GEOLOGIC FRAMEWORK AND PETROLEUM POTENTIAL OF THE ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

^^^*mmm

^iTlfi".^- -"^ -|"CtS. V is-^K-i- GEOLOGICAL SURVEY PROFESSIONAL PAPER 659 cV^i-i'^S^;-^, - >->"!*- -' *-'-__

' ""^W^T^^'^rSV-t^^feijS

GEOLOGIC FRAMEWORK AND PETROLEUM POTENTLY L OF THE ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

By JOHN C. MAHBR

ABSTRACT less alined with a string of seamounts extending down the continental rise to the abyssal plain. The trends parallel to The Atlantic Coastal Plain and Continental Shelf of North the Appalachians terminate in Florida against a southeasterly America is represented by a belt of Mesozoic and Cenozoic magnetic trend thought by some to represent an extension of rocks, 150 'to 285 miles wide and 2,400 miles long, extending the Ouachita Mountain System. One large anomaly, known as from southern Florida to the Grand Banks of Newfoundland. the slope anomaly, parallels the edge of the .continental shelf This belt of Mesozoic and Cenozoic rocks encompasses an area north of Cape Fear and seemingly represents th** basement of about 400,000 to 450,000 square miles, more than three- ridge located previously by seismic methods. fourths of which is covered by the Atlantic Ocean. The volume Structural contours on the basement rocks, as drawn from of Mesozoic and Cenozoic rocks beneath the Atlantic Coastal outcrops, wells, and seismic data, parallel the Appalachian Plain and Continental Shelf exceeds 450,000 cubic miles, per­ Mountains except in North and South Carolina, where they haps by a considerable amount. More than one-half of this is bulge seaward around the Cape Fear arch, and in Florida, far enough seaward to contain marine source rocks in sufficient where the deeper contours follow the peninsula. Tl * basement proportion to attract exploration for oil. A larger fraction, surface is relatively smooth and dips seaward at rrtes ranging perhaps three-quarters of the volume, may be of interest in from 10 feet per mile inland to as much as 120 fret per mile exploration for gas. near the ocean. A decided steepening of the slope is apparent The Coastal Plain consists of land between the crystalline below a depth of 5,000 feet in most of the area. Tve principal rocks of the Piedmont province of the Appalachian Mountain structural features are the Southwest Georgia embayment, System and mean low tide from southern Florida to the tip of South Florida embayment, Peninsular arch, Bahama uplift, Long Island plus a few small offshore islands and Cape Cod. Southeast Georgia embayment, Cape Fear arcl, Salisbury This is an area of more than 100,000 square miles. embayment, Blake Plateau trough, Baltimore Canyon trough, The continental shelf extends from mean low tide to the Georges Bank trough, and Emerald Bank trough. break marking the beginning of the continental rise, which is Triassic, Cretaceous, and Tertiary rocks crop out roughly somewhat less than 600 feet in depth at most places. It is parallel to the present Atlantic coastline. Triassic outcrops are a gently sloping platform, about 350,000 square miles in area, confined to scattered down-faulted basins within tl * piedmont. that widens from less than 3 miles off southern Florida to Lower Cretaceous outcrops are recognized in tl«> Salisbury about 285 miles off Newfoundland. embayment of New Jersey, Delaware, Maryland, a^d Virginia, The Blake Plateau occupies an area of about 70,000 square and may be represented farther south as thin clastic beds miles between the 500- and 5,000-foot bottom contours from mapped with the basal Upper Cretaceous. Upper Cretaceous the vicinity of Cape Hatteras to the northernmost bank of rocks crop out almost continuously along the Far Line from the Bahamas. It has a gentle slope with only minor irregulari­ eastern Alabama to the north flank of the Cape Fear arch in ties and scattered patches of Holocene sediments. North Carolina and from Virginia to New York. Tertiary Gravity and magnetic anomalies along the Atlantic coast rocks crop out in broad patterns throughout the Costal Plain primarily reflect compositional differences in the earth's crust except on the Cape Fear arch and where masked by a veneer at great depths, but they are also related to some extent to of alluvial deposits. the structure and composition of the Coastal Plain sedimentary The Cretaceous and Tertiary rocks exposed from southern rocks and shallow basement. Four alternating belts of predom­ Georgia northward to Long Island are mainly continental inantly positive and predominantly negative Bouguer gravity elastics interspersed with some thin lignitic layers and marl anomalies extend diagonally across the region from southwest beds. Seaward, these rocks become marine in character and to northeast These correspond roughly with the continental thicken to more than 10,000 feet at the coastline. Cretaceous rise and slope, the continental shelf and Coastal Plain, the rocks do not crop out in southern Georgia and Florida, and Appalachian Mountain System front, and the Piedmont Tertiary rocks are only partially exposed. Both are predom­ Plateau-Blue Ridge-Appalachian Basin region. inantly marine carbonates in the subsurface and exceed Long, linear, northeastward-trending magnetic anomalies 15,000 feet in thickness in the Florida Keys and Bahama roughly parallel the Appalachian Mountain System and the edge of the continental shelf. These trends are interrupted Islands. along the 40th parallel, about 50 miles south of New York, by The subsurface correlations of the Mesozoic and Cenozoic a linear anomaly, suggesting a transcurrent fault, more or rocks beneath the Coastal Plain are traced along eight cross PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF sections. One section extends subsurface correlations from the is not far beneath the sea bottom where artesian submarine marine carbonate facies beneath the Florida Keys northward springs issue along the east coast of Florida. Short cores into the mixed marine and continental clastic facies beneath and dredgings of Tertiary rocks, mostly Late Eocene (Jackson) Long Island. The other sections trace units of the predom­ and younger in age, have been recovered at n^re than 3 inantly clastic outcrops downdip into marine facies along the dozen localities concentrated lor the most part between coast. Georges Bank and the Hudson Canyon and ir the Blake The pre-Mesozoic basement rocks beneath the Coastal Plain Plateau-Bahama Banks region. Pleistocene silts an^ clays have are primarily igneous and metamorphic rocks of Precambrian been found in many cores, and gravel afcd boulde-s of glacial and Paleozoic age. Some Paleozoic sedimentary rocks ranging origin have been dredged north of New York City. from Early Ordovician to Middle Devonian in age are in the Tertiary strata beneath the continental shelf have been basement in northern Florida. The oldest rock recovered from penetrated by two test holes about 10 miles off Srvannah, Ga. the sea bottom along the Atlantic coast has come from the The test holes, which stopped in the Ocala Limestone, revealed Paleozoic granite pinnacles at a depth of about 30 feet on that rather uniform thicknesses of Oligocene, lover Miocene, Cashes Ledge near the middle of the Gulf of Maine. and middle Miocene strata extend from the shore seaward for Triassic(?) rocks, which consist of red arkose, sandstone, at least 10 miles; that the upper Miocene rocks and the Pleis­ shale, tuff, and basalt flows, in places intruded by diabase, tocene and Holocene deposits decrease in thickness seaward; are present in downfaulted basins in the basement. Rocks of and that only the Oligocene rocks exhibit a pronounced facies Late Jurassic or Early Cretaceous (Neocomian) age are pres­ change, from carbonates to elastics in a seaward direction. ent beneath southern Florida. There the sequence, as much Tertiary rocks beneath the continental shelf have also been as 1,100 feet thick, consists principally of limestone, dolomite, penetrated by six test holes 27 to 221 miles off Jacksonville, and anhydrite with a marginal clastic facies at the base Fla. Stratigraphic data from these test holes indicate that where it rests on igneous basement. Equivalent rocks about Paleocene beds probably continue from the Coastal Plain to 900 feet thick are present at Cape Hatteras, N.C., and the edge of the Blake Plateau and are exposed a'' sea bottom extend northward along the coast into New Jersey. along the lower part of the slope. The Eocene, Oligocene, In Florida, the Lower Cretaceous rocks, subdivided into rocks and Miocene beds appear to be prograded seaward beneath of Trinity, Fredericksburg, and Washita age, are predom­ the outer shelf and slope and are greatly thinned on the pla­ inantly carbonates and exceed 6,700 feet in thickness beneath teau. They appear to be especially thin or even absent along the Florida Keys. Northward along the coast, the rocks wedge the lower slope, which corresponds approximately with the out on the Peninsular arch and then reappear as a thin clastic axis of maximum velocity of the Gulf Stream. Conclusions unit across Georgia and South Carolina. They are missing drawn from the test-holes data and some sparker profiles are from the higher parts of the Cape Fear arch in North Carolina that the shelf was built seaward rather continuously during but are present on the east Sank as a thickening wedge of Tertiary time and that the edge of the continental shelf has mixed clastic and carbonate rocks more than 2,800 feet thick been prograded about 9.3 miles by a mass of sediment 300 to at Cape Hatteras and 2,600 feet thick in Maryland. Lower 600 feet thick. Cretaceous rocks probably extend into northern New Jersey Upper Jurassic and Lower Cretaceous rocks offer the most but do not reach Long Island. Lower Cretaceous submarine promising prospects for oil and gas production in the Atlantic outcrops are present in the Blake Escarpment. coastal region. Offshore, their combined thickness probably Upper Cretaceous rocks, which can be subdivided into rocks exceeds 7,500 feet in the South Florida embayment and Blake of Woodbine, Eagle Ford, Austin, Taylor, and Navarro age, Plateau trough, 5,000 feet in the Southeast Georgia embayment are about 1,200 to 3,000 feet thick in wells along the coast. In and Baltimore Canyon trough, and 3,000 feet in the Georges Florida, they are almost totally marine carbonates. These Bank trough. Marine beds generally regarded as potential grade northward along the coast into mixed marine carbonates sources of petroleum are predominant, and the environment of and elastics in North Carolina and then into marine and their deposition, at least in the southern areas, probably continental elastics beneath Long Island. Rocks of Taylor favored reef growth. Thick, very porous salt-v^ater-bearing and Navarro age have been dredged from Oceanographer and reservoirs, both sandstone and carbonate, ar^ numerous. Gilbert Canyons off Georges Bank and rocks of probable Important unconformities are present not only at the top but Woodbine age from the Blake Escarpment. In addition, cobbles within the sequence. Three small accumulations of oil have of chalk containing Cretaceous Foraminifera have been found been found in Lower Cretaceous rocks of southwestern in a core from the floor of Northeast Providence Channel, Florida. 11,096 feet beneath the sea between the Bahama Islands, and In rocks of Late Cretaceous age good possibilities for oil reworked Cretaceous Foraminifera have been identified in a and gas production exist beneath the continental s^elf, but only core of coarse glauconitic sand on the continental rise, 155 fair possibilities, chiefly for gas, exist in the Coastal Plain. miles southwest of Cape Hatteras. Although the thickness of these rocks does not exceed 3,500 Tertiary rocks and thin Quaternary deposits are present feet onshore and may be only a few thousand feet more beneath along the Atlantic coast. The thickness of Tertiary rocks along the coast ranges from 4,300 feet in southern Florida to 130 the shelf, the beds are buried sufficiently beneath the Tertiary feet on Long Island. In general, the Tertiary rocks are pre­ rocks to provide ample opportunity for the accumulation of dominantly carbonates along the southern half of the Atlantic petroleum. Reservoirs are thick and numerous in the Upper coastline and are mostly sandstone and limy shale along the Cretaceous rocks of the. Coastal Plain and the^e reservoirs northern half. Marl of early Miocene age crops out on the seem to extend beneath the shelf, where marine source rocks fishing banks known as Black Rocks off the coast of North may be expected. Rocks of Woodbine and Earle Ford age and South Carolina. The Ocala Limestone of late Eocene age appear to be a favorable reservoir-source rock combination INTRODUCTION whose thickness probably exceeds 2,000 feet offshore. The basal ia.) More than one-half of this is far enough seaward unconformity is important from the standpoint of petroleum to contain marine source rocks in sufficient proportion accumulation, as in places it permits the basal Upper Creta­ ceous sandstones of Woodbine age to overlap the underlying, to attract exploration for oil. A larger fraction, per­ more marine Lower Cretaceous rocks. haps three-quarters of the volume, may be of interest Tertiary rocks along the Atlantic coast exhibit very good in exploration for gas. reservoir and fair source-rock characteristics; however, they This report outlines the structure along th«. Atlantic are less promising for large accumulations of petroleum than coast from southern Florida to northern Nova Scotia the Jurassic and Cretaceous rocks. Tertiary rocks are prob­ (fig. 1) and discusses the stratigraphy of the area be­ ably less than 4,000 feet thick in most of the area north of southern Florida and the Bahama Islands; they contain fresh- tween southern Florida and Cape Cod, Mass. The con­ to-brackish artesian water in much of that area; and they tinental shelf off Newfoundland is omitted because of crop out in part along the continental shelf and in other places lack of geological and geophysical information. Par­ give rise to submarine springs in sink holes. In addition, ticular emphasis has been placed on the regional strati- structural features are reflected less distinctly in the Tertiary graphic aspects of the subsurface rocks. rocks than in the older rocks, and unconformities and overlaps within the Tertiary rocks are less significant regionally than The purpose of this report is to establish a strati- those in older rocks. graphic framework within this large sedimer tary mass, The continental shelf offers more promise as a potential to outline the structure of the continental margin, and petroleum province than the Coastal Plain because it has a to evaluate the petroleum possibilities of this relatively thicker sedimentary column with better source beds and unexplored province to the extent that is possible at trapping possibilities. The probabilities for discovery of large accumulations of petroleum in 'the Atlantic coastal region on a this time. It is not intended to be a summation of all well-for-well basis seem to favor the Upper Jurassic and geology and oceanography along the Atlantic coast but Lower Cretaceous rocks beneath the continental shelf. rather a selective review and synthesis of the regional aspects of the possible petroleum-producing rocks be­ INTRODUCTION neath the Coastal Plain and continental shelf, based on data available October 1, 1966. A preliminary version AREA AND PURPOSE OF REPORT of this report (Maher, 1967a) was released to open The Atlantic Coastal Plain and Continental Shelf of file on October 30,1967. North America is represented by a belt of Mesozoic Earlier reports and maps prepared by the U.S. Geo­ and Cenozoic rocks, 150 to 300 miles wide and 2,400 logical Survey have provided a broad review of the miles long, extending from southern Florida to the general characteristics, problems, and potential mineral Grand Banks of Newfoundland (fig. 1). This belt resources of the continental shelves of the Western encompasses an area of about 450,000 square miles, Hemisphere (Trumbull and others, 1958) ; an estimate more than three-fourths of which is covered by the of the potential petroleum reserves of the Atlantic Atlantic Ocean. The submerged part forms the Atlan­ Coastal Plain and Continental Shelf based primarily tic Continental Shelf, which widens northward from on thickness of sediments (Johnston and others, 1959); 3 miles off Florida to about 285 miles at the Grand a representation of the basement structure along the Banks off Newfoundland. The area of the continental Atlantic coast from Florida to the Gulf of Maine shelf, including the Gulf of Maine, approximates (Cohee, 1962; Bayley and Muehlberger, 1£18) based 350,000 square miles. The emergent part, the Coastal on both geological and geophysical data published up Plain, narrows northward from a 200-mile width in to 1959; a report on correlations of subsurface Meso­ Georgia to the terminal point of Long Island. Beyond zoic and Cenozoic rocks along the Atlantic coast this point, remnants of the Coastal Plain are present (Maher, 1965); and summary discussions of petroleum in the form of the New England Islands of Wood- possibilities in relation to the stratigraphy (Maher, worth and Wigglesworth (1934) and Cape Cod. The 1966a, b; 1967b). In addition, numerous publications area of the Coastal Plain, including the eastern half have resulted from cooperative investigations with the of the Florida Peninsula, approximates 100,000 square Woods Hole Oceanographic Institution. These include miles. a map showing the relation of land and submarine The volume of Mesozoic and Cenozoic rocks beneath topography, Nova Scotia to Florida (Uchupi, 1965a), the Atlantic Coastal Plain and Continental Shelf of a summary of the geology of the continental margin North America exceeds 450,000 cubic miles, perhaps by off Eastern United States (Emery, 1965a), and many a considerable amount. (See Gilluly (1964, p. 484) for reports of lesser scope, most of which are mentioned estimates of volume between Nova Scotia and Virgin­ herein where appropriate. PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

90° W. 80° W. 70° W. 60° W. 50" W.

50° N.

40° N.

30" N.

20° N.

