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GENERAL GEOLOGY - REGIONAL TECTONICS

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t'' APPENDIX 2FV)

GENERAL GEOLOGY - REGIONAL TECTONICS

1 JNTRODUCTIOU

This report tets forth the results of a literature search designed to outlinethe general 6eology of the State of Florida, the history of diastrophism andthe influence of these elements upon the structural integrity of the geologyat the preposed nuclear powered generating facilities at the Crystal RiverPower Plant of the Florida Power Corporatien. Eeference to puolished sourcesis made in the text and sources are listed alphabetically in the SelectedReferences 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 Pleistocenedeposits , of which two principal kinds are recognized. The most widely dis-tributed is a series of ". . . littoral, sublittoral and estuarine sandy formationscorresponding to . . .different stages of sea level." "The other kind, whichunderlies the east coast and the souchern part of the State is divisibleinto three contemporaneous marine formations. . ." (Cooke,1945); these arecomposed of marine sediments constituted by a coquina, an oolite, and a coralreef facies.

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Interspersed throughout the Pleistocene formations aro Recent marine sedimentsalong the coasts which are composed of quartz sand with local broken shelladmixtures as far south as Cape Romano on the west coast and Miami on theeast 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 siltand sand are being deposited in tidal areas and along rivers. Muck and peatdeposits are accumulating in shallow lakes , ponds and swampy areas. "A kindof 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, thewhole of Florida-would be represented by Tertiary Formations , oldest ofwhich would be the Avon Parx Limestone of late Middle Eocene Age (Cooke,19h5). This oldest -lithologic unit is exposed in Citrus and Levy countiesjust 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. Northof a line drawn between Levy and Nassau counties the sequence of sedimentaryrocks is constituted basically by clastic sediments (Pressler 1947). Theplant site is located in the zone of allochemical carbonates.

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Underlying Tertiary rocks and resting upon a post Pale: sie erosionalsurface are the m arine limestones and clastic rocks of Cretaceous age, gThe thickness of thi; sequence of Cretaceous and the overlying Tertiarysedimentary rocks is variable throughout the state, ranging from less then3,500 feet around Gainesville to more than 13,000 feet as vn on Figure2F-1. From the same reference, the thickness o f the Cre ,aceous and Tertiarysedimentary rocks at the Crystal River Plant Site is approximately 5,000feet as substantiated by Vernon (1951).

The framework of sedimentation for the Cretaceous rocks is roughly givenby the PRI'-MES0 ZOIC contours shown on Figure 2F-1. This south-southeasterlytreading high was not completely covered by lover Cretaceous sedirents,as it constituted.a positive area during early Cretaceous deposition. Thisstructure is called the Peninsular Arch and forms the backbone of the FloridaPeninsula.

Little is known about its structural elements or its stratigraphy exceptfor Ehe spotty information obtained from deep exploratory oil wells. Thisdata 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 Tertiaryand 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 erosionwhich were regulated by n% mal tectonic adjustments of the earth's crustin a foreland area.

Following deposition of Paleozoic sediments and possibly as early as post-Silurian, the Florida Peninsula is thought to have experienced no sedimentationuntil 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, recognizedand termed the Peninsular Arch (Applin 1951) a thick sequence of basicallymarine carbonate sediments were deposited as the Peninsular Arch slowlysubsided beneath a slowly encroaching sea. "Only the northern part of Floridawas emergent. It was otherwise a platform, and with the Bahama platformmade up a large region of carbonate deposition and slow subsidence," (Eardly,1962). The depositica of marine carbonate rocks continued throughout thelate Cretaceous as Florida progressively sank.

Data from oil exploration holes reported by many authors substantiates arather non-descript period of marine carbonate deposition throughout theremainder of Cretaceous time and well into the Tertiary..

