the original map by referring to Structure Section C-B. An interpretation at Cretaceous depth of the Laguna Canyon and Temple Hill faults, plus some additional minor faulting have been added in the San JoaqUin Hills area because they have been shown by former workers (1) and (4). They probably disturb the Cretaceous, and they show the direction of faul~ing in this area. An interpretation is also shown at Cretaceous depth of the offshore anticline (near, the shore line) cut by the "Dana Point", "Vaciadero lt , and "Carr" faults, (discussed above at Monterey depth). Fu~ther Cretaceous mapping offshore was not attempted since the horizon would fall below the "Acoustic Basement" mapped by Western Geopnysical (2). Seismic data is undiag-nostic below this horizon off'shore. STRUC~URE SECTIONS
, Sections A-B, D-E, a-B, and H-G accompanied the 1975 report (6) but they have been corrected to ref'lect revisions made on Exhibit B and to conform with the Monterey contours and faults shown on Exhibit A-l. Sections C-13 and H-G have been extended seaward along seismic lines (2) ,and two additional sections, I-J and K-L have been prepared along Amended: April 2009 TL: E048000
STRUCTURE SECTIONS (con t.) Page 10 seism ic lines to furth er demo nstra te the geol ogic inter pre-tatio n and relat ions hip betw een the onsh ore and offsh ore in the vici nity of the San Onof re Site . Seism ic horiz ons "B" and <<c>>, mapped by ',iest ern Geop hysic al (2), have been con-verte d to depth on these secti ons. The loca tion of the South Coas t Offs hore faul t zone , discu ssed abov e, is noted on the offsh ore porti on of e~ch secti on. Sect ion C-li shows the offsh ore antic line orig inati ng with a hors t block (pro jecte d from Dana Poin t) and with cons idera ble relie f. Also , note that Sect ion C-B shows the "B" horiz on undi sturb ed by the Sout h Coas t Offs hore faul t zone . However, this horiz on is shown offs et by the landw ard edge of this faul t zone on Sect ion H-G. struc ture Sect ion I-J was selec ted to fall dire ctly o . undez the San Onofre Site where ,a shall ow hole botrtomed at 989' in San Mateo Sands that appe ar in age to be eqUi valen t to the lowe r part of the Capi stran o. The offsh ore porti on of this secti on is tied to seism ic line No. WS 70-1 8, whic h illus trate s the Sout h Coas t Offs hore faul t zone that form s a large hors t bloc k. The inter pret ation is part ially sup-porte d by two shall ow core hole s, No. 92 and No. 93. These hole s were drill ed in 1968 by an oil grou p that was gath er-ing data in prep arati on for offsh ore sale s. These hole s supp ort the prese nce of a thin vene er of Quat ernar y and Uppermost Tert iary sedim ent in the offsh ore area . Based on these data , a thin , shall ow inter val of'si mila r age sedim ents is presumed to be pres ent also in the offsh ore porti on of Sect ion H-G and Sect ion K-L. Struc tul.'e Sect ion K-L is supp orted by the I~lobil "San Clemente" No. 1 offsh ore core hole , tota l depth 6,130 feet Amended: April 2009 TL: E048000
STRUCTURE SECTIONS (cont.) Page 11 seismic offshore data, and onshore surface geology. ,For reasons given under general commen!s, Exhibit A-l, the location of the fault immediately shoreward of the above core hole differs from Western Geophysical's interpre-tation (2). This fault is the landward edge of the South Coast Offshore fault zone. Annotated Onshore Seismic Reflection Profiles The following profiles (lines) have been annotated with geology and are discussed below in response to part (c), NRC question 361.35. The line locations are shown on Exhibits A-l and B. In general, these profiles have some value in relation to the dip of shallow beds and they have been used to support contours on Exhibit A-l.However, seismic reflec-tions at Cretaceous depth are very poor and have less value. Line 147, the eastern part of line 152, and the Mobil vibroseis lines have partially aided the construction of the Cretaceous map, Exhibit B. Seismic Line No. 152 The original records (1964), even with modern process-ing (1975), have resulted in very poor data to interpret. The ,eastward one-half ot this line shows reflections with westward dip. The westward one-half has unreliable data at Cretaceous depth, however, some indication of minor folding at shallow depths occurs between shot points 21 and
- 28. ,EVidence of faulting is very weak: and, wi thout the benefit of surface geology and well data, the fault inter-pretation on the Cristianitos fault zone and branch faults Amended: April 2009 TL: E048000
SEISMIC LINE no. 152 (cont.) Page 12 as shown on the annotated section could not be made. Only with the knowledge of the fault locations at the ground surface can the fault planes be extended in depth in the manner shown based upon the appearance of retleptions. The dips shown on the fault planes are partly influenced by regional geologic evidence of westward dipping "down-to-the-west lt movement on the Cristianitos and associated branch faults. Therefore, the seismic line alone, with no geologic supplementary data, has very little value in determining the age and capabi~ity of faults. It does, in general, help to confirm the west dip of the sediments east of the Cristianitos fault,. Vibroseis Line No.8 This seismic section (1971) has slightly more useful data than-N-152. Some evidence of faulting exists which can be interpreted without 'the aid of surface and SUb-surface supplementary geologic information. The best fault evidence consists of the termination and apparent offset of reflections between shot points No. 190 and No. 200, which coincides with a surface fault that is a branch of the Mission Viejo fault. The Mission Viejo fault, however, which is a large fault, has little evidence of offset in the reflections. With the aid of surface geology and well data that falls on this line, a fairly good geologic inter-pretation is shown on this annotated seismic section. How-ever, in respect to defining and evaluating the age and capability of faults, this seismic line alone--without surface and sub-surface geology has little value. Geologic structure section a-H, which falls partly on this seismic
- J..i.ne, auggeatis that the Mission Viejo Fault and its branches Amended: April 2009 TL: E048000
VIBROSEIS LINE NO.8 Page 13 occu rred sometime afte r the Lower Tert iary. ¥ith the surfa ce geolo gy, however, the refle ction s on vibr osei s line No.8 aid in deter mini ng the amount of faul t displ acem ent. Seism ic Line No. 147
'This line was shot in 1954 and repro cesse d in 1964 by Stan dard Oil. More usea ble data is pres ent on this line than any othe r onsh ore seism ic line examined in this area . Stil l the refle ction s are comp arati vely of low qual ity, but they do defin e an antic line and a sync line.
Faul ting is indic ated where shown as the poss ible exten sion of the Shady Canyon Faul t that is mapped on the surfa ce in the San Joaq uin Hill s area to the north west . A predo mina nce of north ward dipp ing refle ctor s (1.5 tQ 2.5 secon ds) is shown on the secti on-- main ly on the south ern half . ' 'Thes e' data prob ably do not repre sent geolo gy in the plane of the secti on. They are belie ved to be refra ction s from a sourc e away from the plane of the secti on-- poss ibly from faul ts loca ted to the west on the, easte rn slope of the San Joaq uin Hill s. The secti on is supp leme nted by well data shown anno tated along with an inter pret ation of the geolo gy. Faul t evide nce is not stron g, but the refle ction s indic ate distu rban ce in the area where the Shady Canyon Faul t is inter prete d as poss ibly pres ent. In this case the seism ic data sugg est that the late st movement on the Shady Canyon Faul t was jU&t prio r to the depo sitio n of the Mont erey, prob ably durin g the Middle Miocene. Seism ic Line No. 160
'~his line was rece ntly acqu ired from Stan dard CJll aloHg with line No. 147. It was also shot in 1954 and repro cesse d
Amended: April 2009 TL: E048000
SEISMIC LINE NO. 160 Page 14 in 1964 by Standard. Reflections on this line are very poor and there does ~ot appear to be any substantial evidence to support faulting. Some minor folding is sug-gested in the more shallow beds as shown by the annotated geology. ~he poor data does partly support the general geology where, the line is located on the contour maps-- Exhibits A-l and B. Well Data Well data comprise all available information pertaining to logs of Itborings" requested under part (d.) of NRC question 361.35. In August of 1977 all of the well data was compiled and annotated on electric logs of all holes that had run electric logs. ~he annotations showed in briefed form all significant data such as dipmeter, cores, sidewalls, tops of geologic horizons, fault'interpretations, and pal~ontology. Where electric logs were not run the history and drillers log were compiled., All of these data were forwarded 'to the NRO in December 1977" CONCLUSION In addition to responses to specific portions of NRC question 361.35, this report includes an illustration (Exhibit A-l) of the most extensive, shallow, and mappable sub-surface horizon onshore and offshore in the San Onofre region. ~he interpretations shown on this and the additional illustrations suggest that the major tectonic activity within ten miles of the site took place prior to the termination of the Pliocene epoch, possibly two million years before present; and since that time the area has been tectonically quiet-- with the exception of the South Coast Offshore fault zone along which some movement probably occurred in the Late Pleistocene. Data that I have examined reveal no additional faults of this or younger age within about five miles of the San Onofre site. Amended: April 2009 TL: E048000
Page 15: SELECTED REFER3NCES
- 1. 110RTON, P.K. 1973- Geo-Environmental Maps, Orange County,
~IILLER, R. V. California: Calif. Div. of Mines &
FIFE, D.L. Geology, Preliminary Report 15 So. Calif. Edison San Onofre Nuclear Generating Station Company Units 2 and 3--Preliminary Safety Analysis Report, Amendment No. 11, Appendix 2E, April 1972 VEDDER, J.G. 1959- Geologic Map of The San Joaquin Hills, YERKES, R.F. San Juan Capistrano Area, Orange SCHOELLHAMER, J.E. County, California: U.S. Geological Survey Oil and Gas Investigations Map OM 193
- 4. EDGINGTON, W.J. 1974- Geology of The Dana Point Quadrangle, Orange County, California: Calif.
Div. of Mines & Geology, Special: Report 109
- 5. VEDDER, J.G. Revised geologic map, structure sections, and well table, San Joaquin Hills--San Juan Capistrano area, California; USGS Open File Report 75-552
- 6. So. Calif. Edison San Onofre Nuclear Generating Station Company Units 2 and 3--Recent"Geotechnical Studies, Southern Orange County, California, Vol. II, Enclosure 3, February 1976
- 7. :2HLIG, P.L. Geology Map Adjacent to San Onofre FARLEY, T. Nuclear Generating Station--
Unpublished 1978 Amended: April 2009 TL: E048000
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San Onofre 2&3 FSAR Updated APPENDIX 2.51 PRESENTATION TO NRC/USGS SEPTEMBER 1980 Site File Copy Amended: April 2009 TL: E048000
ENCLOSURE 1 EDITED TRANSCRIPT OF DR. P. ELHIG DISCUSSION OF GEOLOGIC SETTING, SONGS AREA - SEPTEMBER 23, 1980 This is in response to questions raised con~ern1ng 1) the interrelationship between the Cr1stianitos fault and the Offshore Zone of Deformation (OZD) and
- 2) the likelihood of future seismic activity along the Cristianitos fault.
The main conclusions presented here are:
- 1. The trend of the Cristianitos fault is parallel to and ,controlled by the structural grain of the Peninsular Ranges. The trend is not a product of wrench fault tectonics*
- 2. The Cristianitos fault is a westward-dipping normal fault which moved in association with subsidence in the Capistrano Embayment during the Late
- v. cliocerie and Early Pliocene in the interval between apout 10 and 4 million
'years (m. y.) before present.
- 3. Activity on the Cristianitos fault was caused by crusta~ extension in a westward direction and occurred simultaneous with the develop~nt of a deep submarine depression within the Los Angeles Basin.
- 4. The Cristianitos fault is probably a listric normal faul!: produced by gravity gliding into the Los Angeles Basin. The inclination of the Cristianitos' fault probably decreases downward and merges into a bedding plane fault within deep strata of Cretaceous or Late Jurassic age.
2.51-1 Amended: April 2009 TL: E048000
- 5. The Cristianitos has been inactive since Late Pliocene. The Cristianitos fault can no longer move because filling of the Los Angeles Basin prevents gravie! gliding and because the tectonic stress has changed from extension in an east-west direction ,to compression in a northeast-southwest direction.
- 6. The open folds and minor faults observed in acoustic profiles in the nearshore area between the Cristianitos fault and the OZD do not represent an interconnection between the Crist1anitos fault and the OlD. The displacement on the Cristianitos fault dies out near the coast as a result of *downwarpin~ of the coastal area underlain by thick d~posits of San Onofre Breccia directly east of the Cristianitos fault.
- 7. Moveme~t on the OZD would not trigger movement on the Cristianitos fault.
In order to understand the structural evolution of the .region surrounding SONGS it is necessary to regress in time to the Mesozoic. At the beginning of the Mesozoic the Nort~ American Craton terminated along the eastern margin of the present Peninsular Ranges. During the Late Jurassic, sedimentary strata of Triassic and Jurassic age, referred to as the Bedford Canyon Formation near SONGS, weI': accret:ed against this part of North America, presumably as a result of eastward subduction of oceanic crust (Hamilton, 1978; Criscione and others, 1978). Volcanic and volcanic~astic rocks were emplaced on top of the accretionary wedge along the western side of the Peninsular Ranges during the Late JuraSSic: and Early Cretaceous (Gaseil and others, 1915). Batholithic rocks intruded the accretionary wedge during the Cretaceous. The initial batholiths were emplaced along ehe west 'side of the Peninsular Ranges starting 2.51-2 Amended: April 2009 TL: E048000
about 120 m.y. ago but the belt of later :4ntrusiol1s shifted progressively eastward with time (Silver and others, 1979). Batholithic intrusion was accompanied by uplift and erosion, but, by Late Cretaceous, subsidence along the western margin of the Peninsular Ranges permitted the sea to transgress eastward to form a rugged shoreline near the western margin of the batholithic intrusions (Figure 1). As seen today, the eastern limit of Upper Cretaceous marine strata forms a relatively straight line from the Santa Ana ~ountains at the northwest corner of the Peninsular Ranges to the Vizcaino Peninsula in Baja California- Gastil and others (1975, p- 47) refer to this as the Santillan and Barrera line in honor of the geologists who. 1n 1930, firs t called attention to it in a publication. The line was originally thought of as the eastern edge of a geosynclinal basin analo~ous co che Graat Valley of California but in terms of modern nomenclature we ~lould refer to i : as a forearc basin- The Santillan and Barrera line is a t eccont.c hing',; line .\-/ separating the thick, buoyant, dominantly batholithic continental crUst, to the east from the westward-thinning. accretionary* ~'1edge which adjoins oceanic crust to the west. Downwarp1ng to the west of this line was probably controlled primarily by isostatic adjustments and proceeded gradually through time in response to loading by sediments eroded from the continent to the east of the line_ The surface trace of the Cristianitos fault is subparallel to the Santillan and Barrera line and lies at an ayerage distance of about 6 miles (10 km) west of it. As interpreted here, the Cristiani.tos fault is a westward-facing listric, normal fault which passes downward into a bedding-plane fault within the lower part of the post-batholithi~ Cretaceous strata or underlying Santiago Peak Volcanics which contain interfingered marine shale. Structural 2.5I-3 Amended: April 2009 TL: E048000
factors controlling the Cristianitos fault would be the westward dip of the deep strata and the eas~ward pinchout of clay-rich strata which might serve as surfaces of low shear strength during gravity gliding. Keep in mind that the dip of the strata would be essentially perpendicular to the Santillan and Barrerea line and that the dips would be steeper at the base of the sedimentary sequence than near the top because of the progressive westward tilting through time. During the period from the Late Cretaceous through the Lo~ver :tiocene, the position and configuration of the coastline varied slightly, probably as a result of fluctuations in relative sea level and minor c.rustal vtarping. During the Eocene the coast transgressed landward across the Santillan and Barrera line but most of the time it was on the seaward side of the line. During the Lower Miocene (about 2.0 m.y. ago) the shoreline *"as immediately west of SONGS and. trended north...n orthwesterly across the present Capistrano EmbaYment as shown diagramatically in Figure 2. (after Campbell and Yerkes, 1976). At that time the Vaqueros Formation was deposited under shallow marine conditions on the seaward side of the shoreline while the continental Sespe Formation was deposited on the landward side. At the beginning of the Middle Miocene (about 16 m-y. ago) conditions changed radically along the southern California coast and adjacent offshore borderland_ The change may have been brought on by passage of the East
*Pacific Rise beneath this part of the cont:inental margin or by divergent transform faulting postdating the overriding of the rise. The major changes included: 1) the sudden appearance of Catalina Schist at the surface in the area offshore from the present c9ast with local shedding of schist debris in a 2.51-4 Amended: April 2009 TL: E048000
northerly to easterly direction to form the onshore occurrences of the San Onofre Breccia; 2) widespread volcanism including volcanic intrusions within and to the north of the San Joaquin Hills; and 3) crustal extension and fragmentation causing the initial opening of the Los Angeles Basin (Figure 3). Figure 4 (after Stuart, 1979) shows the distribution of San Onofre Breccia which consists of Catalina Schist debris and the probable landward limit or schis t bedrock. The juxtaposition of the schist against Peninsular Range basement is significant because the t.-10 formed in very different environments. Whereas the Peninsular Ranges basemeut formed in a sha.l Low continental margin environment with batholithic magma believed to be derived from a subduction zone 125 to 175 km deep, the Catalina Schist experienced low temperature, high pressure metamorphism characteristic of a subduction zone at a depth of 30 to 40 km (Platt, 1974, 1976). The limited available data indicates the schist was metamorphosed synchronous ~ith batholithic ~ntrusion (Suppe and Armstrong, 1912); consequently, the two terraces were probably generated further apart than at present and have been brought together by faulting. In the area offshore from SONGS the contact between the. two terraces is generally assumed to lie along the OZD but the presence of a thick sedimentary cover inhibits verification. The greatest known thickness of San Onofre Breccia is exposed on San Onofre Mountain east of SONGS Where it was deposited on a piedmont alluvial fan (Figure 5). Details of its depositional environment in the SONGS area are described by Ehlig (1979) and Stuart (1979). Volcanism was Wide spread within southern California during the Middle Miocene but in the region around SONGS it occurred mainly within and to the north of 2.5I-5 Amended: April 2009 TL: E048000
the San Joaquin Ii1lls. Here, the volcanic rocks occur as flows and
\.....)
pyroclastic debris interbedded with the Topanga Formation and as intrusions along faults (Vedder and others, 1957; 1975). A southward plunging domal uplift developed in the San Joaquin Hills and area tc the north simultaneous with emplacement of volcanic rocks. McCulloh (1960) has mapped steep-gradient positive gravity anomaly over this area. Although McCulloh suggested the ano081y might be caused by a gabbro intrusion in the underlying basement. it appears more likely that the area is underlain by a shallow laccolith of Middle Miocene age. A microfauna! analysis of the Topanga Formation in the northwestern 'San Joaquin Hills indicates water depths increased from about 250 m (800 ft.) at the start of the ~Uddle aiocene' (16 m.y. ago) to about 1800 m (5900 ft.) in late lUddle Hiocene (about 14.5 m.y. ago) as determined by Ingle (1979) (Figure 6). This reflects tne initial opening of the Los Angeles basin. As subs Ldence progressed thoughout the area, and a silled basi.n with oxygen-deficient bottom water developed, sedimentation changed to the laminated diatomaceous shale of the Monterey Formation and the paleogeography was as shown in Figure 7. In the areas southeast of SONGS massive sandstone deposited as small submarine fans interfingers with shale 1n the Monterey Formation. This reflects the presence of a relatively steep submarine slope along the western margin of the Peninsular Ranges. About 10 m.y. ago during the Late Miocene, the Cristianitos fault began 1:0 move in association with subsidence in the Capistrano Embayment as described by Ehl1g (1979a). The initiation of faulting occurred while the area was below sea level and is marked by a change in sedimentation from the dominantly 2.51-6 Amended: April 2009 TL: E048000
laminated diatomaceous strata of the Monterey Formation to the poorly bedded mudstone, siltstone and sandstone of the Capistrano Formation. Beds within the two formations are concordant and are gradational in lithology within the interior of the embayment but are discordant and change abruptly from shale to sandstone adjacent to the Cristianitos fault. During deposition of the Ca~istrano Formation, two large submarine fans had their heads along the base of a west-facing submarine scarp along the Cristianitos fault. One is in the northeastern part of the Capistrano Embayment and is represented by massive sandstone of the Oso Member of the Capistrano Formation. Recent grading for residential development along the west side of the Cristianitos fault east of Oso Creek has created .excellent temporary exposures of the contact between the Oso Member and underlying Monterey Formation. Here, conglomeratic sandstone .of the Oso Member rests upon a scoured surface cut on slightly upturned beds of Monterey shale. In one place, Oso sandstone abuts against Honterey shale along a stee~ -sided channel.~all which was previo~sly mappe4 as a fault by Vedder and others (1915). The sand of the Oso Member was probably fed into the area by the ancestral Trabuco Creek which drained across the present trace of the Elsinore fault. The second submarine fan had its head along .the Cristianitos fault in the area between. SONGS and San Mateo Creek and, although its massive sandstone"is referred to as the San Mateo Formation, it interfingers with and is part of the Capistrano Formation. The coarsest part of the fan-head deposits is restricted to a small area between San Onofre and San Mateo Creeks. This suggests that the fan was fed by a submarine canyon cut into the scarp along the Cristianitos fault, probably the ancestral San Mateo Creek which drained a large area extending east of the Elsinore fault during the Late Miocene. 2.51-7 Amended: April 2009 TL: E048000
Simultaneous with the development of the Capistrano Embayment t the Los Angeles Basin deepened rapidly in the vicinity of Newport Bay on the west side of a submarine ridge which occupied the present position of the San Joaquin Hills. Faunal Analyses by Ingle (1979) indicate water deptRs were at least 3,000 m (9840 ft.) in the Newport Bay area during the Late Miocene (Figure 8). At the same time water depths were a maximum of 2,500 m (8 t 200 ft.) in the Dana Point-capistrano area at the mouth of the Capistrano Embayment (Figure 9). The paleogeography for this period is shown in Figure 10. Notice that the arrangement of the Doheny and San Mateo submarine fans indicate" a relatively steep south-facing submarine slope existed at the mouth of the Capistrano Embayment with a deep ocean basin to the south. FaUlting, ~lhich occurred in the area of the San Joaquin Hills during the Middle and Late Hiocene, was probably caused _by extension associated with domal uplift and gravity gliding toward the Los Angeles Basin. Most. of the faults trend between north and north-northwest and are steeply dipping"with the west side down. In cases where th.e east side of a fault is down, the fault pattern commonly suggests a graben structure. The c.ross section in Vedder and others (1975 t Figure 10) favors a gravity glide origin for the Pelican Hill fault. The diagnostic features are the decrease in the dip of the fault plane with depth and the reverse drag along the down thrown side of the fault. The Pelican Hill fault* has a stratigraphic separation of about 6,000 feet, Which could easily be accommodated by gravity gliding into the Los Angeles Basin where crustal extension and basin deepening removed lateral support from the west flank of the San Joaquin Rills structural high. 2.5I-8 Amended: April 2009 TL: E048000
Movement on the Cristian1tos fault and extension within the Capistrano Embayment is also probably the result of gravity gliding in a westward direction into the Los Angeles Basin. That the Cristianitos fault is a west-facing normal fault can readily be seen in the coastal exposure southeast of SONGS. Here t the fault dips 57 degrees west with slickensides oriented down the dip. The west side is down and reverse drag on the downthrown side indicates a flattening of the fault plane with depth (Ehlig, 1977, Figure 4). Similar features exist along the fault within the Capistrano Embay~ent. For example, cross section C-B by West (1978) shows reverse drag on the down side (west) of the fault. Cross section C-B i~dicatas a regional dip of about 15 degrees west along the base of the Cretaceous to the east of the Cristian1tos fault where the structure is well known_ Although cross section C-B indicates gentle dips along the -base of the Cretaceous beneath th~ Capistrano Embayment, structural control is restricted to the upper half of the sedi~ntary sequence. The base of the Cretaceous sedinents is likely to continue to dip westward beneath the Capistrano Embayment as a result of westward thickening and the addition of older strata at the base of the sequence in the seaward direction from the Santillan and Barrera line- The base of the Cretaceous may also dip westward beneath the San Joaquin Hills structural high 1f the domal uplifting of the high was the result of a Middle Miocene laccolithic intrusion as appears likely. The Cristianitos fault 1s likely to flatten with depth and become a bedding plane fault near the base of the Cretaceous sediments. Movement on the Cristianitos fault was probably caused by gravity gliding of the hanging wall block and was the result of inadequate lateral support within the Los Angeles Basin where the ocean floor was very deep and where the westward continuation of the Middle Miocene and older rocks of the Peninsular Ranges had been removed boy crustal extension 2.51":'9 Amended: April 2009 TL: E048000
and/or strike slip faulting. It should be noted that Los Angeles Basin had a different configuration during the Late Miocene and Early Pliocene than at present. A deep trough extended southward across the present coast to the west of the San Joaquin Bills structural high whereas a northwest-trending structural high has subsequently developed along the landward slide of the coast to the west of the San Joaquin Hills. This 1s shown by the fact that Opper Miocene strata exposed above sea level on the west side of San Joaquin Sills were, according to Ingle, (1979), deposited at an ocean depth of about 10,000 feet (3,000 m) whereas strata of the same age are 20,000 feet below sea level within the deepest part of the present Los Angeles Basin. The Cristianitos fault: appears to have stopped moving about 3 or 4 million years ago during the Pliocene in a6sociatio~ with filling of the Los Angeles Basin and the start of a new tectonic regime involVing uplift (Figure 11). The Capistrano Embayment emerged above sea level during. deposition of the 0 Niguel Formation in Late Pliocene. The greatest. uplift has occurred along the present coast where stratat ~~hich ~Y'ere deposited at a depth of 6 t 500 feet (2,000 m) during the Early Pliocene (Ingle, 1979), are now above Sea level. The uplift is occurring along a northwest-trending arch as indicated in Figure
- 12. The uplift is interpreted to reflect crustal compression oriented in a northeast-southwest direction with the axis of least compressive stress oriented vertically. This present tectonic regime is probably the result of compression'across the bend in the San Andreas fault. Most of the activity on the Cristianitos fault and associated opening of Capistrano Embayment predates 240 km of right slip on the San Andreas fault and occurs at a location far from the bend in the San Andreas fault.
2.5I-10 Amended: April 2009 TL: E048000
One of the most puzzling problems associated with the Cristianitos' fault has been the nature and cause of its southward termination. In spite of the fact that the fault is well exposed in the sea cliff southeast of SONGS. it cannot be located in the offshore area. The most likely explanation is that the fault dies out immediately offshore with part of the dying out being acc.ommodated by downwarping toward the southwest as seen -in Woodward-Clyde sparker profile 849. The fault probably dies out because of a change in the physiography and geologie structure which existed in the vicinity of the present coast during the Late Miocene and Early Pliocene. In the inland area to the east of the Cristianitos. exposed bedrock consists mainly of Eocene and Cretaceous strata striking nearly parallel to the fault and dipping gently in a westerly to southwesterly direction. The San Onofre Breccia forms the principal exposed bedroc.k east of the fault near the coast. It strikes in northwesterly to westerly directions at an angle to the Cristianitos fault and dips seaward at angles* typically ranging b.etween 35 and 45 degrees along the south flank of the San Onofre 11:ountains (Ehlig t 19779)*. If this change in structure is present at depth to the west of the surface trace of the Cristianitos fault. it would tend to prevent gravity gliding toward the Los Angeles Basin *in the area south of the present coast and the steeping of the dip would tend to cause the Cretaceous beds to be buttressed. An alternate possibility 1s that the downwarpi~g of the coastal area southeast of the Cristianitoa fault tended to reduce the gravitational driving force along the southern edge of the gravity glide block causing displacement to die out in the offshore area. Other possibilities exist but they do not alter the conclusions that the Cristianitos fault dies out a short distance offshore. 2.51-11 Amended: April 2009 TL: E048000
Neither do they alter the concl~sion that the Cristianitos fault is presently inactive and has been demonstrably inactive since it was overlain by the coastal terrace about 125,000 years ago and has probably been inactive since the Pliocene. The present tectonic and physiographic setting are inconsistent with future activity along the Cristianitos. 2.51-12 Amended: April 2009 TL: E048000
BiBLIOGRAPHY Ehlig, P. L., 1979a, The late Cenozoic Evolution of the Capistrano Embayment: Geologic Guide of San Onofre Nuclear Generating Station and adjacent regions of Southern California, Pacific Section !APG, SEPM, and SEG, 1979. Ehlig, P. L., 1979b, '~1iocene Stratigraphy and Depositional Environments of the San Onofre .Area and Their Tectonic Significance," in Uiocene Li tho-facies and Depositional Environments. Coastal Southern California and Northwestern Baja, California, Pacific Section SE~{, 1979. Gastil, R. G. Phillips, R. P., and Edwin, C. A.,1f Reconnaisance Geology of the State of Baja, California." Geological Society of America Memoir. 140, r'71... Ingle, J. C. Jr., "Biostratigraphy and Paleoecology of Early Mioene Through Early Pleistocene Benthonic and Planktonic Forminifera, San Joaquin Hills-Newport Bay-Dana Point Area, Orange County, California," in Miocene Lithofacies and Depositional Environments, Coastal Southern California and Northwestern Baja, California, Pacific ~ection SEPM, 1979. Vedder, J. G., et a1., 1957, Geologic Map of the San Joaquin-San Juan Capistrano Area, Orange Couney, California: U. S. Geological Survey, Oil and Gas Investigation Map, OM193. 2.51-13 Amended: April 2009 TL: E048000
Vedder, J. G., 1975, The Revised Geologic Map, Structure Sections, an~ Well Table, San Joaquin Hills-San Juan Capistrano Area, Orange County, Cal1fornia,1l u. S. Geological Survey Open File Report 75-552. 2.5I-14 Amended: April 2009 TL: E048000
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ENCLOSURE 2 EDITED TRANSCRIPT OF DR.. D. MOORE DISCUSSION OF OFFSHORE RECENT SEISMIC REFLECTION PROFILES SEPTEMBER 23, 1980 This first slide (Fig. 13) shows track lines of the majority of the seismic reflection data now available to us. For your orientation, let me point out the coastline and the locations of SONGS and the onshore Cristianitos Fault where it meets the shoreline_ The chart includes some early sparker data by Harine Advisors and General Oceanographics which is scattered rather Widely through the area off SONGS in a reconnaissance ne two rk . Also included are several 3.5 KHz transect~ and a few of the high powered, deep penetration data lines of Western Geophysical- Please note the dart co r es saap Le locations, shown in red. These have provided samples from which paleontological data have given ages for rocks that we can see in our recorded seismic sections.
