ML19319D702
| ML19319D702 | |
| Person / Time | |
|---|---|
| Site: | Crystal River, 05000303  |
| Issue date: | 08/10/1967 |
| From: | FLORIDA POWER CORP. |
| To: | |
| References | |
| NUDOCS 8003240694 | |
| Download: ML19319D702 (22) | |
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t APPENDIX 2F V) GENERAL GEOLOGY - REGIONAL TECTONICS 1 JNTRODUCTIOU This report tets forth the results of a literature search designed to outline the general 6eology of the State of Florida, the history of diastrophism and the influence of these elements upon the structural integrity of the geology at the preposed nuclear powered generating facilities at the Crystal River Power Plant of the Florida Power Corporatien. Eeference to puolished sources is made in the text and sources are listed alphabetically in the Selected References follcwing Appendix 2G. 1.1 GEOLOGY OF FLORIDA 1.1.1 SURFACE GEOLOGY The Omnediate surface at mest places in the State is underlain by Pleistocene deposits , of which two principal kinds are recognized. The most widely dis-tributed is a series of ". . . littoral, sublittoral and estuarine sandy formations corresponding to . . .different stages of sea level." "The other kind, which underlies the east coast and the souchern part of the State is divisible into three contemporaneous marine formations. . ." (Cooke,1945); these are composed of marine sediments constituted by a coquina, an oolite, and a coral reef facies. Interspersed throughout the Pleistocene formations aro Recent marine sediments along the coasts which are composed of quartz sand with local broken shell admixtures as far south as Cape Romano on the west coast and Miami on the east coast. Wind blown sand is added to a white limy ooze which is accumulat-ing along the remainder of the coast line. Continental deposits of silt and sand are being deposited in tidal areas and along rivers. Muck and peat deposits are accumulating in shallow lakes , ponds and swampy areas. "A kind of travertine or caliche locally forms at the surface in southern Florida" (Cooke 19h5). 1.1.2 SUBSURFACE GEOLOGY If the surface were denuded of these Recent and Pleistocene deposits, the whole of Florida-would be represented by Tertiary Formations , oldest of which would be the Avon Parx Limestone of late Middle Eocene Age (Cooke, 19h5). This oldest -lithologic unit is exposed in Citrus and Levy counties just a few miles from the Crystal River Plant Site. All of these Tertiary sedimentary rocks of Peninsular Florida are pre-dominantly allochemical limestones which are in part dolomitized. North of a line drawn between Levy and Nassau counties the sequence of sedimentary rocks is constituted basically by clastic sediments (Pressler 1947). The plant site is located in the zone of allochemical carbonates. p) q. 0345 2F-1
Underlying Tertiary rocks and resting upon a post Pale: sie erosional surface are the m arine limestones and clastic rocks of Cretaceous age, g The thickness of thi; sequence of Cretaceous and the overlying Tertiary sedimentary rocks is variable throughout the state, ranging from less then 3,500 feet around Gainesville to more than 13,000 feet as vn on Figure 2F-1. From the same reference, the thickness o f the Cre ,aceous and Tertiary sedimentary rocks at the Crystal River Plant Site is approximately 5,000 feet as substantiated by Vernon (1951). The framework of sedimentation for the Cretaceous rocks is roughly given by the PRI'-MES0 ZOIC contours shown on Figure 2F-1. This south-southeasterly treading high was not completely covered by lover Cretaceous sedirents, as it constituted.a positive area during early Cretaceous deposition. This structure is called the Peninsular Arch and forms the backbone of the Florida Peninsula. Little is known about its structural elements or its stratigraphy except for Ehe spotty information obtained from deep exploratory oil wells. This data substantiates the fact that the Peninsular Arch was formed after deposi-tion of Paleozoic sediments and possibly after, or contemporaneous with, the intrusions of Triassic diabase. The areal extent and relationship of the surface exposures of the Tertiary and Quaternary Systems of rocks are shown on Figure 2F-2. 