Tertiary Stratigraphy 

of South Carolina

GEOLOGICAL SURVEY PROFESSIONAL PAPER 243-B
Tertiary Stratigraphy 

of South Carolina

By C. WYTHE COOKE and F. STEARNS MAcNEIL

SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1952, PAGES 19-29

GEOLOGICAL SURVEY PROFESSIONAL PAPER 243-B

A revised classification of Tertiary formations

of the Coastal Plain, based mainly on new stratigraphic

and paleontologic information

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1952
UNITED STATES DEPARTMENT OF THE INTERIOR 

Oscar L. Chapman, Secretary v 

GEOLOGICAL SURVEY 

W. E. Wrather, Director

For sale by the Superintendent of Documents, U. S. Government Printing Office 

Washington 25, D. C. - Price. 15 cents (paper cover)
CONTENTS

Abstract- ______ _____.. _________

Introduction ________._!________

Paleocene (?) and Eocene series-. 

Deposits of Wilcox age _____

Deposits of Claiborne age___ 

Congaree formation____

Warley Hill marl ______

Me Bean formation___ 

Santee limestone_____

Castle Hayne limestonePage 

19 

19

19

20

21

21

23

23

24

25

Paleocene (?) and Eocene seriesDeposits of Jackson age.

Barnwell formation. _ _. 

Oligocene series______________

Cooper marl._________

Miocene series_______________

Hawthorn formation. _.

References. ____________l_-___.

-Continued

Page

26

26

27

27

28

28

28

ILLUSTRATION

Figure 2. Correlation of Tertiary formations of South Carolina. 20

in

99308T—52

TERTIARY STRATIGRAPHY OF SOUTH CAROLINA

By C. WYTHE COOKE AND F. STEARNS

ABSTRACT

The following changes in the current classification of the 

Tertiary formations of South Carolina are proposed: The Black 

Mingo formation, mainly of Wilcox age, may include some Paleocene deposits. The McBean formation, heretofore including all 

the deposits of known Claiborne age in South Carolina, is restricted to the Ostrea sellaeformis zone, of late middle Claiborne 

age, and the names Congaree formation (equivalent to the 

TaJlahatta formation) and Warley Hill marl (equivalent to the 

Winona formation) are revived for deposits of early Claiborne 

and early middle Claiborne age. A large part of the deposits 

mapped as Barnwell formation (of Jackson age) proves to be 

Congaree. The Santee limestone, heretofore supposed to be of 

early Jackson age, represents the Ostrea seMaeformis zone and 

seems to be an offshore facies of the restricted McBean formation. The Castle Hayne limestone, heretofore known only in 

North Carolina and referred to the middle Jackson, occurs under 

cover in South Carolina. Its fauna shows it to be equivalent 

to the Gosport sand, of late Claiborne age. The Cooper marl, 

currently referred to the late Eocene (Jackson), is reassigned 

to the early Oligocene? on the basis of its mollusks, foraminifers, and cetaceans. A gravelly facies of the Miocene Hawthorn 

formation similar to that in Georgia is recognized for the first 

time in South Carolina, where the formation had previously 

been recognized only by its offshore facies.

INTRODUCTION

The Coastal Plain of South Carolina has received 

somewhat less attention than that of the neighboring 

State of Georgia, and in comparison with the Coastal 

Plain of the Gulf States, which in recent years have 

been the center of extensive oil exploration, little is 

known. Since the days of Lyell only three general accounts of the stratigraphy of the Coastal Plain of South 

Carolina have been published, one by Tuomey in 1848, 

one by Sloan in 1908, and the most recent by Cooke in 

1936 as Bulletin 867 of the United States Geological 

Survey.

The present paper presents a revised classification of 

the Tertiary formations of South Carolina, and indicates some of the changes necessary on the existing 

geologic map of the State. However, the greater part 

of the information on which this revision is based comes 

from entirely new exposures and new collections of 

fossils, and even the interpretation of the molluscan 

faunas is based on revised knowledge of the range of 

species.

Travel in the Coastal Plain is now much easier and 

faster than it was before 1936. Many new roads and

bridges have been built, and places formerly inaccessible are now within easy reach. The spoil bank of 

the Santee-Cooper Diversion Canal, cut about 1940, 

has brought to the surface an abundance of fossils of 

the Santee limestone, including species that had not 

been collected since the 1830's, wheji the original Santee 

Canal was dug. The associated fauna of the more 

characteristic of these species is now known for the first 

time. New pits sunk in the flat, featureless Pleistocene plain yield unsuspected evidence as to the age of 

the underlying limestones.

Since 1935 MacNeil has been making stratigraphic 

studies on the Tertiary formations of Mississippi, Alabama, Georgia, and Florida. These have resulted in 

more accurate information as to the geologic ranges of 

fossils, and familiarity with the stratigraphy of the 

formations containing them. Using this information 

he was able, during a three-week reconnaissance during 

1950, presumably preliminary to the preparation of a 

new geologic map of the Tertiary formations of South 

Carolina, to make closer correlations with the type sections in Mississippi and Alabama than had been possible 

in 1936. The writers made two short trips to South 

Carolina together in May and June of 1951.

PALEOCENE (?) AND EOCENE SERIES

The name Paleocene series was not adopted by the 

U. S. Geological Survey until after the publication of 

Cooke's 1936 paper. The deposits in the southeastern 

States now referred to the Paleocene form the Midway 

group, which had previously been treated as the oldest 

division of the Eocene series. Since the removal of the 

Midway group to the Paleocene, the Eocene series in the 

Southern States has included only three groups—the 

Wilcox, Claiborne, and Jackson, represented in South 

Carolina, though the group names have not been applied there. In addition there is somewhat meager 

evidence to indicate that the lowest of the units here 

recognized may include beds of both Paleocene and 

early Eocene (Wilcox) age.

The only known representative of the Wilcox group 

in South Carolina is the Black Mingo formation. There 

is some evidence that the beds now included in the Black 

Mingo may be in part of Paleocene age, but the evidence 

is inconclusive, The Claiborne group is more fully

19
20 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1952

Mississippi Alabama

Yazoo clay ^ . Cocoa sand ^

\ member \

^" S Sand, silt,

Ocala 

limestone

Barnwell 

formation

Moodys Branch formation

^-^X~^--~^X~^'''"^-'-^^-N-'

Cockfield formation

.^x^..XX^x-^^^^X-^x-VtaX^x-.*^.„

Cook Mountain formation

Sparta sand 

(Koscinsko sand)

Zilpha clay

Winona formation

Gosport sand

Ostrea sellaeformis zone

•~^s~*~<~***r^'

(Present)

(Absent?)