~!ost significant to this discussion are these close spaced tlood~vard-Clyde sparker transects on the shelf Just south of SONGS and the detailed NEKTON water-gun survey lines that extend from ,the Woodward-Clyde data south to Oceanside. The Woodward-Clyde data, collected in 1918 for studies in connection with a possible LNG terminal site, have allowed us to study geological structure in this area in unusual detail. These Woodward-C1:yde data were specifically examined with the intent of tracing an offshore extension of the Crist1anitos Fault. The close spacing of the lines allows a high degree of confidence in correlating geologic structure from one line to the next.
'the 1980 NEKTON water gun survey lines are also close spaced and were spec1f1call~ positioned and collect to cover the area south of the Woodward-Clyde data, where an offshore projection of the onshore Crist:ianitos Fault
\.....--i trend might intersect the hypothesized OZD (ROZD). 2.51-27 Amended: April 2009 TL: E048000
The follow in$ concl usion s resul t from exten sive studi es of the data:
- 1) The seiantl.c data do not revea l a seawa rd exten sion of the Crist ianito s Fault beyond about 6 tOOO feet.
The next slide (Fig. 14) shows selec ted sectio ns of, the north ern Woodward-Clyde seism ic lines . Horiz ontal scale s vary somewhat from profi le to profi le as a resul t of ship speed chang es during the shoot ing. On these illust ratio ns, the avera ge horiz ontal scale is shown by the bar graph line indic ating 5,000 feet. The verti cal scale s are 1 secon d of reflec tion time and are all equal . As a resul t of the short spacin g on these lines t which is relate d to the ship' s speed when they were runt the profi les have a verti cal exagg eratio n of about 6 to 1. This is usefu l ,when interp reting the record s t becau se it empha sizes 2.51-2 8 Amended: April 2009 TL: E048000
features which otherwise would be difficult to see. To illustrate vertical exaggeration, note that on these illustrated profiles the apparent dip is about 16 to 17 degrees. It is actually about three degrees. Within the three colored units there is an increased degree of folding with depth. It is clear that sedimentation has occurred with the folding as indicated by the unconformities. The most pronounced intensification of the folding with depth has taken place beneath the blue youngest Monterey unit. 2.5.1-29 Amended: April 2009 TL: E048000
We will now examine the major features that. are shown by this series of \..,.) sections. The HOZD which occurs out near the edge of the shelf is best developed as we go south towards the central portion of the sections. Here the HOZD is displayed as prominent complex anticline or ant1clinonoriam, that in most places, although not everywhere, is pro~nently faulted. As seen in these selected sections, the OZD and its contained faults commonly extend up to the sea floor. where the Monterey formation is outcropping or slightly covered by young outer shelf deposits. One of the most ?ersistent features seen in these profiles is the broad asymmetrical syncline developed along the east flank of the HOZD. As is illustrated by the onlapping relationships, you can see that the folding which took place in the BOZD and to the east was accompanied by deposition of the younger sedi~ents. TIle Capistrano for~ation in places, pinches out: against the youngest Honterey formation. In other places it does not entire~y pinchout, but instead it .lap~ across the yo~ngest Monterey folding. East of the ROZD and its east flank syncline we see the other clearly defined feature of the area. That is the broad, low amplitude, more northerly trending anticline and syn~line couple that exists beneath the shelf sediments east of the HOZD. Although one can see the multiple smaller anticlines and synclines developed in this general area, it is clear that the primary features are the broad anticline and syncline with the complicating smaller structures superimposed. These principally broad low amplitude folds have some faults within them. These faults, we believe, are the result of the folding or bending of the thick Monterey sediments. The Monterey formation, as Perry Ehlig has pointed out, is a soft, fine-grained commonly impermeable material d~osited 1n an oxygen-poor environment. A thick section of that 2.51-30 Amended: April 2009 TL: E048000
- kind, if bent even slightly, can develop very high pore pressures and V
consequent low strength. When gently folded, these sediments typically develop many anticlines and synclines along the crests of large anticlines. Along with this, they develop very commonly intra and interformational faulting both in the anticline's and syncline's axes. This type of faulting is yell developed as illustrated in sections 836, 839 and 841. In addition to this interformational faulting associated with folds, several deep faults occur in the uncolored section in what appears to be the acoustical basement, probably the San Onofre Breccia. These prominent faults in the acoustic basement occur in the eastern part of the area studied. These old faults, however) cannot penetrate significantly up into the overlying older Monterey,
~ecause we see unbroken seismic reflectors through the section slightly above them.
Turning now to a section showing a detail from line 836 (Fig. 15): .The position of the detail is identified in the series of sections. This detail is intended to explain a fault at this location- However, if we look at the untouched enlarged original profile, we can see that there is considerable continuity to the section near the top of the syncline, but with depth there appears to be some fuzziness bf arriving defractive signals- This is probably a function of bedding plane slippage; the result is relatively tight folding with slippage much, like slippage along the leaves of a book, Because the "leaves" are stack.ed one on top of another, the subject slippage resembles a single fault in section_ Again, it appears to be an intra-formational feature and does not extend up to the Pleistocene unconformity. as we can see reflectors passing across the location where the fault would project. 2.51-31 Amended: April 2009 TL: E048000
The next detail is from profile 841 (Fig. 16), identified in the series of\.....,.J sections from the earlier figure. This is a similar section showing clear evidence of through-going bedding passing beneath "book leaf" type intra-formational faulting. It appears that there is continuity of reflectors above this feature as well, although somewhat obscured by the bottom mutiples in the seismic profile. The interpretations of this section are shown in line drawings below the untouched profile.
- iext t I 'Nill discuss a somewhat different situation as axemplified in the detail of section 847 (Fig. 17) from a region east of the folds. We have indicated a fault here overall in the section. However, as we look at it very closely in the detail, it is difficult to see exactly where the fault should be located. Again, there is probably continuity of bedding across the top. of it. With regard to this zone, wher.e. it is difficult to trace the bedding* ......,)
plane reflectors through, this .type of feature is typical of sections of Monterey formation that have high quantities of gas diffused through the sediments. There are other explanations for this type of record, but gas diffusion is the most plausible explanation for the feature. The line draWing interpretation of this detail is shown in the lower half of the 'illustration. The next. slide (Fig. 18) shows a series of Woodward-Clyde profiles to the south. These sections again show the linear features of the northern section proceeding to the south. The ROZD is very prominently displayed in the upper three of these records. Again we can see the very well developed asymmetrical syncline that lies on the east flank of the ROZD and also* we can see the lower amplitude anl=icline and syncline developed to the east and beneath the shelf. As was poiheed out earlier, there are complicating, additional smaller folds developed Within these structures. These will show up in the structure 2.51-32 Amended: April 2009 TL: E048000
map which will be shown in a later figure. The main point to make here again is that the faulting that occurs in the folded section east of the HOZD is a function of squeezing of the beds by the gentle folding of these very incompetent, and impermeable beds which develops high pore pressure and results in faulting and buckling along the crests of the folds. Most of the displayed faults are intra-formational and relatively minor and "do not extend" from deep in the section to the surface. In many places we can trace reflectors across the tops of the folds. In most places, we cannot extend these faults up into the younger Monterey show.n in blue. Let us move on to the NEKTON profiles (Fig. 19) further to the south,and we will see that the broad anticline-syncline pair that we have been tracking from the north to the south will project into the uppermost of the NEKTON lines. Before discussing the NEKTON sections, I would like to point out that these are of a different scale than the Woodward-Clyde lines. These are a different type of seismic profile and were shot at a higher repetition rate. As a result, they have a vertical scale exaggeration which averages only about 3 to 1. The water-gun device, as used, allows clearer definition of thin layers and minor" structures. It does not get deep penetration, but was designed to identify deformation and faulting in the upper two hundred meters of the stratigraphic section. With the NEKTON survey we were attempting to look in this southern region for any possible extension of the Cristianitos fault and particularly for evidence as to whether or not it might interconnect with the BOZD. In the uppermost profile, we see the typical development of Offshore Zone of Deformation. Also evident are the folds of the anticlinesyncline"" pair projecting from the 2.5I-33 Amended: April 2009 TL: E048000
north. The feature has become distinctly narrower here, appears to be dying out and, at the level of line 26, becomes more parallel to the HOZD as i t extends to the southeast. This will be seen better on the plan view structure map to be shown later. The projection of the anticline-syncline from the Woodward-elyde data into the N~ON data is best seen in NEKTON lines 30 and
- 28. Figure 20 shows a detail of that part of line 30 that contains the fold. The new, narrower and somewhat steeper-s1ded fold does not appear to be faulted. Spurious "crossover" type reflections are developed on the deeper flanks of the fold. These are the result of the inability of the relatively broad beam of the receiving system to define abrupt changes in slope where the strata on the flanks of the anticline are flexed in their change to a synclinal configuration.
South of NEKT9N l1:t;le 24 there is' a . r~ther striking .change in* the seismic* reflection. expression of the HOZD. The HOZD is no longer expressed as a very large, complex, faulted anticline, but appears to show well bedded Monterey-type reflectors juxtaposed by- a single fault against a very fuzzy and incoherent zone of poor reflectors. Such fUZZiness is very reminiscent of the type of records obtained from traverses over kuowo. San Onofre Breccia-:-type rocks. You will note that we have not put interpreted line drawings in the lower three of these' profiles. Because of the change in geology, good reflecting horizons are difficult to see. The structures may be there, but they are very difficult to recognize. Furthermore. we are well south of the region of a possible intersection of the aoZD and Cristianitos. We do see a juxtaposition of the bedded. Monterey-type sediments against the homogeneous section without coherent reflectors. Note that at the level of line 22 the syncline flanking the east side of the aOZD has disappeared. This expression 2.51- 34 Amended: April 2009 TL: E048000
of the HOZD is seen on the four southern profiles from the NEKTON data- The position of this single HOZD fault can be seen on the lower three profiles of the NEKTON data posted on the wall (Fig. 19). A feature that should be noted is that, as the anticline-syncline folds that we tracked from north to south dies out, a second zone of folds develops to the east - These in turn become less prominent further south and become gentle, very broad folds. The upper colored units are the same as those similarly colored in the ~:joodward-Clyde lines to the north. No Plio-Pleistocene unit can be traced this far south and only a very thin green, Capistrano. eqUivalent unit is present in the upper three profiles> Even the blue, youngest 110nterey unit is missing on. the lowe+ three sections. , The prominent unconformity between the blue and the older Monterey below and the onlapping of the blue over the older sediments again shows that most of the folding had d~veloped prior to deposi-tion of the latest Monterey. That unit was, however, deposited as the less intense folding of that time took place. To summarize what we have seen in these sections, the main structures are the HOZD and the very prominent syncline that lies on its eastern flank. In the central part of the' surveyed area, the other main features we see are the anticline-syncline foldS which trend north northwest, diverging from the HOZD 2.51-35 Amended: April 2009 TL: E048000
in the area of the Woodward-Clyde data, and dying out to the north- These .~ same features are more parallel to the HOZD in the northern part of the NEKTON data area- Further south they disappear- These folds have associated faults with an axial development- Other folding and associated faults are developed to the east in the area covered by NEKTON lines 26, 28, and 30. Fig_ 21 is the composite structural map resulting from this work. The structural map shows all of the features that are displayed within the data sections, inclUding the folds and the faults t both in the shallow and deeper parts of the recorded section- Because the map displays all of the folds and faults from all depths, it is cluttered with data- To sort out this plethora of data, the various el~ments should be considered separately_ If we look .first at the trends of the major fol,d axes j we can -aee that t.he* most prominent and continuous feature is the major syncline that lies to the east of the HOZD. The folded zone to the east of the HOZD comprising the broad anticl1ne-syncl1ne pair is also well displayed- It is apparent that these folds converge with the HOZD in the region of the Woodward-Clyde lines in the northern area and then become parallel to it in the NEKTON data area to the south. These folds also die out to the north and south, being best developed in the central Woodward-Clyde data area. The folds still further to the east in the area of the juncture of the two survey areas are well shown on this map-Next we will strip away the folds and look at a series of maps shOWing faults af different ages. Figure 22 shows the oldest faulting that occurs largely in San Onofre Breccia. These faults are seen only in the northwestern area.
- 2. 5I- 36 Amended: April 2009 TL: E048000
There are probably similar faults further to the south, but they were not: detected in the profiling. Where they are recorded, the San Onofre Breccia is shallow enough to have been picked up by the geophysical techniques used. Faults that occur in the older Monterey are seen in the next map (Fig. 23). These faults are best exposed in the central portion of the area where they are coincident with the development of the anticline and syncline pair. Faults of this age pick up again to the east in the NEKTON data to the south. Displacement an these faults is very difficult to determine because one does not see clear offsets of the reflectors or horizpns. Displacement is probably from a few meters to a few tens of meters. The next map (Fig. 24) shows faults that occur in the blue, upper Monterey unit. We see it only in the northerp fold area east of the HOZD where we see .V faults penetrat~ng to the I,1pper Monterey. . .These faults* do not cut the Capistrano formation and are therefore at least-four million years old. Our final map (Fig. 25) shows faults that extend to the sea floor or the Pleistocene unconformity. They are confined within the HOZD. To summarize once again, the seismic data does not reveal a seaward extension of theCristianitos fault beyond about six thousand feet. Faults east of the aOZD are of two types. They are either very old faults deep within the section that cut the San Onofre Breccia and do not extend very far up through the older Monterey section, or they are types of faults that result from deformation associated with folding. These appear to be interformational faults generated by the folding of the sediments. The seismic data does not show these faults extending aeep into the section nor to the Pleistocene unconformity and their apparent zonal distribution is a function of their association with the broad folds east of the HOZD. 2.51-37 Amended: April 2009 TL: E048000
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ENCLOSURE 3 A, B, C AND D FEATURES The purpose of this enclosure is to document the relationship between the A~ B, C~ and D features and the present tectonic framework for the San Onofre area. The A, B, C, and D features are minor non-tectonic features which were carefully mapped and analyzed as reported in "Analysis of Geological Features at the San Onofre Nuclear Generating Station", Fugro, Inc ** July, 1974 and "Final Report on Geologic features at the San Onofre Nuclear f:naneratin3 Station ll , Fugro~ Inc., August, 1976. The current, regional stress field at depth in the Southern California area is oriented with the maximum {N-S} and intermediate (E-W) stress axes lying in the horizontal plane while the minimum stress axis is 'J'ertical. This is supported by:
- 1. Local mechanisms determined for local events;
- 2. The regional uplift along the Peninsular Ranges and, locally, the Southern California Coast; and,
- 3. The regional north-south compzessdon and crustal shortening observed within the region south of the Transverse Ranges. Such an arrangement is characterized, in part, by vertical movement.
By contrast, the features described by Fugro (1974, 1976) display no vertical movement;< rather, only horizontal conjugate movement. Such movement is more consistent with both the maximum and minimum stress axes oriented horizontally While the intermediate axis is vertical. 2.51-51 Amended: April 2009 TL: E048000
These joints responded to local conditions such as unloading due to erosion, and configuration of the sandstone body and therefore have no regional significance. These features clearly pre-date the stage Se deposition which is at least 125,000 yrs. old. These features post-date the deposition of the Pliocene-age San Mateo formation. Therefore, these features are at least 125,000 years old and may be sold as several million years.
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2.51-52 Amended: April 2009 TL: E048000
ENCLOSURE 5 Trail Five Landslide San Onofre State Beach October 2, 1980 A landslide was reported by the California Division of Mines and Geology in a letter to the Nuclear Regulatory Commission, dated August 12, 1980 and signed by ~!r. James F. Davis, State Geologist California D1*"ision of Nines and Geology. The location described in the letter was inspected to determine the origin of the offset gravelbed exposed in the barranca and seen on the walls. Trail 5 is located about 1800 ft. south by Unit 1 containnent structure. The location of the inspection is shown on Figures 1 and 2. The feature described in the August 12 lett9r is about 120 ft. downstream of the stai~lays at Trail Five, San Onofre State Beach. The feature is seen on V the east barranca wall; exposed in the lower 15 ft.* of the approximately 75 ft. high cliffs. The sediments have been mapped by an SeE geologist as a unconsolidated, weakly cemented Quaternary non-marine deposits consisting of silty and clayey sand interspersed with lenticular gravel and c.obble beds. Surface run-off typically cuts deep, steeply sided barrancas's into these sediments. The canyon was inspected and a geologic profile drawn from observations and photographs taken at the location. The exposures disclosed a gravelbed within the Quaternary non-marine sediments that is down dropped along dip about 2 ft. The down dropyed block is about ~O ft. wide and extends from the barranca bottom up to about 14 ft. above the canyon floor.. Close inspection of the slide surface identified small plant rootlets growing along the surface and 2.51-53 Amended: April 2009 TL: E048000
ac.c.umulations of caliche which had precipitated on the sediments. The gravelbed can be recognized on the upstream side and can be traced beyond the '~ downdrop block to the downstream side. An illustration of the 'slide and gravelbed is shown in Figure 3. A relatively thin block of Quaternary soil slabbed off the barranca wall and a gravel bed within the slab was downdropped about 2 ft. down dip (18 inches vertically)
- The extent of this soil fall is limited to the "rock shown on Figure 3. It is concluded that the offset bed is a landslide. This landslide is due to undercutting by stream erosion and weakening of Quaternary deposits comprising the canyon walls.
2.51-54 Amended: April 2009 TL: E048000
c c ( LEGEND: 01, LANDSLIDE Ob 001 BEACH SAND ALLUVIUM QUATERNARY , { Oln NON- MARINE TERRACE OEPOSITS .r Tm MONTEREY FORMATION} MIOCENE Qol I Qln ~ 5 STATE BEA C H ONOfRE SAN
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CD C. ~ ~ N o o <0 --I r m o ./>. OJ o o SEPTEM8ER 1980 o FIGURE 3
Edited Transcript of Dr. Roy J. Shlemon \.J Quaternary History of the San Onofre 'Area Presentation to NRC/USGS - September 23, 1980 Menlo Park, California The purpose of this presentation is to relate the Cristianitos Fault to the Quaternary geology and geomorphology of the San Onofre area; particularly with reference to a now-dated terrace and sea level chronology, both onshore and offshore. This presentation has three major objectives: First, to briefly review the late Quaterna~y geologic and geomorphologic framework of the area. Second, to relate the late Quaternary geological history to tectonics of the San Onofre area, based mainly on marine terrace chronology, and compare this with coastal terrain elsewhere in southern California. And third, to note the probable ages of offshore terraces described by preceding speakers and illustrated in various profiles for the Cristianitos Fault area. With respect to the Quaternary geologic history of the San Onofre area, I call your attention to the now well-known marine isotope stage chronology useful to date coastal marine terraces and related deposits, independent of any radiometric dates that may be available. Shown on this viewgraph (Fig. 1), are relative changes of glacio-eustatic sea level over the last 1,000',000 years. Since publication of this paper, there have been some 2.51-58 Amended: April 2009 TL: E048000
n
§.
Fig. 6. Relative change In s,la level in Middl. and Latt Pleistocene time, based on oXYgen I,atop. composition of foraminifera in Q mid-Pacific core (C1fter Shackleton Qnd Opdyke_ J973.,.48). Leto Plolstocene boundary lrl}m Yl),9.n i.otop. sub,to;, 5. (CtJ.I30.000 yeon BP) to present\
~icidle Pleistocene from BrunnesiMatuyama magneric reversal (ca.
700,000 year. BP) to substaoe e*. -_ \...,t'-
, I llO,OOO 100.000 fiq. 1. Glacio-eustatic sia levil curve for the past 130,000 yean derived frem oXY96n Isotope m,asuremtnts in mid-Pacific cor. compared with dated terrace corals from Barbados (81, B1I,B~ Broecker. and others 1968) and Nt. Guinea (NGm, Veeh and Chappell,1970). Curve from Shacklaton and Opdyk. (1973, p. 45).
APPENDIX 1.S! FIGURE 1 2.51-59 Amended: April 2009 TL: E048000
refinements to the chronology. These changes, however, are minor, and essentially the broad framework indicated here remains the same. First, with respect to the upper diagram, the dark line indicates the Brunhes/Matuyama paleomagnetic boundary, approximately 700,000 years b.p. Relative high and low stands of sea level are indicated by the curves. The odd numbers refer to relative high stands of sea level~ for example, 3, 5, 7, 9, 11, etc., whereas, the even numbers refer to relative low stands of sea level (glacial-eustatic): e.g., 2, 4, 6, 13, etc. uf particular i~portance to the San Onofre area are marine isotope stages 5, 4, 3, and 2 (lower diagram). Isotope substage 5e, shown on both the upper diagram, and the enlarged lower diagram (Figure 1), is especially significant. It is part of stage 5 (~U,OOO - 125,000 years b.p.). During substage Se time, about 125,000 years ago, sea level appears to have been above the present, perhaps the only time during the last 700,000 years. The 5e shoreline, measured in tectonically stable places of the world, was on the order of about 6 to 10 m above present, and therefore, serves as a stratigraphic marker to compare uplift rates regionally. Isotope stage 4 (Fig. 1) is essentially equivalent to the early Wisconsinan of the classical midcontinental chronology, about 2.51-60 Amended: April 2009 TL: E048000
60,000 to 70,000 years ago. Isotope stage 3 is mid-Wisconsinan, about 35,000 to 4U,OOO years ago1 and substage Sa, is about 80,OOu years SP (Fig_ 1). All of isotope stage 5 is frequently termed "late Sangamonian." Isotope stage 2 is generally equivalent to the last major low stand of sea level (late Wisconsinan), a level about 100 m below the present. Sea level rose to its present elevation (Flandrian trangression) about 5,000 years ago. Of interest to the San Onofre area is isotope stage 5, especially sUbstage 5e, because onshore'terrace deposits of that age overlie the Cristianitos Fault. 'Isotope stages 3 and substage Sa are also of some interest, becaus~ suomarine pl~tfotms ot these ages now appear to have been located offshore. The onshore terrace chronology and Quaternary geology at San Onofre is presented in this viewgraph (Fig. 2), taken from a repor~ submitted a few years ago (Shlemon, 1978). In brief, locality No.1, is the first onshore terrace at San Onofre. The other numbers refer to marine terraces and respective shoreline-angle ~levations here indicated in feet. The highest terrace is about 1,250 feet. All these terraces, their cpntinental covering deposits, and shoreline-angle elevations, were mapped by Dr. Perry Ehlig (1977). 2.51-61 Amended: April 2009 TL: E048000
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to en APPENDIX 2.51 2.51-62 fI:GURE 2 Amended: April 2009 TL: E048000
Only the first marine terrace deposit and wave-cut platform at San Onofre is dated radiometrically. However, several dating methods corroborate the ages assigned. 'First, there is relative dating based on faunal associations. The fossils found in the first terrace deposits are of a warm water association (substage Se), describe by Kennedy and Lajoie (USGS, Menlo Park). Second, amino-acid dates are also available from comparable terraces south of San Onofre. Third, laterally continuous deposits have ceen dated by uranium-series methods (Richard Ku, Univ. Southern California). Fourth, the age of the first terrace'has also been determined by relative dating techniques. These include calculating averaging sedimentation rates, and determining the. age of buried paleosols within covering continental sediments. Kadiocarbon dates from the ban Onofre and adjacent areas likewise date the younger sediments. The age of the higher Sari Onofre terraces (Fig. 2) is based mainly on association with glacio-eustatic changes of sea level (Figure 1). As yet, there are no absolute dates for the higher terraces. However, by assuming that each terrace was cut by a trangressing sea, in turn superimposed on a tectonically rising block, it appears that the high surfaces can be dated as pertain-ing to isotope stages 7, 9, 11, etc; that is, in the order of acout 200,000, 360,000, 470,000 etc., years b.p. (Fig. 2). The 2.51-63 Amended: April 2009 TL: E048000
highest terraces are presumably more than 700,000 or 800,000 years old, and these ages are probably conservative for the following reasons: First, there are some gaps in the terrace sequences (Fig. 2). For example, about 1,000 feet above sea level there may have been a terrace, now since eroded (Fig. 2). Second, there is a major gap between the first and second terraces; and hence it appears probable that at least one and possibly even two shoreline-angles are here buried beneath some 100 feet or more of continental sediments (Fig. 2). It thus seems quite plausible that the ages assigned to each of these onshore sequences may be in fact one or two isotope ages too young. In sum, there are at least nine terraces at San Onofre, as noted on Figure 2, and there may be two or more additional platforms now either eroded or buried. The ages of these terraces range in age from the well-dated 125,000 year old, substage Se (first terrace) to well over 780,000 years and possibly older. The highest surfaces may be more than a million years old. The next question: "What is the significance of this chronology with respect to the relative tectonic stability of the San Onofre area?" Relative rates of uplift, for 15 to 20 km on either side of San Onofre, are calculated based on approximate elevations of the substage Se shoreline angle (Table 2) [There is no Table I, 2.51-64 Amended: April 2009 TL: E048000
APPENDIX 2.5! T.b1~ 2 Average Uplift late of Terrace 1 for the last 125,000 Years (Stage 5e level) Between Laguna Beach (North) and Target Canyon. Camp Pendleton (South) Measured or Projected Uplift Rate (em/lOaD years) Locality Shoreline Angle Elevation Original Shoreline Elevatio (ft) (m) +6 m +10 m rarget Canyon/Camp Pendleton 42 13.0 6 2 San Onofre South 57 17.7 9 6 San* Clemente State Beach 66-68 20.8 17 c South San Clemente State Beach 68-70 21.4 12 9 North San Clemente Pier South 97 30.1 19 16 San Clemente Pier North 83 25.7 16 13 North San Clemente #3 90 27.9 18 14 North San Clemente #2 97 30.1 19 16 North San Clemente #1 116 35.9 24 21 Capistrano Beach 100 31.0 20 17 l)~na Poi nt 125 *126 ';\0 1 v., ... ?f. ?;< Niguel Beach State Park 122 37.8
,'~ ~I.
!::l t.(.
South laguna 112-114 35.0 23 20 Aliso Beach 72-74 22.6 13 10 Laguna Beach Recreation 30 9.3 3 -1 Park
~ee text for descril'tions of easured locality and projection of grajient for
;horeline-angle elevation .
2.51-65 Amended: April 2009 TL: E048000
since these were selected from other reports.] Particular uplift rates are given for the Target Canyon area at Camp Pendleton, and for other specific localities northward to about Laguna Beach. Tne uplift rates, expressed in cm/I,OOO years, are shown for two assumed shoreline-angle elevations at 125,000 years b.p.; namely, at +6 and +10 m. There is a divergence of opinion as to the absolute elevation of sea level during substage Se. For convenience and comparison, however, it is assumed that sea level about 125,000 years ago was approximately +6 m. Thus, from Table 2, we observe the tilting of coastal terrain northward from San Onofre to at least Dana Point and probably farther northward to the. Laguna ae acb area. The upl ift ra te south of San Onofre
- .is approximately 6 cm/I,OOO yrsi at San Onofre Units 2 and 3, it is about 9 cm/I,OaO years; but these values increase to about 26 cm/l,UOO years at Dana Point (Table 2). In fact, as observed in the almost continuous sea cliffs north of San Onofre to Dana Point', the shoreline-angle elevations appear to be rising towards the San Joaquin Hills.
The uplift rates at San Onofre for the last 125,000 years take on particular meaning when compared wi th other southern Ca Lf f or n r.a localities. This is illustrated in Table 3. Here, from the literature, rates of uplift are expressed in cm/l,OOO years. Three uplift rates are given for the San Onofre-Dana Point area (Table 3); viz, 9 em and 26 cm/l,OOO years, respectively: values 2.5I-66 Amended: April 2009 TL: E048000
APPENDIX 2.51 Table 3 Comparison of Late Quaternary Uplift Rates Southern California Coast *
--~--~
Reference Area length of Record Approxima t.e Up 1i ft (Thousands of Years) Rdic (elll/lOOO VEtd rs ) Wehmiller et a1.. Ventura/Pitas Point 40-50 620 (197£:. p. 513) W~hmil1er et al ** Ventura/Pitas Point 2.5 640 (H08. p , !f3; Wehrni 11 er ct a1. I Ventura 80 200 (1978. p. 513) Wehmil1er at .al , t Santa Barbara. 30-50 140 (1977. tab1e 13) Goleta Wehmil1er et al .* Cayucos 135 13 (l9n. tabTe 13)
~eh~iller et al .* San Pedro (First 120-140 18 0;77. t~ble 13) Terrece )
0 Wehmi ll&r et a1" . Newpbrt eeach" (First 120-140 15 : (1977 t table TI) Terrace) Wehmill er et a1. t San Diego/Pt. Lorna 120 16 (1977. table IT) Wehflii11 er et a1.* San Diego/Pt. lama 70-90 23 (l977 t table 13) Dirkeland (1972 r~alibu Coast 105 30-45
- p. 441)
Bandy &Harin- Baldwin Hills. L.A. 36 500..800 covich (l973 Basin
- p. 65J)
Wooch/llrd & Narcus Rancho La Brea~ LA. 100 40..50 (1976. p. 128) Basin Ku &Kern (1974 San Diego Coast 120 11-14
- p. 1715) lern (1977 , 1563) San Di.ego Coast 120 16..2t (This Report) Dana Point 125 26 (Thi s R<<:lport) 5aa Cletlleftte 125 12-19 (This Report) san Onofre 125 9
- San Onoft'e-{lal1a PGi.t IIpl ift rates calculated fr'om sea level assumed at +6 m. Cu.
l?fi tVJ. . 2.51-67 Amended: April 2009 TL: E048000
useful for comparison with other published rates for the southern California coastal area (Table 3). In the Ventura area, for example, late Quaternary uplift rates are quite high, typical for the southern flanks of the Transverse Ranges. At Pitas Point (Table 3), amino-acid dating of terrace deposits shows an uplift rate of some 620 cm/l,OGO years; and for a Holocene terrace, the uplift rate is a calculated 640 cmll,OOO years (Table 3). These uplift rates decrease southward from the Transverse Ranges toward the Los Angeles Basin. Even here, however, a very high uplift rate has been reported; some 500 - bOU cmll,OOO in the Baldwin Hills (Table 3). This rate" however, is subject to some dispute, and has since been refuted by other .~ investigators. The revised uplift rate is now about 40-50 cmll,OOO years. But all these rates, when compared to those at ban Onofre, point to relative stability of the immediate San Onofre area for at least the last 125,000 years.