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/7 Chen (1965) perforc2d a regional lithostratigraphic analysis of PaleoceneV Eocene rocks of Florida which substantiates that carbonate deposition was

prevalent up through the Eocene. Vernon (1951) states, that the peninsulaof Florida was covered by shallow marine waters throughout the period extendingfrom the Pliocene to the Recent, except for brief periods when it stoodas land and was weathered and eroded.

As reported by Cooke's (19h5) stratigraphic column (Fig. 'F-3) depositionwas interrupted by nine eresional periods during the cov- 3 of the approxi-mately 1h5 million years taken for the deposition of the sequence of LowerCretaceous through Pliocene rocks ; which, except for the Cretaceous , Paleocene ,and Lower Eocene, compose the outcroppin formations of the State.a

After the latest unconformity (most important to the study), representingan erosional period about 45-50 million years ago, the remaining Tertiaryhistory of sedimentation affected the site very little.

According to Vernon (1951) a structural high developed just east of the westcoast of Florida prior to Fiocene time to which Vernon says the U. S. GeologicalSurvey had applied the name "Ocala Uplift" as early as 1921. This structurehas been influential in establishing the existing subsurface geology atthe Crystal River site as will be discussed later. The devalopment of otherstructures in the State occvrred during Tertiary time, but discussion ofthis 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 arereported to have existed at elevations of 220, 150, 100 to 105, and 25 to30 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 -200foot elevations. Such a statement precludes the possibility that the solutionof limestone can occur below base level, an interpretation which is thoughtto 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 beenin evidence throughout much of Tertiary time (Chen 1965 and Cooke 19h5).

The depositional sequence of the Pleistocene as su=marized by Figure 2F-kand the progressive emergence of the Florida Peninsula stfostantiated by thesuccessively 1cwer terrace elevations is attributed by Vernon (1951) ". ..to be associated with the thick' alluviation of the Gulf of Mexico, principallyby the Mississippi River, and adjustment to this alluviation." More thanone million tors of sediments per year are being deposited in the Gulf of,s

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Most significant is the fact that marine sedimentation was curtailed byprogressive emergence of the Florida peninsula throughout Pleistocene time, gRecent continental sediments (as described in Surface Geology of this appendix)have accumulated on the peninsula to the present time.

The nature of the layered rock subsurface, as described above, has beenmodified throughout much of Florida by action of slightly acidic groundwaterupon the ,arbonate-rich sediments which has produced a network of solutionchannels, sink holes , and karst features. The extent of this solutioning,the expected intensity of the process in the future, and the effect of theprocess 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 literaturewhich 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 PeninsularArch 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 havebeen the subject of considerable discussion and presents provocation forceademic thought. Most important to this study, however, is the fact thatthis south-southeasterly trending core of pre-Mesozoic rocks has provideda relatively stable nucleus for the superjacent marine carbonate sedimentationof the Mesozoic and Cenozoic Eras (King 1951). The whole of the Florida gPlatform extended into the Bahama Islands and is believed to have remainedas a stable foreland to the Antillean deformed belt of Cuba (King 1951).

Puri and Vernon (1964) vividly set forth the structur 1 framework of theFloridian Platform. The location of the tectonic ele..ents of Florida andin 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 Puriand 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 Georgiainto central Florida and crests in the center of northern peninsular Floridaaround Union and Bradford counties ( Applin 1951, p. 3). This structurewas 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."

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1.3.2 BROWARD SYNCLINE

"A subsurface, local feature named by Applin and Applin (1964, Ms. ) for aCretaceous syncline in Broward and Paln Beach counties. '*he synclinal axisis UW-SE, and approximately parallels the inner edge of the South FloridaShelf."