Ostrea smithvillensis zone 

Ostrea lisbonensis zone

Tall aha tt a formation

Wilcox formation

Hatchetigbee formation 

Bashi marl member

Tuscahoma sand

Nanafalia formation

Fearn Springs sand member

South 

Carolina

North 

Carolina

Castle Hayne limestone

•N^-V—•

McBean

Warley Hill 

marl

Congaree 

formation

Black Mingo 

formation

1 Nonfossiliferous, nonglauconitic limestone at Cave Hall may be of this age.

2 May include some Paleocene.

FIGURE 2.—Correlation of Tertiary formations of South Carolina.

represented. As here revised it includes the Congaree 

formation of early Claiborne age, the Warley Hill marl 

(both included in the McBean in Bulletin 867," Cooke, 

1936), the restricted McBean formation and its offshore 

equivalent the Santee limestone of middle Claiborne 

age, and the Castle Hayne limestone, as here restricted, 

of late Claiborne age. The Jackson group is represented by sandy limestone and perhaps down dip by a 

less sandy facies. At the present, outcrop beds of 

Jackson age are almost completely reduced to oxidized 

sandy residues. The name Barnwell formation was applied to leached residues of the sandy limestone and no 

type locality was ever designated. It now appears that 

actually the railroad cut at Barnwell was made in a 

part of the Miocene Hawthorne formation, although 

many geologists must have regarded it as typical Barnwell. Residues of limestone of Jackson age certainly 

are present elsewhere in Barnwell County beneath the 

Hawthorne cover, and there is no reason why the name 

Barnwell cannot be applied to the unleached Jackson 

beds farther down the dip even though its type area 

falls entirely within the area of solution.

The relationships of the Eocene formations in the 

Carolinas to one another and to the generalized standard section in Georgia and Alabama are indicated in 

the correlation chart (fig. 2).

DEPOSITS OF WILCOX AGE

The Black Mingo formation was referred to as being 

of Wilcox age (Cooke, 1936) primarily because of the 

presence of Ostrea arrosis Aldrich. Although this 

oyster was stated by Aldrich to be from the Nanafalia
TERTIARY STRATIGRAPHY OF SOUTH CAROLINA 21

formation, and has since been found to be restricted 

to it, in the correlation table (p. 40) the Black Mingo 

was placed opposite the Tuscahoma sand of Alabama 

because of the occurrence in both of Twrritella mortoni 

Conrad, a species now known to be abundant in both 

the Nanaf alia and the Tuscahoma. Mapped with this 

oyster-bearing bed were underlying siliceous clayshales and an overlying massive red sand now known 

to be of early Claiborne age. A revised map would 

show the Black Mingo to be confined to a much smaller 

area, chiefly along valley floors. Beds mapped by 

Cooke (1936, pi. 2) as Black Creek (Cretaceous) formation in western Sumter County are now regarded by 

MacNeil as Black Mingo as here restricted to the siliceous clay-shale and oyster-bearing bed, whereas the 

overlying more widely distributed sands in Eichland, 

Lee, Sumter, Clarendon, and Williamsburg Counties 

that were mapped as Black Mingo are now placed by 

him in the Congaree formation, of early Claiborne age.

Among fossils collected by Cooke in 1922 on the Eiver 

Eoad Sy2 miles west of Pinewood, Sumter County 

(U.S.G.S. collection 10401) and referred to the Black 

Mingo formation (Cooke, 1936) is a Turritella he identified as Turritella mortoni Conrad, a species typically 

of early Wilcox age. Later Bowles (1939, p. 271) identified it as a new subspecies, T. mortoni media/via 

Bowles, which occurs typically in the lower part of the 

Midway group at Prairie Creek, Alabama. He found 

this same subspecies also in U.S.G.S. collection 10403, 

from the Kingstree road east of Deep Creek, 5 miles east 

of Manning, Clarendon County.' On the basis of this 

subspecies, Bowles was o^ the opinion that the Black 

Mingo is of Midway age, and not Wilcox, to which 

Cooke had tentatively referred it.

The section at Warley Hill includes in the lower part 

(bed 3, p. 23) 8 feet of clay or shale overlain by a quartzitic sand containing an oyster resembling Ostrea 

crenulimarginata Gabb, a species found at many localities in tiie Midway group in Alabama and western 

Georgia. Cooke (1936) included these beds in the McBean formation but they are now recognized as belonging to the Black Mingo formation. Ostrea 

cremilimarginata is related to the Wilcox oyster 0. 

arrosis, but the material at hand more closely resembles 

the Midway species.

The Black Mingo formation as mapped by Cooke 

(1936, pi. 2) is now known to have included some beds 

of early Claiborne age, and (even as here restricted) 

may include beds of both early Eocene and Paleocene 

ages. However, further subdivision of the Black 

Mingo is deferred until more definite evidence of Paleocene age is produced. If the lower shales of the Black 

Mingo should prove to be of Paleocene age, one of

Sloan's names (1907,1908), Rhems shale or Lang Syne 

shale, may be available.

DEPOSITS OF CLAIBOBNE AGE

All the then-known deposits of Claiborne age were 

included by Cooke (1936) in one formation, the McBean. This was the original usage in Georgia, where, 

according to Veatch and Stephenson (1911, p. 237), the 

McBean "formation is equal to the Tallahatta buhrstone 

plus the Lisbon formation of Alabama, and the top of it 

may include the base of the Gosport greensand of the 

Alabama section." The Claiborne group throughout 

the States from Alabama to Texas has been divided 

into well-defined formations, each characterized by its 

distinctive fossils, and it now seems desirable to divide 

the McBean of Cooke (19^6) along similar lines into 

three formations. Names proposed by Sloan in 1907 

and 1908 are already available. For the lowest beds of 

Claiborne age, equivalent to the Tallahatta formation, 

Sloan's name (1908, p. 455) Congaree is revived. For 

the intermediate beds, equivalent to the Winona formation of Mississippi, Sloan's name (1908, p. 457) Warley 

Hill is revived. The name McBean formation is retained, in a restricted sense, for the zone represented by 

the type locality of that formation. This zone, the 

Ostrea sellaeformis^ is equivalent to the Cook Mountain 

formation of Texas and Mississippi, the upper part of 

the middle Claiborne.