~ne next question: "Can we relate the onshore chronology to the offshore area at San Onofre?" This question is in part answered by reference to the diagram (Figure 3) which illustrates schematically the various onshore and offshore marine terraces "and platforms, The offshore geophysical profiles show that there are at least two -- and perhaps more -- offshore platforms comparable in extent and morphology to those onshore. In review, tne first onshore terrace, for comparison, is dated radiometri-2.51-68 Amended: April 2009 TL: E048000
'tto\
\
~.
\
APPENDIX 2.51 2.51-69 FIGURE 3 Amended: April 2009 TL: E048000
cally and by other techniques as pertaining to sUbstage Sei i.e., about 125,000 years old. The higher terraces are correspondingly older, dated by association to the marine isotope chronology. A more detailed schematic of the onshore and offshore geomorphic relationships is shown in this diagram (Figure 4), traced from Woodward-Clyde geophysical line 849. Superimposed on this drawing are two of the five new radiocarbon dates now available for sediments covering the offshore marine platforms. These dates were obtained by Woodward-Clyde from sediments immediately offshore of the Cristianitos Fault (Table labeled 2B-l). As indicated in this viewgraph (Figure 4), the hachured line indicat~s bedrock. Also indicated are three offshore lines *(by the symcol "X"). These particular shoreline angles can be identified not only on this geophysical line, but also on other Woodward-Clyde lines to the south over a distance of at least several kilometers. These platforms also appear on other geophysical profiles to the 'north toward Dana Point, and to the south toward Oceanside. The radiocarbon date of approximately 9,500 years, shown on this diagram (Figure 4), was taken from sediments some 148 feet below sea level. This date comes from younger cover indicated on the diagram by the symbol "YC." The designation "OC" indicates older cover, also overlying the bedrock platforms (Figure 4). Another radiocarbon date of about 8,500 years was obtained from sediments 2.51-70 Amended: April 2009 TL: E048000
APPENDIX 2.51 TABLB 28-1 SUMHAJlY or ME DATING JESULft Age Date in Years Core No. Sample No. DepUl ( ft) Material TIp! 8efore Present.- 1-1 2 16.4 Shell. .,510 ! 265 1-2 6 19.7 Shell. ,,09'5 .:!:. 335'" 1-3 14 23.4 Organic 9,400 .:!:. 300 1-3 1-4 15 22 25.*7 21.1 Shell. Organic S,065 + 11:10'** 11,355 .:!:. '50 1-5 28 30.6 Organic 13,160 .:!:. S50 1-5 31 38.5 Organic 12,270 .:!:. 340
.. These age dates are referencea to the year A.P. 1~SO * .... Thorough leaching not possible during pretreatment. du. t.o limited liz. of .ampl.~
\.J 2.51-71 Amended: April 2009 TL: E048000
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~ C-/4 DATES (+J DEPTHS FROM OCt fSU8MERGI?D wee ON AD.JACEN r t-xj
~cl sHORF..LINE:. L..
FUG/?O LINE" # S H 'U (-4tJ.()DO Y"'$. 8.P. !) o tM (-80,000 yr5. e.>>: 1)
~
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Further observable on this transparency (Figure 4) is the younger, dated fill, "graded" to the uppermost submarine platform. This platform corresponds almost exactly to where one would expect sea level to be about 5,000 years ago, based on world-wide sea level curves (Figure 1). In brief, the geophysical and radiocarbon dates indicate that offshore from San \ ...J 2.51-73 Amended: April 2009 TL: E048000
unofre there are at least two distinct platforms, each covered by two younger sedimentary fills and the youngest cover is definitely post-glacial in age. The offshore and onshore geomorphic features at San Onofre are summarized in Figure 5. Here the onshore terraces and their inferred ages (in thousands of years) are shown diagramatically. Specifically, the lowest onshore platform pertains to isotope stage 5e, dated radiometrically as about 125,00 years old. Terrace deposits of this platform continue unbroken over the Cristianitos Fault, clearly visible in *sea cliffs. Shown diagrammatically also are perhaps the first data available useful. to correlate the orishore and offshore ge6morphic chronology. Seen here are three submerged geomorphic platforms. Based on the geophysical data and the radiocarbon dates, the upper platform was apparently cut about 5,000 years ago when sea level first reached its approximate present position. The absolute ages of the two lower platforms are presently unknown. However, based on world-wide sea level curves, it is probable that these relate to isotope stages 3, about 35,000 to 40,000 years ago; and to SUbstage Sa, about 80,000 years ago. From late *Quaternary sea-level fluctuations, it is expected that such submarine shoreline angles and related platforms should exist. Similar features have been reported elsewhere along the southern California coast. At San Onofre, the two platforms are covered by two fills, the
- 2. 5I- 74 Amended: April 2009 TL: E048000
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APPENDIX 2.51 2.51- 75 f!GURE 5 Amended: April 2009 TL: E048000
youngest of which is dated by radiocarbon as post-glacial; that is, post stage 2, or younger than about 17,000 - 20,000 years. In conclusion, with respect to the late Quaternary geomorphic history in the San Onofre area, three generalized points can be made. First, onshore there exists a sequence of marine terraces (wave cut platforms) ranging in age from about 125,000 years to perhaps in excess of a million years. The marine isotope substabe 5e platform and related deposits, dated radiometrically, can be traced unbroken across the Cristianitos Fault. This particular platform is identified in almost continuous sea cliff exposures northward to Dana Point. Second, from the new geophysical data of offshore San Onofre there are at least two sedimentary fills covering submarine platforms. The youngest cover is dated by radiocarbon as pertaining to the Flandrian transgression (post-isotope stage 2). The radiocarbon dates range from about 13,000 to 8,000 years b.p. The absolute age of the underlying, or older cover, is yet unKnown. However, based on its stratigraphic position, it is older than isotope stage 2, and thus inferred to be older than about 17,000 to 20,000 years. Both of the offshore sedimentary covers are apparently not displaced by the Cristianitos Fault, as interpreted by the geophysicist.
\J 2.51-76 Amended: April 2009 TL: E048000
Third, and finally, the existence of platforms offshore of San Onofre is expectable based on world-wide, glacio-eustatic sea level changes. The absolute ages of these platforms is likewise unknown 1 however, from geomorphic position, and relationship to onshore terraces, they are likely associated with isotope stages 3 or Sa; that is, abot 40,000 and 80,000 years b.p. The surface upon which these platforms are cut is likewise not displaced along projections of the Cristianitos Fault. !n sum, therefore, both the onshore and offshore Quaternary sequences at San Onofre show that last displacement of the Cristianitos Fault probably tOOk place at least 125.,000 years ago, and possibly long before that. Rw:mpw 2.51-.77 Amended: April 2009 TL: E048000
ADDENDUM TO SUBMITTAL OF OCTOBER 6, 1980 During a presentation to the NRC staff in August, 1980, a discussion was presented concerning two onshore borings drilled to determine the amount of offset across the Cristianitos fault. Both of the borings were south-east of SONGS 2 and 3, on the alignment of E1 Camino Real. Boring 1 was drilled to a depth ofappraximately 557 feet where it was abandoned due to caving. The second boring was located 30 feet to the west along Camino Real and was drilled to a total depth of 749.5 feet. The results of the drilling were reported in "Summary Report on Basic Data from Two Onshore and Six Offshore Geologic Borings, SONGS Units 2 and 3, San Onofre, California", dated August 4, 1980. This report presents the boring logs, description of the drilling and location of the borings. Boring 2 will be discussed here because of the penetration through to the Cristianitos fault to San Onofre Breccia. The initial rock unit encounter~d was Pleistocene terrace sediments and gravel to a depth of 48 feet. From 48 feet to a depth of 444 feet~ San Mateo Sandstone was encountered. Monterey formation extended from a depth of 444 feet to 669 feet wht're the Cristianitos fault was crossed. Below 669 feet San Onofre Breccia was encountered to the bottom of the hole. 2.51-78 Amended: April 2009 TL: E048000
At the conclusion of the drilling program) a geologic profile was drawn between the 987 foot deep onsite boring drilled by Dames and Moore and these borings. See Plates 1 and 2, Enclosure 6. Measurement of the stratigraphic separation on this profile illustrates that there is an offset of approximately 550 feet between the base of the Monterey formation on the west side of the Cristianitos fault com-pared to the contac~ exposed in outcrop on the east side of the fault. The stratigraphic separation found in the boring supports the decrease in vertical separation along the strike of the Cristianitos fault. The maximum separation to the north decreases from about 4000 feet inland to about 50 feet vertical separat~on found in thes~ borings. 2.51-79 Amended: April 2009 TL: E048000
N EL CAMINO REAL RD. r VCRISTIANITOS FAULT S.O.N.G.S. UNIT I N INTERSTATE 5 DAMES a MOORE
\Jl
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00 o BORING I o .5 I P.tles I f I SAN ONOFRE NUCLEAR GENERATING STATION
~
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~
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) 2 2' 400' WOODWARD' CLYO E 200' DAMES a MOORE Bor.- t Bor.-1 80r.- 2
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[-5 [-5 \ / Ool/Oln __ SEA LEVEL 0 -b==--------=-- T"", T.m I I I I CRISTlANlTOS FAULT I I
-200' I Tsm !
I- -400' Tm
) -600' Tim
-800'
----1'
-1000' GEOLOGIC CROSS - SECTION 2 - 2' GEOLOGIC CROSS-SECTION SAN ONOFRE NUCLEAR GENERATING STATION UNITS 2 a 3
) AUGUST, 1980 PLATE 2 2.51-81 Amended: April 2009 TL: E048000
Woodward-Clyde Consuftants
SUMMARY
REPORT ON BASIC DATA FROM TWO ONSHORE AND SIX OFFSHORE GEOLOGIC BORINGS SONGS UNITS 2 AND 3 SAN ONOFRE, CALIFORNIA Prepared for: Southern California Edison Company p~ O. Box. 800 Rosemead, California 91770 2.51- 82 Amended: April 2009 TL: E048000
4000 West Chapman Avenue Post Office Box 1149 Woodward-Clyde Consultants Orange. California 92668 (714) 634-4440 Telex 68*3420 4 August 1980 Project No. 412991 Southern California Edison P.O. Box 800 Rosemead, California 91770 Attention: Mr. H. G. Hawkins Gentlemen:
SUBJECT:
SUMMARY
REPORT ON BASIC DATA FROM TWO ONSHORE AND SIX OFFSHORE GEOLOGIC BORINGS SONGS UNITS 2 AND 3 SAN ONOFRE, CALIFORNIA We have completed the drilling operations onshore (north of the Cristianitos fault) and the vibratory core borings to sample seafloor sediments offshore SONGS Units 2 and 3. These assignments were conducted under the direction of Messrs. H. G. Hawkins and J. L. McNey of Southern California Edison. This report provides a summary of field operations, drilling logs, and the results of age dating analyses. The data on onshore borings and offshore borings are presented in Sections 1 and 2, respectively. We hope that this summary report of basic data meets the project needs at this time. If you have any questions, please call at your convenience. very truly yours, .".---;" John A. Barneich George E. Brogan Associate Associate
.JAB:GEB/ea Attachments Consultmq Engineers. Geologists and Environmental Scientists Ottices in Other Prmcrpat Cities 2.51-83 Amended: April 2009 TL: E048000
Woodward.Clyde Consultants TABLE OF CONTENTS LE~TER OF TRANSMITTAL TABLE OF CONTENTS 1.0 ONSHORE BORINGS ......... 1 1.1 Introduction
- 1 1.2 project Organization and Staffing 1 1.3 Field Operations * *
- 1 1.4 Summary of Boring Logs * * * * . * * . 3 2.0 OFFSHORE BORINGS ............. 5 2.1 Introduction. 5 2.2 project Organization and Staffing 5 2.3 Field Operations * *
- 5 2.4 Summary of Cores.. * *.** 7 TABLE 1 - Summary of Vibratory Cores F'iGURE 1 - Site Plan APPENDIX l-A - Logs of Borings
.~PPENDIX I-a - Geophysical Log'S 7\PPENDIX l-C - Microfossil Age Dates APPENDIX 2-A - Vibratory Core Logs APPENDIX 2-B - Age Dating Results 2.51- 84 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants
SUMMARY
REPORT ON BASIC DATA FROM TWO ONSHORE AND SIX OFFSHORE GEOLOGIC BORINGS SONGS UNITS 2 AND 3 SAN ONOFRE, CALIFORNIA 1.0 ONSHORE BORINGS 1.1 Introduction Two onshore borings were drilled about 500 ft north of the Cristianitos fault at EI Camino Real Road. The locations of borings are shown on Figure 1. This program was conducted under the direction of Southern California Edison. Geologic interpretations are being made by Southern California Edison. The purpose of this report is to present the logs of borings and to provide a brief description of the operations. Additio~al operationa~ details are being kept on file by Woodward-Clyde Consultants. 1.2 Project Organization and Staffing The program was conducted under the direction of Messrs. H. G. Hawkins and J. L. McNey of Southern California Edison. Messrs. J. A. Barneich and O. S. Ghuman from Woodward-Clyde Consultants coordinated and supervised the effort. The drilling contractor for the onshore borings was Continen-tal Drilling-U.S. from Madera, California. Mud engineering and supplies were obtained from Baroid and the geophysica 1 logg. ng was done by Welenco from Bakers field, Cali fornia . The boring logs were kept by staff geologists. t.3 Field ~erations The onshore borings were drilled using a Longyear 44 dri 11 rig with HQ size drill pipe. The borings were advanced using \ .../ 2.51- 85 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants the rotary drilling method to depths at which coring was desired. Continuous wire line coring was then a t t emp t e-t using a 5 or 10 ft Longyear core barrel. Mud, as engineered by Baroid, was used as the cirCUlating fluid. Core diameter was 3-1!2-inches. Bo_rin~:.~ Boring 8-1 was started on 22 May 1980. The boring was located about 500 ft north of the projected trace of the Cristianitos fault at its intersection with El Camino Real Road. After drilling into the San Mateo formation, a 4-inch diameter casing was installed to a depth of 58 ft. Attempts to obtain cores of the San Mateo sand were generally unsuc-cess ful. I t was decided to attempt further coring in the siltstone of the Monterey formation. cores were obtained from 480 to 557 ft. When the boring had advanced to 557 ft, it was decided t o advance the casing to improve the drilling rate. During this 0peration about 100 ft of casing*dropped into the hole. Repeated att.empts to recover the casing were unsUCC!9SS fu l , and the b)ring was abandoned for later closure. Bori~B-2 Boring 8-2 is located about 30 ft south of Boring B-1 along El Camino Real Road. It was started on 5 June 1980. The horing was advanced rapidly to about 400 ft using a roller tricone bit~ and 4-inch-diameter casing was installed to 379 ft. Continuous wire line coring was done from about 483 to 750 ft. An attempt was made to remove the casing followins; completion of the hole, but only 15 ft of casing was re-trieved. 2.51-86 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants Geophysical logs were run in Boring B-2 after drilling was completed. The runs included an electrical log giving the spontaneous potential and resistivity and a radioactivity log providing gamma ray and neutron logs. After completion of the drilling and logging operations, the mud was weighted and the viscosity increased for closure, Both Borings 8-1 and B-2 were then capped with a 3-sack cemerrt e-s lurry plug. About 1 cu. yd. of slurry was placed in each boring. The logs of the borings are presented in Appendi x I-A and the geophysical logs in Appendix I-B. 1.4 Summary of Boring Logs The following is a summary of the stratigraphy obtained from the borings and a preliminary interpretation of the geophy-sical logs: o to 48 ft - Terrace Deposits - Sand. The colors range f'r om pale brown (5YR5/2) to yellowish brown (10YR5/4) to red brown (lOR5/4). The sand is fine to coarse grained, subrounded to well rounded, moderately to well sorted, with occasional tenses of clay and silt. Gravel and cobbles occur at the base of the "terrace d ep cs.Lt.s , The deposit is poorly to moderately consolidated. 48 to 428 ft - San Mateo Formation - Sandstone. The colors of the San Mateo formation sandstone in Boring B-1 from a depth of 48 ft to about 200 ft are shades of yellowish brown" ranging from dusky yellow (SY6/ 4) to pale yellowish brown (10YR6/2) to ~ark yellowish brown (lOYR4/2). Between depths of 200 ft and 432 ft, the colors are shades of olive gray, mostly light olive gray (SYRS/2). The San Mateo formation in Boring B-2, consists of sandstone having a color of mostly light olive gray {5YR5/2}. The texture of the San Mateo 2.51-87 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants formation consists of medium-to coarse-grained with some fine-grained sands. The sand grains are subangular to moderately well rounded. The formation is massive to thickly bedded, contains occa~ional pebbles and cobples, and is slightly silty and micaceous locally. The approximate mineralogical composition is: Quartz 85-90%, feldspar 5-7%, and other minerals 5%. The basal contact with the Monterey formation occurs abruptly where drilling becomes harder. 428. t~. 669 ft - Monterey Formation - Siltstone. The forma-tion is generally olive black (5Y2/l) in color, micaceous and contains highly fractured, slickensided and contorted areas. Bedding dip varies from horizontal to as much as 70 degrees and commonly includes thin 1/4-inch bluish gray beds. The siltstone is friable to well indurated with occasional sandy Lnc e r beds , Some sandy interbeds may contain volcanic ash. Core samples between depths of 485 ft and 654 ft were exam-ined for microfossils to estimate the age of the cores. The results of these analyses are presented in Appendix I-C. Foram inifera samples collected from depths of 485 ft to 495 ft yield an age of Lower Mohnian (upper Miocene). Foram ini fera s amp Las collected from 654 ft are from the Luisian age (upper Miocene). The base of the Monterey formation from 658 ft to 669 ft contains abundant blue schist fragments and appears to be reworked San Onofre Breccia. 669 to 749.5 ft - San Onofre Breccia. This formation con-sists of bluish gray sandy breccia (5B5/1), with moderate to well cemented clay and silt matrix. The clasts range in size from sand particl~s to 4-inch cobblesi larger clasts mostly consist of chlorite and glaucophane schist and smaller c Las es consist of quartzite and amphibole. The clasts are generally angular and are less weathered at increasing depths. 2.51-88 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants 2.0 OFFSHORE BORINGS 2.1 Introduction Vibratory cores were obtained at six selected locations offshore from San onofre, California. The core locations are shown on Figure 1. This program was conducted under the direction of Southern California Edison. Geologic interpre-tations are being made by Southern California Edison on the basis of the results of the vibratory coring work. The purpose of this report is to provide a brief description of the field operations, to present the vibratory core logs and the results of age dating analyses. Additional opera-tional details are being kept on file by Woodward-Clyde Consultants. 2.2 Project Organization and Staffing The program was conducted under the direction of Messrs. H G. Hawkins and J. L. McNey of Southern California Edison. Messrs. J. A. Barneich, O. S. Ghuman and K. Bhushan from Woodward-Clyde Consultants coordinated and supervised the effort. The vessel M/V Calcasieu belongi1Jg to Ocean Services, Inc. was mobilized in San Pedro for the vibratory' coring work. Oceanmasters International Inc. provided the vessel Ocean Command as the crew boat. Woodward-Clyde Consultants oper-ated the vibratory coring unit, logged the cores, and pro-vided the navigation. 2.3 Field OEerations The sampling unit consists of a seafloor-supported quadruped frame with a vibrator - drill pipe assembly. The vibrator is operated by air supplied from a shipboard compressor and is muunted on a 40-ft long drill pipe. The drill pipe consists 2.51-89 Amended: April 2009 TL: E048000
Woodward*Clyde Consultants of a standard 4-in. pipe with a cutting shoe and a sample retainer at the bottom. Samples are recovered in a removable 3-1/2-in. diameter plastic liner. The unit is also equipped for jetting in materials where full 40 ft penetration is not achieved in a single run. The water for jetting is supplied by a shipboard fire pump. Generally, a maximum of 40 ft of core can be recovered using this sampler. However, for the last run in boring 2-1 a 7-ft sampler extension was fitted and an attempt was made to penetrate as much as 47 ft. Electronic navigation was provided using a Motorola Mini-Ranger I I I positioning system. This is a short range ( 20 nautical miles) line-of-sight system. The basic Mini-Ranger consists of a range console, receiver-transmitter, and omni-directional antenna installed on the boat. TwO or three reference transponders are located at surveyed ground points. The measured ranges to the transponders
, . . ' . are
. directly dis-played in meters. The accuracy of the ranges is +3 meters at 20 nautical miles. The actual accuracy of the system is a function of the ranges and the angle of intersection of the two range lines. Conventional tri lateration techniques are used to reduce the data. For the sampling program, two transponder stations were located along the coastline.
The boat was *maneuvered using reference anchor locations that were calculated based on known anchor cable lengths. A three-point mooring system was used to maintain position. The vibratory coring assembly was carried horizontally suspended alongside the boat from two A-frames. After anchoring the boat on location, the bottom end of the corer was released so that the coring assembly was suspended ver-tically from the A-frame. The corer was lowered to the sea-floor using a 20-ton capacity hoist. The air hoses connected to the vibrator were lowered along with the corer. After the 2.51-90 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants
~orer was seated on the seafloor, the air compressor was started to begin the coring. The penetration rate was recorded on a strip chart recorder. The air supply to the vibrator was stopped when no further penetration occurred.
The core barrel was pulled out of the seafloor and the coring unit was retrieved. The bottom end of the coring unit was pulled with an air tugger to bring the unit into a horizontal position, and to remove the liner. The liner was cut at the point where the core stopped and the length of the core was measured and recorded. The recovered core (inside the liner) was then cut into convenient lengths (3 to 4 ft) ~ logged by a geologist; capped and sealed at both ends; marked and stored. In all cases, full penetration to the desired depth could not be achieved on the first run. For each succeeding run, the liner, cutting shoe and sample retainer were reassembled, the coring unit was lowered to the seafloor, and the core barrel was advanced by jetting to a depth close to the bot~om of the penetration aChieved in the preceding run. After jetting to the desired depth, the vibratory coring operation was carried out as described previously. The number of runs at each site ranged between 2 and 5 and the maximum penetration achieved ranged between 25.5 and 44.1 ft. A total of six sites were sampled, five on Line No.1, and one on Line No.2. Lines 1 and 2 refer to geophysical lines run by Fugro (Line l) and Woodward-Clyde Consultants (Line 2). The location of the sites are shown on Figure 1. A summary of the vibratory coring operation is given on Table 1. 2.4 Summary of Cores The six offshore borings, advanced utilizing the vibratory coring unit, penetrated to depths ranging from 25.5 to 44.1 2.5I-91 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants ft:.. In these intervals the materials encountered were in;~inly sa nds and si.lty sands with two of the cores (1-1 and 1-3) contai.ning zones of clay and clayey silt. The sandy sections of the cores were mainly fine grained, dark greenish gray in color, and contained variable amounts 'of silt. Cores 1-1, 1-2, 1-4 and 2-1 contained intervals of coarser grained sands ranging from fine to coarse grained and having a yellow gray to olive gray color. The clayey intervals recovered in the cores were greenish black in color, and were found to be from 22.4 to 24.0 ft in Core 1-1, and froln approximately 38.0 ft to the bottom (at 39.5 ft) in Core 1-3. Fossils and other organic debris, such as wood and carbona-ceous fragments, were ~lso encountered in the cores. All of .,0 the cores contained random shells and shell fragments, and all of the cores, except 2-1, had' small horizons that were rich enough in organic debris to collect.samples for age dating. These organic rich horizons were mainly encountered from 0 to 25 ft, with the exception of Core 1-5 which had an abundance 0 f organically rich material as deep as 38.5 ft. Detailed logs of the cores are presented in Appendix 2-A. Age dates obtained from the analysis of organic materials and shells are presented in Appendix 2-B. 2.51-92 Amended: April 2009 TL: E048000
Woodward-Clyde Consultants TABLE 1
SUMMARY
OF VIBRATORY CORING PENETRATION BELOW SEAFLOOR, FEET RECOVERY, APPROXIMATE CORE NO. RUN NO. FROM TO FEET WATER DEPTH, FEET 1-1 1 0 7.0 6.0 72 2 5.0 25.5 20.1 72 1-2 1 0 .22.4 22.4 100 2 21.0 34.8 11. 3 100 3 32.0 39.5 6.5 100 1-3 1 0 22.4 24.4 125 2 19.0 24.0 8.0 125 3 25.0 30.8 9.2 125 \..../. , 4 31.0 39.5 8.5 125 1-4 1 0 20.0 22.0 165 2 16.0 23.0 9.0 165 3 22.0 31. 0 4.0 165 4 31.0 39.5 10.0 165 1-5 1 0 21. 5 21.5 200 2 21.0 32.0 11.0 200 3 31.0 35.8 5.0 200 4 36.0 39.5 3.0 200 2--1 1 0 18.0 20.0 165 2 19.5 30.0 11.0 165 3 30.0 34.5 5.5 165 4 35.0 39.3 4.5 165 5 40.0 44.1 4.0 165 2 *.$1-93 Amended: April 2009 TL: E048000
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APPENDIX l-A LOGS OF BORINGS - 2.51-95 Amended: April 2009 TL: E048000
412991 B-1 Project No. Field Log of Boring No. Sheet of .2L BORING LOCATION El Camino Real, East Side ELEVATION AND DATUM El. 145 (approx.) DRILLING AGENCY continental Drilling DRILLER DATE STARTel:'5/22/~nlUP. I c I"INl5HED / ! 80 6 2 DRILLING EQUIPMENT Longyear 44 COMPLETION DcI' I ~57' MVI,,;r;. DEPTH SIZE AND TVPE OF CASING 4" Sta.r'rlard OF S~~PU:S: DIST. I UNDIST. ICOR~
- HO Drill piPe with wireline coring 1:~Ut~ I FIRST I COMPL. :24 HRS.
Lon", ear HO i LENGTH 5' COR~ BAIlR'vEL and 10' BIT LOGGED BY: CHECKED BY; N/A N/ A N/l., J. Glcmb O. S. Ghun.o.n J:- o..W ROCK CORE o o. ,; WW DESCRIPTION Z 0 a!!:. Sketch
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aex: a:: SAND, mcderate yellOil'ish broNn, lOYR5/4, coarse grained, 1 !- well sorted. SM 2
- 1I becares more dense.
sl sane gravel to I" diameter. 6 ... cobbles and gravel sand beccmes mediun to coazse grained. 7-r 8 r no gravel, color change to pale yellOil'ish bt'l::'.\7n, lOYR6/2. 9 CJ...Ki:, very san::iy, dark yellCMish bt'l::'.\7n, lOYR4/2, mediun grained, sane gravel, 3-4" thick clay. CL I SAND, reddish brown, lORS/4, mediun to coarse grained, with occasional gravel 1/4-1/2" in diameter, dense. SP less dense. 15 16 Woodward*CI~Amended: ConSUllants ~~ April':ZO()9 TI': E048000
Field Log of Boring No. B-1 Sheet 2 of -l2.- ROCK CORE DESCRIPTION Sketch SAND, pale yello....i sh bravn, lOYR6!2, mediun to coarse grained with sore fines. 8M becanes more dense yellowish bro.vn, lOYR5/4, fine to mediun grained, m:Xler-ately well rounded, well sorted. grades to grayish oranqe, lOYR7/4. less dense moderate yellowish brown, lOYRS/4, grades to medium grained. 34 2.51-97 ~:::......' //CAt. Woo d ward . C Iy~ ,-onsuftants 'IRS' Amended: April 2009 TL: E0481J00
4J2991 Field Log of Boring No. B-1
- I:-
l-l-Q.W wW DESCRIPTION ~,;. 0 01:; Sketch c 8.= a a::,,'" a:: a:: SAND, mcrlerate yello,..,rish brown, lOYRS/4, fine and reedi.tm graine:i, well rounded, well sorted, bright }lellON' grains ccmprise about 5%. SP 37 38 -p. 39 40 41 42 gravel about 3" in diameter. 43 I-cobble layer nedium graine:i, mcx1erate yellON'ish bro..-n'l, lOYRS!4, roomed 46 quartz grains carprise 50-70%. 47 - L/SANDS'IDNE 1 48 (San Mateo Fomation), IOOderate yellON'ish brr.:::7Nn, IOYRS!4, coarse grained, well sorted, subangular, datX ar:d colored grains 85% quartz. SP 149 cuttings are darker in color, probably due to ~-up i J cobbles, dark gray cobble chips, imJUlar, canprise 3()-40%. Iso *t-. t 51 ~ 52 - 53 - grades to rnecri.im grain size. 2.5I-98 I .. Woodward*Clyde Consultants 'J!J7 Amended: April 2009 TL: E048000
Project No. Field Log at Boring No. Sheet'" of J" ROCK CORE
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l-l- o ll.Ul UlUl DESCRIPTION z ~ . c o!!: Skelch ~.:: 0 J. c a: a: SANDSI'ONE (San Mate::> lonnation), par~ yldIlCMish orungt', lOYR8!6, rnediun to coarse grained, 55 well sorted, quartz 85% sub-rounded, dark gray grains 10% subangular to sub-rcurded, others 5% sub-angular. sp drilling 610.-:, formation very dense. 56* grades to mediun grained, sane angular grains. 57 58 59 60 - 61 62 63-64 - 65 66 67 very uniform coring. 68 72 ~73 2' 51-99 . irA Woodward-Clyde Consultants ~ Amended: April 2009 TL: E048000
Field Log of Boring No. B-1 ROCK CORE DESCRIPTION SANDSTONE, pale yellONish brown, lOYR6!12, rnediun grained, very dense, well sorted, quartz 85% sub-ramded to rounded, 74 dark gray grains 10% subangular to sub-ramde:i, others 5%. SP 75-76-'r-- 77 78 I 79 i I 80 81 82-83 841-85 ... 86 i 87- I-88 I-89! 90+ 91t 92 :t
" * .:>.I.-'IUU lAo Woodward*C1yde '~suttants \llI!P" Amended: April 2009 TL: E048000
4J:l':J';;l} Field Log of Boring No 0-1
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ll.W ROCK CORE W W DESCRIPTION ~ ~ . 0 0::: Sketch " ~.::: 0 Ii a: a: SANDSTONE, pale yella....i sh bI'Otm, lOYR6/2, mediun to coa.rse grained. well screed, quartz 85-90% sub-roonded, dark 93 ,.. minerals 10% subangu1ar. SP 94 95-1 96 Jt 97 99+ 100 101 102 ~~
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Project No. ,,*1.1.'1':'.1 Field Log of Boring No. 3-1 Sheet-Lof~ ROCK CORE
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WW DESCRIPTION 2 ~ , 0 a!: Sketch e "':: a a: a::
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SANDSTONE, pale yellOflish broNn, lOYR6/2, mediun grained, 112 well sorted, dense, quartz 85% sub-roonded to roomed, dark gray grains 10% subangu1ar to sub-roundai, others 5% sub-rounded to subangular. Sane silt present. SP 113-0:> ::': 115 .