FIGURE 1. Physiographic province map of eastern North America, showing area discussed in this report. SOURCES AND RELIABILITY OF DATA North Carolina Department of Conservation and De­ velopment; Virginia Division of Mineral Resources; Many organizations provided well records and geo­ Maryland Department of Geology, Mines, and Water logical information: The Pure Oil Co. permitted use Resources; and New Jersey Department of Conserva­ of nonconfidential data from a reconnaissance report tion and Economic Development. The U.S. Geological prepared by J. C. Maher and Irvin Bass in 1959; the Gulf Oil Corp. and Anchor Gas Co. loaned samples and Survey field offices include those at Tallahassee, Fla., cores of their wells; State agencies and U.S. Geological Atlanta Ga., Columbia, S.C., Raleigh, N.C., Baltimore, Survey field offices engaged in ground-water investi­ Md., Trenton, N.J., Mineola, N.Y., and Boston, Mass. gations supplied a wealth of shallow subsurface data. The amount and reliability of subsurface well data The State agencies involved were the Florida Geolog­ on which this report is based differs greatly from one ical Survey; Georgia Department of Mines, Mining, part of the region to another. For example, the records and Geology; South Carolina Development Board; of 422 oil and deep water wells in 12 states r.nd the Ba- INTRODUCTION hama Islands have been used (pi. 1 and table 1), but 1962), Georgia (Antoine and Henry, 1965, fig. 1), and 213 records are for wells in only two states Florida Florida (Rona and Clay, 1966). The profiles are well and Georgia. Also, the geological records for the wells distributed from northern Florida to Nova Scotia but in Florida and Georgia are more complete and accurate little agreement exists on their stratigraphic interpre­ than those for wells in the northern part of the Coastal tation, partly because of the pronounced effect of Plain. No deep tests have been drilled in offshore lateral facies changes on seismic velocity measurements. waters on the continental shelf, except in the Florida Some seismic profiles off southern Newfoundland Keys area. In general, the geological data is much more (Press and Beckmann, 1954; Bentley and Worzel, reliable south of the Cape Fear arch than north of it. 1956) have been published, but little or no information Especially useful publications on regional stratig­ is available on the Grand Banks. The available geo­ raphy and structure of the Coastal Plain are those of physical information outlines the regional stricture of Cooke and Munyan (1938), Applin and Applin (1944, the shelf, but provides only speculative results for the 1947, 1965), Richards (1945, 1948, 1950), Southeastern stratigraphy. Geological Society (1949), Spangler (1950), Spangler Systematic investigations of subbottom rudiments and Peterson (1950), Skeels (1950), Bonini (1957), and strata along the Atlantic coast by means of dredg­ Meyer (1957), Pooley (1960), Bonini and Woollard ing, coring, and undersea photography we^e begun (1960),LeGrand (1961), and Murray (1961). Local re­ about 1930 by several oceanographic institutions. Large ports that present important basic data in detail in­ quantities of data have been accumulated in these con­ clude those of Cederstrom (1943, 1945), Siple (1946), tinuing programs. Data on the composition and age Swain (1947, 1951, and 1952), Anderson (1948), Ap­ of samples and cores have been reported by many plin (1951), Brown (1958), Puri and Vernon (1959), workers including Burbank (1929), Alexander (1934), Herrick (1961), Herrick and Vorhis (1963), and Sea- Shepard, Trefethen, and Cohee (1934), Shepard and ber and Vecchioli (1963); most of these are publica­ Cohee (1936), Bassler (1936), Cushman (19f«- 1939), tions of State geological surveys. Other reports on the Stephenson (1936), Stetson (1936, 1938, 1949), North­ Coastal Plain geology are included in the list of rop and Heezen (1951), Ericson, Ewing, and Heezen references. (1952), and Heezen, Tharp, and Ewing (1959). The Geophysical data on the continental shelf have been regional aspects of bottom sediment and submarine taken from reports prepared by the Woods Hole outcrop distribution in the Atlantic Ocean are dis­ Oceanographic Institution and the Lament Geological cussed at length by Ericson, Ewing, Wollin, and Hee­ Observatory. These include articles by Miller (1936), zen (1961), and Uchupi (1963). Detailed studies of Ewing, Crary, and Rutherford (1937), Ewing, Wool- samples and photographs of the bottom of th**. Tongue lard, and Vine (1939, 1940), Ewing, Worzel, Steen- of the Ocean in the Bahama Islands have been reported land, and Press (1950), Oliver and Drake (1951), by the Miami University Marine Laboratory, (1958), Officer and Ewing (1954), Drake, Worzel, and Beck- Busby (1962a, b, and c), and Athearn (1962a, b). The mann (1954), Press and Beckmann (1954), Katz and location and age of samples and cores listed in these Ewing (1956), Hersey, Bunce, Wyrick, and Dietz publications are shown on plate 2. (1959), Drake, Ewing, and Sutton (1959), Heezen, ACKNOWLEDGMENTS Tharp, and Ewing (1959), Ewing, Ewing, and Ley den (1966), and Sheridan, Drake, Nafe, and Hennion Numerous individuals have contributed to the com­ (1966). Bathymetry of the shelf has been taken from pletion of this report. E. R. Applin and P. L. Applin, the tectonic map of the United States (Cohee, 1962) who pioneered in the Mesozoic stratigraphy of Florida, and charts of the U.S. Navy Hydrographic Office provided much basic data that are summarized in (1951, 1952b, 1955, 1962a, b), the U.S. Coast and numerous publications by the U.S. Geological Survey. Geodetic Survey (1945, 1957, 1959, 1961, 1962), and They also made available much unpublished paleonto- the International Hydrographic Bureau (1958). logic data for wells in Alabama, Georgia, South Caro­ Numerous seismic refraction profiles of the conti­ lina, and North Carolina, offered useful suggestions nental shelf have been published. The locations of on many stratigraphic problems, and reviewed sections most of these are shown on plate 2, but space does K-L, M-N, and O-P. E. R. Applin, who contributed not permit plotting of some short ones such as those the paleontologic basis for age assignments discussed off Sable Island (Berger, Blanchard, Keen, McAllister, in this report in the section on stratigraphy, worked and Tsong, 1965), Rhode Island (Birch and Dietz, on the project several months studying paleontology PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF of selected wells in Florida and the Anchor Gas Dickin- and Bahama Banks where calcareous sediments pre­ son 1 well in New Jersey. dominate, the surface is covered with quar+s silt that S. M. Herrick, of the U.S. Geological Survey, Heezen, Tharp, and Ewing (1959, p. 58) suggest may Atlanta, Ga., whose paleontologic studies have estab­ come from the Cape Hatteras region or the Hudson lished the stratigraphic framework of subsurface rocks Canyon. (See fig. 2.) Numerous seamounts are present in Georgia, was most generous with unpublished data. on the northern part of the abyssal plain. His cooperation and knowledge of regional subsurface The continental rise extends westward and upward concepts were important to the completion of the cross from the edge of the abyssal plain to the continental sections. Sections I-J and K-L were reviewed by Mr. slope. It is relatively wide, reaching sever-*! hundred Herrick. miles in places, and has gentle slopes, generally between P. M. Brown, of the U.S. Geological Survey, Raleigh, 5 and 50 feet per mile. The depth of water ranges N.C., provided data for several wells in North Caro­ from 4,200 to 16,800 feet. The relief is low for the most lina. He reviewed section G-H. part but is represented by an outer ridge adjacent to R. E. Peck, of the University of Missouri, identified the eastern side of the Blake Plateau. Several sub­ and gave an age opinion for a specimen of Charophyta marine canyons extend across the continental rise from the Anchor Gas Co. well in New Jersey. J. M. (Ericson and others, 1951, p. 964), and r^veral sea- Schopf and R. H. Tschudy, of the U.S. Geological mounts rise above it off the New England coast. Survey, provided opinions of the age of spores and The relatively steep and narrow continental slope pollen in the same well. parallels the continental rise and continental shelf at N. M. Perlmutter and Ruth Todd, of the U.S. depths ranging from 600 to 10,500 feet. The base is Geological Survey, allowed the writer to read the marked by a gradient in excess of 132 feet per mile manuscript of their report on the Monmouth group (Heezen and others, 1959, p. 19) and the top by the in the well at the Bellport Coast Guard Station, Long sharp break at the edge of the shelf. Numerous sub­ Island (well 6, pi. 1). marine canyons traverse the continental slope. Cores, samples, and data for key wells were pro­ The continental shelf extends from mean low tide vided by the following: R. S. Stewart, of Anchor Gas to the shelf break, or beginning of the continental Co.; L. J. Franz and Roy A. Worrell, of Gulf Oil rise, which is somewhat less than 600 feet in depth at Corp.; W. D. Lynch and Marvin Horton of Chevron most places. It is a gently sloping surface with a Oil Co.; L. R. McFarland, of Mobil Oil Co.; K. N. gradient generally less than 5 feet per irile, and it Weaver, of the Maryland Department of Geology, ranges in width from a few miles off Florida to more Mines and Water Resources; H. G. Richards, of the than 285 miles off Newfoundland. The relief is rela­ Philadelphia Academy of Natural Sciences; W. E. tively low, although the surface is cut by numerous Wilson, of the North Carolina Geological Survey; submarine canyons. J. L. Ruhle, of the Virginia Geological Survey; and The Coastal Plain is the belt of nearly flat land Clarence Babcock of the Florida Geological Survey. that lies between the Piedmont province of the Appa­ lachian Mountains and the shoreline; iso^ted parts PHYSIOGRAPHIC FEATURES include Cape Cod and a few small offshore islands. PROVINCES OF WESTERN NORTH The width narrows northeastward from a maximum ATLANTIC REGION of about 200 miles in Georgia. The altitude decreases gently seaward from about 800 feet at the edge of the The physiographic provinces of the western North Piedmont province. Atlantic region, as defined by Heezen, Tharp, and The Appalachian Mountains form a highland of Ewing (1959) and as outlined in figure 1, are the Precambrian, Paleozoic, and Triassic rockf stretching abyssal plain, the continental rise, the continental slope, the Continental Shelf, the Coastal Plain, and the from the Canadian Maritime Provinces southwestward Appalachian Mountains. The abyssal plain is a part into Alabama. In the central and southern part, the of the ocean-basin floor; the continental rise, continen­ Appalachian Mountains comprise, from es^t to west, tal slope, and continental shelf make up the continental four distinct, subparallel physiographic subdivisions: margin. (1) the Piedmont province, of moderate reMef, carved The abyssal plain is the nearly flat ocean bottom in deformed crystalline rocks with maximum altitudes that has slopes generally less than 5 feet per mile. of about 2,000 feet, (2) the rugged Blue Pidge prov­ Except in a small, isolated area near the Blake Plateau ince, composed of igneous and metamonhic rocks PHYSIOGRAPHIC FEATURES

FIGITKB 2. Principal physiographic features of the Atlantic Coastal Plain and Continental Shelf. 8 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF that rise to a maximum altitude of 6,711 feet at Mount PROMINENT COASTAL FEATURES Mitchell, N.C., (3) the Valley and Ridge province of GULF OF MAINE considerable relief carved in deformed sedimentary rocks with maximum altitudes of 5,000 feet, and (4) The Gulf of Maine, about 25,000 square, miles in the Appalachian Plateaus province of highly dis­ area, is the largest reentrant in the Atlantic coast sected, flat-lying sedimentary rocks, mostly 1,000 to south of Cabot Strait. (See fig. 2.) It is almost enclosed 4,000 feet above sea level. These belts are less readily by banks and shoals that are submerged beneath 18 to recognized in New England and Newfoundland. 300 feet of water and that swing southward in an arc The physiographic setting of the Coastal Plain and linking Cape Cod and Nova Scotia. (Se?. Murray continental margin is represented graphically on plate (1947) for topography of the gulf.) One deep channel, 3. The gradient of the continental slope in this diagram 600 to 900 feet deep, cuts through the enclosing banks is exaggerated considerably to emphasize the steeper and shoals near Nova Scotia to connect with the deeper slope of the shelf break along the Blake Plateau in floor of the ocean (Torphy and Zeigler, 1957). The contrast to the gentler slope to the north. waters behind the banks are 300 to 1,140 feet deep; the somewhat irregular floor relief is suggestive of ATLANTIC COASTAL PLAIN a former glacial lake-and-river drainage system behind AREA AND CONFIGURATION a cuesta of Cretaceous and Tertiary rocks (Johnson, 1925, p. 267; Chadwick, 1949, p. 1967; Uchupi, 1965b; The Atlantic Coastal Plain, shown in figure 2, has 1966, p. 166-167). A long arm of the gulf, the Bay of an area in excess of 100,000 square miles. It is a rela­ tively low area when compared with the Appalachian Fundy, extends northeastward between New Bruns­ Mountains that border it on the west, but it is not a wick and Nova Scotia. featureless plain. Terrace remnants with 200 feet of CAPE COD relief are present in much of the inland area. Marine and fluvial terraces are well developed on its surface Cape Cod, a seaward projection of Massachusetts, is as a result of ancient changes in sea level. These ter­ the most prominent emergent feature of th low and marks the upper limit of river navigation and many swampy, whereas that facing the ocean is more abrupt important cities, including Trenton, Philadelphia, and indented farther by inlets. The topography of the Wilmington, Baltimore, Washington, Fredericksburg, peninsula is dominated by morainal ridges and glacial Richmond, Columbia, and Augusta, are located along hills with altitudes of 200 to 300 feet. Glrcial drift it. masks the underlying geology, but Cretaceous and The Coastal Plain is deeply indented by branching Tertiary rocks have been reported in v^ells near bays or drowned river valleys, and the highly irregular Provincetown at the tip of the peninsula (Zeigler and shoreline at its eastern edge exhibits numerous large others, 1960; 1964, p. 708). Hoskins and Knott (1961) spits and bars from Cape Lookout, off North Caro­ have interpreted continuous seismic profiles in the lina, northward to New York (pi. 3). South of Cape adjacent bay as showing marine Tertiary strata and Lookout, drowned river valleys and barrier beaches are erosional remnants of Cretaceous rocks. The age and not as common. Numerous small islands fringe the development of the hook have been discussed by Zeig­ coast of the Carolinas and Georgia. ler, Tuttle, Tasha, and Giese (1965). PHYSIOGRAPHIC FEATURES 9

DELAWARE BAY CAPE FEAR Delaware Bay is the drowned lower valley of the Cape Fear protrudes about 20 miles beyond the Delaware River, which separates New Jersey from general coastline midway between Cape Lookout, N.C., Delaware and Pennsylvania. (See fig. 2.) It is about and Cape Romain, S.C. (See fig. 2.) Shoals associated 52 miles long and, at its broadest point, about 28 miles with the cape jut out another 34 miles into the Atlantic wide. Although most of the bay is less than 120 feet Ocean. Two cuspate bays that are about 95 iriles long deep, the main channel ranges in depth from 210 feet and indent the coastline 20 to 25 miles flank the point in the upper reaches to 900 feet near the mouth. The in concave symmetry. Cape Fear is related net only to lower end is partially closed by Cape May of New Jer­ marginal eddies in the Gulf Stream but slso to a sey and Cape Henlopen of Delaware. Shoals ring the structural arch prominent in the ancient roc1rs. point of Cape May and parallel the channels upstream. The shoreline of the bay is predominantly marshland. CAPE KENNEDY Cape Kennedy, about midway along the eastern CHESAPEAKE BAY coast of Florida (see fig. 2), projects about 14 miles Chesapeake Bay, which splits Maryland and Vir­ eastward as a low, triangular mass of islards, bars, ginia (see fig. 2), represents a drowned drainage and coastal lagoons whose highest land surface is about system that includes the lower valleys of the Susque- 12 feet above sea level. Shoals extend onhT a few hanna, Potomac, Rappahannock, York, and James miles seaward from Cape Kennedy; another si oal area, Rivers. It is over 160 miles long, more than 25 miles known as False Cape, lies about 8 miles to the north. wide in its central part, and about 13 miles wide at The suggestion has been made by White (19£8, p. 47) its mouth between Cape Charles and Cape Henry. The that Cape Kennedy is the result of deformation, and main channel ranges in depth from 20 to 82 feet and perhaps faulting, of the ancient rocks along a line leaves the bay close to Cape Henry on the south shore. from Indian Rocks on the west coast to Cape Kennedy. A crescent-shaped series of shoals parallels the north shore around Cape Charles. ISLANDS At times during the Pleistocene, the Coastal Plain CAPE HATTERAS has included a considerable part of the present conti­ Cape Hatteras, about 32 miles eastward from the nental shelf. The numerous islands along the Atlantic mainland of North Carolina, marks the meeting point coast were then the higher parts of the emerged of two series of offshore bars. These offshore bars Coastal Plain. The larger of these include Long Island, extend almost without interruption from a few miles Block Island, Martha's Vineyard, the Elizabeth Is­ south of Cape Henry at the mouth of Chesapeake Bay lands, Nantucket Island, Sable Island, and the Florida to Cape Lookout (see fig. 2), a distance of about 120 Keys, most of which are shown in figure 2. miles. The bars are as much as 2 or 3 miles wide and Long Island, Block Island, Martha's Vineyard, the 25 feet high, but generally they are less than 1 mile Elizabeth Islands, and Nantucket Island, which make wide and 10 feet high. They enclose two sizeable shal­ up most of the New England Islands of Woodworth low bodies of water Albemarle Sound at the north and Wigglesworth (1934, p. 3), represent a former and Pamlico Sound at the south. These sounds include cuesta of Cretaceous and Tertiary rocks continuing not only the lagoonal area behind the bars but also mostly submerged from the New Jersey coa'st to the parts of the drowned valleys of the Chowan and Cape Cod Peninsula (Johnson, 1925, p. 108). Thick Pamlico Rivers. The waters of the sounds are 24 feet Pleistocene glacial deposits that mantle thes°- islands deep in some places, particularly near the rivers, but suggest that the scarps of older rocks interfered with they are mostly less than 15 feet deep in the lagoonal the southward advance of the ice masses an<1 caused areas. A part of the large tract of marshland that the local accumulation of glacial debris in moraines separates the two drainage systems is known as East and outwash plains. A comprehensive report on these Dismal Swamp. The formation of the offshore bars at islands written by Woodworth and Wigglesworth Cape Hatteras has been attributed by Davis (1849, p. (1934), articles by Kaye (1964a, b, c), and summaries 148) to reverse flow of great eddies along the shore­ by Shafer and Hartshorn (1965, p. 115-116) H.ve been ward margin of the northward-flowing Gulf Stream. drawn upon for the brief descriptions that follow. 10 PETROLEUM POTENTIAL, ATLANTIC COASTA1 PLAIN AND CONTINENTAL SHELF LONG ISLAND is lined with glacial hills and ridges, 100 to 200 feet Long Island, 1,411 square miles in area, projects higher than the central and southeastern lowlands. The eastward from the East River of New York City to the lowlands slope gently southeastward ^numerous embay- longitude of Rhode Island. The island is about 120 ments closed by sand bars indent the south shore. The miles long, less than 25 miles wide, and less than 200 hills and ridges are composed of coarse glacial debris feet in altitude except for a few ridges and hills and the lowlands are composed of glacial outwash in reaching a maximum of 340 feet. The topography is which Kaye (1964a, b) recognizes six glacial drifts and essentially that of a glacial outwash plain sloping to one interglacial deposit. Cretaceous and TeHiary rocks the south, interrupted by two ridges of terminal are at or near the surface in several places (Shaler, moraines joined at the western end but extending 1885, p. 325-328, pi. 20; WiggleswortK 1934, p. separately eastward along the remainder of the island's 140-160; Kaye, 1964c) and form 1 the westernmost length. One ridge runs along the north shore and the promontory of the island known as Gay Head. other through the middle to the eastern end, where ELIZABETH ISLANDS t they diverge as peninsulas about 14 miles apart. The southern shore of the island is flat and protected by The Elizabeth Islands compose a short chain of a long barrier beaches most of its length. The eastern half-dozen islands, too small to show in figure 2, part of the northern shore is relatively straight and extending 16 miles southwest from Cape Ccd. They are smooth due to active wave erosion, but the western alined subparallel to and 4 to 5 miles nortl west of the part of the northern shore is deeply embayed. The ridges on Martha's Vineyard. These islands are steep-sided bays and inlets there are related to pre­ covered with glacial materials for the mo^t part, but existing valleys eroded into southward-dipping Cre­ one island, Nonamesset, next to the mainland, is taceous beds. Long Island Sound, a shallow arm of reported to have exposures of Cretaceous lignite and the sea less than 20 miles wide and 160 feet deep, Tertiary (Miocene) greensand on its pouth shore intervenes between the northern shore and the New (Woodworth and Wigglesworth, 1934, p. 309-310). England coast. The geological formations underlying Long Island are late Cretaceous and Pleistocene in NANTUCKET ISLAND age. The geology is discussed in Veatch (1906), Fuller Nantucket Island, 51 square miles in area, is the (1914), Suter, deLaguna, and Perlmutter (1949), southeasternmost island off New England. It is about deLaguna (1963), and Perlmutter and Geraghty 15 miles east of Martha's Vineyard and 10 to 20 miles (1963). south of Cape Cod. The land surface is covered with BLOCK ISLAND glacial drift and is relatively low and flat. The few Block Island, approximately 6 miles long and 4 isolated hills range from 50 to 108 feet above sea level. miles wide, lies about 15 miles northeast of Long The harbor on the north side of the island is pro­ Island and about 10 miles south of the Rhode Island tected by a long barrier beach. Cretaceous and Tertiary coast. A small inlet separates the island into north rocks may underlie the several hundred ferst of glacial and south parts connected only by a strip of marsh­ deposits penetrated by wateY wells on the island. land and beach. Steep cliffs, 100 to 150 feet high, mark Reworked Eocene pollen has been reported in Pleisto­ the southern coast. The island is formed of thick cene deposits penetrated by a boring on nearby glacial deposits thought to rest on and against a higher Nantucket Shoals (Groot and Groot, IS 64, p. 488; part of the former Cretaceous cuesta between New Livingstone, 1964). The geology of Nantucket Island Jersey and Cape Cod (Fenneman, 1938, p. 14, 15). has been described by Shaler (1889) and Woodworth Tuttle, Alien, and Hahn (1961) have correlated a (1934c). seismic velocity zone beneath the glacial deposits with SABLE ISLAND the Magothy clay outcrops identified by Woodworth Sable Island, about 1 mile wide and 30 miles long, (1934b, p. 212). is a thin arc of sand bowed seaward about 100 miles MARTHA'S VINEYARD east of Nova Scotia. It is the emergent part of a large Martha's Vineyard is a triangular-shaped island shoal area called Sable Island Bank. The surface con­ approximately 4 miles off the southwestern part of sists of stabilized sand dunes at the e'ast en^l and along Cape Cod. It is about 20 miles long and 10 miles wide the north side. Sand flats surface the remainder of the and rises to 308 feet above sea level near the south­ island. A narrow lake, a few miles long, splits the western Corner. The northwestern side of the island island down the middle near its widest part. According PHYSIOGRAPHIC FEATURES 11 to Willmore and Tolmie (1956, p. 13), the island may Hydrographic Office (1948, 1949, and 1952a) and the be composed entirely of glacial deposits reworked in U.S. Coast and Geodetic Survey (1961, charts 1000 part by waves, or it may have a glacially mantled scarp and 1003; 1962, charts 1001 and 1002) is used to repre­ of Cretaceous or Tertiary rocks as a shallow substruc­ sent the seaward limit of the shelves around tH United ture. Recent deep seismic observations by Berger, States. In this report, the 500-foot bathymetric con­ Blanchard, Keen, McAllister, and Tsong (1965, p. 959) tour from the tectonic map of the United States suggest that the ridge in the basement which has been (Cohee, 1962) is used. Because of the abrupt declivity proposed to underlie the shelf edge off Halifax (Officer at the edge of the Continental Shelf, no appreciable and Ewing, 1954, fig. 2) continues northeastward difference in position or area of the shelf is apparent beneath Sable Island and that the thickness of sedi­ on the small-scale maps of this report. mentary rocks under the island approximates 14,750 feet. AREA AND CONFIGURATION FLORIDA KEYS The Atlantic Continental Shelf is a 2,400-mile-long The Florida Keys, well described by Cooke (1939, submerged platform, about 350,000 square miles in p. 68-70; 1945, p. 11, 256-265), constitute a low island area, which widens from less than 3 miles off southern arc curving along the Straits of Florida from Biscayne Florida to about 285 miles off Newfoundland (fig. 1). Bay near Miami 200 miles southwestward to the Dry It extends subparallel to the shoreline and without Tortugas. (See fig. 3.) Between Biscayne Bay and Big interruption from the Straits of Florida to Cape Cod Pine Key, the arc of islands consists of an ancient coral (fig. 2). At Cape Cod, the continental she^f swings reef that is interrupted by tidal channels, and the eastward about 200 miles to include George Bank; islands are elongate parallel to the Straits of Florida. there it is interrupted by the deep outlet of the Gulf Between Big Pine Key and Key West, the islands are of Maine. It continues off Nova Scotia and parallels composed of Miami oolite, such as crops out on the the open coast around Emerald Bank, SaHe Island mainland, and the islands tend to be elongate to the Bank, and Banquereau to Cabot Strait. Cabot Strait, northwest at right angles to the chain. The Marquesas, the deep entrance to the Gulf of St. Lawrence, breaks about 20 miles west of Key West, and the Dry Tor­ the continuity of the continental shelf, but the shelf tugas, about 45 miles beyond the Marquesas, are coral resumes around Newfoundland and eastward as the sand banks in the form of atolls (Cooke, 1939, p. Grand Banks. This report discusses the part of the 70-72). About 5 miles seaward from the Florida Keys Atlantic Continental Shelf south of Cabot Strait, is a submerged living coral reef that parallels the including the Gulf of Maine. island arc throughout the entire length. The largest Along the entire Atlantic coast, the 50-fatl om (300- island of the Florida Keys is Key Largo south of foot) bathymetric contour, as shown on U.S. Coast Biscayne Bay. It is 27 miles long and up to S1/^ miles and Geodetric Survey charts 1000, 1001, and 1002, wide; most of the islands are less than 6 miles long, closely parallels the edge of the Continental Shelf at a mile wide, and 10 feet in altitude. The Florida Keys a distance of only a few miles. Farther inshoro adjacent are separated from southern Florida by the Florida to nonglaciated regions, the bottom contours are more Bay, a shallow embayment mostly less than 12 feet widely spaced and show more parallelism to coastal deep containing many mud banks and shoals. Man­ shapes than to the edge of the continental s^elf. This grove swamps occupy much of the shallow water at 50-fathom (300-foot) contour may approximate the the head of the Florida Bay and behind the Florida limit of subaerial erosion near the close of Pleistocene Keys. (Wisconsin) time. Earlier Pleistocene shore1 ines may ATLANTIC CONTINENTAL SHELF have ranged from this level to greater depths on the continental shelf. DEFINITION The 5,000-foot bathymetric contour, as shown on Continental shelves, which exist along the margins the tectonic map of the United States (Coh<*?., 1962), of oceans throughout the world, extend from the mean parallels the edge of the Continental Shelf at a sea­ low-water line to the abrupt change in slope known as ward distance of 10 to 20 miles from Nova Scotia to the continental slope. The depth at which this change as far south as Cape Lookout (pi. 1), wher\ instead occurs differs considerably around the world but the of following the coastline and shelf, it continues almost average depth is about 432 feet, or 72 fathoms. Com­ due south along a steep slope east of the Bahama monly, the 100-fathom (600-foot) bathymetric contour Banks. The 150-to-200 mile wide flat area between this shown on the hydrographic charts of the U.S. Navy steep slope, the shelf edge, and the Bahana Banks 12 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