MacNeil concluded in 1950, on the basis of field profiles and a restudy of its molluscan fauna, that the Santee limestone, long supposed to be of early Jackson age, 

represents the Ostrea sellaeformis zone of the Claiborne group, equivalent to the restricted McBean formation, of which it is an offshore f acies.

Another astonishing result of the present investigations is the discovery of the Castle Hayne limestone in 

South Carolina. That formation (typically developed 

in North Carolina, where it was called a marl) had been 

considered to be equivalent to the Santee limestone and 

to be of Jackson age. As here restricted, it is younger 

than the Santee and is of late Claiborne age, equivalent 

to the Gosport sand of Alabama and the Avon Park 

limestone of Florida.

CONGAREE FORMATION

Though Sloan's "Congaree phase" (1908, p. 455) was 

vaguely defined, he evidently intended to include in it 

clay, sand, and buhrstone of early Claiborne age. 

Veatch and Stephenson (1911, pp. 238, 267) accepted 

Congaree in this sense for use in Georgia and described 

the Congaree clay as the basal member of the McBean 

formation, the oldest formation of Claiborne age known 

to them there. How much of their Congaree is really
22 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1952

Claiborne, however, is still uncertain; some deposits 

referred to it, notably the thick bed of fuller's earth at 

Pike's Peak, in Twiggs County, Georgia, are now believed to be of Jackson age because of their supposed 

equivalence to similar clay in Houston County, Ga., 

that lies above fossiliferous Jackson limestone. Cooke 

and Shearer (1918) supposed that all their Congaree 

clay member was of Jackson age and transferred it to 

the Barnwell formation under the name Twiggs clay 

member. Later Cooke (1943, p. 61) restored that facies 

consisting of thin-bedded or laminated sand and clay 

to the McBean formation but did not have an opportunity to revise his map, which had been published in 

1939.

It now appears that the deposits of Claiborne and 

Jackson age have never been properly delimited in 

either eastern Georgia or South Carolina. Though 

Veatch and Stephenson (1911) mapped too much Claiborne in Georgia, both Cooke (1939; 1943, pi. 1) and 

MacNeil (1947) showed too little. Cooke's map of 

South Carolina (1936, pi. 2) included beds of Claiborne 

age in the supposed Jackson south of the Congaree 

River, but north of that river the lower Claiborne was 

mapped as Black Mingo formation (Wilcox). After 

studying the section of Claiborne age of South Carolina 

and its fauna, MacNeil is of the opinion that a large part 

of the deposits in eastern Georgia mapped as Barnwell 

is of Claiborne age. This would include several of the 

better-known fossil localities, such as Little Keg Creek 

(Cooke and Shearer, 1918, p. 48; Cooke, 1943, p. 55) and 

much of the Twiggs clay member of the Barnwell formation of eastern Georgia.

The Congaree is now deemed of f ormational rank because it is equivalent to the Tallahatta formation of 

Mississippi and Alabama, which presumably is separated from younger deposits by an erosion interval. 

The name Congaree formation rather than Congaree 

clay or shale is preferred because much sand as well as 

clay and shale are included.

Sloan specified no single locality as the type of his 

Congaree "shale," "sands," or "buhrstone." The name 

is evidently taken from the Congaree River, and it has 

been suggested (Cooke, 1936, p. 59) that Sloan's locality 505 on the Elmore Williams' place at the head 

of First Creek, a tributary of the Congaree River, be 

regarded as typical. This locality is difficult to find 

without a guide. However, ledges of similar rock are 

exposed on the road south of Bull Swamp Creek 2% 

miles west-northwest of Swansea and also at a waterfall north of the east-west county road about 2^4 miles 

west by north of Swansea.

A Tallahatta-like facies of the Congaree formation 

is well exposed in a cut on State Highway 33 half a

mile east of Creston, Calhoun County, and west of 

Halfway Swamp; and for all practical purposes this 

can be regarded as a typical exposure. The section is 

as follows:

Section in road cut west of Halfway Swamp 0.5 mile east of

Creston

Warley Hill marl. Feet 

4. Coarse weathered sand___—————————— 5 

3. Rusty highly glauconitic sand————————— 2 

Unconformity? 

Congaree formation.

2. Alternating fine rusty unconsolidated sand and

shale; borings in top_————————————— 5 

1. Light-gray shale alternating with thin-bedded 

fine-grained sandstone, most beds less than 

3 inches thick. Contains Anodontiaf auffustana Gardner. This bed closely resembles 

a facies of the Tallahatta formation. 

About ______—_____————-—— 16

The materials of the Congaree formation strongly 

resemble those of the Tallahatta formation. Both contain hard, brittle siltstone, which is the dominant component of the Tallahatta near the Mississippi-Alabama 

line. Well-sorted and poorly sorted sand are common 

to both formations. Brittle clay or fuller's earth is 

a conspicuous feature of the Congaree in the Congaree 

Valley, although the larger clay masses are local lenses. 

In Aiken and Lexington Counties coarse to fine gravelly 

sand makes up the greater part of the formation. The 

Congaree formation in this area resembles the coarser 

facies of the Tallahatta in northern Mississippi.

Several species of mollusks characteristic of the Tallahatta occur also in South Carolina, and are restricted 

there to the Congaree forflfation. The recently described guide mollusk Anodontiaf augustana Gardner 

(1951, p. 9) was recorded by Gardner (1951, p. 10) from 

U.S.G.S. collection 7728, bed 8 of the section at 

Warley Hill (p. 23) and from a road cut on the south 

side of Halfway Swamp about 2% miles northwest of 

Creston, Calhoun County. In Alabama this species 

occurs only in the Tallahatta formation. Ostrea johnsoni Aldrich, a species now known to be confined to 

the Tallahatta, has been found near Salley (Cooke, 

1936, p. 59) and 2 miles south of Gaston (Cooke, 1936, 

p. 60). An oyster found in bed 2 of the section at 

Lang Syne (Cooke, 1936, p. 69) and reported as Ostrea 

divaricata Lea seems to be an undescribed species, related to O. perplicata Dall, which occurs also in the 

Tallahatta.

Hard sandstone and sand exposed in Aiken and Lexington Counties supposed by Cooke (1936) to be referable to the Barnwell sand prove on further study 

to be of Congaree age. The most important of such 

outcrops are Calico Spring (locality 185, p. 93), Decaradeaux place (locality 189, p. 94), and Bethel church
TERTIARY STRATIGRAPHY OF SOUTH CAROLINA 23

(locality 190, p. 95). The last two localities have 

yielded recognizable fossils formerly interpreted as of 

Jackson age. Two corals, however, Endopachys 

maclurii (Lea) and Platytrochus stokesi (Lea), found 

elsewhere only in beds of Claiborne age, occur at both 

places. Fossils, including Turritella tncbeanensis 

Bowles, were recently found by D. H. Eargle and B. F. 