1.3.3 SOUTH FLORIDA SHELF

"A term used by Applin and Applin (1964, Ms. ) for a shallow area, whichincludes parts of Charlotte, Sarasota, Hendry, Glades, Palm Beach, Broward,Monroe counties, and all of Lee, Collier and Dade count'.es. The boundariesgenerally 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 definean area 'which separated the continental border from the Eocene and MioceneIslands' in which the argillaceous sediments of the Hawthorn vere deposited.He thought that the area north and west of the straits was indicativeof much deeper water because the sediments contained less clay and a welldeveloped Miocene fauna. Dall (1892, p. 121-122) included in the Straitthe Okefenokee and Suvannee Swamps and the trough of the Suvannee Riverand estimated its vidth to 've less than 50 miles. Vaughn (1910, p. 160)discussed Suvannee straits and cited Dall's evidence for the erosion ofsediments 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 clasticand carbonate facies of the Cretaceous. This feature is considered byHull (1962, p. 118-121) to represent a narrow area (20-30 miles in vidth)of non-deposition, rather than an erosional channel that traverses over200 miles of territory. Whatever the cause of this channel, it has affecteddeposition of both Mesozoic and Cenozoic sediments."

"The strait is considered by Applin and Applin (196h, Ms.) to be a saddlethat 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 clasticbeds of Navarro Age (?) on the north and northern limit of Lawson Limestoneon the south."

1.3.5 OCALA UPLIFT

" Adequately documenced by Vernon (1951, The anticline, pp. 54-58), is a gentleflexure of Tertiary age, about 230 miles long and 70 miles wide, where ex-posed. The crest trends northwest-scutheast and is extensively fracturedand faulted. High-angle, strike faults flatten the crest and increase itscross-section., The anticline merges inconspicuously into several noses and

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troughs along the plunge and to each side. Murray (1961) thought the Ocalauplift was only a time and space variation of the Peninsular arch, but lon6periods of erosion and deposition separate distinctly datable structures ,and geopbysical data presented by Antoine and Harding (1963) justify theseparation of the two structures."

1.3,6 KIESIMEE FAULTED FLEXUPE

"This structure is a fault-bounded, tilted and rotated block that includesmany small folds , faults , and structural irregularities. The southernpart appears to be an anticlinal fold trending vest-northwest-east-south-e as t . The structure was erected by Vernon (1951) for a positive areaextending down the center of the Peninsula and as additional data becomesavailable, 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 byVernon in 1951. The structure appears to be closed fold that has beenhalved along the fault that bounds the Kissiemee faulted flexure. Theother half may be represented by the fold in the distal end of the Kissim-mee faulted flexure. Miocene sediments have been deposited upon thecroded 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 theStata coincide with a poorly defined structural low, centered in OsceolaCounty. Vernon (1951) interpreted the str 'eture as being bound by steeplydipping faults. More information is needed to more adequately define thestructure, 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 abroad flexure in the tri-state area of Georgia, Alabama and Florida. Hemapped the structure on exposures of Cretaceous mud Eocene rocks along theChattahooch?e River in southwestern Georgia and from the inequalitiesof drainage divides of the Chattahoochee and Flint rivers. Veatch thoughtthat the shorter tributaries of the larger Chattahoochee River were devel-oped along the crest of an anticline and the much longer tributaries ofthe Flint River were formed on the eastern flank of the anticline. Thecrustal 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 dipsextending away frcm it towards the southeast, south and southwest. ' Pres-sler (19h7, p.1852, fig.1) refers to the same feature as 'Decatur arch.'"'

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O " Jordan'(1951, p. hk) refers to the Chattahoochee arch as a second Paleozoicv 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 upwarpis 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 generaldescription of the chief structural features of Florida.

"a. An axis extending northwest from about Cape Canaveral on the eastcoast of Florida to south-central Georgia, upon which are locatedtwo large locally high areas ;

b. a channel or trough extending southwestward across Georgia throughthe Tallahassee area of Florida to the Gulf of Mexico, nearly atright angles to the aforementioned axis ;

c. an upwarped area in the vicinity of Jackson County, Florida withdips e:. tending away from it toward the southeast, south and south-west.

d. A structurally lov area with an axis extending northwest from thevicinity of L. Okeechobee toward Tampa, approximately parallel withthe axis first mentioned.