n| ' .<$ f*

M

i

CO

o°Z PHYSIOGRAPHIC FEATURES 13 is termed the Blake Plateau. The gentle slope at the Channel, and the much deeper part of the continental shelf edge is referred to as the Florida-Hatteras slope rise (fig. 4). This platform, which begins abo^t 50 miles to distinguish it from the true continental slope out­ offshore, extends with some interruptions as far south­ side the Blake Plateau. east as Haiti and includes about 50,000 square miles of banks, shoals, rocks, cays, and islands. The north­ BLAKE PLATEAU ernmost banks, about 200 miles wide, are the most The Blake Plateau is a deep-water plateau at depths extensive. They are outlined in figure 2 by lines that from 650 to 3,600 feet (Uchupi, 1965a) between Cape coincide with the 500-foot bottom contours. The edges Lookout, N.C., and the northernmost bank of the of the banks, particularly the oceanward elges, have Bahama Islands (fig. 2). It has a very gentle slope of steep slopes averaging 10° to 20°; some are nearly less than 0.5° with only minor irregularities and little, vertical. Most of the platform is covered by less than if any, cover of Holocene sediments. Small hills and 60 feet of water, and parts of it, such as tl subsidence or block gin until the end of Cretaceous time, whereas the main faulting. The origin of these valleys has bisen attrib­ area of the plateau received nearly horizontal carbon­ uted to coral reef growth on submarine volcanoes ate deposits. The barrier reef appears to have died (Schuchert, 1935, p. 26, 27, 531) or on drcwned pre- at the end of Cretaceous time, and detrital sediments Cretaceous topography (Hess, 1933, 1960; Newell, were deposited on the plateau. Rate of deposition and 1955, p. 314), to turbidity currents (Encson and subsidence was more rapid on the western part. By others, 1952, p. 506), and to grabenlike do^nfaulting the end of Eocene time, the plateau had sunk to (Talwani and others, 1960, p. 156-160). Recently pub­ lished interpretations of seismic records indicate that considerable depth, and deposition of sediments on it reef growth was a dominant factor in the maintenance was restricted mostly to the western edge because of of carbonate banks of the Bahamas (Ewing and the sweeping effect of the Gulf Stream. The Gulf others, 1966, p. 1970) throughout Late Cretn«eous and Stream continued to modify the plateau surface both Tertiary time. This tends to support the conclusions by preventing deposition and by erosion until the of Hess (1933, 1960) and Newell (1955, p. £14). present time. BAHAMA BANKS CAY SAL BANK The Bahama Banks constitute a shallow carbonate Cay Sal is a relatively small, somewhat rectilinear elongate platform parallel to the Florida coast and bank located at approximately lat 24° N. and long situated between the Straits of Florida, Bahama 80° W., midway between the Florida Keys, Cuba, and 14 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF PHYSIOGRAPHIC FEATURES 15 the Bahama Banks (fig. 2). Numerous small islands, Daly (1936), Ewing, Luskin, Roberts, and Hirshman cays, rocks, and shoals outline its periphery, but most (1960), Johnson (1938, 1939), Kuenen (1950, p. 485- of the bank is covered by 18 to 60 feet of water. The 493), and Roberson (1964). The locations of 15 princi­ edges slope abruptly to depths of 900 to 2,400 feet. pal canyons are shown in figure 2. From north to An oil test was drilled on this bank by the Bahama south, these are Corsair, Lydonia, Gilbert, Oceanogra- California Oil Co. and the Bahama Gulf Oil Co. in pher, Welker, and Hydrographer Canyons off Georges 1958 and 1959, but no information has been released. Bank; Veatch, Atlantis, Block, and Hudson Canyons off Cape Cod and Long Island; Wilming^on, Balti­ NORTH ATLANTIC BANKS more, Washington, and Norfolk Canyons of the Dela­ A series of banks on the outer continental shelf ware, Maryland, and Virginia coasts, and Hatteras parallel the North Atlantic coast from a point several Canyon off Cape Hatteras, N.C. Most of the^e canyons hundred miles east of Newfoundland to the vicinity head in broad notches in the edge of the continental of Cape Cod. The Grand Banks off Newfoundland shelf at depths of 300 to 600 feet, but th<5 Hatteras (fig. 1) are the most extensive. They consist of a large Canyon appears to start considerably deeper, in the number of irregular banks that average 180 feet in vicinity of the 1,200-foot depth. The canyons that depth. Cabot Strait separates the Grand Banks from notch the Continental Shelf have steep, winding, those along the Nova Scotian coast. V-shaped gorges with many tributaries and are cut South of Cabot Strait, closely spaced banks less in consolidated and semiconsolidated ro?ks. They than 360 feet deep and 10 to 25 miles wide dominate range in width from about 1 mile to mo^e than 10 the outer continental shelf. Banquereau, which lies miles and extend far down the continental slope to under 120 to 240 feet of water, is the northernmost of depths of 6,000 feet or more. these. Next is Sable Island Bank, less than 120 feet Only the Hudson Canyon has a channel which deep, around Sable Island, and then Emerald Bank crosses the continental shelf to connect with a present- and several other small banks at depths of 240 to 300 day river mouth, although bottom contours for depths feet occur off Halifax. Browns Bank lies south of of less than 300 feet indicate drainage patterns that Nova Scotia parallel to the entrance to the Gulf of may have once connected with Corsair, Oceanographer, Maine in 120 to 360 feet of water. Georges Bank is Hydrographer, Block, Baltimore, and Norfolk Can­ a very large bank stretching from the shoals off Cape yons. This suggests that many rivers drained across Cod eastward to Northeast Channel; it is 6 to 300 feet the continental shelf when it was exposed during the deep and exhibits shoals in the shape of subparallel Pleistocene glacial stages and that their channels were ridges pointing into the Gulf of Maine (Stewart and modified or eliminated by encroaching seas during the Jordan, 1964). Cretaceous and Tertiary fossils and interglacial stages (Veatch and Smith, 1939, p. 44-48). glacial materials have been dredged from Georges Many large gullys, some of which appear to be den­ Bank and Banquereau (Verrill, 1878; Stetson, 1936; dritic, are cut into the slope below the continental Cushman, 1936). Johnson (1925, p. 267) considered shelf. These bear no apparent relation to tita principal both Georges and Browns Banks as parts of a drowned canyons and may have a different origin. cuesta of Cretaceous and Tertiary strata, and Shepard, The Hudson Canyon (Veatch and Smith, 1939, Trefethen, and Cohee (1934, p. 281-302) emphasized p. 14) is the longest and deepest of the North Atlantic the effect of glaciation on and behind the cuesta. coast canyons (fig. 5). The channel of tl^ Hudson Recent seismic profiles over Georges Bank (Emery and River is entrenched about 50 to 150 feet into the Conti­ Uchupi, 1965) and along the Northeast Channel nental Shelf from the mouth of the river to the 360- (Uchupi, 1966, p. 166-167) between Georges and foot depth marking the beginning of the gorge. Browns Banks tend to confirm these earlier views. Beyond this, the canyon walls reach a maximum height of 4,000 feet as they descend the slope and rise to a SUBMARINE CANYONS terminal depth of approximately 15,900 fe^t (North­ Numerous submarine canyons have been charted rop, 1953, p. 223). The lower part of the 180-mile-long along Georges Bank and southward to Cape Hatteras canyon is a relatively shallow trench across a large (U.S. Coast and Geodetic Survey, 1945; 1961, chart alluvial fan on the continental rise. Miocene clays have 1109; and 1962, chart 1108). These have been described been found on the sides of the gorge; coarse sand, and discussed in detail by Bucher (1940), Stetson gravel, shells, and clay cobbles were cored in the (1936), Shepard (1933; 1934; 1948; 1951a; 1951b; canyon at a depth of 12,000 feet; and cleanly washed 1963, p. 327-329), Veatch and Smith (1939, p. 1-48), sand has been sampled in the outer trench and alluvial 16 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