1.2 POST PALE 0 ZOIC HISTORICAL GEOLOGY In general, the post-Paleozoic historical geologv of the State can be sum-anarized as consisting of non-catastrophic periods of deposition and erosion which were regulated by n% mal tectonic adjustments of the earth's crust in a foreland area. Following deposition of Paleozoic sediments and possibly as early as post-Silurian, the Florida Peninsula is thought to have experienced no sedimentation until the early stages of the Cretaceous. Possible intrusion of diabasic material, which is accorded a Trir.ssic age, is thought to have occurred, however. Upon the framework of a quaquaversal seaward dipping peninsula, recognized and termed the Peninsular Arch (Applin 1951) a thick sequence of basically marine carbonate sediments were deposited as the Peninsular Arch slowly subsided beneath a slowly encroaching sea. "Only the northern part of Florida was emergent. It was otherwise a platform, and with the Bahama platform made up a large region of carbonate deposition and slow subsidence," (Eardly, 1962). The depositica of marine carbonate rocks continued throughout the late Cretaceous as Florida progressively sank. Data from oil exploration holes reported by many authors substantiates a rather non-descript period of marine carbonate deposition throughout the . remainder of Cretaceous time and well into the Tertiary. OM6 g 2F-2
/7 Chen (1965) perforc2d a regional lithostratigraphic analysis of Paleocene V Eocene rocks of Florida which substantiates that carbonate deposition was prevalent up through the Eocene. Vernon (1951) states, that the peninsula of Florida was covered by shallow marine waters throughout the period extending from the Pliocene to the Recent, except for brief periods when it stood as land and was weathered and eroded. As reported by Cooke's (19h5) stratigraphic column (Fig. 'F-3) deposition was interrupted by nine eresional periods during the cov- 3 of the approxi-mately 1h5 million years taken for the deposition of the sequence of Lower Cretaceous through Pliocene rocks ; which, except for the Cretaceous , Paleocene , and Lower Eocene, compose the outcroppina formations of the State. After the latest unconformity (most important to the study), representing an erosional period about 45-50 million years ago, the remaining Tertiary history of sedimentation affected the site very little. According to Vernon (1951) a structural high developed just east of the west coast of Florida prior to Fiocene time to which Vernon says the U. S. Geological Survey had applied the name "Ocala Uplift" as early as 1921. This structure has been influential in establishing the existing subsurface geology at the Crystal River site as will be discussed later. The devalopment of other structures in the State occvrred during Tertiary time, but discussion of this is likewise reserved to a later paragraph. Following the development of the Ocala uplift, intermittent marine sedimen-tation occurred throughout the -remainder of the Tertiary period.
\ Following the Tertiary however, the effects that Pleistocene glaciation had upon the elevation of the strand line are of value. Sea levels are reported to have existed at elevations of 220, 150, 100 to 105, and 25 to 30 feet (Vernon,1951) based on occurrence of stream terraces and correspond-ing elevations of old coast lines. Vez. ton's correlation of FJcrida Pleis-tocene terraces is presented in Figure 2F-h.
Regarding the low elevation of eustatic adjustment in response to the ac-cumulation of glacial ice, Cooke (1945) feels that the sea dropped to eleva-t'.ons 200 feet lower than present day values. As substance for this state-ment, he offers evidence of the development of solution phenomena to -200 foot elevations. Such a statement precludes the possibility that the solution of limestone can occur below base level, an interpretation which is thought to be inconsistent with present thinking (W. H. Back, 1963). At any rate , the Floridian platform terminates at a depth of 50 fathoms (Cooke 1943) providing support for a lowering to at least -300 feet. This lowering, however, was not confine.d to the Pleistocene epoch, but rather has been in evidence throughout much of Tertiary time (Chen 1965 and Cooke 19h5). The depositional sequence of the Pleistocene as su=marized by Figure 2F-k and the progressive emergence of the Florida Peninsula stfostantiated by the successively 1cwer terrace elevations is attributed by Vernon (1951) ". .. to be associated with the thick' alluviation of the Gulf of Mexico, principally by the Mississippi River, and adjustment to this alluviation." More than
,s one million tors of sediments per year are being deposited in the Gulf of
( .) M (Grabau 192h).