O A possible second north-west-trending upwarped area at the southe.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 Puriand 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 FloridianPlatform (approximately 100 miles vest of the Gulf Coast) represents a faultscarp 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 theexistence of such a fault. The seismicity analysis presented in Appendix 2-Ilikewise found no evidence of seismic activity of the west coast of the penin-sula.

| In considering the influence of the principal structures outlined upon thestructural integrity of the local geology, only the features related to theOcala uplift are of importance. In 'this regard, we are then confined to thediscussion of the structures which constitute the Ocala uplift as depictedby 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.

|County.

j. Detailed subsurface and surface studies revealed that the Ocala uplift is inj reality not a simple elengated doubly-plunging anticline but more positively

s/ explained as a faulted brachyanticline,

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Vernon (1951) describes the Ocala uplift in detail as follows:

"These sections and the structure map, Plate 2, (Figure 2F-7) indicate that Othe 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) andPlate 2 (Figure 2F-7). Along the Florida-Georgia State line the east foldis separated from the west fold by a shallow trough, 54 miles wide. Thefolds converge southward and in Levy and Citrus counties they are separatedby only a few miles and their crests are extensively fractured and faulted.The crests trend northwest-southeast through Levy and Citrus counties , butin Sumter, Orange and Polk counties they diverge, the east fold merging witha large fault block, named in this report the Kissimmee faulted flexure, andthe west fold continuing in a south-southeasterly direction and graduallymerging with the regional dip."

"The development of vertical dip-slip faults , the traces of which parallelthe crest of the Ocale, uplift, tend to flatten the crest and to lengthenits cross-section. From the limited core hole evidence available for thisstudy 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 numerouspossibilities , one fault may teminate at depth against another or it maycross to fom a graben and horst structure. Figure lh (Figure 2F-9) isone interpretation of the geologic section along the proposed Florida ShipCanal (Cross Florida Barge Canal) and here a graben and horst structureis clearly indicated. The fault planes are drawn in at angles greaterthan 60 degrees and may be steeper. They are thought not to dip at anglesless than 60 degrees because of the straight-line traces of the faultsand because the closely spaced core holes do not penetrate any thinningor thickening of the beds."

The other associated structures (outline by Vernon and Puri) are remotelylocated with respect to the site, and the major defomation feming them isestablished as occurring during the post-Oligocene pre-Miocene interval,with minor adjustments occurring into the Pleistocene. Consideration oftheir affect upon the structural soundness of the site is unwarranted.

According to Cooke (19h5), "There is no evidence that the rocks composingthe outer layers of the Flo*idian Plateau have ever undergone extensivedefomation. "

Referring to the movement of Ocala arch, Cooke (1945) says , "The arch wasabove water in early Pliocene time, as is shown by the presence of landmammals of that age in the belt east and south and presumably west of theland area. The tilting that depressed the western centinuation of the beltpresumably was contemporaneous with the crustal movements that deformed manyother parts of the earth at the close of the Pliocene epoch. All of thedeformation seems to have occurred before the Pleistocene epoch, for eventhe oldest Pleistocene shore lines, so far as they have been traced, remainhori zontal . "

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The northwest trending structural lineament of horst and graben, faulting asshown 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 inFlorida. In association with this uplift and faulting, a well definednorthwest trending fracture system developed, the genesis and orientationof which is described by Vernen as shallow tensional fractures parallelingthe northwest trend of the Ocala vplift, and in part caused by the Ocalauplift deformation. Also, adjustment of the great thickness of unconsoli-dated Tertiary sediments over the stable pre-Mesozoic land mass could accountfor development of such fractures.