Buie in a tough siliceous clay near the mine of the 

Monetta Clay Company along Highway 39 about V/% 

miles northwest of New Holland Crossroads, Aiken 

County. This locality lies well within an area mapped 

as Cretaceous by Cooke in 1936.

One of the striking features of the basal part of the 

Claiborne is the occurrence of boulders of pisolitic 

clay, mainly bauxitic. These boulders of pisolitic clay 

have been found by MacNeil to be common in eastern 

Georgia and as far east as Calhoun County, S. C., 

where they occur sporadically in a coarse sandy 

bed at the base of the Congaree formation and rest 

directly on dark shale of the Black Mingo formation. The occurrence of these boulders of pisolitic clay 

at the base of the beds of Claiborne age agrees with 

what is now known of the age of the period of bauxitization throughout the southeastern States. Bauxite is 

known to have been formed from clays both of Cretaceous and of early Wilcox ages. All these clays are 

believed to have been bauxitized during early Wilcox 

time. The occurrence of these reworked boulders of 

bauxite and pisolitic clay in deposits of the next great 

transgressive period—the Claiborne—is entirely consistent with the current dating of the bauxite.

WARLEY HILL MARL

The "Warley Hill phase," described by Sloan (1908, 

p. 458), was included in the McBean formation by 

Cooke in 1936. The name is here revived in a restricted 

sense to include the dominantly glauconitic beds that 

intervene between the Congaree formation and the 

Ostrea seUaeformis zone, or restricted McBean.

The following section at Warley Hill is modified from 

Cooke (1936, p. 71). It is proposed to restrict the 

term Warley Hill marl to beds 9 and 10. This locality, regarded as the type exposure of the formation, 

is on an abandoned road west of State Highway 267 

and south of Warley Creek 3 miles north-northwest 

of Lone Star, Calhoun County, within the Elloree 

quadrangle.

Section at Warley Hill

Middle Eocene. Feet 

Warley Hill marl (middle Claiborne).

10. Yellow sandy clay at base, passing into reddish-yellow massive argillaceous sand containing many small grains of glauconite__ 16

Middle Eocene—Continued Feet 

Warley Hill marl (middle Claiborne)—Continued

9. Fine green to yellow glauconitic sand containing Venericardia sp. and other fossils. In 

sharp contact with the bed below———— 6 

Congaree formation (lower Claiborne).

8. Greenish and yellow to gray brittle, nonplastic clay resembling fuller's earth; a few 

casts of mollusks, including Anodontiat 

augustana Gardner—————————————— 14

7. Sparsely glauconitic light-weight gray to yellow marl; a few casts of mollusks-———— 2%

6. Greenish-gray glauconitic sand with some 

clay at top; scattered pebbles 0.5 inch in 

diameter along base————————————— 1 

Paleocene(?) and lower Eocene. 

Black Mingo formation.

5. Flaky brown nonplastic clay_———___..— 1

4. Slightly coherent fine yellow or red sand, a 

decomposed sandstone, where fresh containing Ostrea- crenulimarginata Gabb?_— 2

3. Compact, brittle blue-gray shale or clay (fuller's earth) ; lower part with slaty cleavage, upper part more massive and with 

conchoidal or hackly fracture-——————— 8

2. Fine gray to yellow sand mingled with black 

carbonaceous, sandy clay; a 6-inch indurated ledge at top_____________ 2%

1. Concealed to level of Warley Creek__—__ 14

According to Sloan (1908, p. 302) the top of the Warley Hill marl was exposed at Cave Hall and at Whaley?s 

mill on Poplar Creek, both now in Calhoun County. 

At both localities it consisted of harsh, gray-green 

glauconitic marl. Sloan obtained well-preserved specimens of Ostrea lisbonensis Harris (reported as O. sellaeformis), a reliable and characteristic fossil of the 

lower part of the Winona formation of Mississippi and 

of the basal glauconitic marl of the Lisbon formation of 

Alabama, at Cave Hall. At both places, he says, the 

Warley Hill is overlain by the Santee limestone. The 

contact at Cave Hall seems to be unconformable, for 

Sloan describes it as undulating, and he reports 

rounded lumps of the Warley Hill marl in the base of 

the Santee limestone.

Cave Hall is a deep ravine containing a flowing 

stream about 0.4 mile long entering Lake Marion 0.8 

mile south of the embayed mouth of Halfway Swamp 

and 4.5 miles north-northeast of Elloree. Hard white 

limestone, presumably the lower part of the Santee 

limestone, though no fossils were found in it, is still 

exposed at the head of the ravine, but the Warley Hill 

marl there, which Sloan reports as rising 3 feet above 

the base line of the ravine, may now be covered by 

backwater from the lake.

MCBEAN FORMATION

As originally defined by Veatch and Stephenson 

(1911, p. 237), the McBean formation of eastern Geor-
24 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1952

gia was equivalent to the combined Tallahatta formation and Lisbon formation of the Alabama section. 

The McBean is here restricted to include only the Cook 

Mountain equivalent, the Ostrea sellaeformis zone, of 

the Lisbon formation. This is represented at McBean, 

Georgia, and in South Carolina by white sandy marl 

and massive yellow or red sand, which appears to be at 

least partly residual from sandy marl. At Shell Bluff, 

on the Georgia side of Savannah River, a bed of nearly 

80 feet of sandy marl and limestone includes a 6-foot 

bed carrying large Ostrea sellaeformis (Cooke, 1943, p. 

57).

The massive sand contains local patches of silicified 

shells, many species of which occur also in the Lisbon 

formation and in the Cook Mountain formation of Mississippi. Fossils from several such patches in Orangeburg County *are listed in Bulletin 867, notably Caw 

Caw Swamp (p. 63), Pooser's Hill (p. 64), and Orangeburg (p. 65).

A conspicuous component of the McBean formation 

in South Carolina is a very light weight sandstone or 

siltsone that appears to be a marl from which all the 

lime has been leached. This rock commonly contains 

Pteropsis lapidosa Conrad, a thin-shelled pelecypod 

with concentric undulations that seems to be confined to 

the McBean.