%exico by the Mississippi River
. 0347 2F-3
Most significant is the fact that marine sedimentation was curtailed by progressive emergence of the Florida peninsula throughout Pleistocene time, Recent continental sediments (as described in Surface Geology of this appendix) g have accumulated on the peninsula to the present time. The nature of the layered rock subsurface, as described above, has been modified throughout much of Florida by action of slightly acidic groundwater upon the ,arbonate-rich sediments which has produced a network of solution channels, sink holes , and karst features. The extent of this solutioning, the expected intensity of the process in the future, and the effect of the process upon the structural stability of the plant are discussed in Appendi. 2H, " Bedrock Sclution Studies." 13 IDCATION OF TECTONIC ELE!ENTS A considerable quantity of geophysical data has appeared in the literature which infers structural trends in the magnetically heterogeneous rocks con-stituting the pre-Mesozoic " backbone" of the Floridian Platform (Chen,1965). The configuration and areal distribution of the rocks composing the Peninsular Arch are shown by Figure 2F-5, as proposed by Applin (1951). The association of the "relatively undisturbed Paleozoic strata (Eardly, 1962) of the Peninsular Arch with Ouachita and Applachian systems have been the subject of considerable discussion and presents provocation for ceademic thought. Most important to this study, however, is the fact that this south-southeasterly trending core of pre-Mesozoic rocks has provided a relatively stable nucleus for the superjacent marine carbonate sedimentation of the Mesozoic and Cenozoic Eras (King 1951). The whole of the Florida Platform extended into the Bahama Islands and is believed to have remained g as a stable foreland to the Antillean deformed belt of Cuba (King 1951). Puri and Vernon (1964) vividly set forth the structur 1 framework of the Floridian Platform. The location of the tectonic ele..ents of Florida and in particular those which have influenced structural evolution of the sub-surface of the Plant Site are shown by them on Figure 2F-6. A summary of these principal structures of the State is presented by Puri and Vernon (196h) as follows : 1.3.1 PEUINSULAR ARCH "This dominant subsurface structure forms the axis of peninsular Florida, and the arch trends south-southeast and extends from southeastern Georgia into central Florida and crests in the center of northern peninsular Florida around Union and Bradford counties ( Applin 1951, p. 3). This structure was a topographic high during Cretaceous time, and sediments of early Cre-taceous age were deposited around it - but did not completr cover it. Beds of Austin Age (upper Cretaceous) were deposited over tue crest of { .,. thic Paleozoic arch, where they ove-lie Early Ordovician sandstone." 2F-4
1.3.2 BROWARD SYNCLINE "A subsurface, local feature named by Applin and Applin (1964, Ms. ) for a Cretaceous syncline in Broward and Paln Beach counties. '*he synclinal axis is UW-SE, and approximately parallels the inner edge of the South Florida Shelf." 1.3.3 SOUTH FLORIDA SHELF "A term used by Applin and Applin (1964, Ms. ) for a shallow area, which includes parts of Charlotte, Sarasota, Hendry, Glades, Palm Beach, Broward, Monroe counties, and all of Lee, Collier and Dade count'.es. The boundaries generally parallel the axis of South Florida embayment." 1.3.4 SUWANNEE STRAITS "The name Suvannee strait was first used by Dall (1892, p.111) to define an area 'which separated the continental border from the Eocene and Miocene Islands' in which the argillaceous sediments of the Hawthorn vere deposited. He thought that the area north and west of the straits was indicative of much deeper water because the sediments contained less clay and a well developed Miocene fauna. Dall (1892, p. 121-122) included in the Strait the Okefenokee and Suvannee Swamps and the trough of the Suvannee River and estimated its vidth to 've less than 50 miles. Vaughn (1910, p. 160) discussed Suvannee straits and cited Dall's evidence for the erosion of sediments of Miocene age in the Straits. Applin and Applin (19hh, p. 1727), while discussing structures of Florida referred to 'a channel or trough ex-tending southwestward across Georgia through the Tallahassee area of Florida to the Gulf of Mexico. ' The same structure is recognized by Jordan (1954) as an erosional feature in the subsurface, which resulted because the re-gional movements in the c lose of the Cretaceous time caused a e hannel to be formed along the transition zone connecting the predominantly clastic and carbonate facies of the Cretaceous. This feature is considered by Hull (1962, p. 118-121) to represent a narrow area (20-30 miles in vidth) of non-deposition, rather than an erosional channel that traverses over 200 miles of territory. Whatever the cause of this channel, it has affected deposition of both Mesozoic and Cenozoic sediments."