Also, "... Because of inequalities in these forces (forces responsiblefor the Ocala uplift) secondary tensile stresses are developed at rightangles to the primary tensile stresses. Thus tensile fractures would bemost strongly developed along the axis of any folding and along the axesof flank bulges (Vernon, 1951)." Such a combination accounts for thestrongly 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 BargeCanal indicates that movement on steeply dipping (probably greater then60 ) normal faults have produced vertical displacements of 20 to 160 feet,Figure 2F-9. The closest mapped fault to the site has had its northwesternterminous 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 thisinvestigation.

Most significant in terms of the structural competence of the Plant Site asaffected by Tectonic history are the facts that:

Stability of the Florida Peninsular has been predominanta.

throughout the Mesozoic, Cenozoic, and Recent Eras.

b. Regional tectonic elements are those common to a stableforeland.

c. Faulting (not recognized in Florida before 1951) is restrictedo 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.

Regional structures (the Ocala uplift) causing the faultinge.

exist east of the site. No faulting has been mapped westof the reactor buildings.

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f. Faulting was not disclosed by detailed subsurface studiesat the site.

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It is therefore concluded that the site is located on structurally competentmarine sedimentary rocks which have only been subjected to minor regional gdiastrophism which has been inactive for approximately the last one millionyears .

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e .e.

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r m e.= .c...

em.h..k, sJee .Ih, .

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. . e ea =e .

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p

w. . .w . q. c.au ,e = .

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e c. .

a.= =s v e a. = =. =... == .en . -.fp .e a .. .

. n. e. . ==

.s ., .n,a.w ..e u .O.

p...,e=.... e w +aw.a. .n .w -so.n n.e= w o..sc, p =wd * u. .=e

n. .w . . e.- .-. m. w i n waw i u u

w.=a*

m.,=o =.ina. .=a m

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wee ' . ... r. a

ie . .ap . . i.o..a , . ==.a.* . * * * * = * . * * - *e w ta n ..e . 6,. . * . . = . . eee a a.

. ..=.a. =. ., a. - r w. == .*=c./ * *= *==6.* ** 6*" 01.g.c 5. * AI B6.ft M.g. "$

c a o.e =.=w.o.e..=.mr.e.e

.= v\e c . . c.a .m, .a..ww . *.

ch m,h. i p . wan.o m ee eu m -

m a.n

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n... ..L . a -a - e .e. a

. .im.. .. ., .e . -o. .a s.e.~.4=.. .*a.. Li.c. a , ,m

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a r, .n.su.em r.nL....e===== .an

w.a.n. ._- . . . w=ma =. .w. .

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. !.w.. a =L. m s

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e.w.e

m . nin=m..ne u ma s . .= wou,. u.- .

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eh a m.e was~s cm a .

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n,.or s.m. <=. . u o. .La s.a=.-=.e.u.e

TERTIARY 1YSTEM u w-e. .ec

e me se.e wme..a .n.,.a.ra eF .as e.eh.eu.a.. Tn a es. s. e. ..n..

F. .

er ww.,.

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e m.es.a

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cTe..eu.. in-* cm*== m - a* *= Pa **d* . a. m,

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14.

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.

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'

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'

" *;**.".l '* !': ""*" *~ "" \'". *..' .""t.* % *.".".*."" " ":.".C:' V.

. . . . . - . . ,,.~,. , :; - -~~2. =:,,=; - , 1

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,

*( - orn .a ri....--

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*** **'* F L O RID A GEOLCGiC SUN vEYj'"** **d

S PEC 6 A L t U L L E TIN eS. . ..' " * ' ' * * * * * * * " * * * * * " * * * * * * ' - PURI& VE HN ON, 19e 4

c's cI 'I O23)

.< V- _U .)a y$ 't

- w

-

.

#e'~- ,.

.

' GEOLOGIC MAP OF FLORIDA''rs ,,, b f,.-

-= * * , - .

-- CRYSTAL RIVER UNITS 3 & 4

s . __ - .,

f I I I | ,,_

;=. FIGURE 2F 2 ,

- w- -- ... - w

L

s. I-m4

i

GEOLOGY OF FLORIDA-GEOLOGIC FORMATIONSFLORIDA (E

Grot.ocic Fomanoss in F ominA G r.