74° W. 72° W. 70° W

VERTICAL EXAGGERATION ABOUT 6:1

FIGURE 5.- -Physiographic diagram of Hudson Canyon. Sources of information: U.S. Coast and Geodetic Survey (1962, chart 1108) and U.S. Navy Hydrographic Office (1951, BC-0807N). fan. The results of acoustic probes and cores of the and Emery, 1950), turbidity currents (Drly, 1936; canyon walls (Ewing and others, 1960, p. 2849-2855) Kuenen, 1950, p. 496-526), diastrophic movements suggest inclined erosional surfaces between beds adja­ (Wegener, 1924, p. 177), artesian springs (Johnson, cent to the canyon edge at depths of 360 and 480 to 1939), tsunamis (Bucher, 1940), hydraulic and tidal 540 feet. These are thought to correlate with wave currents (Davis, 1934), and landslides and mudslides. erosion of the continental shelf at diflferent times dur­ Shepard (1963, p. 337) points out that all I Tit two of ing the Pleistocene, as suggested by Veatch and Smith these have been generally discarded in recent years. (1939, p. 44-48). The surviving theories are turbidity currents, and The origin of submarine canyons has been a subject subaerial erosion with the drowning and maintenance of speculation, discussion, and investigation for more of the canyons by turbidity currents, submarine slides, than 50 years. The theories that have been advanced and sand flows. The first considers the canyons to have and restated at diflferent times include subaerial ero­ been cut by turbidity currents during low sea-level sion (Veatch and Smith, 1939, p. 48; Du Toit, 1940; stageso of the Pleistocene. The second assume^ the can- Shepard, 1948 and 1963, p. 335-347; Umbgrove, 1947; yons to have been cut by rivers prior to the Pleistocene PHYSIOGRAPHIC FEATURES 17 and modified subsequently by submarine phenomena p. 303-306) and Heezen, Tharp, and Evdng (1959, including turbidity currents. p. 51) have favored normal faulting. Th°. slope ap­ pears to represent the juncture between the heavy ORIGIN OF SHELVES oceanic crust and the lighter continental crust, where The origin of continental shelves is directly related isostatic adjustments might be expected to compensate to that of the continental slopes. Numerous theories for erosion lightening the continental masr and depo­ of origin have been advanced over the years, but none sition weighting the ocean floor. Such adjustments has been completely acceptable for all parts of the could produce long normal-fault scarps, possibly a earth. These theories have been reviewed and discussed band of step faults, dipping away from tha- continent. in detail by Kuenen (1950, p. 157-163) and Shepard Some warping of the continental margin also could (1963, p. 300-310). accompany this. However, most continental slopes are The oldest theory, which prevailed before very much not active fault zones now and their inclination is geophysical and geological data could be obtained much less than most fault scarps on land. Heezen from beneath the seas, postulated that the slope is the (1962, p. 242) believes that the continental slope seems front of a huge pile of sediment eroded from the to be a relic related to normal faulting whHh occurred continent, the inner shelves are wave-cut terraces, and at some earlier time and that the upper part of the the outer shelves are wave-built terraces. This theory slope has been modified since by deposition. and has been generally discredited by then-unknown facts erosion. such as the absence of sedimentation on the outer shelf Emery (1950) suggested that high-angle thrust faults extend beneath the continental mars from the in many regions, the unpredictable grain-size distribu­ margins. This idea is supported by the distribution of tion of sediments on the shelf, the presence of large earthquake epicenters in an ever-deepening pattern areas of bare bed rock on both the shelf and slope, the beneath the continents. Emery thought it possible that irregular topography of the outer shelf, the lack of these thrust faults elevated the continental margins correlation between the size of waves and depths of sufficiently to permit subaerial erosion of the canyons the outer shelf, and the relatively high inclination of now present on the shelf and slope. the slope surface. Drake, Ewing, and Sutton (1959, p. 176-185, 191- Another concept, not in current favor, suggests that 194) have compared the continental shelf and slope the slopes are downwarped remnants of Miocene of eastern North America to the miogeosyncline and peneplains (Veatch and Smith, 1939, p. 35). Du Toit eugeosyncline of the Appalachian Mountain System (1940, p. 398-403) and Umbgrove (1946, p. 251; 1947) and have discussed *the mechanics of thrusting and offered somewhat similar views, involving arching folding necessary to add the contained sediments to along the coast, but with different mechanics. Features the land mass of the continent. Dietz (196^a, p. 1-21; that tend to discredit most of the concept of down- 1963b) has proposed along similar lines that the slopes warping are the presence of exposed bedrock on the have been constructed by the compressional collapse slope where sediments would be expected, the lack of and folding of the continental rise sedimentary prism observed downward bending of strata in the slope and against the continental block the flanks of the result­ outer shelf, and seismic evidence of a rise in the base­ ing eugeosynclinal orogen have become the continental ment along the outer shelf. slope. However, he also suggests that continental drift The most acceptable theories regarding the origin and rifting have given rise to some rift scarps that of the shelf and slope now center around diastrophic have been modified as continental slopes. movements near the contact of the continental and Van Bemmelen (1956, p. 139, fig. 3) depicted a oceanic crust, according to Shepard (1963, p. 310), graben structure along the Atlantic coas* of North who cites as supporting evidence the general straight- America. Later, Engelen (1963, p. 65-72) expanded ness of the slopes, the angular changes in trend, the on this concept and showed diagrams of the develop­ excessive steepness, the association with earthquake ment of the graben structure based on his interpreta­ belts and deep trenches in the Pacific, and the outcrop tion of geophysical profiles published by Heezen, of rocks along the slopes at different places. Tharp, and Ewing (1959, pi. 26). According to his Numerous writers have invoked faulting in their hypothesis, block faulting started in Early Cretaceous explanations of the continental shelf and slope, but time in the northern part and progressed slowly south­ few have agreed on the mechanics. Shepard (1963, ward through Tertiary time. 18 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF STRUCTURE southeastern Georgia, 1,500 feet in southeastern North Carolina, 9,500 feet in southeastern New Jersey, and REGIONAL STRUCTURAL PATTERN 2,000 feet along the south shore of Long Island. A The Appalachian Mountains, raised by late Paleo­ decided steepening of the slope is apparent below a zoic orogeny, form the structural backbone of eastern depth of 3,000 feet in most of the area. Prout^ (1946, North America, extending from Newfoundland south- p. 1918) first recognized this steepening in wells in westward to central Alabama. (See P. B. King (1959, North Carolina. p. 41-66; 1964.) for a comprehensive analysis of this Seismic data (see pi. 2) have been sufficient to per­ mountain system.) In the United States, it consists mit the contouring of the basement surface beneath mainly of a narrow anticlinorium of Precambrian and the continental margin in much of the offshore area early Paleozoic rocks at the west known as the Blue north of Cape Hatteras. There the basement surface Eidge province, and a long, broad belt of intensely slopes abruptly downward offshore and descends into deformed and intruded Precambrian and Paleozoic what Kay (1951, p. 82) has called the Atlantic geosyn- rocks at the east called the crystalline Appalachians. cline. This geosyncline, a paraliageosyncline of Meso­ (See pi. 4.) The crystalline Appalachians, which form zoic rocks along the Atlantic coast according to the New England Upland to the north and the Pied­ Kay (1951, p. 82), consists of parallel troughs sepa­ mont province to the south, exhibit the most intense rated by a ridge beneath the edge of the continental deformation. These intensely metamorphosed rocks shelf. (See pi. 4.) Ewing, Worzel, Steenlstid, and crop out in a fairly continuous belt as much as 130 Press (1950) first concluded from seismic surveys miles wide from Alabama to Canada. Several down- between Cape Henry, Va., and Cape Cod, Mass., that faulted basins of Triassic continental clastic rocks are the basement surface does not slope uninterruptedly present in the Piedmont province and in the basement across the continental margin but upon reaching a beneath Coastal Plain deposits of Mesozoic and Ceno- depth of about 16,000 feet, 40 miles off Delaware Bay, zoic age (Cohee, 1962). The Coastal Plain deposits, rises to a depth of about 10,000 feet at the edge of the which wedge out against the eastern flank of the continental shelf. (See section E-F-F', pi. 5). Similar Appalachian Mountains, reflect the major structural findings off Nova Scotia were reported by Officer and anomalies and trends of the Precambrian and Paleo­ Ewing (1954, fig. 2). Drake, Ewing, and Sutton (1959, zoic rocks. fig. 29) presented a thickness map of total sedimentary The regional structure of the pre-Cretaceous base­ rocks on the basement between Cape Hatteras and ment rocks as known from outcrops and wells, and Halifax, Nova Scotia. They show two troughs, one inferred from geophysical surveys, is depicted by beneath the continental shelf and a second one sub- contours on plate 4, adapted from the tectonic map parallel to the first, beneath the continental slcne. They of the United States (Cohee, 1962), Antoine and liken these two troughs separated by a basement ridge Henry (1965, fig. 9), and Sheridan, Drake, Nafe, and to the early Paleozoic troughs of the Appalachians as Hennion (1966, fig. 9). The basement rocks include restored by Kay (1951, pi. 9) and suggest that the not only the igneous and metamorphic rocks of inner trough may represent the miogeosyncline and Precambrian and Paleozoic age and volcanic and the outer trough, the eugeosyncline. (See sections sedimentary rocks of Triassic(?) age but also unmeta- C-D-D' and E-F-F', pi. 5). morphosed sedimentary rocks of Paleozoic age beneath South of Cape Hatteras, the basement surface has the Florida Peninsula. been contoured to the edge of the continental shelf, The structural contours on the basement rocks across the southern half of the Blake Plateau, and beneath the Coastal Plain parallel the Appalachian around the Bahama Banks. The contours for the shelf Mountain System except at the boundary between area parallel the coast for the most part, tut bulge North and South Carolina, where they bulge seaward seaward off Cape Fear and landward in th°> South­ on the Cape Fear arch, and beneath the Florida Penin­ east Georgia embayment. Contours on the basement sula, where the deeper contours are deflected around beneath the Blake Plateau show a trough, more than the southeasterly elongated Peninsular arch. The base­ 20,000 feet deep, trending northward about T50 miles ment surface dips seaward at rates ranging from 10 east of the coast of northern Florida, and a corre­ feet per mile inland to as much as 120 feet per mile sponding ridge, less than 15,000 feet deep, paralleling near the ocean. It reaches the coast at depths in excess the continental margin (Sheridan and others, 1966, of 20,000 feet in southernmost Florida, 5,000 feet in fig. 9). This combination of trough and outer ridge STRUCTURE 19 beneath the Blake Plateau is very similar to those REGIONAL BOUGUER GRAVITY ANOMALIES reported beneath the continental shelf north of Dela­ Early gravity investigations along the Atlantic sea­ ware Bay. Contours around the Bahama Banks out­ board were concerned primarily with relating gravity line a basement uplift of several thousand feet whose to surface geology and to seismic and magnetic data axis trends northwestward beneath Little Bahama (Swick, 1937; Woollard and others, 1938; Woollard, Bank toward the Peninsular arch of Florida (Sheri­ 1939, 1940a, 1941, 1943, 1944, and 1948). One of the dan and others, 1966, p. 1988, fig. 9). This uplift early papers that dealt with gravity interpretations separates the trough beneath the Blake Plateau from of subsurface geology in the Atlantic region was that an embayment, more than 35,000 feet deep, extending on the Bahamas by Hess (1933, p. 38-53). He con­ from the Gulf of Mexico across southernmost Florida cluded "that the general field of negative anomalies to Andros Island. is due to a great thickness of light sedimerts beneath The structure of the continental shelf between Jack­ the Bahamas, but that the dolomitic reef material is sonville, Fla., and Cape Hatteras, N.C., is illustrated relatively heavy, thus making the anomalies on the by plate 6. Offshore seismic section A-A' adapted reef material less negative than those ove-r the sub­ from Hersey, Bunce, Wyrick, and Dietz (1959, fig. 3) marine valleys." Many years later, Worzel and Shur- is compared with stratigraphic section A-B (pi. 9) bet (1955a, p. 97) estimated the great thickness of of this report. The comparison suggests that the seis­ light sediments beneath the Bahamas to be 93,000 mic velocities approximating 6 kmps (kilometers per feet. In addition, they stated (p. 97), "If this cal­ second) represent the pre-Mesozoic basement rocks careous system were laid down on an oceanic crust, and that these rocks are about 12,000 feet deep off­ and approximate isotasy were maintained at all times, shore north of Cape Hatteras, about 2,500 feet deep the final 16,000 feet would have been laid down in off Cape Fear, and more than 20,000 feet deep offshore water depths less than 2,000 feet." Other papers that south of Jacksonville. Hersey, Bunce, Wyrick, and make geological interpretations from gravity meas­ Dietz (1959, p. 448) have tentatively correlated the urements along the Atlantic coast include those of 5.16- to 5.35-kmps layer off Florida and the 4.30-kmps Woollard (1940b, 1949), Skeels (1950), Vrorzel and layer off North Carolina with the top of the Lower Shurbet (1955b), and Worzel, Ewing, p.nd Drake Cretaceous. The 3.27- to 3.88-kmps layer off North (1953). Carolina is correlated by them with the top of the A summary map of Bouguer gravity anomalies Black Creek Formation (top of rocks of Taylor age) along the Atlantic coast has been published recently but is not correlated off Florida. The Black Creek by Woollard and Joesting (1964). Plate 7, which is correlation off North Carolina seems uncertain, as the adapted from their map, shows the regional anomalies top of rocks of Taylor age is not a distinct lithologic along the Atlantic coast. These anomalies primarily horizon in the nearest wells (pi. 11). The top of rocks reflect compositional differences at considerable depths of Austin age and that of rocks of Woodbine age in the earth's crust but are related to somQ. extent to would seem to offer better possibilities for seismic the structure and composition of the Coastal Plain velocity change. The 2.26- to 2.89-kmps layer they con­ sedimentary rocks and shallow basement. Four alter­ sider to be near the top of the Upper Cretaceous nating belts of predominantly positive aid predom­ rocks offshore between Jacksonville and Cape Hat­ inantly negative gravity anomalies extend diagonally teras. This, too, seems very uncertain as comparison across the region from southwest to northeast. These to the stratigraphic cross section suggests the 2.26- to correspond roughly to the continental rise and slope, 2.89-kmps layer is too shallow to be Upper Cretaceous the continental shelf and Coastal Plain, the Appa­ and may be closer to the top of the Eocene rocks. This lachian Mountain front, and the Piedmont Plateau- velocity layer is less than 1,500 feet deep at Cape Blue Ridge-Appalachian Basin region. Hatteras; the top of the Upper Cretaceous rocks in the Cape Hatteras well (NC-14) has been placed at CONTINENTAL RISE AND SLOPE 3,033 feet and the top of the Eocene (Castle Hayne Positive gravity values extend over a wide area Limestone) rocks at 1,738 feet in this study. The parallel to the outer continental shelf ard increase irregular and rising velocity layers south of Cape rather regularly oceanward across the continental Fear suggest that they result from a general facies slope and rise. They range from 0 to 40 milligals change to carbonate in that direction and cannot be along the outer continental shelf to moro than 300 relied upon for stratigraphic equivalence. milligals near the boundary between the continental 20 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF rise and the abyssal plain (fig. 1). A single, slightly stone, sandstone, and shale beds beneath the Mesozoic. negative anomaly about 20 miles wide and 190 miles The outline of the area underlain by these Paleozoic long is present off South Carolina. The general rocks conforms in a rough way to the zero contour increase of positive gravity values oceanward probably from Alabama to eastern Georgia, but the relationship reflects a transition between the lighter continental becomes vague southeastward in Florida where pre- crust and the heavier oceanic crust underlying the Mesozoic volcanics are found in some wells. ocean basins of the earth. APPALACHIAN MOUNTAIN FRONT CONTINENTAL SHELF AND COASTAL PLAIN Positive gravity values ranging from zero to 50 Negative gravity values predominate on the conti­ milligals extend in a narrow belt 30 to 80 miles wide nental shelf and Coastal Plain, although irregular along the front of the Appalachian Mountains. This positive anomalies are numerous and large enough to belt coincides with the Blue Ridge province in Vir­ create a confusing pattern not readily related to ginia and the Newark Basin in New Jersey (Cohee, known surface and shallow subsurface features. The 1962) but does not conform well to geo^gic and area is underlain by light continental crust on which physiographic boundaries throughout its length. It sedimentary rocks containing some igneous intrusions cuts diagonally across the Piedmont Plateau south­ and flows are irregularly distributed. In general, the ward to Alabama and continues beneath the Coastal areas of negative values are elongate subparallel to Plain to the Florida Panhandle. It also encroaches on the continental shelf and Coastal Plain. The values the Coastal Plain and continental shelf rorthward range from 0 milligals along the eastern and western from Virginia to the Gulf of Maine. The exposed rocks limits of the combined provinces to as little as 40 within this belt are mainly Paleozoic metamorphics, milligals in isolated anomalies in between. In Alabama including the Carolina slate belt (Cohee, 1962). and from Virginia northward, the western zero- gravity contour is as much as 75 miles inside the PIEDMONT PLATEAU, BLUE RIDGE: AND APPALACHIAN BASIN Coastal Plain and continental shelf. A large, positive anomaly breaks the regional pattern across the Coastal West of the belt of positive gravity values along the Plain of Alabama and Georgia and extends about front of the Appalachian Mountains is a broad expanse 60 miles offshore. Another positive anomaly crosses with negative gravity anomalies ranging from zero to the regional pattern in southern Florida, and long 100 milligals. The minimum anomalies of 100 reentrants are present in the negative pattern at milligals are present in the Blue Ridge province in several places south of Virginia. northeastern Tennessee and northwestern North Caro­ The largest unbroken area of negative values in the lina, where, according to King (1964, p. 19), the 80 Coastal Plain and continental shelf is a crescent- milligal contour encloses all the major windows of the shaped anomaly more than 100 miles wide and 600 thrust sheets of the Southern Appalachians. King miles long between Cape Hatteras and the Gulf of suggests that these data indicate that the- "surface Maine. Several sizeable negative anomalies are present Precambrian rocks of the southwestern segment of the within the larger one. One in northeastern North Blue Ridge Province are underlain by a thick body Carolina and southeastern Virginia reaches a value of overridden, deformed Paleozoic and possibly ear­ of 40 milligals. Another smaller anomaly, which lier sedimentary rocks." Anomalies having minimum reaches a value of 20 milligals and is about 200 to values of -80 milligals lie within the Appalachian 250 miles long, is present in the Coastal Plain and Basin, which contains considerable thicknesses of continental shelf near Atlantic City, N.J.; it does not unmetamorphosed Paleozoic sedimentary ro".ks. coincide with the Baltimore Canyon trough, although it crosses one arm of this basement feature. The large REGIONAL MAGNETIC ANOMALIES crescent-shaped negative anomaly as a whole conforms COASTAL PLAIN somewhat to the zone of maximum compression in the Appalachian Mountains. Whether it is related to this Magnetic observations on the Coastal Plain date or to Triassic deposition is not known. back to the early 1930's (MacCarthy and otl QTS, 1933; A large area in southwestern Georgia and the MacCarthy and Alexander, 1934; Jenny, 1934; John­ Florida Panhandle has negative values that seem to son and Straley, 1935; and MacCarthy, 1936). Jenny be related somewhat to the composition of the shallow (1934, p. 413) found northeastward magnetic trends basement rocks; wells there penetrate Paleozoic lime­ in the Coastal Plain of Alabama and Florida and STRUCTURE 21 related them to the structural trends in the Appalach­ an igneous intrusion about 30 miles wide ir the base­ ian Mountains, as did Lee, Schwartz, and Hemburger ment. This magnetic anomaly was noted alsc by Miller (1945) later. MacCarthy (1936, p. 405, 406) drew simi­ and Ewing (1956, p. 412), Drake, Ewing, and Sutton lar conclusions about subparallel high and low inten­ (1959, p. 175), and Heezen, Tharp, and Ewing (1959, sity trends in the Coastal Plain of North and South p. 51). Carolina. He noted also that these trends curve around An analysis of 10 aeromagnetic profiles across the the southeastward-trending basement uplift (Cape continental shelf and slope by King, Zietz, and Demp- Fear arch) at Wilmington, that they outline a subsur*. sey (1961, p. D302, D303) indicated that th?, anomaly face Triassic basin near Florence, S.C., and that they along the outer edge of the continental sHlf corre­ indicate a distinct change in basement slope near and sponds in position with the basement ridge found by parallel to the coast. seismic refraction (Drake and others, 1959) but that Maps of vertical magnetic intensity anomalies on the intensities do not correspond with depth to base­ the Coastal Plain of North Carolina were published ment as suggested by seismic refraction. They con­ by Skeels (1950, pis. 3 and 4) after the drilling of the cluded that although basement topography may have deep well at Cape Hatteras (NC-14) in 1946. He some effect on the magnetic intensity, the anomaly compared these with gravity maps and seismic maps "may be at least partly the expression of a large mass of the same area and noted that both the magnetic or series of masses of more magnetic rocks within the and gravity anomalies showed north-to-south trends basement possibly intrusive bodies along a zone par­ (Skeels, 1950, pis. 1, 2; figs 2, 3, 19, 20). He concluded allel to the continental margin at the transition from that the magnetic maps tend to accentuate effects a continental to an oceanic crust" (King and others, from the upper part of the basement more than do 1961, p. D303). the gravity maps and that the magnetic properties of A marine magnetic survey by the U.S. Nr.vy Ocean- the igneous rocks seem to be much more variable than ographic Office (1962) along the edge of the con­ their densities. tinental shelf between lat 34°30' N. and lat 39°00' N. In 1959, E. R. King (1959, fig. 1) published a also supported the idea that the anomaly is an expres­ regional magnetic map of Florida from which the sion of a large mass of more highly magnetic rocks in structural trends of the Precambrian and Paleozoic the basement. rocks beneath the Coastal Plain were inferred. Two Off Nova Scotia, marine magnetic surveys indicate regional magnetic trends dominate the map: one a broad, low-intensity magnetic anomaly beneath the extends diagonally southeastward from the Florida edge of the continental shelf southeast of S?ble Island panhandle along the southwest side of the peninsula (Bower, 1962, p. 8). The bathymetric position of this and across the tip of southern Florida toward the anomaly is similar to that of the one found by Keller, Bahama Islands; the second, parallel to and east Meuschke, and Alldredge (1954) off the ea^t coast of of the Appalachian Mountains, crosses northeastern the United States. Bower (1962, p. 8) believes that Florida and seemingly intersects the first trend at the the magnetic anomaly near Sable Island could be pro­ gulf coast. Small nonlinear anomalies, possibly due to duced by a large intrusion buried beneath thousands intrusive rocks, separate the two trends in central of feet of nonmagnetic material. The surveys off Nova eastern Florida. Like Woollard (1949), E. R. King Scotia offer no basis for disagreement with seismic suggests that the southeastward magnetic trend is a evidence (Press and Beckman, 1954, p. 308) for large continuation of the Ouachita Mountains whose sub­ thicknesses of sedimentary rocks beneath the conti­ surface extension in Alabama and relationship to the nental shelf in this area. Appalachian Mountains has been the subject of much In 1963, the numerous magnetic observations on the speculation (King, P. B., 1950, p. 667-668). continental shelf and slope were summarized and the anomaly trends were plotted on a chart by Drake, CONTINENTAL SHELF AND SLOPE Heirtzler, and Hirshman (1963). Plate 8 shows these Magnetic observations on the continental shelf and high-intensity trends and significant regional trends slope were reported first by Keller, Meuschke, and are labelled. The width of the trend line! indicates Alldredge (1954), who discussed two aeromagnetic amplitude, not width, of the anomaly. The anomalies profiles from Fire Island, N.Y., to Bermuda, and from are attributed primarily to compositional differences Ludlam Beach, N.J., to Bermuda. They recognized a within the basement, yet the alinement of these linear magnetic anomaly near the edge of the con­ anomalies carries certain connotations of regional tinental shelf parallel to the coast and attributed it to tectonics. 22 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Long, linear southwesterly trends, despite their PRINCIPAL STRUCTURAL FEATUPES crossing and branching at places, roughly parallel the The principal structural features of the basement Appalachian Mountains and the edge of the conti­ rocks beneath the Coastal Plain and continental shelf nental shelf. This dominant pattern, indicated on are outlined by contours on plate 4. All but Emerald plate 8 as the "Appalachian trend," terminates in Bank trough, which is located off Nova £'?,otia, are Florida against a southeasterly magnetic trend that also shown in figure 6. The principal structural fea­ E. R. King (1959) has suggested is an extension of tures are discussed separately in the following sections; the Ouachita Mountains ("Ouachita(?) trend'1, pi. 8). for fuller discussion, see Stephenson (1926, 1928), The Ouachita trend extends from the vicinity of Eardley (1962, p. 135-153), and Murray (1961, p. Tallahassee in northwestern Florida along the south­ 92-98). west coast and across southeastern Florida near Miami CAPE FEAR ARCH to the Bahama Islands. Its identity is lost there in arcuate patterns, perhaps related to an intersection The Cape Fear arch, also known as the Great Caro­ with slope anomaly (?) A of plate 8. lina ridge, Wilmington anticline, and Carolina ridge, The dominant Appalachian trend is interrupted is a southeastward plunging basement nose, the axis along the 40th parallel, about 50 miles south of New of which intersects the North Carolina coartline near York, by a linear anomaly more or less alined with Cape Fear. It is the most prominent structural feature a string of seamounts extending down the continental of the central part of the Atlantic Coastal Plain rise to the abyssal plain. (See pi. 8.) This anomaly (Stephenson, 1928, p. 891) and is evident from the has been interpreted by Drake, Heirtzler, and Hirsh- Cretaceous outcrop pattern, well data, magnetometer man (1963, p. 5270) as a transcurrent fault in the surveys (MacCarthy, 1936, p. 405), and seismic sur­ basement with right-lateral displacement of about 100 veys (Bonini, 1955, p. 1533; 1957; Meyer, 1957). The miles and a total length in excess of 600 miles. general shape is a gentle warp, with the axial plunge The large anomaly along the edge of the continental increasing sharply near the shoreline and gradually shelf, commonly referred to as the "slope anomaly," diminishing updip toward the Fall Line. Along the extends from north of Halifax (Bower, 1962, p. 8) to axis of the arch from the Fall Line to the coast, the Cape Fear (pi. 8) with one offsetting interruption by basement rocks dip at an average of about 13 feet the transcurrent fault (?) trend near New York. South per mile. The arch is asymmetric in cross section, the of Cape Fear, the slope anomaly branches one trend north limb being steeper. Lower Cretaceous rocks and (slope anomaly A, pi. 8) continues parallel to the edge some Upper Cretaceous rocks are missing from the of the Blake Plateau and the other (slope anomaly B, crest of the feature but are present on the f ^,nks. The pi. 8) extends southwest to its termination against the formation of the Cape Fear arch is thought to have Ouachita (?) trend. Slope anomaly A seems to coincide been accompanied by downwarping of the flanks, with a northward trending basement ridge along the which Cooke (1936, p. 158) believed took place during late Eocene time. Other geologists have dated the Blake Escarpment between lat 28° N. and lat 31° N., origin at different times ranging from Early Creta­ as interpreted from seismic refraction data by Sheri­ ceous to early Miocene. Both Siple (1946, p. 37) and dan, Drake, Nafe, and Hennion (1966, p. 1984, and Eardley (1951, p. 131) have suggested that uplift and fig. 9). The significance of slope anomaly B is not erosion probably occurred during more than one stage. yet apparent. Seismic information (Meyer, 1957, p. 81, pi. 2; Recently, Watkins and Geddes (1965) reported on Hersey and others, 1959, p. 445) indicate? that the the slope anomaly between Cape Hatteras, N.C., and Cape Fear arch protrudes seaward across the conti­ Cape May, N.J., where it is 19 to 50 miles wide with nental shelf as a large regional nose in the basement peak intensities generally 350 gammas more than those rocks. At the crest of the arch on the corstline, the of adjacent areas. By comparing this anomaly with basement rocks are present at a depth of about 1,100 those along the Aleutian Islands chain and across the feet. The basement surface slopes northward to a island of Puerto Rico, they drew the inference that depth of 5,000 feet at Cape Lookout, N.C., and south­ the basement ridge along the Atlantic Continental ward to 2,500 feet at Cape Remain, S.C. A t the edge Shelf is a buried, quiescent island arc and that the of the continental shelf, the basement rocks on the slope anomaly reflects intrusive and extrusive phases crest of the arch are 4,000 feet below sea level. Ewing, of volcanism during the active tectonic development Ewing, and Leyden (1966, p. 1965, fig. 16) suggest a of the island arc (Watkins and Geddes, 1965, p. 1357). more southerly direction for the seaward ertension of STRUCTURE 23

85° W. 80° W. 75° W. 70° W.