"The strait is considered by Applin and Applin (196h, Ms.) to be a saddle that is much wider and larger in area than visualized by earlier authors.
The strait is considered by the Applins to form the southern limit of clastic beds of Navarro Age (?) on the north and northern limit of Lawson Limestone on the south." 1.3.5 OCALA UPLIFT
" Adequately documenced by Vernon (1951, The anticline, pp. 54-58), is a gentle flexure of Tertiary age, about 230 miles long and 70 miles wide, where ex-posed. The crest trends northwest-scutheast and is extensively fractured and faulted. High-angle, strike faults flatten the crest and increase its cross-section., The anticline merges inconspicuously into several noses and
,A (~) n . . 0349 2F-5 7
troughs along the plunge and to each side. Murray (1961) thought the Ocala uplift was only a time and space variation of the Peninsular arch, but lon6 periods of erosion and deposition separate distinctly datable structures , and geopbysical data presented by Antoine and Harding (1963) justify the separation of the two structures." 1.3,6 KIESIMEE FAULTED FLEXUPE "This structure is a fault-bounded, tilted and rotated block that includes many small folds , faults , and structural irregularities. The southern part appears to be an anticlinal fold trending vest-northwest-east-south-e as t . The structure was erected by Vernon (1951) for a positive area extending down the center of the Peninsula and as additional data becomes available, io vill be possible to more accu ~ately define the structure." 137 THE SAUFORD HIGH "A half dome in the vicinity of Sanford, Florida, was first described by Vernon in 1951. The structure appears to be closed fold that has been halved along the fault that bounds the Kissiemee faulted flexure. The other half may be represented by the fold in the distal end of the Kissim-mee faulted flexure. Miocene sediments have been deposited upon the croded Inglis Formation and the remaining Ocala Group and Oligocene sedi-ments have been removed." 1.3.8 THE OSCEOLA IDW "One of the most prominent features of magnetic and gravity maps of the Stata coincide with a poorly defined structural low, centered in Osceola County. Vernon (1951) interpreted the str 'eture as being bound by steeply dipping faults. More information is needed to more adequately define the structure, but the resulting basin is filled by Miocene sediments and dis-placements of as much as 350 feet occur between wells to the north and east and those within the structure." 1.3.9 CHATTAHOOCHEE AUTICLIUE "Chattahoochee anticline was first used by Veatch (1911, pp. 62-64) for a broad flexure in the tri-state area of Georgia, Alabama and Florida. He mapped the structure on exposures of Cretaceous mud Eocene rocks along the Chattahooch?e River in southwestern Georgia and from the inequalities of drainage divides of the Chattahoochee and Flint rivers. Veatch thought that the shorter tributaries of the larger Chattahoochee River were devel-oped along the crest of an anticline and the much longer tributaries of the Flint River were formed on the eastern flank of the anticline. The crustal movements which caused this arch were dated by Stephenson (1928,
- p. 295) as late Tertiary or early Quaternary. Applin and Applin (19hh, p.1727) mentioned an upwarped area around Jackson County, 'with dips extending away frcm it towards the southeast, south and southwest. ' Pres-sler (19h7, p.1852, fig.1) refers to the same feature as 'Decatur arch.'"'
O 0350 2F-6
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" Jordan'(1951, p. hk) refers to the Chattahoochee arch as a second Paleozoic high, and it is a prominent feature en a structure map on the top of the pre-Mesozoic rocks. This structure is an elongate anticline that trends northeast-southwest and crests in Jackson, Holmes, and Washington counties. This upwarp is primarily responsible for the exposures of upper Eocene, Crystal River For-mation in these counties."
Earlier work by Applin and Applin (1944) provides the following more general description of the chief structural features of Florida.