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118 SANDSTONE, grayish orange, 10YR7/4, coarse to medium grained, well sorted, massive crumbly, occasional 1/4-1/2" 119-- pebbles, dense, 85% sub-rounded quartz , 15% sub-rourrled r-others. SP 120, ' , cI{)
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t*:,,?, 129 130 2.51-102 Woodward*Clyde Const:.t~n~~ , IA lQI'.' Amended: April 2009 TL: E048000
Project No Field Log of Boring No. B-1 Sheet ~~ of jU
- c- I ROCK CORE I
1 ~~ I~=I 8 o.W w LU DESCRIPTION C!!:. Sketch i 'ex; ex; SANDSTONE, silty, moderate yellowish brown, lOYRS!4, mediun to fine grained, predaninately sub-rourrled quartz .:.: grains. sw SANDSTONE, silty, dusky yellow, 5Y6/4, fine grained, massive, subangular (gritty feel). sw t ,
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150-gravel layer 2" thick, 1/2-1 1l diameter, rounded, SANDSTONE, dark: yellcwish br(),tlIl, lOYR4/2, coarse grained, 151 gravelly, sUbangular to sub-rounded quartz (60%) and feldspar (25%). 152 153 154 155 156-~ 157 158 159 I-160 I-161 ... - 162-- 163-~ 164 .... 165-167 ,;; 16B ~,.,;} . 2.5I-104 t'l'.A Woodward-Clyde Consurtantc "::~.* Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No B-1 Sheet 10 of-L...
- 1:- ROCK CORE J-J-ll.W W W DESCRIPTION cl:. Sketch SANDSroNE, dusky yellcw, 5Y6/4, rred:iun to fine grained, subangular to sub-roonded quartz (65%) wi th occasional ..~
169 rounded gravel (1/2"-2" diameter). SJ? .. (jiJ
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.() ..-t CLAY, sandy layer, light olive brown, 5YS/6, with rounded pebbles. --:0*.
172 173 174 175 176 V 177-178-179 ~ 180 181 -~ 182- ~ 183- ~ 184 185 ~ 186 ~ 187 t
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Project No. 412991 Field Log of Boring No. P-l i Sheet-lL of ':l~_. DESCRIPTION Sketch SANDSTONE (San Mateo Fomation), dusky yellcw, 5Y6/4, medilUll grained, quartz 95!i> sUb-rounded, others 5% 188- sub-rounded I occasional gravel. SP 169-1-- 190 ... 191 192 193 194 I-- 195 -
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196 197 198**: gravel 3/4"-1" diameter. 199 i-200 I-- 201 202 I-203-204 i-
-I-205 I-206 2.51-106 1£....
Woodward.Clyde Consuftants . , Amended: April 2009 TL: E048000
412991 Project No. Field Log of Boring No. B-1 Sheet...L of .....i:2...
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ROCK CORE
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8 Q..U.l WW DESCRIPTION o!: Sketch c ~.:: Ii cr; a: SANDS'roNE, light olive gray, 5YS!2, fine grained, slightly silty, gritty, with occassional (O-S%) very coarse sand 207-~ and pebbles, massive, friable. SP 208 209 210-211* 212 213 214 215-216 217 Thin hard layer. 218 219 1220-221 >- 222 I 223 f-1'---\'---+--+---+ ,_. 224-225 2.51-107
Project No. 412991 Field Log of Boring No. B-J Sheet 13 of 30
- 1:- ROCK CORE W
- a. W DESCRIPTION W
c~ Sketch 226-hard layer SANDSTONE, mediun light gray, N6, mediun to fine grained, 227- silty, very dense, sub-rounded quartz (85%) with small (1 nm) blebs of silt am 2-5% biotite flakes. SIN 228-229 '" 230 I-231* 232 I 233 I I 234 +
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+(Y) alternating 6" hard layers with 12-18" softer layers 235 r-SANDS.TONE, dark gray, N3 , fine to coarse grained wi th sandy SILT ( 40%). SW 236 237 I-238-
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+/- :7""
239 I-CLAY, sandy, dark gray, N3, fine to medium grained 240 ~ (scraped fran core barrel tip). CL 241-242 I-243-- 244
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Woodward*Clyde eol1sult;tnts ,- . Amended: April 2009 TL: E048000
412991 Field Log of Boring No B-1
- x:-
l-l-Q.W
..u UJ DESCRIPTION o~
245 246-248 SANDSTONE, light olive gray, 5Y5!2, silty, with trace of clay, fine-grained, sane iron oxide stains. SW 249 250 251 t :(
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-j-SANDSTONE (San Mateo Fonnation), yello,.;ish gray, 5Y7/2, medium graine:i, sub-rounded to subangular, quartz 95%
other dark minerals 5%, sub-rounded, SP 25E :- 2S7 \258- r-259 ,... 260 261 t;- 262-263
412991 8-1 Project No. Field Log of Bonng No. Sheet--lL of 2L
- r- ROCK CORE 1 (l.W W W DESCRIPTION Sketch
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rE a: a: 1/ 264- I-SANDSTONE, yell"",ish gray, 5Y7/2, mediun grained, sub-265 angular to sub-roonded. Quartz 95%, other dark minerals - :~ f;- 5% subangular. SP 266-t-- - ~{? iX}
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273 SANDSTONE (San Ma.teo Formation), dusky yellav, 5Y6/4, very
?F dense, poorly sortErl, with gravel to 1/4", quartz 85% r-subrounded, feldspars 10% 'sub=-roUndErl, other 5% angular M i)::*
274 to sub-rc>unded, trace of clay. SiN '",
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I'" 282
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Woodward-Clyde Consuttants .... Amended: April 2009 TL: E048000
Field Log of Boring No. H-l Sheet..l.L of..12.- ROCK CORE ci DESCRIPTION :z o,; . 0 Sketch C .,-
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SANDS'l:'Q';IE (San Mate:> Fonnation), yellc::wish gray, 5'£1/2, T. .
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M medilln to fine graine1 90% quartz sub-rounded, SP
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Project No. Field Log of Boring No. H-1 Sheet..1L of ~
- x:-
t-t-ROCK CORE o..W o W W oeSCRIPTION c a!:!:. Sketch Z o a:: SANDSTONE (San Mateo Formation) t mediun light gray, N61/2, fine to medium graine:l t sane 1/4" gravel, gravel sub-302 rounded, massive no bedding 90% quartz sub-rounded, feldspars 5% sub-rounded, dark minerals 5% subangular to sub-rounded, SP 303 304- . 305 306 307 30B 309 310 311 312 313 314 15 ,316 317 318 319 3~Q_l- _
***--*-----*-r.51-112 Woodward*Clyde Consultants ~
Amended: April 2009 TL: E048000
Project No. 412991 B-1 Field Log of Boring No. Sheet..liL of -19.....
- c-l-l-ROCK CORE Q.W WW DESCRIPTION o!!:.
'0 SAtIDSTONE (san MatEO Fbnration), light olive gray 5YS/2, fine to medium graine:i, sane 1/4 11 diameter gravel, sub-321,. rounded, massive no bedding quartz 85% sub-rounded, feldspars 10% sub-rounded, others 5% sub-rounded. SP 322-- - 323 324 325 326 327 f.. 328+' I j I 329- it' 330 331 332 - 333 334-- 335 i-336-337 SANDS'ID~'E, light olive gray, 5Y5/2, fine to medium grainoo, predaninately subangular to sub-rounded quartz, massive 338-slightly silty. SF - 339 11'... Woodward*Clyde Cortsulta"t~ 'ZlV Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. 8-1 ISheet 1<) of.2L
- 1:-
o..W ROCK CORE W W DESCRIPTION ell: Sketch SM'OOl'ONE (San Mateo Fotrnation), light olive gray, SYS/2, rnediun to carse grained, sub-rounded, quartz 80%, feld-340 r- spars 10%, dark minerals 10%. SW 341 -- 342+
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343* 345 II 346
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347 - .I +, iI I 348 . I 349 350 f-351 - 1352 l-I
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'355 I-356 ...
357 ... 358 Woodward.Clyde Consultants ....
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Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. .__ Sheet~ of 22.-
- c- ROCK CORE l-t- ci a.. W UJW DESCRIPTION Z C c.!:!:: Sketch .;:: ~
§A."lDSTONE, light olive gray, 5YS/2, medi.un grained, sub-59 rounded, quartz 80%, feldspc.rs 10% dark minerals 10%.
SF 364 hard layer enc:ountered only a fe.w inches thick. 365 366+ 1 3671" 368 369 370 371- 0 l{) 372 ...-i
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~
374 376* . 377 2.51-115 'Woodward.Cryde Consu!tar:ts ~:t LA Amended: April 2009 TL: E048000
Proiect No. 412991 Field log of Boring No. n-1 Sheet2L of -L ROCK CORE
- 1:-
W a.. W w OeSCRIPTION ~,; 0 o!:!: Sketch c ~~ 0
£ a: a:
SANDSTONE, light olive gray, SYS!2, medium to coarse grained, sub-rcunded, quartz (70%), feldspars (15%) and 378 dark minerals (15%), massive. SP l 379~ 380-- t 381 '" 382 383 384 - 385 386-387 i-388 389 i-t
-r I
390- I-391- I-392- l-I hard layer 393- l-394 - hard layer . dark minerals make up noticeably greater percentage (20%). 395! 396 2.5I-116 /I£~ Woodward. Clyde Consultants 'QIl" Amended: April 2009 TL: E048000
412991 B-1 Project No. Field Log of Boring No. JSheet-lL of ~ ROCK CORE i=t: ~ (l.w WW DESCRIPTION i ci Z ,; o ' C c~ Sketch c v- .,- aee
£ a::
j,i Q t 397- -., f}/. 398 t 399 I V\
;?::-
400 i.:,.. .
- ..;~:
401 \} f I 1tl ~ ; ~ I 402 i II II Ij 403 !
+/-
I i II I 404 f..
.t- I:::V)~
405-i-t+ I~,;i ;
'?:"; I I
I ,. 1 ; I 406 tt ::::;-.
~:jc, I I ,
407- l-t -r-i
-i-
.<~~
408 .... t
.L ":" .
J.
.L ~}
409 !- SANDSTONE, light olive gray, 5YS/2, sub-rounded to suban-
.~
-i- <: I gular, mediun grained, quartz (80%), feldspar (l0%), and T ;:;'
T
>>r 410-I- dark grains (10% ), occasional coarse grains to 1/4 II
- SP .L .:::
("') :::{.: ftrl 411- I-hard layer -t>i
-~
~~ /:
.- :;, t(")
tv? ::\:i ~
~
412-t~ ,I'; T 413 f-
+r ;,?:.':
\......." 414 I-
--- \:;
- :\)
415
- 2.51-117
Project No. Sheet..L.:.:..- of ..l2.- Field Log of Boring No. jj-l ROCK CORE DESCRIPTION ~,: 0 Sketch c: 8..; 0
",'" ex:
~ ex:
~16 418 f.o 419 SANDSTONE, mediun gray # N5 # mediun grained, quartz 75% sub-rounded,: fe1dsp9.r 10% sub-rounded, dark minerals 15% 420 sub-rounded to sl.iba..o3ular. SP 421 422 423 424 425+ 426 I-427 ... 428-1429-~ 430+ r 431-432 I-433 434
~.5I-110 _At.
Woodward*CIyde Consultants ..... Amended: April 2009 TL: E048000
p rojec
. t No . 412991 F'Ie ld L og 0f BOr!'ng No. B-1 Sheet _ 2t10 f 30
- t- ROCK CORE 1 w o ,,;
o ' c ti. UJW DESCRIPTION 2: Cl~ Sketch e <.>~ 0 a: a: a: j'}
\.0 UI 435-r- f-C",':
SANDS'I'OJ.W;, medi.un gray, N5, medi.im grained, quartz 75% ,- sub-rounded, felds}:lars 10%, dark minerals 15-20% sub- Z \ii angular to sub-ra,urled. w -: 436- -f-...::l t-- oct
~
~
437-r- -f-~
;:/.
438 ':c'
~.:
439 t-- 440 -'"~ [ sw 441 ..J
~ Xx U'J j:,:
442
~ }0
, '\"."./ 443 - cc "f 444 Harder drill.irg, color of drilling mud changed to olive gray. -- i---=- 445 - t- ..;::--; SILTSl'ONE , dark gray, NJ, with fine grained micaceous sam. ML 446 - .:-:=- _:... II 447 -f- -~-
-,- I 448- ~ .1-- :"-- .
f'; i:
~-..:
449 t-f-_-_ r:..- 450 l-f- sz; I-'-- f,-_.o:: oct a-. 451 t- -f- 1--:-
~-:..-
1--
\ ..../
452 t-easier drilling. -I-l-- -- j-.:=:-"";' 453
~--=
f-,-- 2.51-119 Woodward*Clyde c..cm..wtfants ~ Amended: April 2009 TL: E048000
Field Log of Boring No. B-1 Sheet~of~ ROCK CORE.
- x::-
.... 1-o.W UJW DESCRIPTION ol!:: Sketch 454-SILTS'roNE, olive gray, 5Y4!1, parallel horizontally bedded 1/2 thick, with very thin lenses of fine grained sand, 455- micaceous. No visible joints or fractures., little or -I- ---l no weathering, lew :permeability. ML -,0
--'11)
-~
456-~ - i--- 1-- 1--- 457 1-- 1-- 1-- 1-_- 458 I-459 -I-460 Light weathering, and lightly jointed generally at 50". 461 462-463
.:(
C
~ CJ 464 ~f':. N II) 8(j)
-,.. ~
0::. 465 .; ~
~
466- -l-
~./ (
I- .:.:.,:;
- ~'.:
-I-~':;~
468 ~ C f.:s Q) k69-M Ii') 8 Q) _... ~ ~.:; ,:.,
~
470-- C z
~ .\,
471 --
~\,
472 Sample yields age of Lower M::>hniGD .(:upper Miocene) 2.5I-120 Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-1 Sheet 26 of 30
- 1:- ROCK CORE 1 ... w d wW OESCRIPTION z ~ . 0 o!:!:: Sketch e ~~ a
£. a:: a:
473-474 475*1-476 477 478 I-SILT~, grayish olive, lOY4!2, parallel horizontally bedded 1 1/2" thick with very thin lenses of fine grained 479 sand, micaceous. Sane 3/4-1" gravel sub-rounded, slick-ensides, mJderately weathered, and fractured, no visible joints, 1C'M penneability* Forarns and fish scales. 480t ~ <jt> .\.......1 ~iV1 "'1 In 0 4811-
\.C'
~
I.-- 482 ,.. . l.?¥-
~
48'> I-
-==-
~
484
- \.C rji'J M
If) M 485 Sample yields age of Lower Mohnian (Upper Miocene). -i-SANDSTONE, olive gray, 5Y4!1, cross bedded, fine graine:i t? well canented, vert well indurated. Jointed at 30" and ~ 486- - 85", mcderately fractured. SP ~ ~ I r-=-
~
.. SILTSTONE, olive black, 5Y2!I, parallel horizontally i-=--
bedded 172" to 'I 1/2 II thick, micaceous with mineral specs 487 '- possibly gypsum. ML - I--- r:-=-- 488 §....;... V1 rji'J L"- a
...c
~
489 '- highly weathered, highly fractured. -- ~
'190- -I-1IfC..
Woodward*Clyde Consultnnts ~ Amended: April 2009 TL: E048000
Field Log of Boring No B-1 Sheet :: I 01 3' 1 ROCK CORE DESCRIPTION Sketch SIIJI'S'roNI;, oli Vt:! black, 5Y2/1 , parallel beiding ranging 492 frOIl horizontal to 35°, 1/2" thick with very thin inter-r- bedding of fine grained sand, has bluish gray 1/4" thick beds. HL Sanples taken at 493.5' and 495 t yield age of Lower f'I.ohnian (Upper Miocene). 49*H.. Highly weathered, m:xlerately fractured, joints vertical to 45° 495 . viell indurated, no fracturing, joints at 30°, 1/4" bluish gray oede are irregularly laid. SILTSl'ONE, olive black, SY2/1, fissile to mex:'ierately frac-turoo, fractures generally parallel to beckling but also highly angled oblique to bedding, siltstone poorly in-durated, irregularly bedded with medium bluish gray micaceous clay, bedd.in:J horizontal to 30°, at 500' beds highly contorted suggesting slumping, clay beds 1/16" to 1/2" thick. Generally in unifonn lenticular shape rot mi nor oblate pods also. ML 507 SILTSTONE, olive black, 5Y2/1, moderately fractured, fractures generally parallel to bedding, becanin:] rrore SOB indurated brittle with lenticular white sand size grains of a micaceous material, also inclusions to 1/2 11 diameter sub-ercunded , tan, fine grained sandstone, interbedded with 50')r- i~'regular spaced lenses of bluish gray micaceous silt-s t.one , bedding dips 15-30" I lenses to 1/4 11 thick. ML 510 2.51-122 irA Woodward.Clyde Consultants .., Amended: April 2009 TL: E048000
Project No. Field Log of Boring No B-1 Sheet_2_ ! _ of _ _ ROCK CORE DESCRIPTION Sketch
-s e-;
'~
Sll .1- I'S .-j 1.0
~
t't::=: S12*i-- f'::< SILTS'IDNE, olive black, SY2/1, with irregular spaced lenses 51 ] and irregular shaped pods of bluish gray micaceous silt-stone. ML ~ I~
~ N
~
514 ~ r.....: 515 c
~
fu N' SIt) '.6 c o, 0 517 SILTSTONE, olive blad~ t SY2/1 with irregular spaced beds f-- 1 of bluish gray micaceous ai.l.t.st.one, bedd.i.n9 10-30°, lenses ~ - 1/8"-1/4" thick, at 518.5' many lenses offset 1/8" along I:::::: I, 518 \ high angle fractures (50-65°). !>IL ==:;" '\.-.I ~ ""t
>.0 ""...,
C 519 I--- 2= c::-- 520 ~ SILTSTOl\1E t interbedded olive black, 5Y2/1 t and bluish gray t micaceous siltstone, highly contorted bedding with minor offset of beds, canpaction or slumping of soft sediments 521 causing pinching out and irregular structures within I-I~ bedding. ML
~
rJf' I!'. 522 l- -l-
~
Lf\ N I I I 523- -- 524- - SILTSTONEt fragmentst olive black, 5Y2/1, disoriented siltstone fragments within matrix of bluish gray micaceous 525 I-silty clay, one siltstone fragment contains imprint of fossil of unknosn affinity. ML I- ~
~ '.0
<1C 526 - .o I"- .....
5""
",I -I-528-SIL'1'STO~'§., olive black, 5Yl/2, very brittle to rooderately indurated, disoriente:1, fractures generally parallel to -I-1&00 beddi.nq , dips horizontal to 20°, siltstone rrore indurated ~d l"-
c:iC e
~
l::clOd 529', irregularly spaced bluish gray lenses 1/16-1/8" ~ I"- 520 thick. ML 0", : . Z.51-123 iC.A Woodward*Clyde Consultants 'lfIjj;i'il" Amended: April 2009 TL: E048000
Project No. Field Log of Boring No. B-1 Sheet 29 of 2.:..- r- ROCK CORE
. - aa: !-!- d .,;
o.W WW DESCRIPTION z o . 0 o!: Sketch e ... z a: ex: J 530 I-
~
df) I'- C
~ -o I'-
531+ ~ """- I-
~
532~ ~ SILTSTONE, brownish black, 5YR2/l, bedding generally -z parallel ranging fran horizontal to 40°, fracture paraIlel ~
?
533- to 'beddiIl3 planes, bedding 1/2-2" thick, sane vertical z joints visible, bluish gray beds 1/8-1/4" thick, highly ? I fractured and weathered at 532-534 I, more indurated belcw 534'. ML 7 2 I 1% a:. cc (jl.. 535 -
~
~
~ ,-l r4
~
536 I 537 ~ ~ I Highly fractured zane, siltstone crumbles easily. ~ l~ 538- r , 1-- I, V 539 Siltstone more induratErl.
~"I..,,:"
~
<7 0"',
540 0\ C
...ol~
!~
541 - -- l~ I
~
,..r I
542- f- -~ r:::-
. 4 less indurated fractured, weathered. ~
543- I- - ~
.I" 0 f~
544 - -- ~ 545 -l- 0 dP I'- r-- !"l 546 I- -I-
~
~""'.f
"-h.
547
~
~ I-
.;\ r 548 Highly fractured 7"; ....
2.51-124 . I .. Woodward-Clyde Consultants ~ Amended: April 2009 TL: E048000
Project No. 4.1.~':H Field Log of Boring No. B-1 Sheet.l.Q.. of..l.9-
- 1:-
o.W ROCK CORE WW DESCRIPTION ~e :d~. 0 c!.!:: Sketch <:1 i a: a: SIL'1"S"l"CNE, bro.mish black, 5m2/l, bedd.ir:g rarY;}'in:j fran horizontal to 40* dip, beddi.n; thidmess fran I" to 3", 549 fraeturin:j generally in direction of bedding, m:xlerate1y indurated, crunbles easily, some bluish gray beds fresent generally 1/8 to 114" thick. ML 550-
+
SILTS'IONE, bramish black, SYR2/1, bedding generally hor:i- .+. 1 551
- zontal to 35- dip, highly fractured be1C1N' 551' with fractures ran:ji.r:g fran horizontal to near vertical. ML.
552
+
553 ~ fr
'r T
554
+
T 555-parallel 'bedding, highly "Weathered. r V 556 '"' 557 t unable to reenter boring after loss of casi.r:g. '1"
.J.
Botton of borirg at ,557*
- 558 .I.i 1-
.;- I SSg-I- or or i
4~. 560 - 561- .. 562- I- " 0 563- r-564* 565- ... -I-566 t 567 t Woodwarc:J.Ctyde f:ot1suttants ... IIl"A Amended: April 2009 TL: E048000
Project No 4J299I Field Log of Boring No. B-2 Shet;'C 1 of 4(\ BORING LOC~~e~.arniTY') Real Sta. 67 + 55 'PMF Survey Worr: ELEVATION AND DATUM El. 145 (appro>;..) DRILl.ING AGENCY Continental Drilling DRILLE~ike u"..'1 ""... DATE STARTE%/05/ad VA
- FINI::5Ht:Df,/IR/80 DRIl.LING eQUIPMENT Longyear 44 -- ~"';TION DEPI,1q .51 PC:':K DEPTH V SIZE AND TYPE OF CASING 4" S... andard NO ._: DIST. I UND1ST:--TCUHE
... ~A OF SAMPLE::;I I I OHll.l.lNu Mi K C1VU : 00 Drill oioe with wireline oorinq ~t1~~ I FIRST 1 COMPI.. ,24 HRS.
CORE B~~~ar H(i LE:NGTH 5' and 10' BIT DiaIOC>rl::J LOGGED BY: CHECKED BY: Hector Reyes O. S. Ghunan J:- ROCK CORE 1 <:>
- a. W Z ~...,.: 0 w
0'6 uJ DESCRIPTION Sketch e .,- a: 0 a: a: SAND, silty, pale brown, SYRS/2, medium to coarse grained, angular to sub-rounded, sand is mainly quartz, sore broken rock fragrrents. SM It . 9 - SAND, silty to clayey, pelle bro.vn, 5YR5/2, fine to coarse grained, angular to sub-rc.unded, p:::lOrly sorted, silt and clay mixed with eore gravel and brcken rock fragrrents. SM-SC i5 ,... - 16 2.51-126 Woodward*Clyde Consurtants ~ Amended: April 2009 TL: E048000
Project No Field Log of Boring No. B-~ Sheet - of~ ROCK CORE DESCRIPTION \-; SAND, light olive gray, SYRS/2, rredium grained, sub-17 angular to sub-rcunded, well sorted, neatly quartz with __ SOtE rock fragnents. SP 18 I9°f-20 2J 22 23 I 24 I \.-; . I! 25 r-26t I II 27+ I 28*1- ,I 29* -- 30* r-31 I- - 32 33 34 .... 35 2.51-127 lirA Woodward.Clyde Consultants w: Amended: April 2009 TL: E048000
Project No 412991 Field Log of Boring No .
- r:-
1 B-2 Sheet 3 ROCK CORE - of :.;,'\
" a:.,-
Q.LU LULU o!!:: oeSCRIP TION Sketch z ..,o:> w. 0 c 0
" a:
a: I 36 l I I l, I 37 I-
.i-38
-l-i I I i I I
I I I I 39 I i II I I I I I 40 I I I I I 41
- 1 I
I Ii I I II I 42 l I. I I , II rI i 43 ! I I , 44 ,. I I I I I I I I 45 l- j I I I 46 I-
-t-- I ,1 I
47 SANDSTONE (San Mateo Forma tion) , light olive gray, I 5YR5 !2, fine to mediu m grain ed, sub-r ounde d, well sorted , rrostl y quartz with eore rock fragrr ents, {XX)rl
<<:t Q
48 y __ L ceman ted, forna tion dense r than al::::ove. SP
~
>-.1 "t?
49- i- ~
>-Ul t9 50 - -I-
~
51-
-I-52 I-S~ID, rredium graine d, grada tional chang e. SW 53- f-I-
54 2.5I-1 28 Wood ward. Clyde Consu nants .." JJr... Amended: April 2009 TL: E048000
Pr oiect J No Field Log of Boring No . B-2 i', Sheet .:.+ of -
- t- ROCK CORE J-J-o G..lU lUlU DESCRIPTION Sketch Z ~
u.:::
. Q 0
Q!::: c
;;l 0:: a:
a: SANDSTONE (San Mateo Formation) , light olive gray, 1.1'\ 55 5YR5/2, nedium grained, sub-ramded, well sorted, nestly I-
- quartz with SOle roonded rock fraglll3rits. sw Q
~
56-I- -I- ~
~
!.I'.
57~ c
~
58 I P" II T 59 - 60 - I 61 l-I 62 I 63- ", 64 - 65 I-66 - I I I 67 I 68 - I- - 1 69
-I- \,;)
z 70 - . ....r,"
'""'(
~...
~
!.I',
71 I-
-()
6: c:; 72 -i-73
..: * .:>J.- l:l'J
Pro]iect No
- c-Field Log of Boring No B-2 Sheet 5 ROCK CORE of 4U Q.w o z
UJW DESCRIPTION Sketch ~ . 0 ol:!:. e I.l
~
0 a: a: a:
- l 74 r-I i 75- -I-76 -
I 77 f'-. 78 lQ t I (San Mateo Fonnation) , light olive gray, I f~ SANDSTONE 4", I t~ 5YP5!2, coarse grained, sub-roomed to subangular, \Nell 79 I- sorted, poorly cerrented, nostly quartz with sore rock I fragrrents. SW u: 80 T t~ f'" II I t I 81 i-' r t I I
- +
82 I I I 83 tT I II 84 fr I I I I 85- t- -f0o-grading to coarse grained. 86 -- I I i-87- r- -l-88 f-l- I 89 -- co ~ z, 90 t- -r-~:s sr: 91 -r- ~ 92 2.5I-130 Woodward*CI~'de Consuft;:!nts 'lIIlP Amended: April 2009 TL: E048000
Proect
- t-f-l-J No 4:lL"":H Field I Lo9 of Boring No B-;G Sheet t*
ROCK CORE of -,' ll.W o z ,; w uJ OeSCRIPTION c . 0 0:: Sketch c: v- a v-a:
" a:
a: 93 f.. SANDSTONE (San Mateo Formation) I light olive grul' , 5\'P5/2, medium grained, sub-rcunded, quartz 90'l., fel(J-spar 5%, other 5%. SW I I i 94 ~ ... ~I-I I! II
- f T I i I t I I
i ! J i I ii 97 + I i; grades torredium grained. Tt Ii I i 98 I I 99l t T t rr I iI I ,,i r-I I i ilOOf I . I I I I-- :",
,i lOll I,
~:: I i
I;' I 102 103 104 105 106 107 grades fine to medium grained. 110 III
Field Log of Boring No. n-2
- c-1 o.W OESCRIPTION o
z'; 0 W W o~ Sketch c ~.::: 0
£ CC CI:
SANoomm, (San Mateo Formation), light o.l ive <:.It'",}' 5YltS/::, 112 med i lin gra Ined , sub-rounded. a*; 113-grades to coarse grained. ll*k:"
,I 1151- +
t i
+/-~ I i I
116 Q
,c_ I 117 ~
.....: I I rI "
T ~ G:. I I T u: i ' I I I 118 l I. I 119
, I 120-- +
I i I : 1211-j I I I I,-, T
.-t :\*',1' I 1
I 122 i- I j
; I II 123
! i I I,
I I ,I I t I! 1/.4 -f-I I N I
...-l i
125~ f-
-s [.l.l
-:l
-" !%w ~
('-I 126 I- I i I I 127 ~ :~::~~y I 128 i-I I 1 I I
-.-J 129 .~ -, :::.
ljO ~'.k : I i Woodward.Clvdp. Consult::tnts "!!!!'!'9 LA Amended: April 2009 TL: E048000
Project No 41:CY**11 Field Log of Boring No. B-2 Sheet~of~ ROCK CORE DESCRIPTION 131-SANDSTONE (San Mateo Formation), light olive gray, 5\1672, medium grained, sub-rcunded., quartz 90%, feld-132- spar 5%, others 5%, dense formation. SP 133 13-1 I I 135 i I
! I 136 I I i
i I I 137 I I 138 I V 139 L4D I-141 142 - - 143-1 144-~ 145 f-
--~ <:r
~ ~
U} 14.;)-
+/- -:.. c.:::
~
147- - -I-
'<::>> 148- - f- :.y:;::
, :(/':;~:
\1.+91 2.51-133 Woodward- Clyde \.;onsutt;; :"'Its ~: .:r"",.