40° N.

35° N.

30° N. Southwest '' . Georgia erpbayment

25° N.

FIGURE 6. Index map of Atlantic Coastal Plain and Continental Shelf showing principal structural features and lines of sections. 24 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF the Cape Fear arch than that indicated by the earlier Bahamas had been controlled by ancient folding of seismic interpretations but do not present basement sedimentary formations. Hess pointed out the need contours. for further geophysical data to determine whether or PENINSULAR ARCH not the folded Appalachians, or a branch of them, The dominant subsurface structural feature of Flor­ extend under the Bahama region. The same gravity ida and southeastern Georgia is the Peninsular arch. data with many more contributed by oil companies It has a southeast trend and extends from southern were interpreted by Talwani, Worzel, and Ewing Georgia down the axis of the Florida Peninsula (1960, p. 159) as indicative of grabenlike downfaulting (Applin, 1951, p. 3; Toulmin, 1955, p. 210). The struc­ along the same trend. ture was topographically high in Early Cretaceous and In 1947, Pressler (1947, p. 1858) suggested on the early Late Cretaceous time, during which sediments basis of the sea-bottom configuration "that th^. Florida were deposited around it, but not over it beds of peninsula is bounded on the east and south by major Austin age rest on Paleozoic rocks in places on the fault zones, and that the Bahaman and Cul^an areas crest. A later (Miocene) auxiliary uplift known as are very large faulted segments of the Gulf of Mexico the Ocala uplift occurred on the southwest flank of plate or basin." His sketch map (Pressler, 1947, fig. 1) the Peninsular arch. The Peninsular arch slopes north­ indicated an anticlinal flexure, which he named the ward toward the Southeast Georgia embayment. Bahama uplift, plunging northwestward through the eastern rim islands of the Bahama group toward Cape SOUTHWEST GEORGIA EMBAYMENT Kennedy (see fig. 6) and terminating agains* a major fault zone at the edge of the continental shelf. Press­ The Southwest Georgia embayment encompasses ler (1947, p. 1853) also suggested a probable close parts of southwestern Georgia, southeastern Alabama, relationship between the Bahama uplift and the and the Florida Panhandle between the Chattahoochee southeast-trending basement ridge now knoT^n as the uplift of Alabama and Georgia and the Peninsular Peninsular arch. arch. It appears to be a relatively shallow reentrant Seismic refraction investigations by Sheridan, in the Upper Cretaceous (Austin) rocks, as shown by Drake, Nafe, and Hennion (1966) have confirmed the tectonic map of the United States (Cohee, 1962). Pressler's general concept of the relationship between However, it is quite prominent in the older sedimen­ the Peninsular arch and the Bahama up Mft. The tary and basement rocks. The contained sedimentary results indicate that the Peninsular arch exteras south­ rocks exceed 7,500 feet in thickness north of the eastward under the western end of Little Bahama Florida-Georgia boundary and probably exceed 15,000 Bank (Sheridan and others, 1966, fig. 9, p. 1986). feet offshore. Considerable thicknesses of Lower Cre­ However, seismic reflection investigations by Ewing, taceous rocks have been penetrated by wells in this Ewing, and Leyden (1966, p. 1960) indicate that the embayment. The stratigraphy suggests that this em­ continental slope between Florida and the Bahama bayment was well filled by Early Cretaceous sediments Islands is a depositional feature and that no major before Late Cretaceous deposits were laid down in it. fault zone is present at the edge of the continental Antoine and Harding (1963, fig. 8) have postulated shelf. Sheridan, Drake, Nafe, and Hennion (1966, on geophysical evidence a protrusion of the Peninsular p. 1976) agree and conclude that seismic refracting arch (Ocala uplift) southwestward into the Gulf of horizons cannot be equated with stratigraphic bound­ Mexico. They present structure maps (Antoine and aries through the marked physiographic changes be­ Harding, figs. 6 and 7) showing this in Cretaceous tween Florida and the Bahama Banks. rocks as well as in the basement rocks. This protrusion in the basement rocks marks the south flank of the SOUTH FLORIDA EMBAYMENT Southwest Georgia embayment (pi. 4). The South Florida embayment as described by Pressler (1947, p. 1856) embraced the synclinal area BAHAMA UPLIFT between the Peninsular arch, the Bahama Islands, and A positive structural element extending northwest­ Cuba. The axis was believed to extend "along a gen­ ward through the Bahama Islands was inferred first eral line through Great Inagua Island to a point near by Hess (1933, p. 42-45 and fig. 9) from the submarine the south end of Andros Island, thence across the topography and gravity measurements in that region. Bahama Banks to the Florida Keys near the north He believed that the formation of the long, parallel end of Key Largo and across Dade and Monroe northwestward-trending submarine valleys between the Counties to the southwest coast of Florida," Patton STRUCTURE 25 (1954, p. 160) restricted the term to the area between tion into the embayment about 15 to 30 miles inland the south flank of the Ocala uplift, a Tertiary feature from the coast. A later, more detailed seirmic survey offsetting the Peninsular arch, to the Straits of Florida by Pooley (1960, p. 21) confirmed the existence of just south of the Florida Keys. Murray (1961, p. 101) an elongate seismic anomaly but located its axis at followed Pressler's geographic name and description the coastline between Parris Island, S.C., and Sea of the area but referred to the feature as a basin Island, Ga. Pooley (1960, p. 21, and pi. 2) depicts rather than an embayment. this anomaly as a basement ridge, about 110 miles" long Applin and Applin (1965, p. 15, 16) applied Press­ and 40 miles wide, with more than 1,000 feet of relief ler's term "South Florida embayment" to the negative that is not reflected in the overlying beds. Data from area, in Lower Cretaceous rocks, whose axis "trends wells drilled since 1960 at the southern extremity of about N. 65° W. from the eastern end of Florida Bay the anomaly do not substantiate these dimensions. across the southern tip of the Peninsula and plunges However, they do not necessarily preclude the existence toward the Gulf of Mexico." Oglesby (1965) used the of a relatively minor structural nose in tH basement term "South Florida Basin" for the same general rocks farther north near the South Carolina border. area on his structural maps of Lower Cretaceous rocks, but he added a hypothetical northwesterly clo­ SALISBURY EMBAYMENT sure at 12,500 feet beneath the Gulf of Mexico. The name "Salisbury embayment" was applied by Sheridan, Drake, Nafe, and Hennion (1966, fig. 10), Richards (1948, p. 54) to the low area in the base­ on the basis of refraction seismic surveys, confirmed ment rocks between Washington, D.C., and Ocean the general structure of the Lower Cretaceous rocks City, Md., without definite north or south limits. as shown by Applin and Applin (1965, fig. 52). How­ More recent well and seismic data (Cohee, 1962) sug­ ever, their structural map of the pre-Jurassic base­ gest that the Salisbury embayment lies I *.tween the ment (Sheridan and others, 1966, fig. 9) extended latitudes of Newport News, Va., and Atlantic City, the negative feature eastward to Andros Island under *N.J. This embayment is fairly prominent in the base­ the name "South Florida-Andros Island Basin." This ment rocks, but it loses form in the younger beds, negative feature, which is more than 35,000 feet deep, which suggests that it is a pre-Cretaceous feature is outlined by the 20,000-foot contour on the basement nearly filled by Cretaceous sediments. At the coastline rocks on plate 4. The original name "South Florida in Delaware, it contains about 10,000 feet of Mesozoic embayment," proposed by Pressler in 1947 (p. 1856), and Cenozoic rocks. is retained in this report. The Salisbury embayment is a part of the much larger Chesapeake-Delaware embayment of Murray SOUTHEAST GEORGIA EMBAYMENT (1961, p. 92), which includes a large part of the The Southeast Georgia embayment (Toulmin, 1955), geosynclinal province north and east of the Cape Fear also called the Okefenokee embayment (Pressler, 1947, arch to the Grand Banks off Newfoundland. Despite p. 1856), is recessed into the Atlantic coast between the fact that both the Chesapeake and Delaware Bays, Savannah, Ga., and Jacksonville, Fla. It interrupts from which the name is derived, are located within the long, uniform slope of the basement away from the more restricted Salisbury embayment, the newer the south flank of the Cape Fear arch and extends name does not supercede the term "Salisbury southwestward to the Peninsular arch. This embay­ embayment." ment is primarily a tectonically passive feature, BLAKE PLATEAU TROUGH although it may have undergone some downwarping Seismic investigations of the continental margin on the continental shelf, where the rocks exceed 10,000 east of Florida by Sheridan, Drake, Nafe, and Hennion feet in thickness. Recently, Murray (1961, p. 96) used (1966) have revealed a broad trough in tl Q- basement the term "Savannah basin" in lieu of Southeast rocks about 150 miles east of the coast of northern Georgia embayment, but he extended the northern Florida. (See pi. 4 and fig. 6.) This trough is more limit to the Cape Fear arch in South Carolina so than 20,000 feet deep and extends from the Bahama that the terms are not synonymous. uplift northward beneath the middle of the Blake A basement ridge, the Yamacraw ridge, was Plateau. The northward limit of this trough is not described from seismic studies by Meyer and Woollard known as yet, but the part now mapped within the (1956), Meyer (1957, p. 71), and Woollard, Bonini, 20,000-foot contour is about 220 miles long and 80 and Meyer (1957, p. 49) as a southwestward projec­ miles wide. The western flank rises gradually into the 26 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Southeast Georgia embayment, which is outlined by EMERALD BANK TROUGH the 4,000-foot contour. The eastern flank rises more Using refraction seismic methods, Officer and Ewing abruptly to an outer ridge, less than 15,000 feet deep (1954, fig. 6) located an oval-shaped trough in the beneath the Blake Escarpment. The name "Blake crystalline basement beneath the continental shelf Plateau trough" is used herein for identification of about 120 to 150 miles off Halifax, Nova Scoria. (See this large negative feature. pi. 4.) Its axis crosses long 62° W. at approximately BALTIMORE CANYON TROUGH lat 43°15' N. (pi. 4) near Emerald Bank (U.S. Navy Hydrographic Office, 1949), for which it is named Seismic work by Drake, Ewing, and Sutton (1959, (Maher, 1966a,b; 1967 a,b). The east end has not been fig. 29) has revealed a long narrow trough in the base­ defined by seismic work, but assuming that th^ 10,000- ment rocks off the New Jersey and Delaware coasts. foot contour closes eastward about as it does westward, According to the tectonic map of the United States the trough may be as much as 120 miles long and 40 (Cohee, 1962), the basement rocks descend below sea miles wide. East of Halifax, the basement rocks slope level from 10,000 feet near the mouth of Delaware Bay very gently from shore to a depth of 8,000 feet; then to more than 16,000 feet about 40 miles offshore and they descend to 14,000 feet and rise to 10,000 feet then rise to somewhat less than 10,000 feet at the edge before dropping abruptly to 20,000 feet beyond the of the continental shelf before dropping abruptly to Shelf edge. Seismic velocities suggest that this basin 20,000 feet beneath the continental slope. The trough, is filled by consolidated sediments that OfT^er and as outlined by the 10,000 foot contour, parallels the Ewing (1954, p. 664) regard as most likeTy to be edge of the continental shelf for about 150 miles from Triassic in age. Woollard, Bonini, and Meycr (1957, about lat 40° N. to about lat 38° N., where it appar­ p. 70) agree that the consolidated sediments could be ently crosses the shelf edge to the slope. Along its Triassic, but believe that they are more likc^ to be western side, it bulges landward toward Delaware Paleozoic in age. The overlying semiconsolidated and Bay. This bulge corresponds somewhat to the much unconsolidated rocks thought to be Cretaceous and wider Salisbury embayment that lies beneath the Cenozoic in age respectively do not seem to reflect the underlying structure or topography (OPcer and Coastal Plain. Ewing, 1954, fig. 2). Inasmuch as this relatively unexplored trough is important not only to the geologic history of the east­ STRATIGRAPHY ern margin, but also to petroleum exploration, this negative feature has been designated the Baltimore By JOHN C. MAHEE and ESTHEB R. APPLIN Canyon trough (Maher, 1965, p. 6). Baltimore Canyon REGIONAL ASPECTS is a submarine canyon shown on the U.S. Coast and Geodetic Survey Nautical Charts (1961, chart 1109; Triassic, Cretaceous, and Tertiary rocks flank the 1962, chart 1108) at the approximate location where crystalline Appalachians from New York southward the trough intersects the edge of the continental shelf. and crop out roughly parallel to the present Atlantic coastline (pi. 4). Triassic outcrops are cor fined to GEORGES BANK TROUGH scattered down-faulted basins within the pedmont. A long, canoe-shaped trough in the basement rocks Lower Cretaceous outcrops are recognized ir part of off Cape Cod was located by geophysical programs of the Salisbury embayment (Stose, 1932) and may be represented farther south as thin clastic beds mapped oceanographic institutions (Drake and others, 1959, with the basal Upper Cretaceous. Upper Cretaceous fig. 29). This trough is outlined by the 10,000-foot con­ rocks crop out almost continuously along the Fall tour shown on the tectonic map of the United States Line from eastern Alabama to the north flark of the (Cohee, 1962) and does not reach 15,000 feet in depth. Cape Fear arch in North Carolina, and from Virginia It is about 215 miles long and 25 to 30 miles wide in to New York. Tertiary rocks crop out in broad pat­ places. Seismic velocities suggest that it also contains terns throughout the Coastal Plain except on the Cape Mesozoic and Cenozoic rocks. The name "Georges Bank Fear arch and where they are masked by a veneer of trough" has been used for identification (Maher, 1965, alluvial deposits. p. 6) because of its close proximity and subparallelism The Cretaceous and Tertiary rocks exposed from to Georges Bank. (See U.S. Coast and Geodetic Sur­ central Georgia northward to Long Island are mainly vey Nautical Charts (1945; 1962, chart 1108).) nearshore marine and continental elastics interspersed STRATIGRAPHY 27 with some thin lignitic layers and marl beds. Seaward, REGIONAL CORRELATIONS these rocks become marine in character and thicken to A regional stratigraphic study such as this is more than 10,000 feet at the coastline. Cretaceous rocks necessarily based to a large extent upon published do not crop out in Florida and southern Georgia, and reports. Many of these reports cannot present detailed only part of the Tertiary sequence is exposed in that supporting data in the form of measured sections, area. Both are predominantly marine carbonates in sample logs, electric logs, and paleontology because the subsurface and exceed 15,000 feet in thickness in of lack of space. It is necessary, therefore, not only the Florida Keys and Bahama Islands. The marine to examine the published reports .critically, but also carbonate units in southern Georgia and Florida, to search out the supporting detail in records, files, though less distinctly separable lithologically, are and unpublished reports. These basic data may be sup­ more uniform in character and thickness and more plemented with later information and then restudied. susceptible to paleontologic dating than the clastic About 400 wells in 11 states and three wells in the beds farther north along the coast. In addition, much Bahama Islands and vicinity (table 1, in back of more subsurface control is available from the more report) were selected for their stratigraphic sig­ than 300 wells drilled in Florida alone. nificance in this study. Drilling records of some sort Although more than 10,000 feet of shelf-type sedi­ are available for all these wells, but sample logs mentary rock is present at the Cape Hatteras shoreline with some paleontology are available for less than (well NC-14, table 1) and refraction seismic surveys half of them. Electric logs for about 200 irells, most indicate more than 10,000 feet of sedimentary rocks of them in Florida and Georgia, were obtained and in several offshore negative features (pi. 4), very little correlated. The regional cross sections of this report is known about the stratigraphy of the continental show 49 electric logs, nine sample logs, and two shelf. The first information came from rocks dredged driller's logs. For the sake of uniformity ard simplic­ by trawlers along the Grand Banks, Banquereau, and ity, electric logs, rather than sample logs, have been Georges Bank. These were collected in 1878 by Upham shown on sections where available. and were reported by Verrill (1878, p. 323) and Both electric logs and sample logs are available Upham (1894, p. 127) to contain Tertiary fossils. for many of the deep wells along the coart. In gen­ Much later, Dall (1925) revised the paleontology of eral, the characteristics of rock units in the region these rocks and noted Late Cretaceous species in one are more distinctively and accurately recorded on the boulder from Banquereau (Dall, 1925, p. 215). He ex­ electric logs than on the available logs prepared from pressed "little doubt that Late Cretaceous and Tertiary rotary samples by many different workers. Selectively, fossiliferous deposits originally existed along the however, the sample logs and detailed paleontology northeastern coast from Newfoundland southward, as of key wells provide the stratigraphic age assign­ far as the area of glaciation extended, though in most ments to which the electric log correlatiors must be cases the only evidence remaining is the presence in the reconciled; so the electric logs serve prir?ipally as glacial debris of fragmentary portions of the original objective records of relatively uniform value for select­ deposits" (Dall, 1925, p. 213). The first Cretaceous ing traceable rock-unit boundaries within paleon­ and Tertiary rocks thought to be in place on the tologic control and for the tracing of these rock units continental shelf were dredged from submarine canyon through areas lacking substantial paleontologic and walls hi Georges Bank (Stetson, 1936; Stephenson, lithologic control. 1936; Cushman, 1936). Since then, dredge samples and Two approaches have been made to the correlation short cores of Cretaceous and Tertiary rocks have been of the Mesozoic and Cenozoic rocks along the east taken at a few places on the continental shelf and coast one from the gulf coast marine facies in Blake Plateau. These have been summarized by Stet­ Florida northward through deep wells at the coast­ son (1949), Ericson, Ewing, Wollin, and Heezen line, and the other from the outcrops at the Fall (1961), and Uchupi (1963). The most significant of Line downdip through shallow wells to the same deep these are located on plate 2 and are discussed under wells at the coastline. The first approach utilized the the appropriate stratigraphic unit. In addition to well-known and documented microfossil zones used in dredging and taking short cores, a few test holes distinguishing both surface and subsurface rock units (pi. 1, wells GA^88 and FL-118 through FL-123) in the gulf coast region. The deep wells along the have been drilled several hundred feet into the conti­ coast penetrate a greater proportion of mrrine rocks nental shelf off Georgia and Florida. than those farther inland and, as a result, offer more 28 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF paleontologic evidence and stratigraphie uniformity. reported tops of geologic units on the electric-log The second approach attempts to relate local rock strips. The principal subdivisions of the rocks and units and names to those carried northward from the bounding unconformities are drawn in key wells with gulf coast. Numerous difficulties are involved in this. paleontologic control. These are extended to adjacent The rocks exposed near the Fall Line are predom­ wells by zoning the electric logs with both a number inantly clastic and relatively nonfossiliferous in char­ and a color code into the smallest traceable units acter, and many subdivisions and contacts in these within the larger units. This permits the recognition rocks are based entirely upon lithology. These rocks of the addition of new beds downdip and the absence thicken and change facies downdip so that many of of rocks at unconformities updip. In effect, it requires the distinguishing features on -which local outcrop an accounting for all changes from well to veil within names are based become indistinct in the deep wells. the larger units controlled by paleontology. In doing Fossils are not sufficiently abundant nor definitive this, no electric log correlations have been rmde know­ enough to delimit the units in many of the shallow ingly in violation of available paleontologic data, wells. although numerous changes of earlier opinions based The technique employed in correlating the electric on lithology have been suggested. logs has been to plot all paleontologic data and In general, the boundaries of most rock units shown