"a. An axis extending northwest from about Cape Canaveral on the east coast of Florida to south-central Georgia, upon which are located two large locally high areas ;
- b. a channel or trough extending southwestward across Georgia through the Tallahassee area of Florida to the Gulf of Mexico, nearly at right angles to the aforementioned axis ;
- c. an upwarped area in the vicinity of Jackson County, Florida with dips e:. tending away from it toward the southeast, south and south-west.
- d. A structurally lov area with an axis extending northwest from the vicinity of L. Okeechobee toward Tampa, approximately parallel with the axis first mentioned.
O e. A possible second north-west-trending upwarped area at the south end of the peninsula." The earlier work of Applin and Applin was developed from less subsurface data, but essentially conforms to the refined structural delineations made by Puri and Vernon (196h). In addition to these structures common to the State of Florida, Jordan (1951) has considered that a steep escarpment on the west edge of the Floridian Platform (approximately 100 miles vest of the Gulf Coast) represents a fault scarp which would of neceasity represent considerable displacement. However, Miller and Ewing (1956) logically attribute the escarpment to nomal sedimen-tary processes, as they found no magnetic or seismic data to substantiate the existence of such a fault. The seismicity analysis presented in Appendix 2-I likewise found no evidence of seismic activity of the west coast of the penin-sula. l In considering the influence of the principal structures outlined upon the structural integrity of the local geology, only the features related to the Ocala uplift are of importance. In 'this regard, we are then confined to the discussion of the structures which constitute the Ocala uplift as depicted by Vernon (1951) en his structural contour map of the top of the Inglis Mem-ber of the Moodys Branch Formation (Figure 2F-7) as t'.ey occur in Citrus l County.
- j. Detailed subsurface and surface studies revealed that the Ocala uplift is in j reality not a simple elengated doubly-plunging anticline but more positively s/ explained as a faulted brachyanticline, l i 2F-7 ()] I
Vernon (1951) describes the Ocala uplift in detail as follows:
"These sections and the structure map, Plate 2, (Figure 2F-7) indicate that O the Ocala uplift developed in Tertiary sediments as a gentle flexure, approx-imately 230 miles long, and about 70 miles wide where exposed in central pen-insular Florida. The anticline is composed of two well-defined shallow folds ,
the more westerly being higher structurally, see Figure 13 (Figure 2F-8) and Plate 2 (Figure 2F-7). Along the Florida-Georgia State line the east fold is separated from the west fold by a shallow trough, 54 miles wide. The folds converge southward and in Levy and Citrus counties they are separated by only a few miles and their crests are extensively fractured and faulted. The crests trend northwest-southeast through Levy and Citrus counties , but in Sumter, Orange and Polk counties they diverge, the east fold merging with a large fault block, named in this report the Kissimmee faulted flexure, and the west fold continuing in a south-southeasterly direction and gradually merging with the regional dip."
"The development of vertical dip-slip faults , the traces of which parallel the crest of the Ocale, uplift, tend to flatten the crest and to lengthen its cross-section. From the limited core hole evidence available for this study the dip of the fault planes could not be detemined, nor was it pos-sible to estimate the extent of faulting at depth. There are numerous possibilities , one fault may teminate at depth against another or it may cross to fom a graben and horst structure. Figure lh (Figure 2F-9) is one interpretation of the geologic section along the proposed Florida Ship Canal (Cross Florida Barge Canal) and here a graben and horst structure is clearly indicated. The fault planes are drawn in at angles greater than 60 degrees and may be steeper. They are thought not to dip at angles less than 60 degrees because of the straight-line traces of the faults and because the closely spaced core holes do not penetrate any thinning or thickening of the beds."