SANTEE LIMESTONE

The "Santee beds" were first correlated with the 

Jackson "stage" by Dall (1898, p. 342), though he says: 

"Tuomey included Claibornian as well as Jacksonian 

marls in his series. The term as adopted here refers 

to the upper green marls from which Zeuglodon has 

been obtained." Dall may have had in mind the Cooper 

marl rather than the Santee limestone as those formations are now divided, though no true zeuglodonts are 

known from the Cooper. The "Zeuglodon" of Tuomey 

was a primitive toothed whale. It was found in the 

Cooper. The only zeuglodontid from South Carolina, 

Dorudon serratus Gibbes, probably was found either in 

the Santee limestone or in the Castle Hayne limestone.

The Jackson age of the Santee limestone was accepted 

by Canu and Bassler (1920), who referred the large 

fauna of Bryozoa at Eutaw Springs and Leneudes 

Ferry to the "middle Jacksonian." They listed a total 

of 130 species from the two places. Eighty-one of these 

species are reported also from Wilmington, N. C., 

and 58 from the Ocala limestone in Georgia. The 

Bryozoa from Wilmington, N. C., are for the most part 

from the Castle Hayne limestone, though some may 

have come from the Santee limestone, which underlies 

it there. It is not surprising that the faunas of the 

Santee, Castle Hayne, and Ocala limestones are somewhat similar, for these three formations represent similar facies. The Santee and Castle Hayne faunas were 

not recognized as of Claiborne age because no similar 

bryozoan-bearing limestone facies occurs in the 

Claiborne west of the Carolinas.

The most conclusive paleontologic evidence for the 

middle Claiborne age of the Santee limestone is the 

presence in it of well-developed specimens of Ostrea 

sellaeformis Conrad. According to Stenzel (1949) 

this species is restricted to beds of middle Claiborne 

age, i. e., of the age of the Cook Mountain formation 

of Texas. This agrees with MacNeil's observations in 

Mississippi, Alabama, and Georgia, where shells of O. 

sellaeformis have not been found in beds younger than 

Cook Mountain except as badly worn and obviously 

reworked specimens.

The middle Claiborne age of the Santee limestone is 

indicated also by the occurrence in it of CMamys waur 

ttibbeana (Dall), a species elsewhere restricted (so far 

as is known) to that horizon, and by several unnamed 

species that seem to have the same range.

The commonly accepted type exposure of the Santee 

limestone is Eutaw Springs, in Orangeburg County, 

3y2 miles east-northeast of Eutawville. Backwater 

from Lake Marion has partly inundated the old exposure, but some limestone still stands above the level 

of the reservoir. Among species recently taken are 

Ostrea sellaeformis and Eurhodia raveneli (Twitchell).

The best collecting from the Santee limestone is at 

the spoil bank of the New Santee-Cooper Diversion 

Canal near Eadytown, at the crossing of Route 45. 

Caution should be used in interpreting the collections, 

for perhaps the Castle Hayne limestone overlies the 

Santee limestone in that region. The Santee fauna 

from this locality has been studied by Harbison (1944). 

The following species were collected by the present 

writers near Route 45 in 1950 and 1951:

Fossils from the Santee-Cooper Diversion Canal

Mollusca:

Turritella sp. aff. T. wechesensis Bowles

Cypraea sp.

Conus sp.

Ostrea sellaeformis Conrad.

0. carolinensis Conrad

0. n. sp. aff. 0. podagrina Dall

Chlamys wautabbeana (Dall)

C. n. sp. aff. C. membranosa, (Morton)

C. sp. aff. C. clarkeana (Aldrich)

Plicatula fttamentosa Conrad.

Spondylus sp.

Venericardia sp. aff. V. alticostata, (Conrad)

Crassatatella n. sp. aff. C. texana (Hellprin) but^with an

obtuse posterior ridge 

Lirodiscus santeensis Harbison 

Pitar (CostacalUsta) sp. 

Solen sp. cf. 8. Hsbonensis Aldricb
TERTIARY STRATIGRAPHY OF SOUTH CAROLINA 25

Echinoidea: 

Cidaris sp.

Coelopleurus infulatus (Morton) 

Protoscutella conradi (Cotteatt) 

Cassidulus gregoryi (Twitchell) ? 

Eurhodia raveneli (Twitchell)

Besides the species listed above, all of which are believed to have been derived from the Santee limestone, 

one specimen of Ostrea trigonalis Conrad was found. 

This probably came from a higher horizon, for there 

are blocks of a harder limestone that apparently does 

not contain 0. sellaefonrvis.

CASTLE HAYNE LIMESTONE

The Castle Hayne limestone, heretofore known only 

from North Carolina, was named by Miller (1910,1912) 

from a town in New Hanover County, N. C. The 

formation has since been described by Kellum (1926) 

and by Richards (1950). It was referred to the 

upper Eocene by Miller, and subsequent writers have 

correlated it with the Jackson group. Canu and 

Bassler (1920), who described a large fauna of Bryozoa 

from Wilmington, specified the age as "middle Jacksonian."

The echinoids, mollusks, and branchiopods from the 

Castle Hayne limestone were studied by Kellum (1926). 

Their evidence seemed to confirm the Jackson age, 

though Kellum says that "The poor state of preservation of most of the fossils, together with the relatively 

large number of new forms and the long range of some 

of the species, greatly limits their value in correlation." 

With the greater knowledge of the range of some species 

since acquired, it seems evident that most of the fossils 

attributed by Kellum to the Castle Hayne are somewhat older than he supposed, and that the Castle Hayne 

as here restricted is of late Claiborne age, equivalent 

to the Gosport sand of Alabama as now restricted.1 

Among the species supposed to indicate the Jackson age 

were Periarchws lyelli (Conrad), Ostrea georgiana 

Conrad ( = 0. gigantissima Finch), Ostrea ttrigonalis 

Conrad, Chlamys deshayesii (Lea) and Crassatella alta 

Conrad. Of these only Ostrea gigantissima, is now regarded as exclusively Jackson, and Kellum reports it 

only from Pollocksville, where its only associate is 

Ostrea trigonalis, also commonly Jackson. The specimens identified as CMamys deshayesii apparently represent a different, probably ancestral species. The 

other fossils occur also in the restricted Gosport sand, 

and Crassatella alta seems to be confined to it.