TABLE 2. Stratigraphie units and their gulf

Sys­ Series Gulf coast equivalent Florida units Georgia un'ts tem

Holocene, Pleistocene, Post-Miocene rocks Post-Miocene rocks Post- Miocene rocks TERTIARY QUATERNARY AND and Pliocene Miocene Miocene rocks Miocene rocks Miocene rocks

Oligocene Oligocene rocks Oligocene rocks Oligocene rocks

TERTIARY Rocks of Jackson age Ocala Limestone Rocks of Jackson a

Lower Cretaceous Lower Cretaceous Lower Cretaceous Lower Cretaceous (Neocomian) or (Neocomian) or Upper (Neocomian) or Upper (Neocomian) or Upper Upper Jurassic Jurassic Jurassic Jurassic absent STRATIGRAPHY 29 on these cross sections are drawn within fossil con­ as accepted communication practice in day-to-day trol on lithology as reflected by electric-log charac­ operations. teristics. These boundaries are not subject to exact The subsurface stratigraphy of the Mesozoic and agreement among geologists. Difference of opinion as Cenozoic rocks is outlined diagrammatic-rlly in this to the top and bottom of units within thick sequences report by eight regional cross sections, v^hose traces of clastic or carbonate rocks may be expected in the are shown in figure 6. Section A-B (pi. 9) follows magnitude of a hundred feet or more in some of the the Atlantic coastline and carries the gulf coast equivalents from the Florida Keys to Long Island. areas without indicating significant disagreement on Sections C-D, E-F, G-H, I-J, and K-L (pis. 10, 11, the regional history. This difference often arises as a 12, 13, and 14) attempt to tie these equivalents to the result of new nonfossiliferous beds appearing down- outcrops and local terminology in New Je^ey, Mary­ dip that can equally well be placed in the overlying land, North Carolina, and Georgia. Section M-N or the underlying rock unit on the basis of current (pi. 15) extends correlations across the Florida Penin­ information. As a region is more thoroughly explored sula. Section O-P (pi. 16) suggests correlations from by the drill, better agreement on correlations devel­ the Florida Keys to Andros Island in the Bahamas and ops, partly on more conclusive evidence but also points out the possible relationship of stratigraphy to coast equivalents in wells along the Atlantic roast

South Carolina units North Carolina units Maryland units New Jersey units Long Island units

Post-Miocene rocks Post-Miocene rocks Post-Miocene rocks Post- Miocene rocks Post-Miocene rocks

Absent on Cape Fear arch Upper and middle Upper and middle Miocene rocks Miocene rocks Lower Miocene rocks Lower Miocene rocks Absent on Cape Fear arch Rocks of uncertain age, No Oligocene known possibly Oligocene in part Miocene and Eocene Tertiary rocks Rocks of Jackson age Upper and middle Eocene rocks rocks undiffer­ undiffcrentiated Eocene rocks undifferentiated entiated Middle and lower Eocene and Paleocene rocks undifferentiated Lower Eocene rocks Beaufort Formation Paleocene rocks Paleocene (?) rocks Rocks of Navarro age Pedee Formation Monmouth Formation Monmouth Group Monmouth Group Rocks of Taylor age Black Creek Formation Matawan Formation Magothy Formation Magothy Formation and Matawan and Matawan Rocks of Austin age Rocks of Austin age Group undiffer­ Grouo undiffer­ entiated entiated Rocks of Eagle T^d age Rocks of Eagle Ford age Rocks of Eagle Ford age Raritan Formation Raritan Formation Tuscaloosa Formation Tuscaloosa Formation Rocks of Woodbine age Rocks of Washita(?) age Rocks of Washita(?) age Rocks of Washita(?) Rocks of Fredericks- Rocks of Fredericks- and Fredericks- Lower Cretaceous Lower Creatacous rocks burg (?) age burg (?) age burg (?) age rocks absent undifferentiated Rocks of Fredericks- Rocks of Fredericks- burg or Trinity age burg or Trinity age Rocks of Trinity(?) age Rocks of Trinity (?) age Rocks of Trinity (?) Lower Cretaceous Mesozoic rocks of Mesozoic rocks of age and older Lower Cretaceous (Neocomian) or Upper uncertain age, possibly uncertain age, possibly (Neocomian) or Jurassic absent Cretaceous (Neocomian) Cretaceous (Neocomian) Uppe~ Jurassic rocks absent 30 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF the sea bottom. The nomenclature used on these cross PRE-MESOZOIC BASEMENT ROCKS sections for subsurface rocks in different states is The surface upon which Mesozoic rocks were summarized in table 2. deposited appears to be relatively smooth, having Keliance has been placed largely on assemblages well-rounded topographic features and few sfructural of Foraminifera for age assignments of lithologic irregularities. Not enough wells have been drilled to units in wells on these cross sections. The age rela­ be certain of this, but the few well records available tionships of these assemblages were first worked out and published seismic work suggest a gentle slope of about 15 feet per mile from pre-Mesozoic outcrops to and used extensively in the gulf coast region, where a depth of about 3,000 feet. Below this depth the slope several hundred thousand wells have been drilled in steepens somewhat sharply to more than 100 feet per the search for petroleum. The most significant Foram­ mile. inifera in the assemblages found in cores and samples The basement rocks are primarily igneous and meta- from the wells on the cross sections are listed in morphic_ *- rocks of Precambrian and Paleozoic age.O table 3 prepared by E. R. Applin. Hundreds of addi­ These include a wide variety of granite, diorite, gneiss, tional microfossil identifications and many detailed schist, tuff, volcanic ash, rhyolite porphyry, gabbro, lithologic descriptions for these wells and nearby wells basalt, and diabase. The basic igneous intru^ives are have been available not only from the published found in both Paleozoic and Triassic rocks, and in sources noted on each cross section but also from some wells the Triassic intrusives have been regarded unpublished sources such as the files and collections of incorrectly as pre-Mesozoic basement. Paleozoic sedi­ mentary rocks ranging from Early Ordovician to Mid­ P. L. and E. R. Applin, State geological surveys, and dle Devonian in age are present in the basement in some oil companies. Publication of complete fossil northern and western Florida and in southerr Georgia lists and lithologic descriptions for wells in this huge (Applin, 1951, p. 11-15; Bridge and Berdan, 1951; province is beyond the scope of this report. Carroll, 1963).

TABLE 3. Distribution cf definitive [Depth in feet; italic number indicates fossil found in core.

Rocks of Late Jurassic or Early Cretaceous Rocks of early Trinity age Rocks of late Tr'nity age (Neocomian) age

Pseudocyclammina Anchispirocyclina Well No. (plate Cuncolina-like Nubeculinella cf.Orbitolina Verneuilinid Coskinolinal DirfyocoTi? fragments numbers in Choffatdla decipiens henbesti Choffatella Dufrenoya Atopochara disciformis floridanus parentheses) decipiens Orbitolina trivolvis Arcellites minuta Orbitolina Caprinid fauna texana Id texana terana sp. form sp. sp. B,cn o j£ £

FL-57 (9, 15)...... 58(15)...... 64(15)...... 73(9)...... -..-.. 86 (9)...... 12, 730 11,736 13,094 11,200 11,100 10, 120 10,674 10,674 11,200 10,360 12,11,580 259 104(9,16)-...... -.. 11,709 11,660 11,709 11,836 11,649 9,780 10,028 10 028 11,847 11.9S3 11,913 10, 122 10 122 109(16)...... 14,684 14, 517 13,400 11,490 12.610 12,190 13, 510 11,680 13, 850 Ill (16)...... 15, 375 15,255 11,624 /*, 614 IS. 82 4 1S.8S4

GA-42(9, 13)...... 59(14)...... 61 (14)... _..._..... 72(14)...... ,.. 75(14)...... 87(9, 14)......

AL-1 (14)...... 2 (14)...... SC-21 (9)...... 14(9,12)..-...... 8,980 9, ISO 8,910 8,505 NJ-25 (9)...... 4,430 4,400 STRATIGRAPHY 31 The oldest rock recovered from the sea bottom along Well GA-61 (Mont Warren Chandler 1) and well the Atlantic coast has come from the granite pinnacles GA-72 (Stanolind Oil and Gas Pullen 1) in south­ of late Paleozoic to early Mesozoic(?) age (Toulmin, western Georgia, shown on section K-L (pi. 14), 1957, p. 914) at a depth of about 30 feet on Cashes penetrated more than 900 feet of red and green shale Ledge near the middle of the Gulf of Maine (pi. 2 and sandstone beds; some diabase sills in well GA-72 and fig. 2). This granite is similar in composition to are generally regarded as representative of Triassic the Quincy Granite exposed in large areas of nearby sequences. Well AI^-3 (W. B. Hinton Creel 1) in eastern Massachusetts and Rhode Island. LaForge southeastern Alabama, about 40 miles updip from well (1932, p. 35) considered the Quincy Granite to be GA-61, penetrated a 700-foot thick sequence of basic either Devonian or early Carboniferous in age. igneous sills interspersed with thin clastic b°-ds beneath rocks of Early Cretaceous age. This predominantly MESOZOIC ROCKS igneous sequence may be Triassic in age al^o, although TRIASSIC(?) ROCKS the lithology is less distinctive. Triassic rocks consisting of red arkose, sandstone, Rocks assigned to the Triassic (?) are present also shale, tuff, and basalt flows, in places intruded by in the subsurface of Maryland along the line of sec­ diabase, are exposed in basins downfaulted in the base­ tion E-F (pi. 11). Well MD-6 (Washington Gas ment rocks of the piedmont. Similar Triassic-filled Light Mudd 3) near the Fall Line is reported (Ball basins are thought to exist beneath the Coastal Plain and Winer, 1958) to have penetrated 237 feet of on the basis of well and seismic data (Bonini and Triassic clastic beds beneath the Lower Cretaceous Woollard, 1960, p. 304, 305; Cohee, 1962). Rocks Patuxent Formation. The presence of these rocks close lithologically similar to the exposed Triassic rocks, to the Fall Line suggests that they may be preserved shown on sections E-F and K-L (pis. 11 and 4), have in a grabenlike feature similar to those downfaulted been penetrated by several wells and are referred to Triassic blocks more or less on strike in the piedmont as Triassic(?). of Virginia. fossils in wells on sections Well numbers keyed to table 1, plate 1, and plates 9-16]

Rocks of Fredericksburg age Rocks of Rocks of Woodbine age Rocks of Eagle Ford age Washita age

subgoodlandensis Nummoloculina AmmobacuHtes AmmobacuHtes infrtguensvar. Coskinolinoides schlumberger comprimatus Acruliammina Trochamm'ma langsdalensis eaglefordensis Trochammina Hastigerinella Gaudryinacf. Dicydinacf. braunsteini rainwattrl Placopsilina Valvulincria wickendeni moremani moremani bosquensis Cuntolina Trocholina Ammotium agrestis Planulina Gumbelina Lituola walteri floridana teiana htimi longa

6,371 5,160 5,090 5,090 4,868 4,868 4,130 4,130 4,060 4,060 6,760 6,984 7,390 6,182 8.963 9,070 7,500 9,000 8,360 6,900 9.840 10, 724 7,736 10,000 8,500 9,470 10,006 7, BOS 10,645 8,445 11.080 8,550 3,920 3,970 4,m 4,00 3,007 3,037 3,034 2,605 2,605 2,605 3,495 3,510 2,830 2,865 3,810 3,810 3,196 3,196 3,196 4,1X6 4,1*6 4,S90 1,0X6 1,0X5 400 840 840 840 3,149 3,149 2,646 2,646 2,64f 6,770 5,790 5,310 5,310 32 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 3. Distribution of definitive Rocks of Austin age Rocks of Taylor age

Well No. (plate numbers in parentheses) If "So 1 TSwfe-f .§! II s s .23 I*

FL-67 (9,15). 3,600 3,610 68 (15)- 3,180 64 (15).. 3,030 3,290 73(9).- 86 (9) 5,785 5,785 106 (16). Ill (16). OA-26» (13). 37(13). 2,157- 2,162 38(13)... ,900 2,580 42(9,13). 3,278 2,740 69 (14) 3,779 61 (14) 2,000 1,940 2,260 1,358 1,213 1,510 72(14).. 2,626 2,370 2,370 1,890 1,906 76(14)-. 3,050 2,863 2,910 1,883 3,126 2,410, 2,447 2,447 87(9,14). 3,830, 3,430 3,430 3,906 AL-1 (14).. . 36 36 2 (14)..- 630 370 370 460 220 SC-21 (9).. ... 2,326 2,145 2,325 1,646 NC-7(9).. ... 2,400 14(9,12)... 4,380 47380 4,380 4,380 3,160 43(12) 1,126 47(9,12) 1,663 MD-11 (11)... 820 12(11).- 1,480 1,480 1,390 1,400 13 (11) ..... 1,894 1,760 14(9,11).... 2,160 NJ-26 (9). 2,020 2,020 2,020 2,160 Paleocene rocks

Well No. (plate num­ bers in parentheses) I*II

FL-62(9)..- 1,835 67 (9,16). g.139 i,800 68(16). 2,000 2,050 2.160 69 (16). 1.668 1,880 2,142 64(16). 2,000 2,030 2,280 2,430 73(9).. 3.460 3,078 3,360 86(9).. 5,950, 4,170 104 (9,16). 3,610 3,800 3,610 106(16)... 3.970 3,310 4,200 3,680 Ill (16). 3,706 4,160 4.600 OA-26»(18)- 1.276 1.275 38(13)... 42(9.13). 1.960 1.960 1.960 69 (14)... 72(14).-. 76 (14)... 1,740 BA-2 (16). 6.940 7.170 6.600 7,700 8,046 8C-21 (9). 1,266 1,316 1,205 MD-11 (11). 660 690 12(11). 1,330 NJ-26 (9).. 1,770 1.770

See footnotes at end of table. STRATIGRAPHY 33 fossils in wells on sections Continued Rocks of Taylor age Con. Rocks of Navarro age

Olobotruncanaarea Anomalinapmguit Rudistidfragments Olobotruncanasp. pteudopapittosa Pseudodavulina Planulinacorrecta i Planulinatexana Lepidorbitoidet S (J Asterorbisrooki a Rotaliatn.sp. Olobotruncana canaliculata Olobotruncana Cibcidetharperi navarroentit plaitumvar. Dorothiabutteta severalsp. Lenticulina Neoflabettina 1 1L Anomalina reticulata. cretacea daoata Loxottomm || * I 8 1s 1 2,910 3,030, 3,030, 3,160 3,160 2,420 2,520 2,520 2,760 2,730 2,660 2,660 3,810 2,890 3,841 3,841 4,870 6,640 6,680 5,110 5,200 1,796 1,851 2, 155 2,480 2,300 2,840 3,090 2 K40 j 240 3,676 1,591 ,213 .,213 RfiO ,845 ,890 890 2,310

290 110 1,325 ,526 . ,435 2460 3.160 1,166 944 738 ,213 760 760 360 1,380 ,390 KQi 1,709 ,709 . 1,709

7! 160 1,980 1,980 ,980 Paleocene rocks Continued Lower Eocene rocks

1 1 Olobigerinatrilo- Vaginulinamid­ Coskinolinaelon- Spiroplectammina S Olobarotaliaaeuta aeguilateralit Mitcettaneanat- Valvulineriawtt- GloborotaliawU- Eponidetdorfi wttcoxentit Ilelicottegina culinoidet tauentit coxentit ! coxentit §S Qyroidina wayana 0 gyralit gata 1 S f \l S *° 1,4S5 1,6SB 1,410 1,640 1,300 1,600 1,300 1,660 1,160 1,330 1,120 1,660

2,845 2,943

1,570 1,670 1,500 1,600 1, 600 1,600 1,646 1,590 1,265 1 256

1,340 1,770 1,890 1,890 1,890 34 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

TABLE 3. Distribution of definitive

Middle Eocene rocks

Well No. (plate numbers Discorbisinornatus Asterigerinatexana avonparkensis Discorinopsis Peronettadatti Lituolawatersi Cribrobulimina semimarginata iensismonttce nassauensis in parentheses) Dictyoconus Dictyoconus americanus I Epistomaria Helicostegina ^iternMifli^a, floridanus Lituonella coryensis gunteri cuslimani Textularia coryensis floridana Spirolina Flintina gyralis Gyroidina

FL-52 (9). .-...... 680 8SO 8SO 57(9, 15)...... 100 470 350 1,100 1,100 1,250 58(15)...... 390 410 600, 870 890 630, 920 69(15)...... 46 75 255, 265 675 675 64(15).. 73(9).... .- 410 410 1,400 oft fn\ 1,040 1,260 1,616 1,300 970 1,010 1,110 1,330 104 (9,16) 1,100 1,140 1,140 1,200 1, 310, 1,360 1,860 106(16).. 2,327 2,327 109(16)... . 1,240 1,240 S,S60 ----- ...... 1,240 Ill (16)... . 1, 370, 1,390 1,390 2,020 1,460 1,960 GA-26 ' (13)...... 83'- 845 37(13) -. 38(13).. - -. 42(9, 13),...... 1,040 1.040 1,040 59(14). - ...- 1,420 1.000 72(14).. 75(14) 810 1,060 960 87(9, 14)...... 1,550 BA-2 (16). 2,460, 4,230 MD-12 (11)...... NJ-25 (9)......