Amended: April 2009 TL: E048000
Project No. Field Log of Boring No. B-2 Sheet () of ~ J:-
- a. W ROCK CORE z
will oeSCRIPTION 0 . 0 o~ Sketch <: g.::: 0 i1:. a: a: 150 151 SANDSTONE (San Mateo Formation). light olive gray. 5Y.R5!2, medium grained, sub-roonded, quartz 90%, feld-I I spar 7%, others 3%. SP 152- ... 153 154 I 156 II I I
'I iI 157 I Ii I
158-Ii I I 159 ! I I I I i I! 160 1 1 161 .... grades to fine grained. 162-163- .... 164 ... 165-
,I 1
167 168 2.51-134 Woodward.Clyde Consultants '-1; Amended: April 2009 TL: E048000
Project No 412991 B-2 Field Log of Boring No. Sheet~of~ J:- ROCK CORE 1 Q.W WW DESCRIPTION Cl~ 169 170 SANDSTONE (San Mateo Formation), light olive gray, 5YR5!2, medium grained, sub-roonded. sp 171 :.. r 172 173 174 175 176 in 178 [ 179 f 180 I-181 182 183 i-187 .:,-: 2.51-135 Woodward.Oyde Consultants ,,~ Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-2 Sheet.lL of ~ ROCK CORE OeSCRIPTION Sketch 188 S;\.t.\iDSTONI: (San "'1ateo Formation), light o Li ve ';)1'd1', 5YRS/2 :-n'lediulll to f i.ne grained, sub-r-oundoo , wd J 189 sorted, dense, quartz 90%, feldspar 7%, others 3t. SP 191 192 193+ t 19.ft I 195 I j I -0 196 I 197 I 198 I I II 199 I I II 200 I 1 I 20i
)02 203 204 205 206 Woodward.Clyde Consultants LA.
'WI:f Amended: April 2009 TL: E048000
Project No. Field Log of Boring No. B-:.! Sheet.l:..... of 4{)
- t- ROCI< CORE
... 1-o.uJ W W essen IPTION o!!:.
I** .; 1207 . '. j .: 208 SANDSTONE (San Mateo Formation), light olive gray, 5YR5!2, medium to fine grained, sub-rounded, well 209*f. sorted, quartz 90% I feldspar 7%, others 3% _ SP - 210 211 tt r 212 213 214 t 21S 216 217 l-218 f..
} 1 219 I i I
I Ir
~20 i-I 11 221- i-2221 1
223 -I-224-225
.4 * .:a- 1.J/
Woodward-Clyde Consultants ..,. JIC... Amended: April 2009 TL: E048000
Project No r - 1 o..W Field Log of Boring No. B-2 Sheet 1 -l of 40 ROCK CORE o W W DESCRIPTION z o,; ' 0 Cl~ Sketch c: ~.:: 0 a: a::" 0::
,~: '.
226 ~ -r
/-
I 227-- SANDSTONE (San Mateo Formation) , light olive gray,
-r .;\:\
SYRS/2, medium to fine grained, sub-rounded, well ?.::W C'J sorted, quartz 90%, feldspar 5%, others 5%. SF :.::': N 228 h t- .- ..
.- i 229 :,C ,,
<i If I
I I I 230 [\r
-'/"
I
+/- I 231
\':, rl I
, I i
I 232 .:.<::\ " 1 233 I-n;;
,:./
234+
- f t :::::
ii. M 235 . N 0 :.:. Z W \./;\ M 236 ....:l eo I, I- ::;.: N
,. ~
en I 237 r- ,I
- ~ (2 f
\j I
238 I- -,.. > It I
~.,
1239- t--- -r
,:. '\i~
f boot - 241-
. m"'
- (,',,::,
2.42 I-
;::.~::~
;:.~
- 43 -!""" I.\N:*
~~):.
r:: 244 2.5I-138
.. .- ,cAt.
Woodward*Clyde Consuttants 'ISIr7 Amended: April 2009 TL: E048000
Project No. 412991 . No, B-2 Field Log of Bonng Sheet --!.i- of ~
- x:- ROCK CORE 1 ,;
Q.W wW DESCRIPTION Z ~ 0 01.: Sketch c u ... 0 a: a: a:
- l f{,\'
245- I- ':': , 246-SANDSTONE (San Mateo Formation), light olive gray; 5YR5!2; trestly fine grained with Sate roodium grained, 247 subangular to sub-rounded, well sorted, quartz 90%, feldspar 5%, others 5%. SP 248 249 250 251 252 V 253-254 255
,~
256 ~ 257' 258- ,.. 259 I-260-261 262 263 2.51-139
Project No. Field Log of Boring No B-2 Sheet...l:..:- of ~
- t- ROCK CORE s* 0g 1 Q.W o WW DESCRIPTION z o Sketch e ~.::
£ ~.
a:: 264 SANDSTONE (San Mateo Formation), light olive gray, I SYF5/2, nostly fine grained, subangular to sub-roonded, ! I 265 I- well sorted, quartz 90%, feldspar 5%, others 5%. SP I 266-~ 267 268 I I 269 - II 270 271 r 273 274 275 - 276 277+- f 279 f 280 I-2.51-140 LA Woodward.C!\. ; Consultants ~,.., Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-2 Sheet l ( of 4\.J
;r- ROCK CORE ... 1-W a..
WW o!!: OeSCRIPTION Sketch
~ ,;
_ 3~ g
..... a:
£ a:
~
283-SANDSTONE (San Mateo Formation), light olive gray, SYR5!2, fine to medium grained, sub-rounded to sub-1284- angular, well sorted, quartz 90%, feldspar 5%, others 5%. SP 285 .. 286 287 288 289 290 291-m:ldium grained with fEMer fines. 292 - 293 294 - 295 f-297 f-f. 298 299 300-301 2.51-141 IT... WOOdward.Clyde COnsuttants . , Amended: April 2009 TL: E048000
Project No 412991 Field Log of Boring No. B-2 Sheet£ of ~
- x:- ROCK CORE
.... 1-o.W WW DESCRIPTION c!:!:
\ .....f 302 SANDSTONE (San Mateo Formation), light olive gray, SYR5!2, fine to medium grained, sub-rounded to sub-303 angular, well sorted, quartz 90%, feldspar 5%, others 5%. SP 305 306 I
307 308 .... I i I I 309-
~.
310"1 , 311 312 313 - 314 ;1" I
-~...-l M
315- t- I-Z 0 ~~;.\ l
~ .....
- M 1316 - i- - ~ ~.
- .:
- .~.
I I 317- -
~ ':'.;;
318- I-
-- f~,;\< :;;;';
1319 -
! r- FF* .'-..../'
320 2.51-142 Woodward-Clyde consenants {¢ Amended: April 2009 TL: E048000 I
Project No. 412991 Field Log of Boring No. B-2 Sheet IH of~
- 1:- ROCK CORE 1 tl.l.LI o .
UJW DESCRIPTION :z ~ . 0 o!!:: Sketch e u,;: d a: a: a: V 321~r-SANDSTONE (San Mateo Formation), light olive gray, 5YR5!2, fine to medium grained, sUbangular to sub-322~!", roo:nded, ......ell sorted, quartz 90%, feldspar 5%, others 5. SP 323- ~ 324 325 326 327 328-- \.../ 329 f-330 I-331 I-o. 332* I-333~ f-
~34- I-335 I-336 337 I-338 I-339 2.51-143 Woodwaro.l;JV(fe-e:;:m,su.tants . ,
tCA Amended: April 2009 TL: E048000
Project No. Field log of Boring No. B-2 Sheet.J.L of ~
- t:-
ROCK CORE 1 ll.W wW OESCRIPTION o~ Sketch 340 SANDSTONE (San Mateo Formation), light olive gray, 5YRS!2, fine to medium grained, subangular to sub-341- rcunded, well sOrted, quartz 90%, feldspar 5%, others 5%. SF 342 ~ 343 344 345 346 347 I-348~1-349 I-350 ~ 351 - 352 . 353- ~ 1354 - 355~ I-356- ~ 357. I-35B
Project No 412991 Field Log of Boring No. B-2 Sheet...1i.:. of ~
- x:- ROCK CORE t-t-Q.W W W DESCRIPTION z ~, 0 o!!: Sketch e :.:.:: a
£. a:; a:;
SANDSTONE (San Mateo Formation), light olive gray, 359 5YR5!2, fine to medium grained, sub-rounded to sub-angular, well sort.ed, quartz 90%, feldspar 5%, others 5%. SP 360 361-362-363 364 365 366 I 367* I 368 +- 369 l-370-371 372- I-1373 I-374-375 376 377 2.51-145 Woodward.Clyde Consultants l"¢ Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-2 Sheet~of~
- t:- ROCK CORE 1 £zo 11 .::.
o.W DESCRIPTION g W W 0 o!:!::. Sketch 378- SANDSTONE (San Mateo Formation), light olive gray, 5YR5!2, coarse to medium grained, sub-rounded, well sorted, quartz. 90%, feldspar 5%, others 5%, trace of 1/4" 379~ gravel. SP 380 381 382 383 384 l-385 ~86. 387 I-388 I-389 - SAl:'l"I>S'J:O:.lli, light olive gray, 5YR5/2,. coarse grained, - sub-rcunded, with sore 1/4" dianeter gravel. SW 390 391-f-392 - 393 394 f- ~95 396 Amended: April 2009 TL: E048000
Project No. 41~'11 Field Log of Boring No B-2 Sheet 22 of--iQ... DESCRIPTION Sketch SANDSTONE, (San Mateo Formation), light o l ive gray, 5YR5/2, coarse to madium grained, well sorted, subroundec r 397 quartz 90%, feldspars 5%, others 5%, trace 1/4" qrave.l . SP 398 .1-399' 400 401 402 403 404 COlor change to medium light gray, N5 , medium grained. 1405 0
"'l' ::> I i
Q a: 406~ I-
- ~
0 G..
~
Ui 1407 -
~,
I-
,. Q
,))
c?i :1{ 408 - ::(' I::F'~ 409 - \.: 1410~ I- - i:~:
':'e :::'
~'!: : :
411 -
'Nr 1412 - :t'~ ,:'
i,: 413 0,'",: -::-
-i
~14 2t 415 l:!.~K:; 2.51-147 Woodward-Clyde Consuttants ~ Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-2 Sheet-LL of ~
- 1:- ROCK CORE 1 o..W oescs IPTION ~,; a wUJ a!::. Sketch
_ 8 ... 0
~ a: a:
416 417- SANDSTONE (San 'Mateo Formation), light olive gray, 5YR4!1, nedium grained. sub-rcunded, well sorteO., quartz 85% , feldspar 5%, others 10%. SP 418~1- - 419 420f 421 1422 I-423+ 1424 I-425 I-426 f-- 427. i-1428 429- I- - ---- 430-
--, I 1':-":::
S1L'I'S':IWE (Monterey Forrration), nedium dark gray,N4, _-:...-. 431- highly micaceous. ML f-=~I.- t.32 I- -- I
~~~ ("'j
<:i"
~33*
~==_.,~1 I-
._. .1 434 -:
'-I 2.51-148 Woodwara*Clyde Consuttants ~
Amended: April 2009 TL: E048000
Projiect No 4LN:'1 F'IeId l og of Boring No . Sheet L"t of 4U
- t- ROCK CORE 1 o z ,;
. - oa:
o.W WW oeSCR IPTION Sketch o..,-' 0 oJ:; c:
- l a: a:
t-_-:. SlL'I'Sl'<NE (Monterey Forma.tion) , rredi\JU dark gray, N4, 1-- 1435 very micaceous. ML -_-: ~36 -- I- ~ 437- - 1--- I-- M I-- "f I-- 438 I-- - f- ..* 0----: 439 ~-:. 440 - .-
... 4'
- 1- --
I- -~ 441 I j _-..- I
~42
_.- I 443 r-.
- =1 1-i::::- -
=--1
-- I 1444 - -- --'1 I 445 r --
446 I- - -- - ~ 447
-I-1--
. 1":-
f448- I- t-= ! 449 I-
-I- --
450- --- I-I-- 451- I-1-- 1-_-:. 1-- 1452 -I- -- 1-- t.rl f- 1----- 1-- '<t 1--- 453
.:: *.)J.-149 . 1--:*
Woodward*Clyde Consultants lIIII:V 1fC,A Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-? Sheet~of~
- 1:- ROCK CORE l-l-o.UJ UJUJ OESCRIPTION z<:> ,;
o . 0 o!: Sketch C
- l u~
0 0:: 0:: 0:: 454 SIL~'E (Honterey FOIllation), medium dark gray, N4, a.b.mdant mica, sore fine sand, .PJ6sible chert lense or concretion fran 456' to 457'. ML SAf:..j'I)b"'I'()t..1E, olive gray, SYR3!2, fine to coarse grained (rrost.Iy n:edium grained), with a snaIl arrount of rounded pebbles and broken gravel, sand is subangular to sub-roonded, pccrly to rroderately sorted (high percentage
+
of silt), quartz 80%, feldspar 5%, others 15%. Note: Sore of t.'l-te above rraterial nay be the solids the driller is trying to wash out fran the inside of the rod. 463 464 465 466 467 68 sand becomes darker in color and fine grained below 468 1
- Also silt content increases.
469 470 SILTs'rONE, dark olive gray, 5YR2!1, very micaceous, slightly sandy. 471 472 2.51-150 /CAt Woodward*Clyde Consultants .... Amended: April 2009 TL: E048000
PrOject No. 412991 Field Log of Boring No. B-2 Sheet 26 0 1 _ ROCK CORE o .
.1 I
DESCRIPTION Z i; 0 Sketch e ~.:::: 0
- > a:: a::
a:: r- - i-- SILTS'IONE (Monterey Fome.tion) I dark. olive gray I 5YR2/1, 473- high mica content, sore very fine aand, ML I- - 474+ 475-476 477 , 1478 I I I 479 t
, i 480 :
I n
; i i
481-1482 Began coring at 482.8' (slight caving in hole at start o~ run #49). ! 483 f _0. f-_-_ I I 1-- 484 f---- 1--:: L=_= L:_, 0\
"<f I
1485 ....... -,
- - -4 SANDSTCNE, light olive gray, SYR6/1, fine grained, very
~86- .... well indurated, bedding at 25°, 1116" to 1/8" thick. - ~
487 - SILTS'IOOE, olive black, 5YR2/1, parallel redding 15°, I" to 4 to thick, interbedded with very fine grained ,I I sand, highly micaceous, little to no weathering, highly I fractured zone, slickensides in some fragments. NL j i488~ - f-- t *
~ I I
(f.~ I
~.o I,{\'
.:jiN - _:...
~I,{\ 1"-1 1' ..... '
7f:: I I I~ ""'-..-/ Unfraetured siltstone. J 49~ l-I I 491 2.51-151 - I
Project No. 412991 Field Log of Boring No. B-2 Sheet.E of -=_" ROCK CORE J:- 0..1..IJ W W DESCRIPTION o!;: Sketch 492 SIL'I'S"!Q'.lE (Monterey Fotm:ltion), olive black, 5YR2/l, parallel bedding dipping 15 0 to 23 0 , 1" to 2" thick with rrany intert:eds of bluish gray mi.caceoas siltstooe 1/16" to 1/4" thic:k. pal:alle1 to bedding, rTal'¥ very snall 'White, 493 lenticular, sand 'sized grains of micaceous rraterial (7) within the da:t:k siltstone, rroderately fissile with nost 94 joints parallel to bedding, well indurated, little or no weathering. ML I l-Ii i I
._~
SIL'!'STCll."lE, olive black, 5YR2/l, with bluish gray inter-beds, occasional dark olive green fine sand lenses, =- dips' range fran vertical to horizontal, with fraet:ures t parallel to lJedding, nost, of the cored section is highly 502 brecciated with contorted bedding, minor offsets of beds anJ. irregular cx:xrpaction or slurrping structures; also with some slickenside surfaces indicating movement, 50:; tedding thickness ranges fran less than 1/16" to 4", material is highly micaceous, weathering ranges fran very little to rroderate. ML
+
T 1507 2.51-152 If!"~ W00d wartf.e,\,d c Consuli;)r,t~ ,." r Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-2 Sheet 2b of~
- r: -. ROCK CORE f-t;; 0 ,,;
~w z oOW. 0 m{
DESCRIPTION cl;!:. Sketch c IX: 0 IX: 0 a:: SIUl'S'I"CNE (Mont.erey Fonnation), olive black, 5YR2/1, contains l/S" to 1/16 11 thick bluish gray contorted interbeds (to 516'), horizonta.l bedding 1/4" thicl:, fractures ,Parallel to l:edding, sliCkensided surfaces, 51~ sare thin lenses of very fi..re grained sand, very highly fraet.ured (to 512' L angular unconformity at 516', bedding dips 70°, still displays slickensides alons 51.J bedding planes and fractures, moderate weathering.
+I
~lL I
I 1
- mf(
1::: t ....? f'-I' ("'"I lfi N co 51"t 5.1 7,- I t 518
~~Zl
'!!;~
519 SILTSTONE, olive black, 5YR2!1, bedding 1/4" to 2" thick with thin 1/4" *to 1/16" bluish gray interl:eds and discon-tinuous lenses of claystone, dips range fran 20° to 35 0 with an apparent angular unoonfonnity at 522', fractures generally parallel beddin:J, very highly fractured at 523' with slickenside surfaces o:::mron throughcut cored section, m::>derate weathering. ML522523524 525 The upper 16" of the core in Run #55 appears to be 526 material . that has fallen into the botton of the hole and was then shoved into the core 'barrel. No structure to it. 527 32" of Run #56 was extracted from the core 'barrel, ha...rever. the upper 16" of this core appeared to be mate- ~I 528 rial that had fallen into the hole while the rods were
~
lfi 81 pulled. The actual cored material is as above with angularunoonformities in the core, with dips of approxi-s- Ci>' r-529 matel 20 0
- ML It'l 2.51-153 L;.
Woodward*t,;lyae f.;onsultants ~ ..<'. Amended: April 2009 TL: E048000
Project No. 4 U' HI Field Log of Boring No. Sheet....::.:::...of~ ROCK COHE I'art of core very jumbled, lower part is intensely f.ractured siltst.one with slickensides and a snoll con-cretion @ 529', with a poorly preserved clam shell cast. t-1L SIL'I'S'I.'rnE (Honte~ey Fonnation), olive black, 5YR2/1, with some bluish gray inter'beds of clayey material 1/16" to l/S" thick, upper 10" of core is rubble fran caving of the hole (not cnlculated in % reoovery) , the majority of tll.e core is very jumbled with randcrol.y oriented siltstone pa.rticles in a clayey matrix, sore beOOi.ng is corrcort.ed and sene is parallel with dips 30" to 45" and fractures along bedding planes I many slickenside surfaces and intensely fractured zones. ML S:LTS"I'Ot.'E, olive black, SYR2/l, upper 20" of core is rubble t..'1at has fallen into hole, jumbled and oontorted to 537.S I, last 2 to 3" is a very 'fine sandy layer. ML SILTS':oct-lE, olive black, 5YR2/1, inte:r:'bedded with bluish gray siltstone ranging fran 1/16 to I" thick, bedding generally diping 30" to 45", disp1acerrent of 1/2" in
\5.;Q beds displayed across fractures ronnal to bedding planes, i slickensides exhibited along bedding planes, rroderately fractured and weathered. ML !5*~1
- T Upper 2' of core very jumbled with broken siltstone particles in a bluish gray clay matrix, some minor offsets beds and a feN slickensides. ML
§.!LTS'I'Orx"E, olive black, 5YR2/3, with very feN bluish gray i claye.j interbeds (1/16" to 1/4"), be<1ding is parallel and
.~
S*i7-!- dips at 20" to 25", high percentage of fine sand in the
!'3.Bt_
lower 1 1/2 I of me cored section, rrost fractures are along bedding planes almough sore ranqe to >70". a few 2.51-154 I .. Woodwara.\';IYtf~"COn~tlttants ... Amended: April 2009 TL: E048000
Project No. Field Log of Boring No. B-2 Sheet~of ROCK cores
~ ;;
DESCRIPTION Sketch c g.::: g if. a: a: did'.ensides found along- fractured surfaces, v.eathering
.:,nd frueturi:lg tire rroderace, ML I~A9-I
\550 5:)1 f:rurS'1'0t:I: (r-loncerey Fonnation), olive black, 5YR2!1 T pcor ly defined bedding planes distinguiShed by sand size I
.t,..
Icnt.Lcul.ar' micaceous (1) grains, rrany bluish gray lenses of clayey rraterial which pinch out, sore of which sho>> offset and display lIflame-like" structures, dips fran 0° t to 90°, sare intensely fractured zones, arrl slickensides t, 0:1 lllany fractured surfaces, m:Xierately weathered. ML .L
+
tl
+
554
- .;;ILTSTGT.C, upper 11 of cere intensely fractured with nany sliCkensides and bluish gray clayey layers, fran t
555' to 556 I a clayey' zone with broken, angular silt-stone particles mixed in, below this is another fracture zone follow~ by a contorted, jumbled siltstone zone, dips highly variable, sore fine sandy lenses and offse::. beddi.nq*. t*;:..
~.
i r 559 560 1 lSiJl-+- 562 563 SILTS'1U'1E still highly fractured with nay slickensides, , mien of the core consists of fractured siltstone parti-I. . j ::H;-t cles with offset bedding and variable dips in a bluish gray clay rratrix. ML
~ ;:\{:,:>"
LA. Woodward*Clyde Consuttants ~ Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. p-2 Sheet...J..L of .1.':'__ ROCK CORE o oeSCRIPTION z ~ . o Sketch c g s: 0
<i a: a:
SlUl'STONE (l'ionterey Fonnation), olive black, 5YR2/1,
-.1I:terbedied widl bluish gray siltstcne and cx::casional thin beds of claystone, siltstone beds rang'e in dip fran horizontal to 50", fractures occur parallel to bedding planes, intennittent zones of contorted bed:ll.ng with minor offset of beds, slickenside surfaces ccmron, highly fractured in zones, rroderately weathered. ML S!L'1'S'I01~r.;, bluish gray claystone beds beocsre thicker, rz.mging from 1/16" to 1/2".
Lens of fine grained sand. Siltstone becoming less fractured. l" I SlLTSTc~n:, l:::edding cup changes drastically fran 50" to horizontal in 2' of core, at 584 1 , bluish gray claystone beds are pinched out and slightly offset, siltstone becomes well indurated below 584', highly jointed, slic."'ensides comron, ML
.' ...J
- 1-156 Wl')odw:'!"d*cr~:deCOr':~..ult21"t<;
Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. B-2 Sheet...J.L of x-1 ROCK CORE d a:>>~ <<:-10c D"W wW DESCRIPTION 01:: Sketch zc
~ 0:
a: 587 SIL'I'SfO:\JE (Monterey Formation), olive black, 5YR2/1, int.erbec1::led with bluish gray claystone and sandstone, beds range from 1/16" to I" thick, dips range from 588 horizontal to 18°, no weatheririg:, sane jointing {verti-tt cal}, occasional thin lenses of sand (ash?) at 590', layer of very well indurated sandstone, fish-scales seen 1 589 at 594 , highly polished beading plane surfaces. HI., 590 591 Very well indurated sans tone at 589.6' to 590.4' .:J:.
;.+
592 l~+ ~l .
+/-+ ~l !~,
iI 593 T j~! : i 1II-~
.~ i i 594 t ~ II SIL'I'S'I'Ol:\1E, beds dipping rrostly 35°, with clay-filled joints. ~1L 595 1.+
.s:
596 597 l Highly contorted bedding, bluish gray claystone prevalent f t in this zone, highly fractured, clay-filled joints. 601 602 603f V 6 605 I .. Woodward*Clyde Consuttants ~ Amended: April 2009 TL: E048000
Project No. . Field Log of Boring No. B-2 Sheet ~:' of.!::- J:- ROCK CORE 1 a. W ci ,; wW DESCRIPTION z o " Q a!::. Sketch c
- l t.I a::
~ a ex:
0: SILTSTONE (Monterey Formation), olive gray, 5YR4/1, G06 interbedded witil ec:tre fine sandstone and bluish gray claystone. Bedding frcm 1" to 7" thick with the inter-beds less than 1" thick, dips are 3$° to 40° with joints 607 rrostly parallel to bed:'ling, sere are vertical, occasional slickensides surfaces, well indurated with very little weathering. ML I I I f I
! I
+---!=-"'>I----l:---H
~;2"LTS'ID~'IT::, slightly fissile, bedding from I" to 8" with a
- j fe,,, thin- cl.ayey interbeds and fine sard beds, slightly fractured area frem 616.5' to 617', with slickepside ,
surfaces, dips at 40°', most. fractures display slick I surfaces. ~1L I 614 I f~1 6] 5 tr H'I -TI~I~ I i r- \ t~ 616 l I I I'
~
t~ 617 SILTSTQ~E, slightly higher percentage of fine sand, slickenside surfaces en fractures, dips average 25 Q
- I, 1 I
.~ ; , !
.-. i "'""-l I
61 621 622 SILTSTONE, light olive grav, 5YR5/2, SetTe fine grained 623 sand,* silicified., rrod.eratel~T fractured with mirx::>r offset 1Jedding, scsre visible forams, dips approx.inately 25°. 24
- 1-158 Woodwara. (;fyde t;onsuftants ~
Amended: April 2009 TL: E048000
Project No. Field Log of Boring No. B-2 Sheet~of~
- 1:- ROCK CORE t-t-
... UJ 0 ,,;
llJLU DESCRIPTION z o . 0 o~ Sketch e
,,~
0 a: a: a:: SIUfSroNE, light olive gray, 5YR5/2, sare fine sand, very hard, silicified, lTOderately fractured, visible forane , 625 dips 25°. ML 626 SIL'l'S'.rCNE (Monterey Fo:mation), light olive gray, 5YR5/2, interbedded with a fM bluish gray clay lenses, highly I fractured and contorted zone at 626 I to 627', dips 20" 627 above fractured zone and 35° belON it, general fracture trend Parallel to bedding with sane slickenside surfaces. sore joints near vertical, occasicnal pods or thin lenses of fine sand, well indurated, slightly weathered. ML I 630 Iii I ' , I I;.-. 631 i I ,If" I>C I ~. I I*&~' 632 I I f' I I j * : I ,. I II
--+-1+- "!':
634 I
, II I
t ! 635 r::: I , i
.- i 1 i I '-I SILTSTONE, olive gray-olive black, 5YRl/2, appears t
brecciated thrcugh the entire run, .containing ltOstly I 637 angular fragrrents of siltstone in silty matrix, dip of fractures is 55° to 60°, one 2.5" to 3" zone of shearing
@ 638.5', also a very light gray, N8, fine sandy layer, 638 I" or less thick @ 640.6'. ML Nurrerous s:rre.ll pieces of siltstone at 639 .8' .
640 lilllOOrous polished surfaces, rrostly not well indurated. 6-12 643 2.51-159 lirA, Woodward.Cfyde consultants '4iBl' Amended: April 2009 TL: E048000
Project No. 41 ~:9':H Field log of Boring No. l:hL Sheet ,.' of-=:':"" ROCK CORE 2 ,; DESCRIPTION o . Q Sketch e u - 0 a: a: a::"
~., "
.~
()44-SILTh"IWE (~lonterey Forma.tion), olive gray-olive blad~, ~
' ;.'l, I
SYR2!2, less brecciated, cemented layer @ 645.(,', ~ ! q , fraet.url;:':; with 55° to 60 0 dip. ML 645 -I-
',~.,., I
" (]
~
~.*,
6*16 i
,of 04,t I
().~ cJ 6~19 650 I"tnu3iv~~ ,,,ith p.:lSsible 1::ak.ed uwer cx:ntact 651 652 SILTS'IONE olive black, 5YR2/1 , 1:leccrres' nore dense an~ I cerrented, fractures are s~horizontal, 65 0 , and ver-tical, .lithologic manges at 653 .4', 653. 7', 654.2 I I 653 654.4' and 658.2', upper ones are light gray, N7, sandy I beds. one at l:ottan is light bluiSh gray, 5.86/1/ brecci-ated siltstone. ML 654 Sample taken at 654' yields age of Louisian (l*liddle
.. . Miocene)
- 655 656 .i,
.i\....(.
657- I-658 I-
"~
-r- r~'
Monterev Fonmtion, basal unit consist.ing of glaucopj':a.:l~ r--- schist (low grade), dusky blue, 5PB3/2, sandy !latrix ./it.:-, I G59 rounded quartz grains. - I 660 - -- 6(*:- 662 2.5I-160 Amended: April 2009 TL: E048000
Project No. Field log of Boring No. Sheet..J£.... of ...!ill...- ROCK CORE DESCRIPTION o z Sketch BR!:.'CClA, dark bluish gray, 584/1, lON grade blue schist, (63 very weathered/reworked. 6":"'~ 665 BRECCIA, dark bluish gray, 5B4/l, core is less broken-nore intact. proncunced brecciation, bard layer on top 1 606 I naterial is possibly reworked. 6(;7 6G81. f:i t 1': 669 1 670 '-" en BRECCIA, (San Onofre Breccia), medium bluish grlly I SB5/l, core contains rrany angular clasts fran sand size 672 i to clasts larger than the core diameter (2 1/2"L nate-rial is in a fine grained bluish gray chloritic rratrix I v,hich is highly weathered, rnich difficulty in keeping' I 673 core intact, clasts are minty glaucoplane shist, with i sare nuscovite, lepeCblit.e, plagioolase, quartz, garnet, 674 and pyrite, well developed schistcsity in lTOSt frag- "'.~I , ments. 1.:': I j***..,s 01 676 677 [;) ~ i 679 680 1'--!-='i---f--- u I, 681
-161 Woodward*Clyde Co"sult:-int~ lit"" ..:' I Amended: April 2009 TL: E048000
Project No. Field Log of Boring No. B-2 ROCK CORE DESCRIPTION Sketch Z ci ,; e ..,c '
.,- - 0 aa:;
a:: a::
- J 682 illillXlA (San Onofre Breccia), roodium bluish gray, 585/1, rrany angular clasts ranging fran sand-sized to 4" to 5" (larger than,2 1/2" core diameter) in a blue gray, fine grained chlorltic rratrix, generally rroderately to highly weathered, nest clasts display a well developed sdlistosity and contain glaucophane, miscovi.t;e, garnet, plagioclase, an:i pyrite.