The other associated structures (outline by Vernon and Puri) are remotely located with respect to the site, and the major defomation feming them is established as occurring during the post-Oligocene pre-Miocene interval, with minor adjustments occurring into the Pleistocene. Consideration of their affect upon the structural soundness of the site is unwarranted. According to Cooke (19h5), "There is no evidence that the rocks composing the outer layers of the Flo*idian Plateau have ever undergone extensive defomation. " Referring to the movement of Ocala arch, Cooke (1945) says , "The arch was above water in early Pliocene time, as is shown by the presence of land mammals of that age in the belt east and south and presumably west of the land area. The tilting that depressed the western centinuation of the belt presumably was contemporaneous with the crustal movements that deformed many other parts of the earth at the close of the Pliocene epoch. All of the deformation seems to have occurred before the Pleistocene epoch, for even the oldest Pleistocene shore lines, so far as they have been traced, remain hori zontal . " 2F-8
I The northwest trending structural lineament of horst and graben, faulting as shown by Vernon (1951) on Figure 2F-7, defines the axis of the Ocala uplift proper. Prior to his publication, faulting had not been recognize 1 in Florida. In association with this uplift and faulting, a well defined northwest trending fracture system developed, the genesis and orientation of which is described by Vernen as shallow tensional fractures paralleling the northwest trend of the Ocala vplift, and in part caused by the Ocala uplift deformation. Also, adjustment of the great thickness of unconsoli-dated Tertiary sediments over the stable pre-Mesozoic land mass could account for development of such fractures. Also, "... Because of inequalities in these forces (forces responsible for the Ocala uplift) secondary tensile stresses are developed at right angles to the primary tensile stresses. Thus tensile fractures would be most strongly developed along the axis of any folding and along the axes of flank bulges (Vernon, 1951)." Such a combination accounts for the strongly developed northwest trending fracture pattern and the perpendi-cularly oriented minor northeast trending pattern. Regarding the faulting mapped by Vernon as it applies to the Plant Site, reference is made to Figure 2F-10, which has been reproduced after Vernon. Data obtained from exploration and construction of the Cross Florida Barge Canal indicates that movement on steeply dipping (probably greater then 60 ) normal faults have produced vertical displacements of 20 to 160 feet, Figure 2F-9. The closest mapped fault to the site has had its northwestern terminous about three miles east of t he site. No faulting has been mapped () or was revealed by the detailed studies (discussed in Appendix 2G) of this investigation. Most significant in terms of the structural competence of the Plant Site as affected by Tectonic history are the facts that:
- a. Stability of the Florida Peninsular has been predominant throughout the Mesozoic, Cenozoic, and Recent Eras.
- b. Regional tectonic elements are those common to a stable foreland.
- c. Faulting (not recognized in Florida before 1951) is restricted o to reFional structures such as the Ocala uplift and is dated to be at least one million years old. (pre-Pleistocene)