Upper Eocene rocks

Well No. (plate Pseudophragmtna moodysbrancllensis numbers in Operculinoides mariannensis Operculinoides jacksonensis jacksonensis Sphaerogypsina parentheses) Lepidocyclina Heterostegina Amphistegina Asterocyclina nassauensis Marginulina cooperensis Varginulina floridensis flintensis Operculina Lenticulina virginiana cocoaensis cocoatnsis texasensis ocalana ocalana cosdeni Bulimina Eponides Eponides Uvigerina globula Nonion advenum

FL-62 (9). ... 420 520 460 460 64 (15). ._.---.--... 35 35 73(9)...... 300 300 360 oft fn\ 104(9, 16)... .---. 105 (16). .-.-- . 1,656 1,656 1,772 1,772 1,772 1,656 1,772 109(16)... . Ill (16)...... GA-82(13)... ------132 765-815 37(13) 740 38(13) 650 780 41(13) ------730 511 42(9, 13)...-. 520 680 460 600 600 820 960 59 (14)...... 780 900 600 700 780 60(14) ... 636 72(14)...... 460 75(14). 470 570 420 MD-11 (11)...... 470 12(11) 1,160 1,160 1,240 NJ-25 (9) ... 1,420 1,420 1,420- 1,520 1,520 1,520

See footnotes at end of table. STRATIGRAPHY 35 fossils in icells on sections Continued

Middle Eocene rocks Continued

1'S.S amerkanusvar. Spiropkctammina cedarkeysensis l§ alatolimbatus Lepidocydina walnutensis mauricensis tattahattensis efi umbonata Amphistegina Didyoconus Lepidocydina soldaniivar. Valvulineria plummerae blanpiedi mexicanus Lenticulina mexicanus Lenticulina Anomalina Lockhartia cushmani cubensis lopeztrigoi Globrotalia spinulosa Valvulineria cubensis assulata persimOis fe-8 Eponides Gunteria floridana Fabiania Claeulina floridana Cibicides aniittea Cibicides Cibicides Discorbis Oyroidina li Cibicides westi Cibicides f

870 890 1,040, 1,220 1,220 67ft 945 130

2,572 2,572 2,572 i,t60 2,250 2,200 815- 915 825 760 760 760 1 ?60 1,570 1,460 1,460 1.420 1,000 860 760 1,045 1,045 1,030

2,370. 2,460 1,280 1,290 1,610 1,610 1,610 1.610

Upper Eocene Rocks Continued Oligocene rocks

(r.w.)walnutensis striatoTeticulatus mexicanusvar. byramensisvar. Quinqueloculina jacksonensis Operculinoides gunttri(r.w.) Operculinoides inexcavatum Heterostegina diaCamirina Discorinopsis Lepidocydina Valrulineria Mlogypsina Didyoconus Miogypsina Pararotalia Pararotalia Astertgtrina subacuta Dictywonus Didytonus mantelli Nonionetta hantkeni Discorbis assulata gunteri antillea (r.w.)sp. floridanus leonensls Nonionetta leonensis Nonion Camerina sp. sp. sp.

880 880 980, 990 1,020 1,070 1,210 1,210 1, 140 1,140 1,260 132 132 765-815 512-520 44

TABLE 3. Distribution o/ definitive

Miocene Bocks

Well No. Amphictegina concentrica a Textulariella procanrellata mediocostatum GloboTOtalia menardii mansfleldi Lenticulina Hanzawaia .e a Miogypsina (plate numbers lessonii americana floridanus staufferi banettii pizanense flaridanus in parentheses) Bucella Archaias gs Chione ulocyma Chione Nonion Nonion Cibicides |1 <

FL-57(9, 15)- - 47 73(9)....-.-.-.. 130 Rft fQ\ 510 510 104(9, 16)- . . 250 280 320 330 610 7i6 750 770 105 (16). ------270, 620 109(16). - - 380 845 905 111 (16)------580 920 920 900 MD-12 (11) --.. .- 650 NJ-25 (9)...... 920 920 1,080

» Fossil data for well GA-26 from nearby Root and Ray Fowler 1 (Herrick, 1961, p. 408-410). 2 Fossil data for well GA-8 from nearby Layne-Atlantic City of Sandersville 5 (Herrick, 1961, p. 424-426).

Well MD-12 (Ohio Oil Hammond 1), well MD-13 they have been partially penetrated by deep wells. (Socony-Vacuum Oil Bethards 1), and well MD-14 Applin and Applin (1965, p. 18-25) have described (Standard Oil of New Jersey Maryland Esso 1) near these rocks in the Amerada Petroleum Cowles Maga­ the coastline on section E-F (pi. 11) penetrated rock zine 2 in St. Lucie County and have named the sequences, 165 to 525 feet thick, that were assigned sequence the Fort Pierce Formation for a nearby city. to the Triassic by Spangler (1950, p. 121). Anderson The type sequence is 2,220 feet thick and consists of (1948, p. 100) regarded the same sequences in well a lower red clastic unit, 170 feet thick, that rests on MD-12 and MD-13 as Triassic, and the sequence in highly altered igneous basement rock, and f.n upper well MD-14 he regarded as the Lower Cretaceous carbonate unit, 2,050 feet thick. The upper carbonate Patuxent on the basis of differing hardness and color. unit is made up of alternating finely crystallir^, partly This unit in wells MD-12 and MD-13 consists of beds oolitic and bioclastic limestone, dolomitic limestone, of hard dark-gray shale and sandy shale with maroon and dolomite beds interspersed with thin gray shale mottling, quartz conglomerate with some white feld­ and anhydrite beds. The characterizing faunal assem­ spars, and hard reddish-brown and green shale, sandy blage of the Fort Pierce Formation contains fossils shale, and arkosic sandstone. In well MD-14 farther that are partly of Late Jurassic and partly of Early downdip, the sequence consists of beds of coarse­ Cretaceous age. The distinctive features of tl ^ micro- grained sandstone containing pebbles, gravel, and faunal assemblage were illustrated in an earlier report kaolinized feldspars, beds of gray, green, and brown by Applin and Applin (1965, pis. 3, 4). The fauna is shale, and some calcareous layers. characterized, mainly, by abundant specimens of Fo- The lithologies and electric-log curves for these non- raminifera belonging to the family Ataxophrr.gmiidae, fossiliferous sequences are not dissimilar enough to subfamily Verneuilininae, that are small and biserial rule out the possibility that these sequences may be throughout the larger part of their development. A correlative facies. If so, they could be either Trias- large conical species of Cuneolinal is another defini­ sic(?) or equivalent to the Upper Jurassic or Lower tive fossil, and several undescribed species of Pseudo- Cretaceous (Neocomian) rocks in the Cape Hatteras phragmma are moderately common. well (NC-14, pis. 9 and 12). For these reasons, the Rocks in part equivalent to the Fort Pierce Forma­ broad, relatively noncommittal term "Mesozoic rocks tion may crop out along the base of the Blake Escarp­ of uncertain age, possibly Neocomian" is used on both ment. Dredgings of algal limestone of Neocomian to plates 9 and 11. Aptian in age from depths exceeding 10,000 feet have been reported by Heezen and Sheridan (1966, p. 1645) UPPER JURASSIC OR LOWER CRETACEOUS and are discussed herein under "Lower Cetaceous (NEOCOMIAN) ROCKS rocks." Rocks of Late Jurassic or Early Cretaceous (Neo­ The Fort Pierce Formation has been penetrated by comian) age, which do not crop out in eastern North wells FL-104, FL-86, FL-111, and FL-109 on sections America, are present beneath southern Florida, where. A-B and O-P (pis. 9 and 16). The deepest penetra- STRATIGRAPHY 37

fosstts in wells on sections Continued

Miocene rocks Continued

Spiroplf.ctammina mississippiensls o yurnagunensis maTylandica superegrina * vtsicularis Marginulina Amphisteginachipolensis Lepidocyilina Valvulineria Rotorbinellat Angidogerinaoeddentalis Buliminella elegantitsima Textularia §2 Peneroplis Gyroidina. Ise« mayori St: Gypsina fr- floridana rosacca Bulimina inflata Lvigerma K. ^ 3 bradyi Sl«^~s dubia *^a O £*- i* a;"1° 'Cs «ft « P

630 600 915 380 420 745 420 370 580 700 790,900 920 1,080 910 1,100 1,100 1,020 1,080 1,080 1,080 920 920 X.

tion (1,115 feet) was made by well FL-109 (Gulf Oil be at 8,800 feet, where it is drawn tentatively in this State lease 373 1) on Big Pine Key, Fla. (pi. 16). The report, or it may be as deep as 8,960 feet. formation wedges out northward along section A-B The sequence of rocks termed "Mesozc'c rocks of and is absent from well FL-73 (Humble Oil and Re­ uncertain age, possibly Neocomian" in well MD-14 on fining Carroll 1) in Osceola County, Fla., where rocks section A-B (pi. 9) may be equivalent tc the Upper of Trinity age rest upon biotite granite of pre- Jurassic or Lower Cretaceous (Neocomir.n) in well Mesozoic age. NC-14 at Cape Hatteras. The same rocVs probably Rocks of Late Jurassic or Early Cretaceous (Neo- are represented in the lower part of the interval comian) age are also present in well NC-14 (Standard marked "rocks of Trinity (?) age and older" in well Oil of New Jersey Hatteras Light 1) on section G-H NJ-25 (Anchor Gas Dickinson 1) in New Jersey and (pi. 12) in North Carolina. There the sequence, 8,960 wedge out updip between that well and well NJ-26 to 9,878 feet in depth, grades downward from finely (U.S. Geological Survey Island Beach 1). As pointed crystalline, partly oolitic limestone and gray shale out in the discussion of Triassic( ?) rocks, the relation beds to red and green sandy shale layers and red- of the hard reddish clastic sequence resting on base­ stained, fine- to coarse-grained sandstone beds, partly ment in wells MD-12 and MD-13 on rection E-F conglomeratic and arkosic, at the base. The lower red (pi. 11) to the lower soft-gray clastic Hds in well clastic beds may correspond roughly to those noted by NC-14 is in doubt. Applin and Applin (1965) in the Amerada Petroleum Cowles Magazine 1 in Florida. Swain (1947, p. 2058) LOWER CRETACEOUS ROCKS assigned the beds between 9,150 and 9,878 feet to the SUBDIVISIONS pre-Trinity (Coahuila?) in 1947. Later, in 1952, he The Cretaceous system in the gulf coa^t region is reassigned the beds from 8,500 to 9,878 feet to the divided into the Comanche Series and the Gulf Series. Upper Jurassic(?) and referred to them as "beds of The Comanche Series is subdivided into the Trinity, Schuler(?) age" (Swain, 1952, p. 66). E. R. Applin Fredericksburg, and Washita Groups. Th*, lower two reports molds of Atopochara sp., suggestive of early groups are entirely Early Cretaceous in age, but the Trinity age, between 8,505 and 8,515 feet and Anchi- Washita Group is regarded as mostly Early Creta­ spirocyclina henbesti Jordan and Applin in a core at ceous but partly Late Cretaceous in age by the U.S. a depth of 9,115 to 9,116 feet. Maync (1959, p. 66) Geological Survey (Imlay, 1944) on the basis of world­ considered the latter fossil to be closely similar to wide fossil zones. The boundary between Lower and Iberina lusitanica (Egger), which in Europe "strad­ Upper Cretaceous rocks on the cross sections of this dles the Jurassic-Lower Cretaceous boundary." It is report is indefinite because of lack of p aleontologic possible that Ancliispirocyclina henbesti is also indica­ detail and is shown diagrammatically with a query. tive of beds of Late Jurassic or Early Cretaceous age. The top of rocks of Washita age can be readily identi­ Therefore, the base of rocks of Trinity (?) age may fied within a few tens of feet in most sets of drill 38 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF cuttings and can be mapped consistently in the sub­ that the sample of calcilutite from a depth of 7,790 surface. In discussion of distribution of Lower Creta­ feet represents sediment laid in water about as deep ceous rocks in this report, all rocks of Washita age are as the waters over the Blake Plateau today (650 to grouped with those of Trinity and Fredericksburg 3,600 feet). This indicates continuing subsidence since age as a matter of convenience only. Early Cretaceous time in a total amount exceeding The Lower Cretaceous is subdivided on these cross 15,000 feet. sections only in Florida, North Carolina, and Mary­ In southern Florida, the Lower Cretaceous rocks land, and in one well in New Jersey where the rocks are predominantly carbonates and exceed 6/700 feet are sufficiently thick, uniform, and fossiliferous to pro­ in thickness in the Florida Keys (well FL-10S, pi. 16). vide fairly reliable unit correlations. These subdivi­ Northward along section A-B (pi. 9), the rocks sions and fiteir correlations from well to well are most wedge out on the Peninsular arch, then reappear as a reliable in the southern Florida carbonate section and thin clastic unit across parts of Georgia ard South least reliable in the mixed clastic and carbonate sec­ Carolina. They are missing from the higher parts of tion in Maryland and New Jersey. Little fossil evi­ the Cape Fear arch in North Carolina but am present dence suitable for subdividing the Lower Cretaceous on the east flank as a thickening wedge of mixed rocks exists north of Cape Fear, and the dashed cor­ clastic and carbonate rocks more than 2,800 feet thick relation lines on the cross sections represent an opinion at Cape Hatteras (well NC-14), as corrected on based mainly on lithology and electric log data avail­ Foraminifera by E. R. Applin (written coimnun. to able in 1965. J. B. Reeside, Jr., 1957), and 2,600 feet thick in Mary­ land (well MD-14). Lower Cretaceous rocks probably LITHOLOGY AND DISTRIBUTION extend into northern New Jersey but do rot reach Rocks of Early Cretaceous age, several hundred Long Island. feet of sandstone and shale beds, are recognized at the Considerable thicknesses of Lower Cretaceous rocks surface in part of the Salisbury embayment, as shown are present in southwestern Georgia. Section K-L (pi. by the geologic map of the United States (Stose, 14) shows more than 2,500 feet of dominantly clastic, 1932). They may be represented at or near the sur­ undifferentiated, Lower Cretaceous beds in wells GA- face in northern North Carolina, western Georgia, and 61 and GA-72. Alabama by thin clastic beds inseparable lithologically REGIONAL THICKNESS from the basal Upper Cretaceous beds. Lower Creta­ ceous beds dip seaward from the Fall Line at rates that The regional thickness of Lower Cretaceous rocks increase from about 15 feet per mile to more than 60 and the underlying rocks classed as Late Jurassic or feet per mile (pi. 11). The thickness and marine con­ Early Cretaceous (Neocomian) in age in this report stituents increase accordingly. is outlined on plate 17J.. These rocks are present at Submarine outcrops of Early Cretaceous age have or near the Fall Line in New Jersey, Maryland, Vir­ been reported by Heezen and Sheridan (1966). They ginia, northern North Carolina, western Georgia, and dredged four samples from the Blake Escarpment at Alabama but are absent beneath most of th?. Coastal depths of 7,790, 10,266, 10,496, and 15,574 feet. The Plain in southern North Carolina, South Carolina, and samples from 15,574 and 10,496 feet were algal cal- eastern Georgia and on the crest of the Peninsular carenite and algal dolomitic calcarenite, respectively; arch in northern Florida. Thicknesses of about 3,000 both were assigned an age range of Neocomian to feet at Cape Hatteras and about 6,000 feet in the Aptian, which corresponds to that of the Coahuila Florida Panhandle and Keys are present beneath the Series and Trinity Group of the gulf coast. The sam­ Coastal Plain. Thick sequences are probably also pres­ ple from a depth of 10,266 feet consisted of gray, ent offshore on the Atlantic Continental Shelf, where oolitic, fragmental calcarenite to which was assigned geologic data are lacking and seismic data too sparse an Aptian (?) age, corresponding to Trinity (?) in the and contradictory to permit representation of thick­ gulf coast. The upper sample from a depth of 7,790 nesses on plate 17. Form lines are used to suggest dep- feet was gray and tan calcilutite of Aptian to Albian ositional shapes, and minimum estimates of maximum age, the age range of the combined Trinity and thicknesses are shown for general use in exploration Fredericksburg Groups of the gulf coast. Heezen and planning. It seems probable that thicknesses may ex­ Sheridan (1966, p. 1645) concluded that the calcare- ceed 7,500 feet in the South Florida embayment and nites from depths of 10,266, 10,496, and 15,574 feet Blake Plateau trough, 5,000 feet in the Southeast represented sediments deposited near sea level and Georgia embayment and Baltimore Canyon trough, STRATIGRAPHY 39 and 3,000 feet in the Georges Bank trough, judging Another type of microfossil, the mega^ore Arcel- by the rate of thickening onshore and the scattered lites disconjoi^mis (Miner) Ellis and Tschudy (Ellis seismic profiles offshore (pi. 5). and Tschudy, 1964, p. 75), was identified by R. H. Tschudy in a sample of cuttings at 4,400 to 4,410 feet ROCKS OF TRINITY AGE in the Anchor Gas Dickinson 1 (NJ-25), Cape May, LITHOLOGY AND DISTRIBUTION N.J. In his analysis of the sample, Tschudy (written commun., April 30, 1964) stated that "Arcellites dis- Rocks of Trinity age along sections A-B and O-P conformis is found in Lower Cretaceous samples. In (pis. 9 and 16) have a maximum thickness of 3,030 eastern United States it has been found only in the feet in well FL-111 (Gulf Oil SFL 826-Y 1) at thfc Patuxent Formation. I am fairly confident of a pre- western end of the Florida Keys, where they are prin­ Albian, Early Cretaceous age determinrtion * * *." cipally anhydrite, limestone, and dolomite. The thick­ Tschudy listed a number of other plant fossils in the ness decreases northeastward to 2,200 feet in well FL- sample and stated, "The absence of any Angiosperm 104 (Sinclair Oil and Gas Williams 1) on Key Largo pollen suggests pre-Albian." and continues to decrease northward along section A-B (pi. 9) to a wedge edge of clastic rocks against ROCKS OF EARLY TRINITY AGE the Peninsular arch (well FL-57). Rocks of Trinity age are absent from wells on section A-B (pi. 9) in LITHOLOGY AND DISTRIBUTION northern Florida, Georgia, and South Carolina. In Florida, rocks of Trinity age have been divided A sequence largely of sandstone, siltstone, and shale by Applin and Applin (1965, p. 36, 45) into rocks of beds in well NC-14 at Cape Hatteras, N.C., and in early and late Trinity age within which two forma- wells MD-12, MD-13, and MD-14 in Maryland (pis. tional units have been defined, The rocks of early 9, 11, and 12) has been assigned an age of Trinity (?). Trinity age are about 1,500 to 2,100 feet thick in wells This sequence is at least 1,150 feet thick and may be along the Florida Keys (pi. 16). At the west end of as much as 1,455 feet thick if the overlying beds of the Keys (well FL-111), the 1,589-foot interval is Trinity or Fredericksburg age are included. It is pres­ composed primarily of thick anhydrite Hds contain­ ent in well NJ-25 (Anchor Gas Dickinson 1) at Cape ing some lenses of salt. This evaporite facies has been May, N.J., but has not been differentiated from under­ termed the Punta Gorda Anhydrite (Applin and Ap­ lying sedimentary rocks of Mesozoic age. In well NJ- plin, 1965, p. 39). Eastward along th?. Keys, the 26 at Island Beach farther north in New Jersey, rocks evaporite facies continues to mark the top of rocks of of Early Cretaceous age are thought to be about 518 early Trinity age, but it gives way to thick oolitic feet thick, but no fossil evidence was reported from limestone and dolomite beds and thin dark shale lay­ these beds and no subdivisions are apparent. ers in the lower half. (See well FL-104, pi. 16.) The Limestones of Trinity age crop out along the mid­ Punta Gorda Anhydrite is 783 feet thick in well FL- dle of the Blake Escarpment (Heezen and Sheridan, 104, on Key Largo; no anhydrite was penetrated in 1966, p. 1645). Samples of gray oolitic limestone of well BA-2 on Andros Island in the Bahamas. Evap­ Aptian(?) age and gray slightly pyritic limestone of orite beds have been reported in well BA-1 drilled Aptian-to-Albian age have been dredged from depths to a depth of 18,906 feet on Cay Sal (pi. 1 and fig. 3), of 10,226 and 7,790 feet, respectively. but no samples have been available to confirm this or to suggest any correlations. However, known thick­ CHARACTERISTIC MICROFAUNA nesses do suggest that a sizeable evaporite basin Many specimens of Atopochara trivolvis Peck were existed in Early Cretaceous time to th