686 607 688 689 69C 691 692 1 I o(j(J 'I o 693 Clay natrix with clasts to 3 11 * .-1 1 I 694 Cores fracture easily. Most pieces less than 2" long. 695 696 697 7 ,IV t * ! .... 2.51-162 f Woodward.Clyde Consultants ~ 1..- Amended: April 2009 TL: E048000
Project No. _ _ 411YY..l Field Log of Boring No. Sheet~of~ ROCK CORE ci . DESCRIPTION z ~ . 0 Sketch e <>.::: a0:: 0:: << BREO:IA (San Onofre Breccia), medium bluish gray, 5B5/1, 701 sdlistcse clasts are contained in a light bluish gray cnolorite natrix in various degrees of weathering clasts vary in size fran sand size (medium grained) to larger 702 than core size. clasts are nestly chlorite and glauco-phane sdlist. 55'" fracture surface dip. 703 704 705 706 707 708 Minerals embedded in natrix include quartz. biotite, garnets,. amphibole. and glaucophane schist clasts. 709 10 711 712 713 714 715 , f:'~l co 0
......; i 716 717 ~.
0\ 0 18 0 cr:;
......; (,.J 71 IC..
Woodward*Clyde Consuftants w.- Amended: April 2009 TL: E048000
Project No.
- 1:-
412991 Field Log of Boring No. 13-2 Sheet 3q of 40 ROCK CORE o.UJ ci DESCRIPTION z o",;, -. 0 UJW o~ Sketch e .,- a a:
- J 0::
a: 0 Only clasts recovered, no matrix. Clasts are angular, blue schists with gamet, biotite, t-pyrite, quartz, potphyroblasts, fran pebble size to 3". o..... "., Clasts are fairly fresh. ,..., N,... f~ One fresh blue schist clast recovered. BRECCIA (san Onofre Breo:::ia), medium bluish gray, 5B5/1, rratrix supporting angular to zounded, generally rretarco-rphic clasts from sand size to clasts longer than 2 1/2", pcorly to m:::x1erately ce.rrented matrix, matrix and clasts fresh, no orientatirn, sorting, or stratificaticn to clasts within natrix, rratr!x is fine grained chlorite material. I BRECCU" highly fractured to massive, well indurate::l clasts to 5" or more in length. (V') o,e I 6','
~ ~f~J
,j II BRECCIA, bluish gray matrix with rounded to angular clasts. Friable to well indurated, rroderately fractured.
Woodward*C!yde Consultants ~~ Amended: April 2009 TL: E048000
Project No 41:lYYl Field Log of Boring No. B-2 Sheet 4~1 of 4; ROCK CORE DESCRIPTION Sketch ~ ~:: g
& c:: c::
739 BREL"Cll, (sen Onofre Breccia), nedium bluish gray, 585/1, d110ritic clay matrix oontains nore sanc.1 than before, 740- node.tate to well oemenced with clasts ranging in size fran sand size to larger than core barrel size, clasts are angular to sUbangular, larger clasts are mostly 741 chlorite and glaucophane schist, smaller clasts of - quartzitp" an::l anphi1:::o1e, sare lenses of poorly i.ncluratoo medium grained sandstone, joints at 35 \), moderately 742 weathered in zones, 'Nell induratal at 740.5 1 to 743'. 743 -- 744 745f Clast is faulted and displaced. 1/2". 7415 r-y 747-748 - 749 750 I- Botton of Boring at 749.5 ft. - I 2.51-165 I .. Woodward.Ctyde Consultants . " Amended: April 2009 TL: E048000
APPENDIX 1-8 GEOPHYSICAL LOGS 2.51-166 Amended: April 2009 TL: E048000
WELL ENGINEERING SURVEYS >. u ELECTRIC LOG a*
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Project No. 412991 SONGS 2 & 3 2.51-167 Amended: April 2009 TL: E048000
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- WELL ENGINEERING SURVEYS,. : .
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Project No. 412991 Fig. SONGS 2 & 3 1-8-2 2.51-168 Amended: April 2009 TL: E048000
APPENDIX l-C MICROFOSSIL AGE DATES 2'5I-169 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. CONSULTING MICROPALEONTOLOGY 11526 Sorrentc valley Road Suite G San Diego. California 92121 (714) 755*1524 TWX: 9103221735 MICROPALEO SDG July 3, 1980 TO: Southern California Edison Co. RE: So. Cal. Edison Core B-1, Samples 1 to 5 San Onofre Area Orange County, California NANNOFOSSIL REPORT Introduction Four (4) "samples were examined for calcareous and siliceous nannofossils and siliceous microfos.sils. These samples re-pre s en t; scattered depth intervals "from near 485 feet to about 654 feet cored in this test hole and provide the basis for the age determinations of this report. The initial preparations of the four samples were void of calcareous nannofossils but "did contain fragments and parts of siliceous microfossils (siliceous spicules, spines and radiolarian parts). The samples were then treated and pre-pared specifically for siliceous microfossils and on exam- "ination, were found to contain reasonably diverse assem-blages of siliceous microfossils. Though the majority of diatom species present are benthonic forms, the assemblages do contain" some pelagic species along with silicoflagellates, which allow the placement of these samples into their repre-sentative biostratigraphic zones. The high ratio of ben-thonic to planktonic forms suggest the marine environment 2.51-170 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. RE: Southern Calif. Edison - Core B-1, San Onofre Area during the deposition of these materials was moderately shallow, probably ~eritic or a continental shelf setting. The provincial ages of each of these samples are given in the following stratigraphic summary and are based on the included siliceous microfossils or siliceous nannofossils. The age and zonation framework used is based on the data and definitions provided by Barron (1975, a-b) and Koizumi (1975, 1977) for the ,diatoms and from Bukry (1975) and Ling (1977) for the silicoflagellates. A limited list of spe-cies of .the total number identified from each of the samples is included as support for the age determinations. This suite of species given as representative of each sample in-clude the age diagnostic forms and the more common species observed in each sample. The frequency or abundance of each species is also noted by ~etter symbols. The key to these symbols are as follows: V = very rare, R = rare, S = sparse, F = frequent. Stratigraphic Summary 485' 4-8" (sample 3) AGE: Late Miocene, near the top of the lower Mohnian DIATOM ZONE: Denticula hustedtii/D. lauta, uppermost part SILICOFLAGELLATE Distephanus longispinus, upper-ZONE: most part 2.51-171 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. RE: Southern Calif. Edison - Core B-1, San Onofre Area 485' 4-8" (sample 3) (con't.) DISCUSSION: Selected species occurring in this sample include Actinocyclus ingens (V), Actin-optychus gruendleri (V), Coscinodiscus gigas dio-
~ (V), ~. marginatus (F), C. robustus (V),
Cyclotella kelloggi (V), Denticula hustedtii (R, including narrow ended form), D. lauta (V), Diste-phanus longispinus (V, with angled basal ring) , Lithodesmium minusculum (V), opephora schwartzii (S)', Endictya japonica (V), Rhabdonema japonicum var. sparcicostatum (V), Stephanopyxis schenckii (S). 491' 24-37 lt (sample 1) . AGE: Late Miocene, lower Mohnian DIATOM ZONE: Denticula hustedtii/D. lauta SILICOFLAGELLATE Distephanus longispinus, lower ZONE: part or "Mesocena hexagona sub-zone" DISCUSSION: Some of the species present here include Actinocyclus ingens ($), ~. tsugaruensis (S), Actinoptychus gruendleri (V), Arachnoidiscus decora-tus (F), Bruniopsis mirabilis (V), Coscinodiscus margi~atus (S), ~. robustus (R), ~. vestustissimus (V), Cyclotel1a kelloggi (R), Denticula hustedtii (S), Q. lauta (V), Distephanus longispinus (R, with rounded basal ring), Endictya japonica (R), Melosira sulcata (F), Mesocena hexagona (R), M. septenaria (R), Stephanopyxis schenckii (V). 2.5I-172 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. RE: Southern Calif. Edison - Core B-I, San Onofre Area 491 1 50-55" (sample 2) AGE: Late Miocene, lower Mohnian DIATOM ZONE: Denticu1a hustedtii/D. lauta SILICOFLAGELLATE Distephanus 1ongispinus, lower ZONE: part or "Mesocena hexagona sub-zone lt DISCUSSION; Distinctive or more common species here include Actinocyclus ingens (R), ~. tsugaruensis (R), Actinoptychus gruendleri (V), Arachnoidiscus decoratus (R), Cannopilus schulzii var. longispinus (V), Coscinodiscus sigas diorama (V), ~. marsinatus (S), ~. robustus (R), Cyclotella keIloS9i (V), Denti-cula hustedtii (V), ~ .. lauta (V), Distephanus lonsi-spinus (V), ~. parva (V), Endictya japonica (V), Melosira sulcata (F), Mesocena hexasona (V), M. sep-tenaria (V), 5tephanopyxis schenckii (R). 650.3 1 43-46" (sample 5) AGE: Middle Miocene, Luisian DIATOM ZONE: Denticula lauta SILICOFLAGELLATE Corbisema triacantha ZONE: DISCUSSION: Miocene radiolarians were noted in this sample in addition to the diatoms and sili-coflagellates. Selected representative species of all the siliceous forms include Actinocyclus insens (F), ~. i. var nodus (F), ~. tsugaruensis (5), Ac-tinoptychus gruendleri (V), Cannopilus boliviensis major (R), C. hemisphaericus (V), 2.51-173 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. RE: Southern Calif. Edison - Core B-1, San Onofre Area 650.3' 43-46" (*sample 5) (con't.) DISCUSSION (con't.): Clathrocyclas sp. (V), Corbisema cf. triacantha (R) I Coscinodiscus endoi (V), ~. marginatus (F), f. ro-bustus (R), Denticula lauta (R), Dictyocha epiodon (V) I Diploneis crabro (S), Distephanus parva (F), Dorcadospyris sp. aff. pannosa (R), Endictya japon-ica (S) I Hemiaulis Eolymorphus (V), Isthmia nervosa (F), Lamprocyrtis hannai (R) I Lar"nacantha Eolyacan-tha (R) I LiribsEyris reticulata (V) I Phorticium regu1are (V), SEongodiscus spp. (F) I SteEhanogonia" hanzawae .(V) , .£" Eolyacantha (V)," S.tephanopyxis V turris s.l. (V), Stylacontarium cf. bisEiculum (R), Synedra jouseana (V), Xanthopyxis lacera (R). Interpreted by: ANDERSON, WARRE~ & ASSOCIATES, INC.
~~.L_J~
A. D. Warren 2.51-174 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. RE: Southern Calif. Edison - Core B-1, San Onofre Area References Cited Barron, J. A., 1975a, Late Miocene-Early Plio~ene marine diatoms from Southern California. Palaeontographica, vol. l51{B), pp. 97-170,15 p Ls ; , 6 text-figs., 13 tables. _____ , 1975b, Marine diatom biostratigraphy of the Upper Mio-cene-Lower Pliocene strata of Southern California. Jour. Paleont., vol. 49, no. 4, pp. 619-632, 8 text-figs. Bukry, David, 1975, Silicoflagellate and coccolith stratig-raphy, Deep Sea Drilling Project, Leg 29. In Kennett, J. P., Houtz, R. E., et al., Initial Reports of the Deep Sea Drilling Projec~ vol. 29. Washington (U. S. Govt. Printing Office), pp. 845-872, 7 pIs, 9 text-figs. Koi~umi, Itaru<, 1975, Late Cenozoic diatom biostratigraphy in the circum-North Pacific region. Jour. Geol. Soc., Japan, vol. 81, no. 10, pp. 6l1~627, 2 pIs., 5 text-figs. _____ , 1977, Diatom biostratigraphy in the North Pacific re-gion. Proc. First Intern. Congr. Pac. Neog. Stratig., Tokyo, 1976, pp. 235-253, 14 text-figs. Ling, H. Y., 1977, Late Cenozoic silicoflagellates and ebri-dians from the eastern North Pacific region. Proc. First Intern. Congr. Pac. Neog. Stratig., Tokyo, 1976, pp. 205-233, 3 pls., 10 text-figs. 2.51-175 Amended: April 2009 TL: E048000
ANDERSON, WARREN & ASSOCIATES, INC. CONSULTING MICROPALEONTOLOGY 11526SonantC' Valley Road Suite G San Diego, California 92121 (714) 755-1524 TWX: 9103221735 MICROPALEO SOG July 3, 1980 TO: Sout hern Cali forn ia Ediso n Co. RE: So. Cali f. Ediso n Coreh 01e B-I Core s San Onof re Area Oran ge Coun ty, Cali forn ia FORAMINIFERAL REPORT This repo rt is based on proc essin g and anal ysis of 5 core samp les recei ved June 18, 1980 on a rush prio rity basis Resu lts of this study are deta iled as follo ws: Samp le #1 (491' +24- 26", +29- 31", +3S-3 7") Barre n of Fora mini fera. Fish debr is (C), spicu les CR). Proc essed resid ue cons ists of few shale part icles in the coar se fract ion and very fine- grain ed, clea r, angu lar quar tz sand abun dant "in the fine fract ion. AGE: Poss ibly prov incia l Late Mioc ene (base d on litho logy and orga nic re-main s) ENVIRONMENT: ,Mari ne undi ffere ntiat ed Samp le '2 (491' +50-5 S") Barre n of Fora mini fera. Fish debr is CA, spicu les RF, stato - cysts F. Litho logy of proce ssed resid ue same as samp le #1. AGE: Poss ibly prov incia l Late Mioc ene (base d on litho logy and orga nic re-main s) ENVIRONMENT: Mari ne undi ffere ntiat ed 2.51-1 76 Amended: April 2009 TL: E048000
~ - --
ANDERSON, WARREN & ASSOCIATES, INC. RE~ Southern Calif. Edison - Core B-I, San Onofre Area Sample #3 (485'+4-8 t1
)
Barren of Foraminifera. Diatoms F. Tan dolomitic limestone with few diatoms locked in the matrix. AGE: Indeterminate ENVIRONMENT: Marine undifferentiated Sample #4 (470'+26-30") Bolivina marginata var. F, B. vaughani F, B. sp. FC, Buli-mina uvigerinaformis F, Buliminella brevior R, Eponides rosaformis R, Pulvinulinella subperuviana FC, Uvigerina angelina R. Diatoms F, fish debris F, radiolaria F, spi-cules F. Sil~y, micaceous shale. AGE: ~Prov~ncial Late Miocene, Early Mohnian Stage ENVIRONMENT: Outer Neritic- to Upper Bathyal Sample #5 (650.3'+43-46") Bolivina advena(?) molds F, Dentalina obliqua(?) molds R, Pullenia miocenica(?) molds F, Siphogenerina(?) sp. molds R, UVigerinid molds R, Valvulineria californica{?) molds C. Diatoms F. Brown to tan dolomitic limestone full of foramini-feral molds with test material very badly leached. Some molds are of possible Middle Miocene Foraminifera. AGE: Probably provincial Middle Miocene, Middle Luisian Stage or older ENVIRONMENT: Outer Neritic to, Upper Bathyal or deeper ANDERSON, WARREN & ASSOCIATES, INC. c:::>* <.'J o . ~ ~ A. D. Warren 2.51-177 Amended: April 2009 TL: E048000
APPENDIX 2-A LOGS OF VIBRATORY CORES 2.51-178 Amended: April 2009 TL: E048000
Frojcct ilJo. 412991 Field Log of Boring No. 1-1 Sheet of 2
- ,OAING lOCATION SONGS CFFSllORE _ E-L 597,186' N-427.655 ELEVATION AND DATUM Water D.:pth n I 15R'iLl.1N.:i AGENCY W::::C DRILLER Iverson DATE STARTED 6-7-80 DATE FINISHtoU 6-8-l:W l)RILL:NG EQUIPMENT CQMPCETTOl'f DEP"l)'2, '" HuCK OEPTH SIZE AND TYPE OF CASING 4" Plaati C . NO 10lST, I UNOIST. I CORE OF SAMPLESI i I DRILLING METRoD VIBRATORY CORE -WATER I FIRST I COMPL. 124 HRS.
ELEV. i CuRE BARREL L.ENGTH BIT LOGGED BY: CHE:-=C"""KE""O:O-::B'y:'--;----I ROCK CORE
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- > Sl
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.. Sand, dark greenish gray, SGY4/1, very fine grained, well 1 1. sorted, micaceous, organic odor, randan shell fragments -
t anJ sanE'! carplete shells (sample 1 taken at 2.2 1 ) . SP *w~:*.::.;
~
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I 2.51-179 1! ,j I ... Woodward-Clyde Consultants . , Amended: April 2009 TL: E048000
P,oject '..Jo. 412991 Field Log of Boring No. 1-1 Sheet::': of 2
- t:- ROCK CORE 1 o..W W W DESCRIPTION 0::: Sketch Age = 8,510 + 265 yrs.
Sand, dark greenish jgray, 5GY4/1, very fine grained, -well
,.., sorted, micaceous, occasional pebbles. SP .LO Abmdant shells am shell fragments fran 15.8' to 16.5 '*
19 - Grades to mediun grained sand at 17.8'.
~'C Grades to coarse grained sand at 19.0' I light yellcwish gray, rst6/2, subangular grains, moderately well sorted, occasional pebbles. SP 21 22 Grades to medium grained sand, medium gray, N5, well sorted Clay at 22.4', greenish black, 5G2/1, very plastic arrl. sticky. CL t
t 23 24 I- Sarrl at 24', dark greenish gray, SGY4/l, fine grained, slightly. clayey. SC 25 _I-26 I- Botton of Hole at 25.5' 27 28 29 -- 30_ t-31 r-32 - 33 - -- 34 - I- . -I-
~~
Project No 412991 Field Log of Boring No 1-2 Sheet -L. of 3 BORING LOCATl0NsoNGS CFFSHORE _ £-1,595 807: N-426.123 ELEVATION AND DATUM Hater Ccpth 100 1 DRILLING AGENCY W::C DRILLER Iverson DATE STARTED 6-8-80 DAl t: fINISHl::D 6-9-tsU DRILLING EQUIPMENT COMPLETION OEP'3'9. 51: ROCK DEPTH SiZE AND TYPE OF CASING 4" Pl.astiIc 'l'K)lOIST, I UNDIST, I CORE y iT *** OF SAMPLES' 1 I r.,U H 1l..'rU N""' P':'l'5< G--.lri\" E
!""Ti'TH'l'?OI'l' Q...-- - - -- VIBRA'IQR'f OORE ~in~.r f FIRST 1 COMPl. : 24 HRS.
C~~E BARREL LENGTH BIT LOGGED BY, CHECKED BY: J'I'J/Bt~ ROCK CORE DSSCRIPTION Sketch
.]: SAND, dark greenish gray, 5GY4/l, very fine grained, we.l.I J-1 sorted, micaceous, random shell fragrrents and sene wilole sheLLs ,' Sl:'
+
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+
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+
1 11 .... 4-t CoTplete gastrcp:::x:i at 11.4'. t 12 1 t 13 + t t T
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1.4 Shells and shell fragments at 14.5'.
-.-/
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. +/-
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It:* t IiCA Woodward.ClYde Con!tulblnt~ .... Amended: April 2009 TL: E048000
Project No 412991 Field Log of Boring No. _ 1-2 Sheet 2 . of 3
- x:-
- 0. us ROCK CORE USUS DESCRIPTIO~
Cl~ Sketch SAND, dark greenish gray, 5GY4/l, very fine grained, well f.;:':~:/ 17 sorted, nucaceocs, very slightly clayey. SP }/
'.\ ....
;:;Y:,'
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Pebbles, shells, and shell fragments from 19.6 I . to - ::t:':'. 20.0' * .hge = 9,095 .! 335 yrs. !--
;l 6 Charcoal fragrrents and a pelecy};XXl at 20.7 I
- I
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,I Bec::x:.m:s fine grained at, 23.7 I
- Large pebbles, at 23.9 I * :': ~;.
- ~ Be<::x:::m3s fine to n:edium grained a'!; 24'. T::
25t T 0
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.Ramded pebbles at 25.4 I
- Becares coarse grained at 25.5'. B~ II 26 Beo:::>nes fine grained at 25.9'.
- *"C 1
i (. 27 ... I Bea:>n:es n:edium grained at 27 .1' * - ~:/. i Becorres fine grained at 27.5'
- y:?-, (""4 Bec::x:.m:s fine to n:ediurn grained at 27.7'
- c':: ::
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{->-:,:./: I SAND, olive gray, SYR4/2, fine to n:edium grained, sub-angular, well sorted, micaceous. SP
~ I SAND, micaceous. SP olive gray, SYR4/2, fine grained, well sorted, '~ I, i-t 33 ... I I I
Grades to fine l'mdium grained at 33.4' iI i Grades to fine grained at 33.7' UII \J
!0 '
I d~....Jo.. . ......,.........- .:::.::::
- 1.* .H-182 I ...
Woodward*Clvd~ Cr.:-*'t$uttants . - Amended: April 2009 IL: E048000
Project No 412991 Field Log of Boring No....*.*.!-2 Sheet 3 of 3
- r- ROCK CORE l-l-o..UI W W . DESCRIPTION Q!=. Sketch SAND, olive gray, 5YR4/2, fine grained, micaceous. Sp -:
';:;\
Grades to J:TediLml grained at 36.3 1
- c... :}). I,
, i Abrupt change to fine grained at 36.7 1
- I i 37 Ro.,mded pebble (3/8") at 37.4 1 * - iii:
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I I Wi: I I T ": ; II
!I No recovery fran 38.5 to 39.5 i I1 til j !
* ~"
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+
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Amended: April 2009 TL: E048000
Project No 412991 Field Log of Boring No. 1-3 Sheet of L BORING LOCATI0NsoNGS CFFSHORE _ E-l,594,479: U-424.709 ELEVATION AND DATUM \'Jater D=pth 125' DRILLING AGENCY ~C DRILLER Iverson DATE STARTE%-lO_8D VAIl: l" IN I:>H I: Ub-l U-8(' DRILLING EQUIPMENT CuMpLETION 1)1:1'3'9.5' HUCK DEPTH 0 SIZE AND TYPE OF CASING 411 Pl.ast.ic NO IDIST. I UNOIST, I CORE IVlC .v.... VIBRA'lURY OJRE SAMPLESI Ed~~ I FIRST
=",.-~-;I-=-~.,.---....4 I COMPL. 124 HRS, CORE I I..C"_, I H BIT LOGGED BY: CHECKED BY:
JVJ/BrJ ROCK CORE oeSCRIPTION Sketch SAND,' silty, dark greenish gray, SGY4/1, very fine y
+
grained. micaceous, random shell frag:t'[ents. SM 1 - :".:
'!\>;
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2 - N'::
- ",}
3{ r- [i.., Atundant shells and shell fra<:JI1ents.
,~
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+
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9 t. scattered shells 19
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- I t f
T 13 141 - lsi +
+
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Project No. Field Log of Boring No. 1-3 Sheet 2 of 3 J:- ROCK CORE l-l-a.. W <;) . ., WW oascaIPTION Sketch Z c o> . - a. . 0 O!::. ;;I:: E Z a.: ex:
;;I
~
SAND, silty, dark greenish gray, SGY4/1, very fine gra:lned, micaceous, ranCbm shell fragments. SM 17+ 18 I organic matter hr 19 - organic matter, shells 21 crab It;K] 22 23 I I Age == 9,400 .+/-. 300 yrs.
- . ~: ~I r-'l' 24 ,
j no recovery at 24.0 1 to 25.0'. 25 ~ gastrcpod, peieC'iIXXl 26 bea:::m=s fine grained 27 I-29 30 31 -I-no recovery at 30.8 1 to 31.0'. 32
- 33 - -I-
-I-SAND, dark gray N3, fine grained, well sorued, micaceous, snaIl laminae of mica. SP 2.51-185 AC..a Woodward*Clyde Consultants .....:;-:
Amended: April 2009 TL: E048000
Proiec .
" t N o. 412991 F"IeId Lo9 0f Boring No. 1-3 Sheat ""::::"-'0 < f 3
- t-1 a. W W W DESCRIPTION HOCK CORE o
z ~ . 0. 0 O~ Sketch e ~~ Ez a: a: Jl
;)
- /.
, 3(; I- :':.:, I
- }
37 -
'" ~~&. ~
38 Gradational change to clayey silt, grayish black, N2. -I- @.~ I! Clayey silt, olive black, 5YR2/1, slightly micaceous. ~ ( t 39 1'iL I t
+
40 Botton of hole. 1-3 t I j I l 1 I I I I I I
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l I-
+
II I I I II I
. -l- I )
I I- -l-I
-I-f-
L..)1.-186 Woodward*C~Amended: Consultants ~ April 2009 ~E048000
Project No 412991 Field Log of Boring No. 1-4 Sheet 1 o f _ BORING LOCATlONSONGS Cf'FSHORE _ E-l,593,040' N-423,369 ELEVATION AND DATUM Water cepth 16~1 DRILLING AGENCY M:C DRILLER Iverson DATE STARTE%_~ LJArl;:; t-lNI:>Ht:~_1:';_80 LrliLLING EQUIPMENT SIZE AND TYPE OF CASING . N~. DIST.
. ROCK DEPTH I UND1ST. ~ CORE 4" Plastic OF SAMPLESI I I METHOD ViA !..t:,H I Fl RST I COMPL. 24 HRS.
VIBRAIDRY COR1:~ ELEV. I COrlE BARREL BIT LOGGED BY; CHECKED BY: ROCK CORE o DESCRIPTION Z Sketch e
- l a:
SAND, silty, olive black, 5Y2!l, very fine graine:l, mica-ceous, a few scattered shell fragmants. 8M i tt 2 -l-Shells and shell fragrrents at 2.2' to 2.6'. r-- H 3 Shells fran 3.9' to 4.4 1
- 4 T r--
i17
+/-
l' I
~
... 1 7 I,I 1
.l.
6 T Shells at 6.1'
- tIt:
Gastropods at 7.1'.
~
~
Shells at 9.2' * - I y~ organic matter at 12.1'. 2.51-187 IA I Woodwara.clvoe \"onsultants ~ Ame1'ldea: April 2oMTL: E04SmO
Project No. 412991 Field Log of Boring No. _ 1-4 Sheet 4 of .J
- t- ROCK CORE l-l-o.W .
wW DESCRIPTION o ' Cl. ' o~ g.::: E~ a: Jl SAND, olive gray 5Y5/1, medium grained, sUhangular, no::lerately -...ell sorte:J., scattered pebbles up to 1/4". 17 51' lS! SAND, olive gray 5Y4!1, fine to coarse grained, suban-gular, poorly sorted, slightly micaceous, SP, fran 17.9 to 194-f 18.2. SAND, dark yell"", gray 5Y7!1, Irediun to coarse grainec1, subangular, m::Jderate1y sorted, occasional rounded pebbles to 3/4", SP, fran 18.2' to 18.4'. 20+ SAND, olive gray, 5Y4/1, fine grained, mc:derately sor'ted, micaceous, sane scatteroo pebbles. SP 21jf Organic matter at 21.1'. Age = 11, 355 +/- 650 yrs. 22 - t 23t 1
,1 I . II
+
* ~
Gastr,oJXXl at 24.6'. Concentration of rounded pebbles up to I" fran 25.0' to , T 25.4' * ~ f r 26t 2-I .L. I I 2,8i - I 1.I. I 'I
.\.
I j 29+ -I- I I 30 -I-31 I-SAND, mediun liqht gray, N6, as above with small blebs arrl 32 -I-discontinuous ienses of sand which contain little mica. - Slightly coarser grained, interval fran 33.0' to 33.6'. -- 2.51-188 Woodw<lrd*C1rde Consultants ,.;: ,- I .. I Amended: April 2009 TL: E048000
PrOJec " t No ,+.lL'::I'=".l 1-*4 F"IeId L og 0f Orlng No. B' Sh eet 3 of -=-- ROCK CORE
- t-1 Q.W o :> Q.' .,
W W DESCRIPTION :2 o . Cl~ Sketch e .,- v- E~
.cr a:
- l CJ)
SAND, olive gray I 5Y4/1, fine grained, subangular, well sorted, micaceous. SP P?\
~S:j 36 l-Small rounded pebbles at 36.3'.
~t~:' I 1
~
37 Scattered shell fragments at 37.3'. 3.':" " i 1
.l 3°.' ';,
T I 40+ Botton of Hole 1-4 at 39.5'
- t I
t.
+ i I I f*
I I i
+t ti T
T
~ I 1
-- I
+
t II
..l..
-- i I-I
-l-
,.1-
- I I t 1
t
-f-
-to I
t r 2.51-189 I ... Woodward*Clyde Consuftants ~ Amended: April 2009 TL: E048000
Project No 412991 Field Log of Boring No. 1-5 Sheet 1 of L BORING LOCATIONSONGS OFFSi~RE - E-1,591,165; N-421,269 ELEVATION AND DATUM Water J.)::pth 200' DRILLING AGENCV \\CC DRILLER Iverson DATE STARTE%-12_80 LlAIt:. r-INISHI;:~12_80 DRILLING eQUIPMENT COMPLET ION Dt!"' I Ii IHUCK DePTH SIZE AND TYPE OF CASING ~ .~~"'~ Me I nvu COHI;: BARREL
- r-1 ROCK CORE o.W W W DESCRIPTION O~
SAND, silty, olive gray, 5YR3/2, very fine grained, 1 ..I... micaCecus, scattered shell fragrrents. SM 2 3 4-'-
.\.
+
st
+
T. 6;-.,.
.J.
.j.
I 71. Organic debris at 7.9' Gradual color change to olive black, 5YR2/l, fran 8.0' to 8.5'
- 2.51-190 iCA Wnndward.CIvde Consutbnts ..,
Amended:-Pipm 2(J09 TL: E048000
Project No. 412991 Field Log of Boring No. 1-5 Sheet_ 2 _ of _"_-,_ r- ROCK CORE 1 o..UJ w UJ DESCRIPTION a~ Sketch SAND, silty, olive black, 5YR2/1, very fine grained, mi.caceccs. scattered shell fragnents. SM 17 t l 181 I i I 19 !; f I t I I i
~'O J. I
++ 1I 21 ..;..
tT r::"::':'!";-"+-h No recovery fran 21. 5 I to 22.0 I t 221 Scattered organic debris fram 22.0' to 27.0'. 23 -t Organic tmtter at 23.9'. i I I II f Organic matter at 29.7 I
- I I
, I I i i I f'-
27 30 r Organic matter at 30.6'
- Age = 13,160 +/- 550 yrs.