1 In 1939 Cooke supposed that the Gosport sand was of basal Jackson 

age, part of his evidence being the occurrence In it of Periarchus lyeltt 

(Conrad) and Ostrea trigonalis Conrad, species then considered as good 

indicators of Jackson age. The base of the Jackson at Claiborne, Alabama, is now drawn below the Ghlamys deshayesti (Lea) bed. which was 

originally included as the top bed in the "Claiborne sand" (Gosport 

sand).

The fossils from Wilmington, Castle Hayne, and several other places listed by Kellum (1926, p. 11) include 

a few species that indicate the presence of middle Claiborne beds as well as the Castle Hayne limestone. 

Among these species are Eurhodia raveneli (Twitchell), 

probably Hemipatagus subrostratiis Clark, and Ostrea 

sellaeformis Conrad. The middle Claiborne beds evidently include the coarse phosphatic basal conglomerate that lies on the Cretaceous at Wilmington and 

Castle Hayne and probably also several feet of limestone coquina that overlies the* conglomerate. The 

name Santee limestone might appropriately be extended 

to these beds. The following section near Wihnington 

is based on a description and a diagram in the field 

notes of L. W. Stephenson, 1909. The locality is no 

longer accessible. The age assignments are by the 

present writers. The thicknesses are all approximate.

Section in the county rock quarry near Wilmington

Pleistocene? Feet 

7. Fine to medium-grained loose yellow sand.

About______________________ 8 

Miocene

Duplin marl?

6. Thin remnants of a sandy shell bed_____ 0-1 

Eocene

Castle Hayne limestone

5. Irregular masses of hard, massive limestone 

penetrated by solution channels; highly 

fossiliferous, containing abundant Terebratula, Periarchus lyelli, several other species of echinoids, many bryozoans__—_ 10-12 

4. Very soft granular limestone with an abundance of bryozoans, Terebratula. The tipper surface is uneven_—____—___ 2-4 

Santee limestone?

3. Hard bluish limestone with small dark phosphatic specks. Evidently formed as a coquina, as cross-bedding is evident in places- 2 

2. Stratified and cross-bedded coquina limestone, 

partly indurated; ledge at base similar to 

overlying bed. Contains bryozoans, small 

pelecypods, and other fossils___———_ 8 

1. Phosphatic conglomerate consisting of darkgreen nodules in a matrix of gray calcareous 

sand, all very hard—————————————— 3

In South Carolina the Castle Jlayne limestone has 

been recognized only in artificial exposures. The deep 

pit of the Carolina Cement & Lime Company 2 miles 

north of Harleyville, Dorchester County, when examined in June 1951, showed the following sequence:

Section at the Carolina Cement & Lime Company

Pleistocene Feet

Wicomico formation?

7. Dirty, clayey, sandy soil__———_———_ 3 

6. Mottled gray and red clay, weathered at top_ 3 

5. Subangular gravel containing pebbles as much

as % inch in diameter at base—————__ 5
26 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1952

Unconformity peet 

Miocene?

4. Fine angular yellow sand containing black

grains and some glauconite_________ 8 

Oligocene (?) 

Cooper marl.

3. Pale greenish-gray granular marl, glauconitic 

throughout and containing phosphatic nodules at the base; Foraminifera and Chlamys 

cocoana (Dall) abundant__________ 3-8 

Unconformity 

Eocene

Castle Hayne limestone.

2. Buff-gray, tough to hard, crumbly limestone; 

Chlamys cooJcei (Kellum) throughout; 

Chlamys n. sp. and Glyoymeris staminea, 

Conrad in upper part; Chlamys n. sp. aff. C. 

deshayesii (Lea), Ostrea trigonalis Conrad, 

and Periarchus lyelli (Conrad) in lower 

part __———_—_______________ 18 

1. Gray soft, fine-grained, granular limestone to 

bottom of pit; Chlamys cookei and Periarchus lyelli_______________________________ 28

In addition to the species listed in the section, which 

were all found in place, the following species were collected from loose blocks of limestone, which apparently 

came from bed 2: Endopachys sp., TumteTla sp. cf. 

T. arenicola Conrad, Miltha sp. aff. M. claibomensis 

Conrad, Crassatella alta Conrad, Lucina sp. cf. L. pandata Conrad, a large Fusinusf, a Cardium, and a 

Panope.

Of the identified species in beds 1 and 2 all but Glycymeris staminea are listed by Kellum from the Castle 

Hayne limestone in North Carolina, and that species 

is a Gosport form.

A sample from the lower part of bed 2 yielded the 

following species of Foraminifera:

Foraminifera from the Castle Hayne limestone at the Carolina 

Cement & Lime Company pit

(Identified by M. R. Todd)

Spiroplectammina wilcoxensis Cushman and Ponton?

Textularia recta Cushman

GlobuMna sp.

Entosolenia sp.

Bolivina sp.

Reussella sp.

Anffuloaerina byramensis (Cushman) var.

Valvulineria n. sp. (cf. V. crassisepta Keijzer)

Oyroidina soManii octocamerata Cushman and G. D. Hanna

Eponides sp. 1

E. sp. 2

Alabamina wilcoxensis Toulmin

Cibioiaes danvillensis Howe and Wallace

C. lobatiilus (Walker and Jacob)

C. plano-conveums Cushman and Todd

A rock pit in Orangeburg County nearly 3 miles north 

of the cement plant also entered the Castle Hayne limestone, and is apparently bed 1 of the above section.

The pit, which is now full of water, is about half a 

mile west of Four Holes Station and 3 miles southsouthwest of Holly Hill. Periarchus lyelli and 

Chlamys cookei were found there.

DEPOSITS OF JACKSON AGE

The formations of Jackson age listed by Cooke in 

1936 included the Santee limestone, the Cooper marl, 

and the Barnwell sand. It has been shown that the 

Santee limestone is of middle Claiborne age, some beds 

mapped as Barnwell are of early Claiborne (Congaree) 

age, and others are of middle Miocene (Hawthorn) 

age. The Cooper marl is probably of early Oligocene 

(Eed Bluff) age. A small part of the supposed Barnwell remains as the only true representative of the 

Jackson among the outcropping formations. It is possible, however, that the Ocala limestone or its equivalent 

is present under cover as the offshore representative of 

the Barnwell. This is suggested by the occurrence of 

Ostrea podagrmct Dall, an Ocala species, at Givhans 

Bridge (Cooke, 1936, p. 86).