, d. No faulting is mapped within a distance of three miles east of the reactor buildings.
- e. Regional structures (the Ocala uplift) causing the faulting exist east of the site. No faulting has been mapped west of the reactor buildings.
i
- f. Faulting was not disclosed by detailed subsurface studies at the site.
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. 0353 2F-9
It is therefore concluded that the site is located on structurally competent marine sedimentary rocks which have only been subjected to minor regional diastrophism which has been inactive for approximately the last one million g years . G t 2F-10
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a y$ 't .< e' V- _ ~ . rs .- ,,, b f, GEOLOGIC MAP OF FLORIDA = s __ - CRYSTAL RIVER UNITS 3 & 4 ., f I I I l ,,_ - w- -- ... - w ;=. FIGURE 2F 2 , L s . I-m 4 i GEOLOGY OF FLORIDA-GEOLOGIC FORMATIONS FLORIDA (E Grot.ocic Fomanoss in F ominA G r. z Erosion interval. Lake Flirt merl (fresh. water, partly .c$ $3 -~- EE% g Recent). zU
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- 8 I5 3 g Erosion interval. Fresh. water limestone in the b .j g'j*c g f ,
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3x3xry I V r%" ( r . ._. 0358 ( L_m o u ,. . i..... s.ua a., u. 4 e i v.a u n. w ,. , n? 2 y, Erosion interval during e riy Yorktown time. 8 g wd Alurri Blud group: Shoa! River formation (marine). o ,i! w X "G H dH Chipola formation (marine). I M y% e M' Hawthorn farmation (mirine). E $ Fag Tampa limestone (marine, of Anguilla age). ; g [ .** c; a Erosion interval. E q .re > z Suwannee limestone (marine). Flint River formatior. (littoral, of Antigua age). 3 m ~ 0" 8IE M dE 35 Eros:on interval. Byram limestone (marine, of late Vicksburg age). 5! m f {{ g j* h!arianna limestone (marine, of early Vicksburg age). 5 h < g Erosion interval during Red Bluff time. g C w Ocala limestone (marine, of Jackson age). 2 H Erosion interval. g 4 $= Avon Park limestone (marine, of Claiborne age). 2 % d2 Tallahassee limestone (marine, of Claiborne age). ~ s z j$ Lake City limestone (marine, of Claiborne age). d Erosion interval. k Oldsmar limestone (marine). Salt hiountain limestone (marine, of Wilcox age). ] ,a* wz w gw2 Cedar Keys limestone (marine). Porters Creek formation (marine, of Afidway age). =. 8 m i I CRETACEOUS SYSTEh! PRE.CAh1 BRIAN CARBONIFEROUS TRIASSIC SYSTEh! SYSTEh! SYSTEh! COMANCHE SERIES O O m m O F M F F* F o F* 5 E E 5' 5 5,' F h a x - a m n
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/ ' AFTER APPLlH,1951 S TRUCTU R A L GEOLOGY OF NORTH AMERIC A AN D EDITION
- E A RDL E Y , les2 CONFIGURATION AND DISTRIBUTION OF PRE MESOZOIC ROCKS CRYSTAL RIVER UNITS 3 & 4 0361 O_= != FIGURE 2F-5 er v
O CHATTAHOOCHEE 1 j ANTICLINE 7'p/ - , 3OOTHEAST GEORGIA ' g' g, '. MBAYMENT ' ,e" =;a .* , . td, N T r= ~1 *'a s f_ a-, . . , n. ) i , ( ' ..- f, , f fk ' ..., [ . .h .h' GULF OF MEXICO [ ...]EylN ULAT g .* SEDIMENTARY 7 / Ag r.:.h* -
- L ARCH,-, .
KISSIMMEE c ,j e )--k# 79 y0 ,,,, FAULTED FLEXURE . g );, -,- , ... a " - = .y . .\ / BASINAPALACHI O(At.\ EMBAYMENT ?. , n t ' - C'CALA ,._ .< \ t **"SANFORD HIGH -f 7 :: - r UPLIFT * , . Oh/ ~ # - I, AREA OF f - - *" , ":-'.r RYSTALLINE j NORTH GULF COAST PROCKS SEDIMENTARY f / . ' * " '. ;1 ' - " ' . " - ' ., k PROVINCE g -- , ,3 A e FLORIDA .j OSCE5 ' - / PENINSULA 4 _ _ a . , LOW " **" u / ' SEDIMENTARY ....... : ...... i m' -s f PROVINCE =-: - - - . X ""]{ ,: 'fT.....'.Q q."~ > , O, ,' ?' 'f .. %. . . . . . . c. .""(N, 's - ROWARD N.. .. ' SYNCLIN , 3. , gg a; % $g\.. ]W(.'{ ,. i- 1/ g f