31 I 32
~
r organic matter at 33.8' . +
-f; ;,;;.
2.51-191 L..a Woodward*Clvde Con5uitants ~:" Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. 1-5 Sheet 3 of __L
- t-f-f-a..""
w oeSCRIPTION ROCK CORE 0 z ,; .. o . '0.' LLl 0.'::::: Sketch c u- EO
"'Z
" a;. (I)
~:: M SAND, silty, olive black. SYR2/l, very fine grained.
+ t-micaceous, scattered shell frdgm:mts. S~1 -:
36 t I-
+
37+ i-iir r 38..1-t Organic natter in concreticn at 38.4 t -
~q '<j' p~,
+/-, Age = 12,270 +/-. 340 yrs. ffi t
Organic ma.tter at 38 ~ 5'
- 1 39 j;:t !
I II 40- Botton of hole 1-5 at 39.5', I I I I
-l-II T
I I j I I I t ,j ! I T T I i
+ !,
... , i *v T
i
-;- I T i i
*r II t i 1+. -
. I I
I i i t i
+ i I
! t i i t
-- I ,
t I I ) ! I I i i I t I
-f-i I
I j I ! ; 1 r
+/-
t 2.51-192 t Woodward*Clyde ConSUltants ~ Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. _2.:1:..-- Sheet _,_ of 3 80RING LOCA TlONsdI:.JG.S OFFSHORE - E.:-l,597, 74U; N-418 851 ELEVATION AND DATUM DRILLING AGENCY w::c DRILLER Iverson DRILLING EQUIPMENT SIZE AND TYPE OF CASING CORE 4 11 Cas inq I
,24 HRS.
,~.
VIBRATORY __. _ , - I OJRE CHECKED BY: J\tJ/BtJ . ROCK CORE r-
. C. w
"'w DESCRIPTION 0: Sketch 1 -"-
SAND, silty, olive gray, 5YR3/2, very fine to fine graine:'i, subangular, nucececos, randan shell fragnents. 8M t 1 l
~
+
3 1
+/-
1, I 4
+
"t 5.1 I t I
'\..../ 6 1 T I I
.\
I
-l-I "t
7 ;-
.l-
...,I iI T I S
+/-
.I-9 +.
+
t lOt...
~
1 I 11..l.. 12 .;... 1
.I.
13 1 .L it 1'; T
.l. SAND, olive gray, 5YR4/2, mediim to coarse grained. sub-15 i angular, mcx:lerately sorted, slightly mi.caceous, shell fragments. SP 1 SAND, olive gray, SYR3/2, fine grained, subangul¥, poor ly
-I-.j.
J(' to rooderatelJt sorted, slightly silty, micaceotu;. Sp_.L:_.:....*~I:"""_-l 2.51-193 .r~ Woodward*Clyde Consultants .,. Amended: April 2009 TL: E048000
Project No. 412991 Field Log of Boring No. 2-1 SheetL of --- :t- ROCK CORE 1 a.. W DESCRIPTION W W Cl~ Sketch Starting at 15.7' - SAND, olive gray, SYR4/2, rredium to coarse grained, sub-17 - angular, lTOoorately to poorly sorted, slightly micaceous, or ruare roos shell fragments, rurrercus rounded pebbles. SP. T t Sl'>!':'J, olive gray at 17.J*, 5YR4/1, fin<: gruin(,.~, suba.ngular, 18 well sorted, micaceous. SP 19 no recovery at 18.0' to 19.5'. t 20 t+ 21 SAND, olive gray, 5YR4/2, nedium to coarse grained, sub-angular, ITO de rately sorted, micaceous, nurrerous rounded 22 pebbles to 1 1/2" in dian-eter. SP SAND, alive gray, 5YR4/1, fine grained, subangular, well
+
23 t sor't.ed, micaceous. SF 1 I SM"D, olive gray, 5YR4/2, nedium grained, subangular, \VeIl 24 sorted, micaceous, occasional sub-ramded pebbles to 1/4" in
.j. diarreter. SP 25:-
t, SAND, olive gray at 24.3' to 24.5', 5YR4/1, fine grained, subangular, well sorted, micaceous. sp
. ~'D, olive gray, at 24.5', 5Y:K4/2, rredi.um grained, sub-
~ ,
I. - f angUlar, well sorted, micaceous. SP SAND at 25.2 I becomes fine to nedium grained. 26 27 t SAND, olive gray, SYR4/1, fine grained, subangular, well sorted, micaceous. SP 28 29+
..I..
Fran 28.7 I to 29 .3' vertical stringers of coarse grained
+
.i.
~.
30 31 organic ma.tter. I 32 33 ..;... I+ 341-35 i no recovery at 34.5' to 35.0'
-194
___l~ Woodward. ClYde Consultants ~~ Amended: April 2009 TL: E048000
. " 1'1 ...
o "0J~l;\ 412991
-- . . F'Ie ld L og 0f B0 ring No . 2-1 Sheet ~
of 3 ROCK CORE
- t-1 .,
ze ou- .,; 0. 0
- c. W uJuJ a~
DESCRIPTION Skelch c .,- Ez a: a:: III
;\:
SJ\ND, olive gray, 5YR4/1, fine grained, subangular i well sorted, micaceous. SP 36 - r I-Frau 36.2' to 38.2' - blel:s of whitish sand deficient in f" .: mica, up to 1/2" in dianeter. I 37 -I- . .::. I
;/?',':"
-:t 3U ... - '.'
!~. \:
3() r*o' 00 recovery at 39.3 1 to 40.0'. 10:*..*.
- 40 I I 41 - 1':":'\
~+ 2 ~ f>' r If)
,)/
43 Iii!> I 44 I.I Botton of hole 2-1 at 44.1 1 *
.1-
-l-I I I
- l-1 i
l
-l- I-
- \
I I-
-I-r 1
2.51-195 I ... Woodward*Clyde Consutt:mts -':':':.- Amended: April 2009 TL: E048000
APPENDIX 2-B AGE DATING RESULTS 2.5I-196 Amended: April 2009 TL: E048000
APPENDIX 2-B
SUMMARY
OF AGE DATING ANALYSES The results of radiocarbon age determinations performed on selected samples of shell and organic material obtained in cores from vibratory drilling offshore of SONGS Units 2 and 3 are attached in this Appendix. Specifically, Table 2B-l summarizes radiocarbon age date determinations on seven samples. This table is followed by the specific data sheets for each sample for the determinations made by Krueger Enterprises, Inc., Geochron Laboratories Division located in Cambridge, Massachusetts. It is noted that the results for Sample 15 of Core 1-3 appear anomalous when compared to the other results. Also, the quantity of sample was noted to be small enabling only limited pretreatment. Based on a dis-cussion with Mr. Krueger, who made the determination, if this date were in error, it would be too young. For these rea-sons, it is suggested that the results of Sample 15 of Core 1-3' may be treated"' as" anomalous and,' therefore, disregarded in analysis. 2.51-197 Amended: April 2009 TL: E048000
TABLE 2B-l
SUMMARY
OF AGE DATING RESULTS Age Date in Years Core No. . Sample No. Depth ( ft) Material Type Before Present* 1-1 2 16.4 Shells 8,510 + 265 1-2 6 19.7 Shells 9,095 + 335** 1-3 14 23.4 Organic 9,400 + 300 1-3 15 25.7 Shells 5,065 + 180** 1-4 22 21.1 Organic 11,355 + 650 1-5 28 30.6 Organic 13,160 + 550 1-5 31 38.5 Organic 12,270 + 340
- 'These age dates are referenced to the year A.D. 1950.
- Ph or ouqh leaching not possible during pretreatment due to limited size of sample.
2.51-198 Amended: April 2009 TL: E048000
KRUEGER ENTERPRISES, INC.
- GEOCHRON LABORATORIES DIVISION 24 BI.ACKSTONE STREET. CAMBRIOGE, MA. 02139 * (617)*876.3691 PRIORITY BASIS RADIOCARBON AGE DETERMINATION REPORT OF ANALYTICAL WORK Our Sample No. GX- 7327 Date Received: *27 June 1980 Your
Reference:
Project 41299I, Task 3160 Date Reported: 7/7/80 Submitted by: O. S. Ghuman Woodward-Clyde Consultants 4000 W. Chapman St. Orange, CALIF 92668 Sample Name: Sample #2. Offshore SONGS. Boring 1-1, run 2, section C. 15. 8-If\. 5'. Shells. AGE = 8510 +/- 265 C-14 years B. P. (c-13 corrected) \ ......,.1. Desctiption: Small sample of marine shells of various species *. Pretreatment: Shells and shell fragments were recovered after disaggregating the sample with ultrasonics. The shell material was further cleaned and rinsed briefly with very dilute Hel to remove altered surface material. The cleaned shell material was then hydrolyZed under vacuum to recover carbon dioxide for the analysis. Comment: Notes: This date is based upon the Libby half life (5570 yean) for C 14. The error stated is +/-1 a as judged by the analytical data alone. Our modern standard is 96% of the activity of N.B.S. Oxalic Acid. The age is re~erenced to the year A.D. 1960. 2.51-199 Amended: April 2009 TL: E048000
KRUEGER ENTERPRISES, INC. r
- GEOCHRON LABORATORIES DIVISION V 24 BLACKHONE STREET. CAMBRIDGE. MA. 02139. (611)*876*3691 PRIORITY BASIS RADIOCARBON AGE DETERMINATION REPORT OF ANALYTICAL WORK Our sample No. GX- 7 3 3 5 Date Received: 30 June 1980 Your
Reference:
P.O. #: 412 99 I Date Reported: 23 July 1980 Submitted by: O. S. Ghuman Woodward-Clyde Consultants 4000 W. Chapman St. Orange, Calif 92668 Project No. 412991 sample Name: Offshore SONGS. Sample #6. Boring 1-2, run 1, sec. A, 19.8'. Shells AGE- 9095 +/- 335 C-14 years B.P. (C-13 corrected) 1 I
== Description:== Mixed shell fragments in sand. V Pretreatment: The shells were cleaned thoroughly in an ultrasonic cleaner. A brief leaching with very dilute HCI was utilized to remove additional surficial material which may have been altered. Thorough leaching was not possible without severely reducing the size of the sample. The cleaned shells -were then hydrolyzed with HCI, under vacuum, and the carbon dioxide recovered Comment: for the analysis. Notes: This date is based upon the Libby half life (5570 years) for C 14. The error stated i$ +/- 1 a as judged by the analytical data alone. Our modern standard is 95% of the activity of N.B.S. Oxalic Acid. The age is referenced to the year A.D. 1950. 2.51-200 Amended: April 2009 TL: E048000
KRUEGER ENTERPRISES, INC. GEOCHRON LAaORATORIES DIVISION 2-4 BLACKSTONE STRE E T
- CAMBRIOCie, lolA. 02139 * (617).876.3691 P RIO R I T Y BAS I S RADIOCARBON AGE DETERMINATION REPORT OF ANALYTICAL WORK Our Sample No. GX-7328 Date Received: 27 June 1980 Your
Reference:
Pro~ect 41299 I , Task 3160 Date Reported: 2 July 1980 Subm itted by: O. S
- Gh uman Woodward-Clyde Consultants 4000 W. Chapman St.
Orange, CALIF 92668 Sample Name: Sample # 14. Offshore SONGS. Boring 1-3, run 2, section A I 23.4 feet. AGE= 9400 + 300 C-14 years B.P. De5a'iption: . Small sample of organic matter in marine sediment. The entire sample was dispersed in a large volume of Pretreatment: water and the clays and organic matter were eluted away from any sand and silt by sedim~ntation and decantation. The clay/organic fraction was then treated with hot dilute HCl to remove any carbonates. It was then filtered, washed, dried, and roasted in oxygen to recover carbon dioxide from the organic Comment: matter for the analysis.
._-- 01 0 0 .
Notes: This dateis based upon the libby half life (5570 yean) for C 14. The error stated is +/-1 (1 as judged by the analytical data alone. Our modem standard is 95% of the activity of N.B.S. Oxalic Acid. The age is referenced to the year A.D. 1950. 2.51-201 Amended: April 2009 TL: E048000
KRUEGER ENTERPRISES, INC.
... GEOCHRON LABORATORIES DIVISION
-' 24 BLACKSTONE STREET. CAMBRIOGE. MA. 02139. (6m*816.3691 PRIORITY BASIS RADIOCARBON AGE DETERMINATION REPORT OF ANALYTICAL WORK Our Sample No. GX-7336 Date Received: 30 June 1980 Your
Reference:
P.O. #41299I Date Reported: 23 July 1980 Submitted by: O. S. Ghuman Woodward-Clyde Consultants 4000 W. Chapman St. Orange, Calif 92668 Project ~o. 41299I Sample Name: Offshore SONGS. Sample #15. Boring 1-3, run 3, sec. B. Shells. AGE = 5065 +/- 180 C-14 years B.P. (C-13 corrected) Oescription: Mixed shell fragments in sand. v Pretreatment: The shells were cleaned thoroughly in an ultrasonic cleaner. A brief leaching with very dilute HCI was utilized to remove additional surficial material which may have been altered. Thorough leaching was not possible without severely reducing the size of the sample. The cleaned shells were then hydrolyzed with HCl, under vacuum, and the carbon dioxide recovered Comment: for the analysis.
------------------------------------------------------~---
Notes: This date is based upon the libby half life (5570 years) for C 14. The error stated is +/- 1 o as judged by the analytical data alone. Our modern standard is 95% of the activity of N.B.S. Oxalic Acid. The age is referenced to the year A.D. 1950. 2.51-202 Amended: April 2009 TL: E048000 I
KRUEGER ENTERPRISES, INC.
\I
- J GEOCHRON LABORATORIES DIVISION 24 BLACKSTONE STREET. CAMBRIDGE. MA. 02139. (617)*816*3691 PHIOHITY BASIS RADIOCARBON AGE DETERMINATION REPORT OF ANALYTICAL WORK Our Sample No. GX-7329 Date Received: 27 June 1980 Your
Reference:
Project 412991, Task 3160 Date Repol18d: 7/7/80 Submitted by: O. S. Ghuman Woodward-Clyde Consultants 4000 w. Chapman St. Orange, CALIF 92668 SImple Name: Sample If 22. Offshore SONGS. Boring 1-4, run 2, section A, 21.'1'. Organic carbon, AGE = 11,355 +1- 650 C-14 years B. P.
== Description:== Small .sample of organic matter in marine sediment. The enti~e sample was dispersed in a large volume of Pretreatment: water and the clays and organic matter were eluted away from any sand and silt by sedimentation and decantation. The clay/organic fraction was then treated with hot dilute HCl to remove any carbonates. It was then filtered, washed, dried, and roasted in oxygen to recover carbon dioxide from the organic' Comment: matter for the analysis. The sample was quite small, but was counted on each of two days with good concordance. average reported. Notes: This date is based upon the Libby half life (5570 yearst for C I 4. The error stated is t 1 Q as judged by the analytical data alone. Our modern standard is 95% of the activity of N.B.S. Oxalic Acid. The age is referenced to the year A.D. 1950. 2.51- 203 Amended: April 2009 TL: E048000
KRUEGER ENTERPRISES, INC. _. GEOCHRON LABORATORIES DIVISION 24 BLACKS TONE STRee T" CAM8RI DGE. MA. 02139" (617) 876.3691 PRIOR ITY BASIS RADIOCARBON AGE DETERMINATION REPORT OF ANALYTICAL WORK Our Sample No. GX-7 337 Date Received: 30 June 1980 Your
Reference:
P.O. it 412 99 I Oat. Reported: @$ July 1980 Submi tted by: O. S. Ghuman Wood ward- Clyde Cons ultan ts 4000 W. Chapman St. orang e, Cali f 92668 Sample Name: Offsh ore SONGS. Samp le #:28. Borin g 1-5, run 2, sec A, 30.6 '. Orga nic matt er. AGE= 13,16 0 +/- 550 C-14 years B.P.
== Description:== Orga nic matt er from marin e ~edim ent. Pretrea tment: The entir e samp le was dispe rsed in a large wate r and the clays and orga nic matt er were volum elute e of away from any sand and silt by sedim entat ion and d deca ntati on. ~he clay/ orga nic fract ion was then treat ed with hot dilut e HCl to remov e any carbo nates It was then filte red, wash ed, dried , and roast ed in . oxyg en to recov er carbo n diox ide from the orga nic Comm ent: matt er for the anal ysis.
°/00.
Notes: This date is based upon the Libby half life (5570 years) for C t 4. The error stated is +/-1 a as judged by the analytical data alone. Our moder n standa rd is 96% of the activity of N.B.S. Oxalic Acid. The age is referenced to the year A.D. 1950. 2.51-2 04 Amended: April 2009 TL: E048000
I
. KRUEGER ENTERPRISES, INC.
- GEOCHRON LABORATORIES DIVISION 24 8LACKSTONE STREET. CAMBRIDGE, MA. 02139 * (617) 87(,.3691 PRIORITY BASIS RADIOCARBON AGE DETERMINA liON REPORT OF ANALYTICA!- WORK Our Sample No. GX- 7 338 Date Received: 30 June 1980 Your
Reference:
P.O. #412991 Date Reported: 24 July 1980 Submitted by: O. S. Gh uman Woodward-Clyde Consultants 4000 W. Chapman St. Orange, Calif 92668 Sam pte Name: Offshore SONGS. Sample #31. Boring 1-5, run 4, sec A, 38.5. Organic matter. AGE= 12,270 +/- 340 C-14 years B.P.
Description:
Organic matter from marine .sediment. Pretreatment: The entire sample was' dispersed in a large volume of water and the clays and organic matter*were eluted away from any sand and silt by sedimentation and aecantation. The clay/organic fraction was then treated with hot dilute HCl to remove any carbonat~s. It w~s then filtered, washed, dried, and roasted in oxygen to recover carbon dioxide from the organic Comment: matter for the analysis.
--------------~-------------------------------------------
Notes: This date is based upon the libby half life (5570 yean) for C 14. The error stated is +/- 1 a as judged by the analytical data alone. OUf modern standard is 95% of the activity of N.B.S. Oxalic Acid. The age is referenced to the year A.D. 1950. 2.51-205 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J ANALYSIS OF POST-1975 EARTHQUAKE ACTIVITY. Site File Copy Amended: April 2009 TL: E048000 Site File Copy
San Onofre 2&3 FSAR Updated APPENDIX 2.5J ANALYSIS OF POST 1975 EARTHQUAKE ACTIVITY 2.53.1 POST-1975 EARTHQUAKE ACTIVITY WITHIN A 200-MILE RADIUS In this appendix, the post-1975 earthquake activity (January 1975 through September 1979) of magnitude greater than 3.0 is summarized and compared to the preceding reports of activity in the 200-mile region around the site. No significant change in the activity pattern is noted. Data were obtained from the unpublished data file of the California Institute of Technology; these data are in the same form as those reported by Hileman and others (1973). Although the instrumentation coverage within the California Institute of Technology network is sufficient to provide locations of earthquakes of about magnitude 3 and larger within the onshore U.S. portion study area, detection and locations for activity for offshore and in Mexico as provided by the Cal tech array is not necessarily complete and locations are probably less accurate. No better locations are known to be available for this time period, however, so the seismicity of Mexico is described in terms of the Caltech data. The magnitudes reported by the Caltech network are in M (~ocal magnitude). L No earthquakes with M ~6.0 occurred during the post-1975 time period. L Eight earthquakes occurred with M ~5.0 (see figure 2.5J-1). Four of these were in Mexico and four wereL in southern California in regions of known historic activity .(Hileman and others, 1973; FSAR figure 2.5-20). None are closer than 70 miles from the site. In JUly 1975 one earthquake occurred between the San Miguel and Sierra Juarez fault zones with M = 5.0. This event is located near 'the 1974 Pino Solo earthqu~ke (M = 5.0) (A. Nava, in preparation, Doctoral Dissertation, UCSD, referenced in Brune and others, 1979). The seismicity with ML ~4 is dispersed throughout southern California and Mexico (see figure 2.5J-2). The spatial distribution is general~y similar to the 1932-1975 distribution of M ~5 earthquakes (FSAR figure 2.5-20), L suggesting stability of seismic source regions for small earthquakes in time and space. The number of events for the 4-year period (ML ~4) is roughly equivalent to the number M >5 for the 43-ye~r period, which is consistent with a frequency of M >4-about 10 times greater than M >5, as
=
expected from the frequency-magnitude relationship Log N a - bM - (Richter, 1958). The closest earthquake occurred about 45 miles SW from the site. In Mexico, the distribution of earthquakes M >4 is oriented SW-NE, or perpendicular to the general trend of mapped faults. One earthquake, the August 19, 1978, Canon de la Presa event, has been relocated in a special study by Brune and others (1979). On the basis of that study, the true location is north of the Caltech location shown here; i.e., between the NE terminus of the San Miguel fault zone (as shown on the base map) and the City of Tijuana. The Caltech magnitude is ML 4.1; Brune and others (1979) assign M 3.5. At the magnitude 4 level, no activity is associated with the Newport-Inglewood, Offshore Zone of 2.5J-1 Amended: April 2009 TL: E048000
San Onofr e 2&3 FSAR Updat ed APPEND] X 2. 5J Dema rcatio n (OlD), or Rose Canyon fault zones in south ern Calif ornia . Two event s occur red along the Whitt ier-E lsinor e, and four event s along the San Jacin to fault zones . A low level of seism icity again preva ils but is not entire ly absen t for earthq uakes with M ~3.0 withi n 50 miles of the site (see L figure 2.5J- 3). The close st earthq uake is about 9 miles NW of the site; a second is about 25 miles south . Activ ity occur s along the Newp ort-In glewo od (30 to 60 miles NW of the site) in the region of the afters fault zone the 1933 Long Beach earthq uake (Rich ter, 1958) . Scatt ered hock zone of activ ity is observ ed SE and SSE of the site but is not easily assoc iated with known faults . Modest activ ity (seven event s) is observ ed withi n about 25 miles of San Diego , but no earthq uake is close r than 10 miles from the Rose Canyon fault . Subst antial activ ity occur s betwe en the south ern half of the San Migue l and Sierr a Juare z fault zones , betwe en 50 and 100 miles SE of Tijua na. In summary, the seism icity betwe en Janua ry 1, 1975, and Octob er 1, 1979, withi n 200 miles of the site is simil ar to the long term to 1975 and no distin ctive , new patte rns of activ ity are patte rn for 1932 activ ity sugge sts an appar ent decre ase westw ard betwe en evide nt. Seism ic the San Andre as .Ind San Jacin to faults and the hypot hesize d OlD. The offsh somewhat more active than the hypot hesize d OZD for the ore region is post-1 975 perio d. 2.5J.2 RELATIONSHXP BETWEEN THE HYPOTHESIZED OZD AND OTHER MAJOR TOPOGRAPHIC FEATURES IN BAJA CALIFORNIA Follow ing is a discu ssion of the struc tural relati onshi p of the major fault system s of Baja Calif ornia and the possi ble struc tural and geomo rphic conti nuity of these faults to the OlD. The geogr aphic area to be descr ibed consi sts of the region of Baja Calif ornia north of the Agua Blanc a fault to the U.S.-M exico Borde r and the region west of the Sierr a Juare z to the Pacif ic Coast . Speci fic atten tion will be paid to the geolo gic and regio nal tecton ic settin g, the San Migue l fault zones , the Valle citos fault zone, the Agua Blanc a fault , and the possi ble conne ctions betwe en the San Migue l fault zone, the Valle citos fault zone, and the hypot hesize d 020. Geolo gic Settin g The north weste rn corne r of Baja Calif ornia can be divide d into three physi ograp hic and geolo gic provin ces (see figure 2.5J- 4): A. A narrow coast al margi n chara cteriz ed by Terti ary marin e and nonma rine sedim entary rocks and Tertia ry-to- Holoc ene volca nic and volca nic-d erived rocks B. The gently seawa rd slopin g footh ills betwe en the Pacif ic Coast and the centr al high penin sular range s under lain by pre-b athol ithic eugeo clinal accumul~tions of volca nic and sedim entary rocks which were subse quent ly metam orphos ed to varyin g degre es by intrus ion of the batho lith 2.5J-2 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J C. The Peninsular Range of northeastern Baja California compr~s~ng middle Cretaceous plutonic rocks of the southern California batholith Regional Tectonic Setting Structurally, the western two-thirds of the northern part of Baja California consists of an uplifted and westwardly tilted fault block. The high eastern edge of the block is formed by the mountain ranges of the Sierra Juarez to the north and the Sierra San Pedro Martir to the south. Uplift of the eastern edge began about 10 million years ago (Gastil and others, 1975). The eastern escarpment was created by a series of east-dipping normal faults that downstep antithetic fault blocks towards the Gulf of California depression (Gastil and others, 1979). The main structural block has been cut by three major fault zones: the Agua Blanca fault zone, the San Miguel fault zone, and the Vallecitos fault zone. The Agua Blanca fault zone trends westerly from its eastern limit in the Sierra Juarez to the Pacific coast south of Ensenada. Movement along the Agua Blanca system began during late Cretaceous time (Gastil and others, 1975). The major northwest-trending faults of this region (the San Miguel and Vallecitos fault zones) and the adjacent continental borderland faults are believed to have" been formed later in Middle Miocene time (Moore, 1969). Generally, the principal fault systems of the northwest peninsula region are considered to be primarily strike-slip but many show evidence of dip-slip displacement as well. However, they do not appear to connect with the major dip-slip faults of the Sierra Juarez and Sierra San Pedro Martir. The Agua Blanca fault zone is characterized by a relatively continuous main trace while the San Miguel and Vallecitos fault zones are characterized by en-echelon fault segments and associated shorter subparallel faults. Much shorter conjugate sets of left-lateral faults trend northeast across the region. Features along the two major northwest-trending fault zones suggest Quaternary activity. The major northwest and west trending faults are discussed separately "below. San Miguel Fault Zone The San Miguel fault zone consists of two segments. In 1956, a 20-kilometer length of the southern segment broke along a series of short en-echelon ruptures (Shor and Roberts, 1958). Measured fault displacements ranged from 0 to 31 inches horizontally to 0 to 36 inches vertically; the sense of offset was uniformly right-lateral and down to the southwest. The southern segment is mapped as a principally dip-slip fault that dies out in the Sierra Juarez and does not connect with either the Agua Blanca fault or the dip-slip faults of the eastern escarpment (Gastil and others, 1975). There is no evidence that this fault offsets this escarpment or connects with faults in the Gulf of California. 2.5J-3 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J The northwest end of the 1956 break lies en-echelon to the northern segment. The northern segment can be traced on air photos to the area northeast of Valle San Rafael where offset streams and dikes show right-lateral separation; the most clearly expressed fault trace appears to separate Mesozoic dikes only 100 meters (Gastil, 1975, 1979). Vallecitos Fault Zone The Vallecitos fault zone is en-echelon to the northe'rn segment of the San Miguel fault zone, but separate from it by a distance of 6 to , 10 kilometers. The Vallecitos fault has a nearly continuous trace that extends from the western edge of the Sierra Juarez 65 kilometers to the west end of the Valle de las Palmas (about 29 kilometers southeast of Tijuana). As noted by Gastil and others (1979) the main trace of the fault is marked by erosional topographic features and there is no evidence that the Vallecitos offsets anything younger than the crystalline basement rocks. An unpublished map by a former Stanford graduate student shows only 3 kilometers of right-lateral separation of a Cretaceous pluton boundary (cited in Gastil and others, 1979). Calabasas Fault The Calabasas fault is mapped about 5 kilometers east of *the Vallecitos fault zone and trends parallel to it for about 30 kilometers in a northwest-southeast direction. In the Valle de las Palmas area, recent movement may be indicated by small sags and saddles~ breaks in uplifted alluvial deposits, and relatively 'uneroded scarplets (Gastil and others, 1975,' 1979) . Tres Hermanos Fault The Tres Hermanos fault zone is located midway between the San Miguel and Agua Blanca fault zones and essentially parallels the San Miguel fault zone. The trace, approximately 45 kilometers long, begins in the batholithic rocks and dies out east of Ensenada. The fault is indicated by 'pronounced topographic expression and is apparent on high altitude photos, yet recency of movement and sense of displacement are unknown (Gastil and others, 1979). Agua Blanca Fault Zone The Agua Blanca fault zone extends about 129 kilometers across the western two-thir4s of th~ Baja California peninsula. The Santo Tomas fault branches off the western portion of the Agua Blanca fault. These faults are distinctive for their west-northwest trend that is more westerly than the strike-slip faults to the north. The trace of the Agua Blanca fault is indicated by abundant geomorphic evidence (Allen and others, 1960; Hamilton, 1971). Typical features are distinct scarps, offset streams, shutteridges, fault sags and saddles, and fault-controlled valleys. Quaternary fan gravels in the Valle de Agua BI~nca are offset about 4.8 kilometers in a right-lateral sense; between 11.3 kilometers and 22.6 kilometers of similar separation may be indicated by discontinuous 19neous contacts across the fault trace (Allen and others, 1960). 2.5J-4 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J Detailed field mapping (Allen and others, 1960; Gastil and others, 1975) indicates that the east end of the Agua Blanca fault dies out in the Sierra San Pedro Martir and does not intersect the dip-slip faults of the eastern escarpment. The offshore extension of the Agua Blanca fault west of the landward traces of the Agua Blanca and Santo Tomas faults is characterized by complex submarine topography (Krause, 1965). Recent investigations show that the offshore-onshore fault relationship is not present as a continuous through-going feature. Legg and Kennedy (1979) recognized the offshore portion of the Agua Blanca fault as a series of subparallel en-echelon segments. A component of vertical movement is indicated locally by Quaternary sea floor scarps with several hundred meters of relief (Krause, 1965; Legg and Kennedy, 1979). Near the Todos Santos Islands northwest of Punta Banda, the fault zone makes a northwest bend and continues north in the form of relatively short en-echelon segments trending toward either the San Clemente or the Coronado Banks fault zones. A more detailed and complete discussion of the offshore borderland faults is presented in appendix 2.SP. Tectonic Implications
- Evidence for the amount of total displacement on faults within the San Miguel and Vallecitos fault zones is" limited. The suggested amount of lateral offset, where indicated, is poorly defined and ranges from 100 meters to 3 kilometers. "North of the Agua Blanca fault z~ne, the region west of the Sierra Juarez and Sierra San Pedro Mart{r escarpment" has acted as a relatively stable block as indicated by the small amount of overall displacement on the San Miguel fault zone and the Vallecitos fault zone. These two zones are inferred to be relatively young features that, along with similar right-lateral strike-slip faults of the region reflect a change in the relative plate motions from subduction to transform motion along the southern California-Baja California continental margin (Crouch, 1979).