-

.c$$3Erosion interval. Lake Flirt merl (fresh. water, partly-~-z Recent). EE%g

zU p "B E~|$ Pamlico sand (littor , .'iore line at 25 fcer).

*

>Erosion interval.

__=. 3 Ac

c- ;;8-8

ETalbot formation 0 a =_.

*(littoral, shore line at g g42 feet). *c ~. .

g Penholoway formation f f f $ .! .Sc"#(littoral, shore line at *c .c e c 2,< < Ea

E" = "E pi8~na aoHy za 70 feet). 's E E g 3 Co

w< y w a--

# *Wicomico formation j ># x.g (littoral, shore line at < y -5!w .m

p ; 100 feet). 3 .$ e ;"$em W e -

*-% "E -c

*y z

," $$ Erosion interval. Fresh. water limestone in the .h .;; j E_,i g

$a $Fort Thompson formation, j U< w

4Z u -~

M o c

N.{g$,c ._ fW E : Sunderland formation 'k

{$$ kY5. )j,cg (littoral, shore line at 170 feet). @C

< $ Coharie formationD s (littoral, shore line at 215 feet). $ ., A"

a eO E a x -

d * 8 I5<

3zg Erosion interval. Fresh. water limestone in the b .j g'j*c g f ,$gg Fort Thomy->n formation. g li e ! 3.2 * ;;

.

oC~ tw w - ' *% 38*

c c-a:,g

@'a= c<

EE Brandywine formation a g ,j .2 { , j{g (littoral, shore line at 270 feet). M j j gg

, . 'E 8 E Z " ]*

i. -w e

531M3$3x3xry

,,.. *

IV

r%" (

0358r . ._.

(

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,i! w wd Alurri Blud group: Shoa! River formation (marine). o X"G H dH Chipola formation (marine). I M

M' Hawthorn farmation (mirine). E $y% e

Fag [ Tampa limestone (marine, of Anguilla age). ; g. c; Erosion interval. E q*

aSuwannee limestone (marine). Flint River formatior. (littoral, of Antigua age). 3*.re > z m

~ 0" M dE Eros:on interval. 5! f8IE < 35 Byram limestone (marine, of late Vicksburg age). m *

{{ j* h!arianna limestone (marine, of early Vicksburg age). 5 h"

gErosion interval during Red Bluff time. g C< g

w Ocala limestone (marine, of Jackson age). 2"

H Erosion interval. g 4

$= Avon Park limestone (marine, of Claiborne age). 2 %d2 Tallahassee limestone (marine, of Claiborne age). s zj$ Lake City limestone (marine, of Claiborne age). d

~

Erosion interval. kOldsmar limestone (marine). Salt hiountain limestone (marine, of Wilcox age). ]

,a*wz wgw2 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! COMANCHESERIES O

O mm O

F M F F* F o F*

h5 E E 5' 5 5,' 5' E.F

o u y ? m L m o -8 <a x a- n a*

- " O3 T @ M D 8 @ OC o* em 5 2'" 7R S I & 3 S T- C 2- a *O

$ s ;':,

n r" 'y 5' o .T 5' s $ 5' S S y- =,

i I3 3 9. 3 3,

g -.3 -. a -.ax 0 g*

-.32

-- n o,o o o >e c, Bg o , .o c.o - o. n o n-o u .* A R, E; E *5 % 3 4 ". 4. * * * C

- --=- , a < - < ;;- e- o. >x -4 n *

,r . y y a e : e r :! s, Ir- o u r .