BARNWELL FORMATION

On the Savannah River at Shell Bluff, in Burke 

County, Georgia, and extending downstream to Griffins 

Landing, the Barnwell formation consists chiefly of a 

30-foot bed of large shells of Ostrea gigantissima Finch 

embedded in pebbly sand and yellowish marl or hard 

calcareous clay containing Bryozoa (Cooke and 

Shearer, 1918, p. 61). A few occurrences of this oyster 

bed have been noted in South Carolina. Sloan (1908, 

p. 268) reported it along Lower Three Runs on the farm 

of J. W. Ussery, which is probably a mile or more below 

the Allendale-Barnwell County line. A well at Baldock passed through an oyster bed, perhaps of this 

same species, about 30 feet below the level of Miller 

Creek at Baldock (Cooke, 1936, p. 89). However, this 

oyster bed may have been composed of Ostrea sellaeformis and hence may be part of the underlying McBean 

formation.

A small outcrop of cream-colored very sandy, calcareous marl in the bed of Miller Creek at an old dam 

below the water tank at Baldock is probably Barnwell, 

though it was referred to the Cooper marl by Cooke 

(1936, p. 88). Such a marl would leach to a massive 

red sand considered characteristic of the Barnwell, and 

very common in Burke County, Georgia, notably around 

Louisville. Canu and Bassler (1920) list 38 species of 

Bryozoa from this marl at Baldock. None of these 

species are restricted elsewhere to the Santee limestone, 

though nine ranged from a higher horizon down to it. 

One is known only from the Castle Hayne at Wilmington, and 21 species occur there. Nine are restricted to
TERTIARY STRATIGRAPHY OF SOUTH CAROLINA 27

the Ocala limestone, and 27 are listed from it. Seven 

were found only at Baldock. The evidence of the 

Bryozoa indicates that the marl at Baldock is of late 

Eocene (Ocala) age.

The marl at Baldock is very rich in Foraminifera. 

The following species have been identified:

Foraminifera from Eocene marl at Baldock 

(Identified by M. R. Todd)

Spiroplectammina mississippiensis alaoamensis (Cushman)

Textularia adalta Cushman

T. subhauerii Cushman '

Gaudryina sp.

Massilina decorata Cushman

Romulus sp.

Planularia georgiana Cushman and Herrick

Nodosaria latejugata carolinensis Cushman '

Lagena costata (Williamson)

Outtulina byramensis Cushman

Olobulina gibba punctata d'Orbigny

G. sp.

Sigmorphina jacJcsonensis (Cushman) *

8. sp. cf. 8. undulosa (Terquem)

8. sp.

PolymorpMna advena Cushman

Nonion inexcavatum (Cushman and Applin)

Entosolenia orbignyana flintii (Cushman)

Bolwina gardnerae Cushman

B. mississippiensis Cushman

B. mornJiinvegi Cushman

Reussella eocena (Cushman)

R. sp.

Uvigerina sp. cf. U. cookei Cushman

Angulogerina byramensis (Cushman)

Discorbis assulata Cushman

D. subaraucana Cushman="D. georgiana Cushman and

Herrick"

Valvulineria texana Cushman and Ellisor 

Oyroidina sp. 

Eponides sp.

Siphonina jacksonensis Cushman and Applin 

Amphistegina sp. cf. A. alabamensis Applin and Jordan 

Alabamina sp. 

Globigerina sp. 

G. sp. 

Hantkenina alabamensis Cushman ( ==H. longispina of Cushman

and Herrick) 

Anomalina sp.

Cibicides sp. cf. C. americanus (Cushman) 

C. danvillensis Howe and Wallace 

C. lobatulus (Walker and Jacob) 

C. mississippiensis (Cushman) 

C. plano-convexus Cushman and Todd

According to Miss Todd the following species are not 

known from beds younger than Eocene: Nodosaria 

latejugata carolinensis, Nonion inewcavatum, Reussella 

eocena^ and Cibicides danvillensis.

OLIGOCENE SERIES

When Cooke's report was written the only known 

representative of the Oligocene series in South Carolina

was the Flint Kiver formation, which is represented by 

residual blocks of fossiliferous chert, of late Oligocene 

age. It now appears that the Cooper marl, then supposed to be late Eocene in age, is really one stage 

younger, early Oligocene(?), and is equivalent to the 

Red Bluff formation of Alabama and Mississippi. 

Oligocene limestone in Screven County, Georgia, and 

residual cherts derived from it found along the Savannah River are still believed to be of late Oligocene age.

COOPER MARL,

The Cooper marl has been shifted back and forth 

between the Eocene and the Oligocene. Tuomey (1848) 

and Holmes (1870) called it Eocene, but Ball (1898) 

referred it to the lower Oligocene, which then included the Ocala limestone. Stephenson (1914) and 

Rogers (1914) classified the Cooper as uppermost 

Eocene or Oligocene. Stephenson (1914, p. 85) cited 

the supposed occurrence in it of Basilosaurus as indicating its Eocene age. This occurrence presumably referred to the so-called Zeuglodon, which Tuomey (1848, 

p. 166) mentioned as having been found in the long, low 

bluff extending from Greer's Landing to Middleton 

Place on the Ashley River. This specimen has since 

been identified as AgoropMus pygmaeus (Miiller), an 

archaic toothed whale. Other related forms in the 

Cooper marl are Xenorophus sloanii Kellogg, from 

Woodstock, and possibly Archaeodelphis patrius Alien. 

According to Dr. Remington Kellogg (oral communication) , these are the most primitive representatives of 

the toothed whales, and as none have been found elsewhere in known Eocene deposits, he thinks they are 

early Oligocene. Higher zones contain less primitive 

forms.

A more specific indication of early Oligocene age is 

CJdamys cocoana (Ball). The type of this little pecten was supposed to have been found in beds of Jackson 

age near old Cocoa Post Office, Choctaw, County, Alabama, but it bears the same station number as Red Bluff 

(early Oligocene) fossils from that vicinity and it is 

similar to them in color, differing in appearance and 

state of preservation from shells of known Jackson age. 

CJdamys cocoana is abundant in the Cooper marl at 

the Carolina Cement & Lime Company pit (see section, p. 26).

The Foraminifera from the Cooper marl at the 

cement plant were studied by M. R. Todd, who reported 

that the fauna appears to be of Red Bluff age. This 

age is suggested primarily by the occurrence of Bolvoinella rugosa Howe, a Red Bluff species. Bolivinella 

is not known from beds older than Oligocene. The 

list of species follows:
28 SHORTER CONTRIBUTIONS TO GENERAL GEOLOGY, 1952

Foraminifera from $he Cooper marl (bed 3) at the Carolina 

Cement & Lime Company

(Identified by M. R. Todd)

Spiroplectammina mississippiensis (Cushman)

8. mississippiensis alabamensis (Cushman)

Robulw sp.