The Agua Blanca fault is an older tectonic element initiated in the late Cretaceous. The east end of the Agua Blanca dies out in the batholithic rocks before reaching the coastal plain of the Gulf. Seismic profiling along the western Gulf margin has shown that the structural elements of the northern Gulf are not continuous with the onshore fault zones in the northern peninsula (Henyey and Bischoff, 1973). Although some secondary northeast. trending faults with scarce indications of left-lateral motion have been mapped in the region, the evidence is generally poor to support the hypothesis of a conjugate fault system. The northwest-trending strike-slip fault systems of the northwestern Baja region appear to be reacting to regional shear influenced by the relative plate motions and are not directly connected with transform features in the Gulf of California: 2.5J-S Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.53 Possible Connection Between the Rose Canyon and the San Miguel or Vallecitos Fault Zones S~veral authors have suggested that an en-echelon relationship may exist regionally between the Rose Canyon fault zone and the San Miguel and Vallecitos fault zones (see section 2.5K.2 for summary and discussion). A possible northwest extension of the presently mapped limits of either the Calabasas or Vallecitos faults has been inferred by these authors largely on the basis of the regional alignment of discontinuous topographic, structural, and geothermal features in the southern San Diego and southeast Tijuana area. However, geologic maps by Kennedy (1975) and Gastil and others (1975) indicate a 55-kilometer distance between the south end of the Rose Canyon fault and the north end of the Vallecitos fault. Gastil and others (1979) suggest the possibility of a northwest-trending lineament that would continue from the northwesternmost mapped trace of either the Vallecitos or the Calabasas faults, through eastern Tijuana, and across the U.S.-Mexico Border just west of San Ysidro. This suggested lineament crosses an area with a historically quiet seismic record (with the exception of the 1978 Canon de la Presa earthquake). Features (Gastil and others, 1979) that suggest this lineament are: A. The subparallel alignment of the Tijuana River Valley and the Valle de las Palmas, trends of faults in the San Ysidro area, and v the alignment of seve raI t.herma I wells** B. The contrast between Eocene stratigraphy north and south of the lineament C. The mapped traces of northeast-trending dip-slip faults in the southern Tijuana-Rosarito Beach area which do not continue across the lineament If the lineament suggested by Gastil and others (1979) is a fault, it would trend northwest from the Valle de las Palmas area, cross the Eocene bedrock exPosures, continue beneath the deeply alluviated Tijuana River Valley and possibly into the San Diego Bay area (see appendix 2.5K.1 for a discussion of faulting in the San Diego Bay area). Although this lineament has been suggested by Gastil and others (1979), the lack of faulting in the well-exposed Eocene bedrock and the lack of fault features recognized on aerial photographs of the area by Gastil suggest that no significant faulting has occurred in this area since Eocene time. Geophysical data by Kennedy (1977) (see table 2.5K-l, in appendix 2.5K) does not identify significant faulting along the proposed connection of the San Miguel and Vallecitos faults and the Rose Canyon fault in the area south of San Diego Bay and north of the International Border. Therefore, the applicant's position is that the observed evidence is not supportive of a through-going fault that could connect the Rose Canyon Fault Zone (RCFZ) with either the Vallecitos or San Miguel fault zones. 2.5J-6 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J The most prominent faulting associated with the southern part of the RCFZ is to the southwest, rather than to the southeast. The south part of the RCFZ is represented by a widening zone of shorter, principally dip-slip faults that are mapped in the offshore area west of San Diego Bay. These faults generally diminish in expression and die out when traced in a southerly direction. This portion of the RCFZ is discussed in detail in section 2.5K.1. 2.5J.3 SEISMICITY OF NORTHERN BAJA CALIFORNIA Northern Baja California is an area of extremely high seismicity; at least 13 earthquakes of magnitudes greater than 6.0 have occurred since 1900 (Brune and others, 1979). Previous epicenters in this region (Hileman and others, 1973; FSAR figure 2.5-20) appear to scatter across the peninsula, suggesting a broad zone of deformation. Recent investigations, including field studies (Reyes, et al., 1975; Johnson;, et al., 1976) and the relocation of epicenters (Leeds, 1979; Brune and others, 1979) in the region, indicate that the vast majority of earthquakes are associated with a few active faults. The San Miguel Fault appears to be the seismically dominant fault in the northern Baja California region. In 1956, four large earthquakes (magnitude 6.1 to 6.8) occurred along the San Miguel fault near the town of San Miguel (Brune and other, 1979). In addition, Leeds (1979) has relocated five earthquake epicenters with magnitudes greater than ~.O to the San Miguel fault zone;" one of these was re Ioca t.ed near the northwest end of the San Miguel fault near the Vallecitos fault. Relocation errors as large as 90 kilometers were noted in earlier catalog locations. Micro-earthquake activity in the San Miguel fault zone is very high. Reyes and others (1975) operated high-gain portable seismographs at 22 stations in this region with detection level estimated to be less than magnitude 2. Sixteen of these stations reported micro-earthquake rates greater than 27 events per day. The highest rates, exceeding 100 events per day, were recorded near the southeast end of the San Miguel fault. In a study by Johnson and others (1976), and San Miguel fault was found to be seismically active along its length and responsible for the vast majority of recorded earthquakes in this region. Hypocenters on the San Miguel fault ranged in depths from 0 to 20 kilometers. Composite focal mechanisms from this study indicated a mixture of right-lateral and dip-slip (east side up) movement that was consistent with surface evidence. No large historic earthquakes are positively correlated with the Agua Blanca fault (Allen and others, 1960; Brune and others, 1979). Magnitude 6.0 and 6.3 earthquakes of 1954, previously located along this fault, have been relocated to the San Miguel fault (Leeds, 1979). Very low rates of micro-earthquake activity have been recorded on the Agua Blanca fault (Johnson and others, 1976). \,---" 2.5J-7 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J The activity of the plate boundary to the east of the hypothesized OZD is compared with parallel faults in the June 1979 report and a westward decrease in activity is noted. It is clarified in appendix 2.5P that areas to the west of the hypot~esized OZD do not necessarily maintain that westward decrease" in seismicity. In Baja California, the basis for evaluating comparative levels of activity is limited by data availability; however, the seimic activity in Baja during the period 1971 to the present does provide a limited basis for such an evaluation. In considering all the earthquakes with M of 6.0 or greater north of L 31.5 0 latitude, most seismic slip appears to be associated with either the San Miguel fault or with the ridge-transform fault system extending from the Gulf of California to the Salton Sea. These earthquakes are listed in table 2.5J-1 and are taken from Brune and others (1979), Hileman and others (1973), and Caltech (unpublished). The relationship of Thatcher and Hanks (1973) can be used to calculate moment values for these earthquakes. Although the relationship proposed by Thatcher and Hanks was developed for M , the use of M yalues will not produce a significant discrepancy a~d is suitable ror "comparative purposes. The cumulative moment thus calculated for the San Miguel zone is 2.9 x 10 2 6 dyne-em and for the plate boundary zone is 12.4 x 102 6 dyne-cm, Assuming that the fault zones are of similar depth, the total seismic slip is directly proportional to the moment and varies inversely as the fault lengthens. Since the plate boundary zone is about twice as long as the San Miguel fault zone, the total slip on the plate boundary is about twice the total slip on the San Miguel. Thus, for the Baja California area, there is a decrease in historical seismicity to the west of the plate boundary faults, but the westward activity is dominated by the San Miguel fault. Various authors have alternately proposed and contested that the hypothesized OZD, Newport-Inglewood Zone of Deformation (NIZD), RCZD, and San Miguel fault zones are connected (Abbott and Elliott, 1979). At the present time "exact relationships between these fault zones have not been established" Brune and others, 1979). Based on data presently available (Abbott and Elliott, 1979; Hileman and others, 1979; Reyes and others,
~979), large or small earthquakes or micro-earthquakes do not delineate such a connection. A very small number of small earthquakes have occurred in the San Diego and Tijuana regions and near the hypothesized OZD; however, the pattern is highly diffuse (Hileman and others, 1979) ," The only tentative pattern in the seismicity is a short EW trend at San Diego which may intersect a weak NW-SE trending zone of activity near the Coronado Banks fault zone (Legg and Kennedy, 1979). This can only be seen in the more accurately located epicenters. One earthquake (M = 3.5, Brune and others, "1979; M = 4.1, Caltech) has been well located between L
L Tijuana and the mapped trace of the San Miguel fault zone, This event does not constitute evidence of a connection between the San Miguel and Rose Canyon, since events of this size commonly occur in many areas of southern California and Mexico with no proximity to' through-going faults (Hileman and others, 1979). An example of a well located event of this kind in Mexico is the Pino Solo earthquake (M F 5.0) of 1974 (Brune and others, 1979). 2.5J-8 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2. 5J Table 2.5J-l EARTHQUAKES OF MAGNITUDE 6.0 AND GREATER ALONG PLATE BOUNDARY AND IN NORTHERN BAJA Date Magnitude Fault 11-21-15 7.1 Cerro Prieto 12~30-34 6.5 Laguna Salada 12-31-34 7.1 Cerro Prieto 2-24-35 6.0 San Miguel I 5-19-40 6.7 Imperial 12-07-40 6.0 Cerro Prieto 10-24-54 6.0 San Miguel 11-12-54 6.3 San Miguel
'2-09-56 6.8 San Miguel
'\...../ 2-09-56 6.1 San Miguel 2-14-56 6.3 San Miguel 2-15-56 6.4 San Miguel 8-07-65 6.3 Cerro Prieto 4-09-68 6.5 Borrego 10-15-79 6.6 Imperial In summary: (1) The historical seismicity of the northern Baja California area is dominated by the high level of activity of the San Miguel fault, although this level is about one-half as high as that on the plate boundary faults (Cerro Prieto, Imperial, and others) to the east, (2) Based on seismological evidence, the San Miguel fault does not appear to be mechanically connected to the hypothesized OZD to the north. 2.5J-9 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J REFERENCES
- 1. Abbott, P. L., ed., 1979, Geological Excursions in the Southern California Area prepared for the Geological Society of America Annual Meeting, San Diego State University Department of Geological Sciences, 217 p.
- 2. Abbott, P. L. and Elliott, W. J., eds., 1979, Earthquakes and Other Perils, San Diego Region, San Diego Association of Geologists for Geological Society of America, Field Trip Guidebook, pp. 83-100.
- 3. Allen, C. R., Silver, L. T., and Stehli, F. G., 1960, Agua Blanca Fault, A Major Transverse Structure of Northern Baja California, Mexico, Geological Society of America BUlletin, v. 71, p. 457-482.
- 4. Brune, J. N., Simmons, R. S., Rebollar, C., and Reyes, A., 1979, Seismicity and Faulting in Northern Baja California, in Abbott, P. L., and Elliott, W. J., eds., Earthquakes and Other Perils, San Diego Region, San Diego Association of Geologists for the Geological Society of America, Field Trip Guidebook, p. 83-100.
- 5. Crouch, J. K., 1979, Neocene Tectonic Evolution of the California Continental Borderlanq and Western Transverse Ranges, Geological Society of America Bulletin, Part 1, v. 90, p. 338-345.
- 6. Crowell, J. C. and Sylvester A.. G., eds , , 1979,. Tectonics of the Juncture Between the San Andreas Fault System and the Salton Trough, Southeastern California, A gUidebook for the Annual Meeting Geological Society of America, University of California at Santa Barbara, Department of Geological Sciences, 193 p.
- 7. Flynn, C. J., 1970, Post-Batholithic Geology of the La Gloria-Presa Rodriguez Area, Baja California, Mexico, Geological Society of America Bulletin, v. 81, p. 1789~1806.
- 8. Gastil, R. G., Phillips, R. P., and Allison, E. C., 1975, Reconnaissance Geology of the State of Baja California, Mexico, Geological Society of America, Memoir 140, p. 170.
- 9. Gastil, R. G., Kies, R., and Melius, D. J., 1979, Active and Potentially Active Faults; San Diego County and Northwesternmost Baja California, in Abbott, P. L., and Elliott, W. J., eds.,
Earthquakes and Other Perils, San Diego Region, San Diego Association of Geologists for Geological Society of America, Field Trip Guidebook, p. 47-60.
- 10. Hamilton, W., 1971, Recognition on Space Photographs of S~ructural Elements of Baja California, U.S. Geological Survey Professional Paper 718, p. 26.
2.5J-10 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2. 5J
- 11. Henyey, T. and Bischoff, J. L., 1973, Tectonic Elements of the Northern Part of the Gulf of California, Geological Society of America Bulletin, v.* 84, p. 315-330.
- 12. Hileman, J. A., Allen, C. R., and Nordquist, J. M., 1973, Seismicity of the Southern California Region, January 1, 1932 to December 31, 1972, California Institute of Technology, Pasadena, 487 p.
- 13. Johnson, T. L., ~adrid, J., and Koczynski, T., 1976, A Study of Micro-Seismicity in Northern Baja California, Mexico, Seismological Society of America Bulletin, v. 66, No.6,
- p. 1921-1929.
- 14. Kennedy, M. P., 1975, Geology of the Western San Diego Metropolitan Area in Geology of the San Diego Metropolitan Area, California Division-of Mines and Geology, Bulletin 200, p. 113-39.
- 15. Kennedy, M. P., Welday, E. E., Borchard, G., Chase, G. W., and Chapman, R. H., 1977, Studies of Surface Faulting and Liquefaction as Potential Earthquake Hazards in Urban San Diego, California, California Division of Mines and Geology final technical report.
- 16. Krause, D. C., 1965, TectoniCS, Bathymetry, and Geomagnetism of the Southern Continental Borderland West of Baja California, Mexico, Geological Society of America Bulletin, v. 76, p. 617-650.
- 17. Leeds, A. L., 1979, Relocation of M > 5.0 Northern Baja California Earthquakes using S-P times, Master's thesis (unpublished) University of.California, San Diego.
- 18. Legg, M. R. and Kennedy, M. P., 1979, Faulting Offshore San Diego and Northern Baja California, in Abbott, P. L:, and Elliott, W. J., eds., Earthquakes and Other Perils, San Diego Region, San Diego Association of Geologists for Geological Society of America, Field Trip Guidebook, p. 29-46.
- 19. Moore, D. G., 1969, Reflection Profiling Studies of the California Continental Borderland, Structure and Quaternary Turbidite Basins, Geological *Society of America Special Paper 107, p. 142.
- 20. Reyes, A., Brune, J., Barker, T., et al., 1975, A Micro-Earthquake Survey of the San Miguel Fault Zone, Baja California, Mexico:
.Geophysical Research Letters, v. 2, No.2, p. 56-59.
- 21. Richter, C. F., 1958, Elementary Seismology, W. H. Freeman, San Francisco and London, 768 p.
- 22. Shor, G. and Roberts, E. E., 1958, San Miguel, Baja California Norte, Earthquakes of February, 1956--A Field Report, Seismological Society of America Bulletin, v. 48, p. 101-116.
2.5J-11 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5J
- 23. Thatcher t W. and Hanks, T. C. t 1973, Source Parameters of Southern v
California Earthquakes t Journal of Geophysical Research t v. 78, No. 35 t p. 8547-8576. 2.5J-12 Amended: April 2009 TL: E048000
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Units 2 & 3 GENERALIZED MAP OF NORTHERN BAJA CALIFORNIA PHYSIOGRAPHIC PROVINCES AND DISTINCT GEOLOGIC TERRANE Figure 2.5J-4 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5K EXTENT OF ROSE CANYON FAULT ZONE Site File Copy Amended: April 2009 TL: E048000 Site File Copy
San Onofre 2&3 FSAR Updated APPENDIX 2. SK EXTENT OF ROSE CANYON FAULT ZONE 2.5K.1 BASIS FOR ASSUMPTION THAT THE ROSE CANYON FAULT ZONE DIES OUT TOWARD THE SOUTH IN THE VICINITY OF SAN DIEGO The Rose Canyon fault zone (RCFZ) has been studied offshore, north of Point La Jolla, and southwest of the San Diego Bay (Moore, 1972; Moore and Kennedy, 1975). Faults mapped in these areas have been located on the basis of generally wide-spaced acoustic profiles and inferred correlation with bathymetric relief (for further discussion see section 2.5K.2). More detailed acoustic profile surveys by Kennedy (1979) and by Kennedy and others (1977 and 1978) in these offshore areas have refined the location and current understanding of this portion of the Rose Canyon fault zone. The specific-information developed by Kennedy and others is summarized in table 2.5.K-I. The RCFZ in the San Diego area is characterized in general by a series of structural and topographic highs and lows that include (from north to south): the offshore faults, of the Point La Jolla area (low), the Mt. Soledad area' (high), Mission Bay (low), Morena-Old Town area faults (high), and the San Diego Bay area (low). The southernmost of these alternating features is underlain by the San Diego Basin that is roughly defined' by the down-to-the-west faults of the La Nacion system (Artim and Pinkney, . 1973) and the down-to-the-east faults offshore from San Diego Bay (Kennedy and others,1977).* This structural low, or graben, implies' that the southern portion of the RCFZ is characterized by a widened zone of extensional, rather than compressional style faults, and further suggests that toe sense of displacement on this portion of the RCFZ is dip-slip rather than strike-slip. Faulting along the RCFZ in the area south of the Morena-Old Town is not well defined. Onshore evidence of fault displacement is sketchy. (For further discussion, see appendix 2.5N, section 2.5N;11. The bulk of evidence for faulting at the south end of the RCFZ consists of faults identified by acoustic profiling in San Diego Bay and offshore of San Diego (Moore and Kennedy, 1975 and Kennedy and others 1977). Faults identified offshore are more prominent than the faults in the southern end of San Diego Bay. The offshore faults are also expressed as fault scarps where they come onshore at Coronado (Kennedy and others, 1977). This evidence strongly suggests that a southern extension of the RCFZ is associated with the faulting and extends offshore of San Diego and not to the south through San Diego Bay. In summary, the character of the faulting within the RCFZ changes in the southern part of San Diego and becomes a wide zone of faulting characterized primarily by a dip-slip component. The prominent faults extend offshore to the southwest. Current data indicates that the fault-ing within this wide zone dies out to the south and does not connect to the Calabasas fault or the Vallecitos fault zone. 2.5K-I Amended: April 2009 TL: E048000
San Onofr e 2&3 FSAR Updat ed APPENDIX 2.5K Table 2.5K-1
SUMMARY
RCFZ INFORMATION, KENNEDY (1979 ) AND KENNEDY AND OTHERS (1977 J 1978) (Shee t 1) Area Inves tigate d Summary of Data RCFZ off Point Kennedy and other s (1978 ) mapped a widen ing zone of La Jolla west to north west- trend ing faults offsh ore to the north and west of the mapped faults of the RCFZ on-shore near Mt. Soled ad. The more weste rly-tr endin g faults of this zone were inferr ed to be princ ipally dip-s lip and gener ally to defin e a struc tural low under lying the La Jolla subma rine canyo n. Strat i-graph ic separ ations on the young est faulte d sedim ent (late Pleist ocene to Holoc ene) of these dip-s lip faults were on the orde~ of 9 to 18 meter s. Furth er west J a subzo ne of north -north west trend ing faults was mapped obliqu e to the trend of the La Jolla canyo n. These canyo n. These faults were gener ally disco ntinuo us and appea red*to be overl ain by about 5 meter s of unfau lted Quate rnary sedim ent. The easte rn edge of Kennedy and other s offsh ore zone paral lels the coast line to the 33 N.lat itude *which is the limit of profi ling. Along tbe easte rn ed~eJ - acous ticall y transp arent (late Pleist ocene and Holoc ene) sedim ent was not faulte d althou gh near surfac e disru ption of the Quate rnary horizo n was indic ated. The disco ntinuo us en-ec helon patte rn of the easte rn edge of this offsh ore zone is simil ar to that seen withi n the RCFZ at San Diego Bay. RCFZ off San Detai led acous tic profi ling by Kennedy and other s Diego Bay (1977 ) in the offsh ore region west of ~nd includ ing San Diego Bay indic ated subzo nes of north east to north west- trend ing down -to-th e-east faults . Three of the longe r faults (from north to south : the Spani sh Bight fault , Coron ado fault and the Silve r J Strand fault) were seen to have a promi nent centr al portio n (loca lly expre ssed onsho re in the North Island -Coro ndo vicin ity) that gradu ally died out when traced toward the north or south . No- surfac e displa cemen ts were ident ified in these offsh ore faults J althou gh qispla cemen t local ly exten ds to withi n 5 to 10 meter s of the sea floor. When traced in a south erly direc tion J these faults gener ally become less persi stent and appea r to die out in short en-ec helon splay s. The most south erly fault the Silve r Stran d fault , can be traced to the J vicin ity of the Intern ation al Borde r where it also becomes less persi stent and dies out in sever al en-ec helon branc hes. 2.5K-2 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2. 5K Table 2.5K-l
SUMMARY
RCFZ INFORMATION, KENNEDY (1979) AND KENNEDY AND OTHERS (1977, 1978) (Sheet 2 of 2) Area Investigated Summary of Data RCFZ in San Kennedy and others (1977) also describe a series Diego Bay of relatively short <<3 kilometers long) dis-continuous faults east of the Silver Strand fault in the southern San Diego Bay area. Some of these faults appear prominent on acoustic profiles, but all are short and none displace the bay floor. Some of these faults extend to within to within 5 to 10 meters of the bay floor. RCFZ south of Kennedy and others (1977) conducted gravity, ground San Diego Bay magnetic, and refraction surveys to determine if a proposed trace of the RCFZ crossed the Otay Valley area, south of the San Diego Bay, and continued south across the International Border toward the San Miguel-Vallecitos fault zone SMVFZ (see appendix 2.5J for further discussion). Gravity and magnetic p rofd l.es indicated seve ra I anomalies that could be associated with faults of the L~ Nacion . system, but they are located east of a projected RCFZ-SMVFZ alignment. However, no significant anomalies were recognized on profiles across southeast projections of presently mapped faults in the RCFZ. The refraction data collected in this survey were limited by logistic and electronic difficulties. As a result, it was not possible to de t.ermi.ne unequivocally if the section was faulted (Kennedy and others, 1977). \ ....../ 2.5K-3 Amended: April 2009 TL: E048000
San Onofr e 2&3 FSAR Updat ed APPENDIX 2.5K 2.5K.2
SUMMARY
OF EVIDENCE FOR EXTENSION OF THE RCFZ AND REBUT TAL TO THAT EVIDENCE The works which suppo rt the argum ent that the RCFZ exten ds northw ard to conne ct with the SCOZD and/o r southw ard into Mexico will be discu ssed in chron ologic al order (i.e., (A. Corey , 1954; B. Emery
, 1960; C. King, 1969; D. Wiega nd, 1970; E. Moore, 1972; F. Moore and Kenne dy, 1975) .
Each of these discu ssion s will be follow ed by a brief rebut tal. A. Corey (1954 ) compi led paleo geogr aphic and paleo struc tural maps of south ern Calif ornia and the adjac ent conti nenta l borde rland area to interp ret the Terti ary histo ry of the region . On his "pre-Plioce ne fault trend tl map, he inferr ed that sever al offsh ore faults extend from the Palos Verde s penin sula south , rough ly paral lel to the prese nt coast line, to the onsho re RCFZ area, then contin ue south in the offsh ore area west of Baja Calif ornia . Corey 's repor t deals only with Terti ary sedim entary histo regio nal scale and does not deal with the detai led geolog ry on a one area. He depic ted the Rose Canyon fault as being y of any right - later al with schis t basem ent to the west and grani tic basem ent to the east. Explo ratory borin gs have subse quent ly shown that the Santia go Peak Volca nics form the basem ent on both sides of the Rose Canyon fault (Gray and other s, 1971) . This and the prese nce of the same Cretac eous and Eocen e forma tions on oppos ite sides of the fault indic ate the Rose Canyon fault has little displa cemen t along it; there fore, Corey 's interp retati on is incor rect. B. Emery (1960 ) prepa red a fault map of the sea floor off south ern Calif ornia depic ting a long "p r ima ry fault" trend simil ar to Corey 's but along the base of the slope west of the OZD that contin ued on offsh ore and west of Baja Calif ornia . Emer~ , howev er, notes that the faults are locate d prima rily on basis of subma rine topog raphy . Emery assum es that such the topog raphy is for the most part of struc tural origin . Age determ inatio n of these struc tural scarp s is equiv ocal as "some scarp s on the sea floor that are believ ed to be late Mioce ne age appea r sharp and clear from sound ing data" (Emery, p 77). Thus, althou gh Emery ident ified a topog raphic lineam ent rough ly paral lel but west of the OZD, its locati on lies furthe r offsh ore at the base of the topog raphic scarp and its true chara cter and age are undoc ument ed. C. King (1969 ), in a publi cation of the tecton ic histo ry of North Ameri ca, descr ibed the regio nal tecto~ic settin g of Calif ornia and Baja Calif ornia and discu ssed the existe nce of promi nent high angle , northwest~trending right -later al faults . He dealt speci ficall y with the San Andre as fault in Calif ornia and its relati onshi p to the openin g of the Gulf of Calif ornia . No speci fic refere nce was made to the faulti ng offsho re of south ern Calif ornia . 2.5K-4 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2. 5K D. Wiegand (1970) postulated that a fault underlying San Diego Bay was an extension of the Rose Canyon fault that "may be a segment of a longer fault system which includes ... the San Miguel Fault in Baja California. tI This extended fault zone was inferred largely on the basis of the alignment of discontinuous topo-graphic, structural, and geothermal features in the San Diego Bay-Tijuana region. The geothermal wells used by Wiegand to support a fault in the south San Diego Bay area do not align with his proposed fault. The topographic depressions in the bay floor, used to support a proposed fault aligwnent, are underlain by tlslump sand ll of different character from the surrounding sediments, according to Wiegand (p 112). It seems quite likely that these are disrupted sediments resulting from liquefaction rather than a sag pond depression. This area could also be a drainage channel preserved on the bay floor from a lower stand of sea level. Weigand notes faults which are transverse to the proposed fault alignment in San Diego Bay. He suggests that the general quiescence of the Rose Canyon fault zone may be the result of these transverse faults locking off the northwest-southeast trend. It is also noteworthy that Kennedy and others (1977) surveys of the South Bay area did not identify anomalies suggestive of a southward extension of a fault through this area, but rather of a south-southwesterly trend into the offshore area west of
~atl. Diego Bay..
E. Moore (1972) proposed an offshore extension of the Rose Canyon fault north of Point La Jolla based on generally wide spaced acoustic profiles. He acknowledged that the location of the Rose Canyon Fault 1Iis less certain to the southeast beyond San Diego Bay" and only suggested that the Rose Canyon fault might follow the Tijuana River Valley to connect further south with the San Miguel fault. A review of the data in the border area, as discussed in appendix 2.5J, indicates that this proposed connection is incorrect. F. Moore and Kennedy (1975) mapped several faults within and to the southwest of San Diego Bay on the basis of acoustic reflection profiles. The indicated fault pattern suggested that the Rose Canyon fault zone broadens and becomes en-echelon at the San Diego Bay area, roughly defining the west side of a structural low. This portion of the zone is char~cterized by normal down-to-the-east faulting. Their survey found the strongest evidence of faults extending southwestward across the north San Diego Bay area and offshore to the southwest, rather than to the south-east. Their survey .also identified diminishing evidence of faulting to the southwest suggesting that the RCFZ dies out in this direction near the international border. It is the Applicant's position that this interpretation represents the most probable projection of the RCFZ into the offshore area and that it further supports the lack of continuity with the Vallecitos or San Miguel fault zones. 2.5K-5 Amended: April 2009 TL: E048000
San Onofre 2&3 FSAR Updated APPENDIX 2.5K REFERENCES
- 1. Artim, E. R. and Pinkney, C. J., 1973, La Nacion Fault System, San Diego, California, Geological Society of America Bulletin,
- v. 84, p 1075-1080.
- 2. Corey, W. H., 1954, T~rtiary Basins of Southern California, in Geology of Southern California, California Division of Mines-and Geology Bulletin 170, Chapter 3, p 73-83.
- 3. Emery, K. 0., 1960, The Sea off Southern California, John Wiley and Sons, New York, 366 p., cited in Albee, A. L. and Smith, J. L., 1966, Earthquake Characteristics and Fault Activity in Southern California, in Lung, R. and Proctor, R., eds., Engineering Geology in Southern California, Association of Engineering Geologists Special Publication.
- 4. Gray, C. H., Jr., Kennedy, M. P., and Morton, P. K., 1971, Petroleum Potential of Southern Coastal and Mountain Area, California, American Association of Petroleum Geologists Memoir 15, p 372-383.
- 5. Kennedy, M. P., 1979, Recency and Character of Faulting Offshore from Metropolitan San Diego, California--U. S. Geological Survey Contract No. 14-08-001-17699, U. S. Geological Survey, National Earthquake Hazard Reduction Program, Summaries of Technical Reports,
- v. 8, December, p 27-28.
v
- 6. Kennedy, M. P., Bailey, K. A., Greene, H. G., and Clarke, S. H.,
1978, Recency and Character of Faulting Offshore from Metropolitan San Diego, California, California Div.ision of Mines and Geology Final Technical Report.
- 7. Kennedy, M. P., Welday, E. E., Borchard, G., Chase, G. W., and Chapman, R. H., 1977, Studies of Surface Faulting and Liquefaction as Potential Earthquake Hazards in Urban San Diego, California, California Division of Mines and Geology Final Technical Report.
- 8. King, P. B., 1969, The Tectonics of North America, U. S. Geological Survey; Professional Paper 68, 94 p.
- 9. Moore, G. W., 1972, Offshore Extension of the Rose Canyon Fault, San Diego, California, U. S. Geological Survey Professional Paper BOO-C, p 113-116.
- 10. Moore, G. W,. and Kennedy, M. P., 1975, Quaternary faults at San Diego Bay, California, Journal of Research of the U. S. Geological Survey, v. 3, No.5, p 589-595.
- 11. Wiegand, W., 1970, Evidence of a San Diego Bay-Tijuana Fault, Association of Engineering Geologists Bulletin, v. 7, No.2, P 107-121.
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