3 "' r-* 8 * _

-

] > n CD s- 2, .a r- L - 0B^ , , z --

-3 g . Z g : a3 g ,,5 - 0| x Ln g

2 wa ~ m ,- I o ,

< > W g. 5 g. 3 ,s- 5 8a 5 o3 3 4y p. y .a --m 3 g

2 p u a o Z en o g , *EE % E. E 3~' *"o c z --

c'E' .8 ;'I : 7i gc 2'i "- 2

=o D ;; '$. 3 o"

g y"o -;0 a 4 o .- o 2 $Zm m , .

E, " % c,, go.t,

$ Yu w n 0 ,a, ,,

> 37 9' Y'

5* $o a s- !. -*w m-

M o oo- , -

O y*> A " 3

2. o " $-**'t :':"

7 ." i*

%.- --"'a v

._

r n

TABLE 5.-Correlations of Pleistocene Terraces

IVestern Florida Citrus andVisk,1940 Cooke,1945 Vernon,1942 Levy Counties, Florida Tentative Age Assignment

(Elevationsofshorelinesinfeet1 (Elevationsofshorelinesinfeet) Vernon,1951 of Terraces in Florida

Williana Citronelle fm. Delta plain Not present Early Nebraskan and pos-Brandywine,270 sibly pm-Nebraskan

Valley erosion Valleyand sub-acrial erosion Valley and sub-aerialerosion Nebraskan (glacial)

'Bentley Coharie, 215 220 Deposits of Coharie,220 Aftonian (interglacial)

,

Valley erosion Valley and sub-aerialcrosio..*

'alleyand sub-aerialerosion Kansan (glacial)vOu& Afontgomery Sunderland,170 150 Deposits of Okefenokee,150 Yarmouth (interglacial)C

Q Valley erosion Valley and sub-aerial erosion Valley and sub-aerialcrosion Illinoian (glacial)m= Wicomico,100" Prairie Penholoway, 70 105 Wicomico,100 Sangamon (interglacial)

n> Talbot, 42"dw

111 - |oy Valley erosion Valley and sub-aerialerosion Valley and sub-aerial erosion Glacial stage

-er ;;

I m Second bottoms and high Pamlico, 25 30 Pamlico,25 g Interglacial stage'

Ey level flood plains 5mn m !'! u .

~

{ g} Valley erosion Valley and sub-aerialerosion Valley and sub-aerialcrosion Glacial stagem an* *"

h!od I I I"Z Modern delta Afodern submarine plain Sea levely wand streant food ain Itecent (interglacial)

9',

A "4m '

N '

.

O FLORIDA GEOLOGIC SURVEVm BU L L E TIN # 3 3MVERNON, 1999

. _ _ . . _ _ _ _ _ _ _ _ _ _ . . _ _ _ _ . _ _ _ _ _ _ _ _ _ . _ _ _ _ _ _ _

_- _- - - __ -__________

|

|

|

|

.

| O\. \..

0 ..

)1 Oc :' - - ,;, , p v. - - , i<., .,

., p t.C AYg*

,-*~pW.s,,j!! f\,7000- \

wc .i

* * . PA L g og g,.g ,%-* *

$ k ~ ~ ~~ ~ ~ GE P,,R[,Ca M enga y y"*| | i. . . ) ,, , j j - - - - - - -

. , ,

5,. ... 4 - ---- - :.s,

*' *'

.

2 2[." '. "J """*.:"":: as ',*-

j j .-- - SILUR 44 A N D''~ ~ ~ '

ORDOVICI AN ~ - --

| '. ~ ~ SE0lMEN TER~ ~ '$. .=1s,

7,0o) -,-- -

-- -RO CKs .,*.~||,O, ,,,_--

--- a,:::EM:,:,ig

~~|::::,'sooo~~~

--- ...,y .,,_,.-2:: . es.<-

|~:|E,910,,,,?;t.*a.'*o--

t'% c: ?>--o

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a ~C4 ' * *a ::4'IJ,og/ ^$N 'A4)| ^ 1^[.'.^. . .^ *,

J

/ '...' '

.