MarginuUna oocoaensis Cushman

M. sp.

Dentalina sp.

Lagena costata (Williamson)

GuttnUna byramensis (Cushman)

Globulina gibba d'Orbigny

Nonion afflne (Reuss)

Bolivinella rugosa Howe

Bulimina ovata d'Orbigny

BoUvina, byramensis Cushman

B. costifera Cushman

B. gardnerae Cushman

B. sp.

Lovostomum sp.

Bifarina vicksburgensis (Cushman)

Uvifferina yazooensis Cushman

Angulogerina byramensis (Cushman)

A. byramensis (Cushman) var.

Ellipsonodosaria cocoaensis (Cushman)

Discorbis arcuato-costata Cushman

D. subaraucana Cushman

D. sp.

Gyroidina byramensis Cushman and Todd?

G. sp.

Eponides sp.

Siphonina sp.

Cancris sp.

Gtobigerina sp.

Cibioides sp. cf. C. choctawensis Cushman and McGlamery

C. lobatulus Walker and Jacob

C. mississippiensis (Cushman)

C. pseudoungerianus (Cushman)

Stichocibicides n. sp.

Dyooibicides sp.

A well-marked erosional contact of the Cooper marl 

on the Castle Hayne limestone at the cement plant is 

additional evidence of a time break, though it does not 

rule out the possibility that the Cooper is Jackson.

MIOCENE SERIES

HAWTHORN FORMATION

A thin series of sandy clay and gravelly sand beds 

similar to and presumably originally continuous with 

the Hawthorn formation of Georgia emerges from beneath cover at the northern margin of the coastal terraces and overlaps older formations. This facies of the 

supposed Hawthorn is quite different from the offshore 

fades, known only from well cuttings and a very few 

outcrops in Hampton and Colleton Counties, on the 

basis of which the Hawthorn was first recognized in 

South Carolina.

Detailed mapping will be required to determine the 

extent of the Hawthorn formation in South Carolina 

and to distinguish it from similar f acies of the Eocene 

and Cretaceous formations. The formation can generally be recognized by a characteristic mottling of pink 

or yellow and gray, though these colors are by no means 

confined to it. An outcrop that can be referred to the 

Hawthorn with some assurance is in the cut of the Atlantic Coast Line Railroad that extends 1 mile east from 

the station at Barnwell. Cooke (1936, p. 91) referred 

this cut to the Barnwell sand, though it was not considered typical of that formation. Cuts along a new spur 

line extending northwestward from Dumbarton show 

excellent exposures of the Hawthorn formation.

REFERENCES

Bowles, Edgar, 1939, Eocene and Paleocene Turritellidae of the 

Atlantic and Gulf Coastal Plain of North America: Jour. 

Paleontology, vol. 13, no. 3, pp. 267-336, pis. 31-34.

Canu, F., and Bassler, R. S., 1920, North American early Tertiary Bryozoa: U. S. Nat. Mus. Bull. 106, 879 pp.

Cooke, C. Wythe, 1936, Geology of the Coastal Plain of South 

Carolina: U. S. Geol. Survey Bull. 867, 196 pp.

———, 1939a, Equivalence of the Gosport sand to the Moodys 

marl: Jour. Paleontology, vol. 13, no. 3, pp. 337-340.

———, 1939b, Geologic map of Georgia [Coastal Plain]. Georgia Div. Mines, Mining, and Geology. 

-, 1943, Geology of the Coastal Plain of Georgia: U. S.

Geol. Survey Bull. 941, 121 pp. [1944]. 

Cooke, C. Wythe, and Shearer, H. K., 1918, Deposits of Claiborne and Jackson age in Georgia: U. S. Geol. Survey Prof.

Paper 120, pp. 41-81. 

Dall, William Healey, 1898, A table of the North American

Tertiary horizons, correlated with one another and with

those of western Europe, with annotations: U. S. Geol.

Survey Eighteenth Ann. Kept., pt. 2, pp. 327-328. 

Gardner, Julia, 1951, Two new guide fossils from the Tallahatta formation of the Southeastern States: Washington

Acad. Sci. Jour., vol. 41, no. 1, pp. 8-12.

Harbison, Anne, 1944, Mollusks from the Eocene Santee limestone, South Carolina: Notulae Naturae 143, 12 pp., 4 pis. 

Holmes, F. S., 1870, Phosphate rocks of South Carolina and

the "Great Carolina marl beds." Charleston, S. C., 87 pp. 

Kellum, Lewis B., 1926, Paleontology and stratigraphy of the

Castle Hayne and Trent marls in North Carolina: U. S.

Geol. Survey Prof. Paper 143, 56 pp. 

MacNeil, F. Stearns, 1947, Geologic map of the Tertiary and

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Miller, B. L., 1910, Erosion intervals in the Tertiary of North

Carolina and Virginia: Geol. Soc. America Bull., vol. 20,

pp. 673-678. 

———, 1912, The Tertiary formations [of North Carolina]:

North Carolina Geol. and Econ. Survey, vol. 3, pp. 171-258. 

Richards, Horace G., 1950, Geology of the Coastal Plain of

North Carolina: American Philos. Soc. Trans., n. ser., vol.

40, pt. 1, 83 pp. 

Rogers, G. S., 1914, The phosphate deposits of South Carolina:

U. S. Geol. Survey Bull. 580, pp. 183-220.
TERTIAEY STRATIGRAPHY OF SOUTH CAROLINA 29

Sloan, Earle, 1907, Geology and mineral resources [of South Stephenson, L. W., 1914, A deep well at Charleston, South 

Carolina] : South Carolina, State Dept. Agriculture . . ., Carolina : U. S. Geol. Survey Prof. Paper 90, pp. 69-94.

,i - , « «, „ ' Michael- 1848' ReP°rt on the Seol°^ of South Caro- of me mineral locahties of South Carohna: South Carolina Geol. Survey, ser. 4, Bull. 2, 505 pp.

Stenzel, H. B., 1949, Successional speciation in paleontology: Veatch, Otto, and Stephenson, L. W., 1911, Preliminary report 

The case of the oyster of the sellaeformis stock : Evolution, on the geology of the Coastal Plain of Georgia : Georgia 

vol. 3, no. 1, pp. 34-50. Geol. Survey Bull. 26, 466 pp.

o