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- g. ,p, 1-TH FLORIDA v- EMBAYMENT FLO RID A GEOLOGIC AL SURVEY SPECI AL PU BLIC A TION e5 PURI& V E RN ON ,196 4 INDEX TO PRINCIPAL GEOLOGIC STRUCTURES IN FLORIDA CRYSTAL RIVER UNITS 3 & 4 0362 gi =-- _
ei uRe 28 6 l P o 1 i \ G E O R G r- - - - , - _ - . . . . . _ l A y, : .' --- } I 1 l % , % s f ' o t --, N, . .. , , l ~ ' [ - 8 , ., ) / . ~ ~ .5 ( , p-l g'( 'y o / Lf c c 'o I o i o l l\ h c. <, t . , . . ' . . . , l_ , e ,. ; f -- , & b ' ' ,a o , s e' y.>;+. : a' -@ y , e,, '\,' r i ., STRUCTURE MAP O ICRY$TALIilVERk ~ l s P L AN T 5\T O; - Or THE INGLIS MEMBER, M # \N ~, k 0 MOODYS BRANCH og FORMATION 4 CoMove ic'eevol 50 Feet - +50 Elevates above seaievel 50 Elevations below seaievel m u O e Inglis member, Moodys Branch , formation, control well \
- Inglis member eroded k'
- Inglis member obsent I g --,--- ----- ---
-- Eroded Inglis mbr. , Uneroded Inglis mbr. e -d , g ^ d g Outcrop of Avon Park timestone, and . b creas where Avon Park limestone is d covered by Miocene with intervening beds being obsent (l , l . ..... l 0363 t ( ,N'. * { Y %-p a + , p , 1 ( , '.. f( \ l , $," ,n , , . 'v y I , g ) 2
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~- o io no no * .a. CRYST AL RIVER UNITS 3 & 4 .csriaetra arvisco uses 0001 ( j .I 7 7 7 i, 7 i-E m _o - .a as a>3ntwa==2 ' r y, .- , . . . v . . . ; . => r n - 2 a 5 fo - Si IE 55 E. I. !. !. !. !. - !. u u i I r ?K A; f IN N s M ~" n.-4 S- t,- - 8 s~ y-c -cv an ,,,s. . -:s. e c L. E. < , '7..- m, n, m, n, . M, ee e e 4 e I e I e e i c i 3 I ; post wgat , h y 14;a_pJ+~rvb _ .3 - &:;aegna a .< . s- - c c .g .ee t 3: 4-F. g . E- ... . T* '(c . . 0002 \ P ' Y ' - ' Y $ $ .. T l a ,i i. i. i. i. i. : . i. i. i. : . . n. . : . , as se e as b L m. __ k Lt.140 ), # t -O se.e O mO ** O O eO l3_ g . .~_ . - - .a = vT Y 1 Y ? p h! 'I) !. !. . "f !. !. !. !. !. !. !. . !. !. !. !. , 7 3
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D' g" : @ . w, - t -t% a l Series of geologic sections crossing Florido approximately w and illustrating significant structures in the Ocolo upfift. ._0004 '~ a 4 - l A' f h! ! h b :!! !! !! !_! ! !! ! ! ! !I !! I -. ( S m Q , paw-oa.%p,-C % rr3% f Mw~ _ "i np%,g , m. i=J ~~ ~~ ~ ~ ~ ~ ~ ~ ~~ ~ %u ~~ = _, mu==,- 1._,_..__ & ---~ * - _ s 'N -( -- N N? x :i 1 mc ,T ~ Frw - KQ' %. r - 7 7 7 T T r T 7 - ! ! ! . I, ! ! !!! !! ! ! ll!!!!N ! ! ! I I , , . , _ i "" I ' 8- " c ______________; '4weg A -e-c% :- ( P j p, < % g,_ _ k g _ i - %y = _ n- .. , - N % -~I- ~~%u vu~.s m_ ~ N r - r r ; - - -- - r i i i ! ! !) I !! I! 1 ! l l 1 ,.', a ~- m .. w- - - _ ~ - - ' - wf . - _fQ l N"_ _" n __ m . ._.'- ~ * --- r T ? . _ _ _ _ _ l I D' AA I AA ') d . - x==. N...~'---- 1-- t-4 ==. %_ .-= - ____. w - r L J- we, MF__., . [V~- -- , __ _ _ _ _ _ ___M_ [ ;;;- ~" [%d,., ~**** - -kNx ruonion orc tocic so,vev CROSS FLORIDA BARGE CANAL BULLE 'IN eSS '5"" * '"' CRYSTAL RIVER UNITS 3 & 4 =._ eiGuaE 2r.,1 0005 t h _=4 ' N1 3 x - u ..> -- -v: * 'b /- { *r w $l Eg-a : 4 supm9 E 5 %' , ' ~ ,fs ed % 9/ p.O g Tr;?" E dh T' M X ' ;' *l W LQ1^Yfb -(k r l I IIC. U3 h ?[Uh'M'h p ' I i . k' h1,WN-Njt 'T" 4Y, g {'Yt 91 il L _ $$bl b k Y[ - .- f. 'IN fWik'J!VM-' j ~?] - ,8 .[ /-I - [ " ,N, " , _ s. ].(g, . b .'fk.
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