AFTER APPLlH,1951

S TRUCTU R A L GEOLOGY OF NORTH AMERIC AAN D EDITION * E A RDL E Y , les2

CONFIGURATION AND DISTRIBUTIONOF PRE MESOZOIC ROCKS

CRYSTAL RIVER UNITS 3 & 4

O_=0361 != FIGURE 2F-5. .

er v

O.

7'p/ jCHATTAHOOCHEE 1

ANTICLINE , 3OOTHEAST GEORGIA-

' g' g, '.,e" =;a .* , . td, N -'

.

MBAYMENT ''-

, n.s f_ a-,

,( ..- f,

,

T r= ~1 . .*'a '

-

) i

fk ..., [ . .h .h'' '

f

'

GULF OF MEXICO [ A''g .h* * ...]EylN ULAT g .*L ARCH,-, KISSIMMEE

c ,j .. )--k# 79 y0 ,,,, FAULTED FLEXURESEDIMENTARY 7 / r.: - .

/ BASINe

. g );, y .\' ' " - = . .-,- ,. ... a,

APALACHI O(A \ ?. ' , , **"SANFORD HIGHt

EMBAYMENT t. , n t ' - C'CALA ,._ \ -f.<

7 :: - r UPLIFT * , .

Oh/ ~# I,

- r AREA OF-

f "

j- * , ": '. RYSTALLINE

-

" ' . " - ' ., kPROCKS*

NORTH GULF COAST /' * " '. ;1SEDIMENTARY f

.'

-. . .

PROVINCE A--g , ,3

e FLORIDA .j OSCE5 ' -/ PENINSULA 4 _ _ a . , LOW " **" u

-s' SEDIMENTARY ....... : ...... i m'/

f PROVINCE =-: - - - . ' , " .'

'*

. X ""]{ ,: 'fT.....'.Qq."~ >

O,,,

,' ?' 'f " .""( ROWARD%. . . . . . ...

. " ''c. N, 's;' ' N.. .. ' SYNCLINE'- - .

'

..

.''.

g $g .\., 3. ,

]W(.'{ ,.g a; %

i- 1/ g

,. . , .

f*

,

:,-y -

g. ,p,1

-

TH FLORIDAv- EMBAYMENT

FLO RID A GEOLOGIC AL SURVEYSPECI AL PU BLIC A TION e5

PURI& V E RN ON ,196 4

INDEX TO PRINCIPAL GEOLOGICSTRUCTURES IN FLORIDA

CRYSTAL RIVER UNITS 3 & 4

gi =-- ei uRe 28 6_

0362

|

P

o1

i\

G E O R G l Ar- - - - , - _ - . . . . . _

}.': --- - - - - -

.y,I 1 | %

'

% f 's,

N,t --,o .

| ~'' '. .. , ,

[ 8 )-/,

, .,_

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5 p-|

. (,

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/, , Lf

'o c . , ,

I i | hoc 'o |\o c. <,

t|

,

. , . . ' . . . , _ , e* '; f -- , &,.

b ' 'o

,a ,

s e' y.>;+. : :." a' -@ .

*e,,y ,

'\,' r ''.,i,

%O -' %s

ICRY$TALIilVERk ~STRUCTURE MAP l P L AN T 5\T O; -

M \ k#Or THEINGLIS MEMBER, N ~,

0

MOODYS BRANCH ogFORMATION 4

- - - - - ,_

CoMove ic'eevol 50 Feet -

+50 Elevates above seaievel50 Elevations below seaievel

m u

OInglis member, Moodys Branche ,

formation, control well \k'Inglis member eroded*

* Inglis member obsent I ----- ---g --,---

-- Eroded Inglis mbr. ,

e -dUneroded Inglis mbr. , g

d

(l^

g Outcrop of Avon Park timestone, and .

b creas where Avon Park limestone is' d

covered by Miocene with intervening |beds being obsent ,

. ..... l

0363t

-

(- _

,

._ ,

,N'. *

{ Y %-pa + p ,

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