REGIONAL THICKNESS shelf have been too shallow to penetrate rocks of Austin age. The thickness of rocks of Woodbine and Eagle CHARACTERISTIC MICROFAUNA Ford age penetrated by wells ranges from a few feet to a maximum of 1,812 feet in well NC-14 (Standard Citharina texana Cushman is the diagnostic species Oil of New Jersey Hatteras Light 1) as correlated by of Foraminifera that most commonly distinguishes Spangler (1950, p. 113, 114) and E. R. Applin (writ­ the beds of Austin age in Georgia, Alabama, and ten commun. to J. B. Reeside, Jr., 1957). Offshore South Carolina (table 3). In North Carolina, some thicknesses may be expected to exceed 1,000 feet in question seems to exist about the upward range of the Southeast Georgia embayment and 2,000 feet in this species. Spangler (1950, p. 116) stated "* * * a the Baltimore Canyon trough, perhaps by a consider­ macrofauna 'younger than the Austin, perhaos Tay­ able amount (pi. 176"). Uniform thicknesses of less lor', was identified by L. W. Stephenson from these than 250 feet over much of the Florida Peninsula beds in the John Wallace 1 well. As a result, it is perhaps result from a stable platform in the Florida- thought that Vaginulina regina (now Citharina tex­ Bahama region during Late Cretaceous time. Rocks ana) (Cushman) ranges into younger beds along the of Woodbine and Eagle Ford age are absent on the east coast than in the Gulf Coast." Spangler (1950, Peninsular arch and the Cape Fear arch, where rocks fig. 5) recorded the occurrence of C. texana in several of Austin age rest directly upon basement rocks. wells from the Black Creek Formation, and 1 ?. (1950, p. 116, table 2) correlated the Black Creek in North ROCKS OF AUSTIN AGE Carolina with the Taylor in the gulf coast. However, LITHOLOGY AND DISTRIBUTION Spangler and Peterson (1950, p. 8, fig. 4) correlated the Black Creek in North Carolina with both the Rocks of Austin age can be separated fairly con­ Austin and the Taylor in the gulf coast, and this sistently from overlying rocks of Taylor age in deep usage is followed in this report. wells from central Florida northward to southern In the Florida Peninsula, Citharina texana Cushman New Jersey (pi. 9). They range in thickness from and other time-restricted Foraminifera, Globorotalites 225 to 457 feet between central Florida and the Cape umbilicatus (Loetterle), Darbyella brownstmanensis Fear arch and from 550 to 638 feet between the Cape Cushman and Deaderick, and Planulina wwtinana Fear arch and southern New Jersey. The lithology of Cushman, are rare, and certain distinctive and widely the unit changes northward from light-colored lime­ distributed lithologic features are generally used for stone beds that cannot be delimited in the predom­ recognition of the beds of Austin age. inantly carbonate sequence of Upper Cretaceous rocks Kyphopyxa christneri Carsey is frequently reported in southern Florida to dark-gray shale, siltstone, and from beds of Austin age, but this species is present sandstone in southern New Jersey. Chalk, marly lime­ also in the lower part of the beds of Taylor age. stone, and limy sandstone characterize the unit at intermediate points in Georgia and the Carolinas. In ROCKS OF TAYLOR AGE well NC-14 at Cape Hatteras, the entire 628-foot sequence is composed of fine- to coarse-grained sand­ LITHOLOGY AND DISTRIBUTION stone with some beds of conglomerate. This represents Rocks of Taylor age can be identified in drop wells the lower part of the Black Creek Formation (pis. 9 along the coast from central Florida to southern New and 12), a South Carolina and North Carolina unit Jersey; only on the Cape Fear arch do inadequate well that encompasses sandstone and shale beds of Austin records make upper and lower boundaries uncertain and Taylor age. (pi. 9). Along section A-B (pi. 9), they are thickest In New Jersey and Maryland (pis. 10 and 11), in well FL-57 (Sun Oil Powell Land 1) ir central rocks of Austin age, mainly dark-gray shale and sand­ Florida, where 860 feet of light-colored limestone beds stone in deep wells, are equivalent to the Magothy have been assigned a Taylor age. Applin anc1 Applin Formation, which is predominantly sandstone in shal­ (1944, p. 1715) reported a thickness of more than 1,200 low wells near the outcrop. They cannot be separated feet in southernmost Florida (Peninsular Oil and easily from the overlying Matawan Group of Taylor Refining Gory 1, Monroe County), but the unit could age in deep wells of northern New Jersey and Long not be identified readily in the wells used for the Island. cross sections in this report. Thicknesses range from No submarine outcrops of Austin age have been 368 to 482 feet between central Florida and the Cape reported. The few test holes drilled into the continental Fear arch. North of the Cape Fear arch, tH thick- STRATIGRAPHY 45 ness decreases from 585 feet in North Carolina (well They have not been separated from the underlying NC-49) to 176 feet in Maryland (well MD-14). The rocks of Taylor age in well NC-58 on th?< Cape Fear composition also changes from limestone in southern arch, but this is partly because of the inadequate well Florida to marly limestone and limy shale in central records in that area. They range in thickness from a Florida to sandstone and shale in northem Florida maximum of 798 feet in well FL-73 (Humble Oil and and Georgia. Northward in the deep wells, it is pre­ Refining Carroli 1) in central Florida tc a minimum dominantly gray marl, limy shale, and siltstone. In of 70 feet in well NJ-25 (Anchor Gas Dickinson 1) North Carolina, it is represented by the upper part at Cape May, N.J. of the Black Creek Formation (pi. 12) and in south­ In northeast and central Florida, rocks of Navarro ern New Jersey by the Matawan Group (pis. 10 and age are represented by a carbonate facie;^ 410 to 798 11). The limits of this group are not apparent in feet thick along section A-B (pi. 9) andrdl85 to 900 deep wells in northern New Jersey and Long Island feet thick along section M-N (pi. 15). Applin and (pi. 10), although rocks of Taylor age are most Applin (1944, p. 1708) called this facies the Lawson likely present. Limestone, and they divided it into upper and lower Rocks of Taylor age crop out someplace between members. The lower limit of the Lawson Limestone is depths of 758 and 1,955 feet in a submarine canyon not distinct in wells in southern Florida, where the in Georges Bank (Stetson, 1949, p. 33). Material entire Upper Cretaceous sequence is composed of dredged from the wall consisted of poorly sorted, sparsely fossiliferous, lithologically similar carbonates. glauconitic and feldspathic, in part silty, coarse­ Northward from Florida, the rocks of Navarro age grained sandstone, assigned to the Matawan Group grade into chalk, marl, and fine-grained elastics con­ (Bassler, 1936, p. 411; Stephenson, 1936, p. 369-370, taining large amounts of glauconite. The Peedee For­ and in Stetson, 1949, p. 8). mation in North Carolina is 114 to 212 feet thick along section A-B (pi. 9) and consists primarily of marl, CHARACTERISTIC MICROFAUNA calcareous and siliceous shale, and fine-grained sand­ Planulina dumblei (Applin) is the diagnostic species stone. The Monmouth Group, 70 to 170 feet thick in for beds of Taylor age in the Atlantic Coastal Plain wells along section A-B in Maryland, Nev Jersey, and from Georgia northward to Long Island, and it gen­ New York, are Navarro in age. The beds rre primarily erally occurs near the top of the unit. The highest dark-colored silty and sandy clay, and at the extremity occurrence of the beds of Taylor age in the Florida of section A-B in Long Island, they consist of greenish Peninsula, however, is generally indicated by many glauconitic clay and sandy clay (Perlmutter and specimens of Stensioina americana Cushman and Dor- Todd, 1965, p. 17). sey and Bolivinoides decorata (Jones). S. americana Submarine outcrops of Navarro age are present in and B. decorata are present in the upper part of the two canyons cut in Georges Bank (fig. 2). Samples beds of Taylor age throughout the report area except were dredged by Stetson (1949, p. 33) from depths of at the southern end of the peninsula. In southern 3,116 feet along the east side of Oceanographer Can­ Florida, rocks of Taylor age are present in a thick yon and from 1,968 to 1,738 feet and 2,486 feet along sequence of very sparsely fossiliferous chalk, but they the east side of Gilbert Canyon. The material dredged are not differentiated in this report. Planulina dum­ from Oceanographer Canyon consisted of a dark- blei has not been reported from the Florida Peninsula, colored, partly indurated, micaceous silty clay that but another species of the Anomalinidae, Anoma7ina contained a late Maestrichtian or Navarro fauna that sholtzensis Cole, is fairly common in the peninsula but J. A. Cushman (in Stetson, 1949, p. 10) correlated rape in the part of the Atlantic Coastal Plain north with the Kemp Clay of northeast Texps. Rocks of of Florida. Tritaxia oapitosa (Cushman) is usually Navarro age from Gilbert Canyon consisted of a found in the lower part of the beds of Taylor age in friable, coarse greensand and limonite-stained, mica­ the northern part of the Florida Peninsula and farther ceous, fine-grained sandstone containing Foraminifera to the northeast. characteristic of beds of Navarro age (Mrestrichtian), according to Cushman (1936, p. 413, and in Stetson, ROCKS OF NAVARRO AGE 1949, p. 10). LITHOLOGY AND DISTRIBUTION CHARACTERISTIC MICROFAUNA Rocks of Navarro age, which mark the top of the Published reports on planktonic specier of Forami­ Cretaceous System, can be traced in deep wells from nifera show that occurrences of the g^.nus Globo- central Florida northward to Long Island (pi. 9). truncana are restricted to beds of Cretaceous 46 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Consequently, the highest indigenous occurrence of at Cape Hatteras (well NC-14) to 130 feet on Long the genus in a set of well samples is prima facie evi­ Island (well NY-6). Beneath the continental shelf, dence of the Cretaceous age of the containing beds. Cenozoic thicknesses in excess of 5,000 feet may be Globotruncana area Cushman and Globotruncana cre- present in the Southeast Georgia embayment and tacea Cushman are the species generally found in the the Baltimore Canyon trough judging by the rate samples from the wells that are shown on the cross of thickening onshore and scattered seismic profiles sections in this report. Because these species range (pi. 6). downward into beds older than Navarro and are not SUBDIVISIONS always present at the top of the unit, other species, In this report, Cenozoic rocks have been subdivided such as Anomalina psevdopapillosa Carsey, Cibicides into the Paleocene, Eocene, Oligocene, and Miocene harperi (Sandidge), and Lenticulina navarroensis Series of Tertiary age, and undifferentiated pos£- (Cushman), reported only from the Navarro, have Miocene rocks of Tertiary and Quaternary age. In been used to delimit the rocks of Navarro age. some wells, mostly in Florida and Georgia, the Eocene The Lawson Limestone of Navarro age in the Flor­ Series is further subdivided into rocks of Wilcox, ida peninsula differs in lithologic character and in Claiborne, and Jackson age. The Miocene Series is microfaunal population from the clastic beds of partially subdivided in wells in North Carolina, Mary­ equivalent age in the Coastal Plain of the Middle land, and New Jersey. Atlantic States. The fauna of the lower member of the Lawson Limestone is characterized by several spe­ TERTIARY ROCKS cies of Lepidorbitoides found also in the Maestrichtian The Tertiary rocks are predominantly carbonates of Europe, the Madruga Chalk of Cuba, and the in Florida but grade northward into heterogeneous Cardenas beds of Mexico. Sulcoperculina cosdeni Ap- sequences of limestone, marl, limy shale, sandstone, plin and Jordan is another definitive species. Globo- tnmcana cretacea and Anomalina, cosdeni Applin and and clay. Thick beds of limestone and sandstone char­ Jordan characterize the lower member in some wells. acterize the sequence in well NC-14 at Cape Hatteras, The upper member of the Lawson Limestone is highly which is farther down the regional dip than other altered chemically; hence diagnostic fossils are rare. wells north of Florida. The faunal assemblage? in the Rudistid fragments are commonly found near the top carbonate rocks of Tertiary age in the Florida Penin­ of the member and are fairly prevalent at irregularly sula are most closely related to faunal groups of spaced lower levels. Specimens of a small, undescribed equivalent age in Cuba, Panama, and other parts of Rotalid are also fairly common in the upper member the Caribbean and Central American region. The of the Lawson. faunal groups of the northern part of the report area The reported stratigraphic ranges of most of the resemble most closely those of west Florida and the Cretaceous species of smaller Foraminifera mentioned central and western gulf coast. A few of the distinctive in this report are given by Cushman (1946). Florida species also are reported from Tertiary beds in the subsurface in Georgia. CENOZOIC ROCKS Shore cores and dredgings of Tertiary sand1 , chalk, DISTRIBUTION AND THICKNESS marl, and Globigerina ooze have been recovered at Outcrops of Cenozoic rocks parallel the Fall Line three dozen localities between Georges Bank and the from Georgia to New Jersey except in South and Hudson Canyon, and in the Blake Plateau-Bahama . North Carolina, where the outcrops swing seaward Banks region (pi. 2 and fig. 2). Silt and sand of around the flanks of the Cape Fear arch. Cenozoic probable Tertiary age have been reported in a sub­ deposits are thickest in the southern Florida-Bahamas marine canyon off Nova Scotia (Marlowe, 19C^). region (pi. 17Z>). Thicknesses in excess of 4,000 feet Offshore, Tertiary rocks have been penetrated by are present in wells in the southern half of the Florida eight test holes that range in depth from 171 to 1,050 peninsula, and a thickness of 8,220 feet is present in feet. Two were drilled by the U.S. Coast G^ard at well BA-2 (Bahamas Oil Andros Island 1) in the one location (GA-88, fig. 7) about 10 miles offshore Bahamas (pi. 16). Along the coast (pi. 9), the thick­ from Savannah, Ga. (McCollum and Herrick, 1964). ness of Cenozoic rocks ranges from 4,307 feet in Six were drilled under the JOIDES (Joint Ocean- southern Florida (well FL-86) to 254 feet on the ographic Institutions Peep Earth Sampling) program Cape Fear arch (well NC-58), and, from 3,020 feet at locations (FL-117 to FL-122, fig. 7) ranging from STRATIGRAPHY 47

77° W

32° N.

3.0° N.

29° N.

EXPLANATION O 119(2) OLDEST ROCKS RECOVERED Well or test-hole location and number in table 1 Miocene and Pliocene (Joides site number in parentheses) undifferentiated

Bottom core location Miocene o: Italic letter indicates core projected in

Oligocene O Submarine spring probably issuing e from Eocene Ocala Limestone Eocene beneath Miocene rocks

Paleocene Sparker line « LJ O Neocomian(?) to Cenomanian o: LJ rocks uu Line of section

Black shale and diabase < N 10 0 10 20 30 MILES Q. I I i I I FIGUBE 7. Location of JOIDES test holes, section, and sparker line off southeastern Georgia and northeastern Florida. See figure 8. 48 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF 27 to 221 miles offshore from Jacksonville and Cape thinned on the Blake Plateau. They appear to be Kennedy, Fla. (Bunce and others, 1965). especially thin or even absent along the lower slope, The U.S. Coast Guard test holes were drilled in which corresponds approximately with the axis of 1962 on the Shelf in 54 feet of water at lat 31°56'53.5" maximum velocity of the Gulf Stream. Bottom cores N., long 80°41' 00" W. The oldest formation reached (fig. 7) show that Eocene and Oligocene strata crop was the Ocala Limestone of late Eocene age. Com­ out in the Blake Escarpment and that Miocene and parison of the test holes with water wells on land Neogene deposits blanket the outer plateau and part reveals that rather uniform thicknesses of Oligocene, of the escarpment. Conclusions (Bunce and others, lower Miocene, and middle Miocene strata extend 1965, p. 715) drawn from the test-hole drta and from shore seaward for at least 10 miles. However, sparker profiles are that the continental sh^lf has both the upper Miocene rocks and the Pleistocene and been built seaward rather continuously during '"tertiary Holocene deposits decrease in thickness seaward, the time and that the edge of the shelf has be<>n pro- most significant decrease being in the upper Miocene graded since Eocene time about 9.3 miles by a mass rocks, which range from about 145 feet inland to of sediments, 300 to 600 feet thick. Rates of deposi­ only 10 feet offshore. No facies changes were reported tion have been estimated for the upper Eocene in the upper part of the Ocala Limestone or in the sequence as 1.6 cm (centimeters) per thousard years Miocene rocks, but it was noted that the Oligocene on the continental shelf and 0.3 cm per thousand rocks grade seaward from a sandy limestone at the years on the Blake Plateau. coast into a limy sandstone facies offshore. The JOIDES test holes (wells FL-118 to FL-123, PALEOCENE ROCKS figs. 7 and 8) were drilled in water 90 to 3,888 feet LITHOLOGY AND DISTRIBUTION deep on the continental shelf, Florida-Hatteras slope, and the Blake Plateau (Bunce and others, 1965; Paleocene rocks equivalent to the Midway G~oup of Schlee and Gerard, 1965; Charm, 1965). In addition, the gulf coast are present along the lines of all cross sparker profiles were made normal to the coast. Two sections of this report, but they are absent or indistin­ test holes reached Paleocene rocks, three penetrated guishable from Eocene rocks in some wells near the middle Eocene rocks, and one stopped in upper Eocene Fall Line and on the Cape Fear arch. Tr °-y are rocks. apparently overlapped by younger Tertiar^ rocks Figure 8 is a cross section made by projecting the toward the Fall Line in northern Georgia (pi. 13). JOIDES stratigraphic data from the test holes to A maximum thickness of 2,270 feet has been tenta­ a 253-mile-long line normal to the seacoast at lat tively assigned to rocks of Midway age in well BA-2 30°30' N. (section X-Y, fig. 7). This line is tied to on Andros Island (pi. 16). two onshore wells, the St. Mary's Kiver Hilliard Tur­ Along section A-B (pi. 9), the Paleocer^ rocks pentine 1 (FL-51) that reached Paleozoic rocks and a range in thickness from 1,210 feet in well FL-104 in Fernandino Beach water well (FL-117) that stopped southern Florida to 0 feet on the flanks of Cape Fear in middle Eocene rocks. The structure and topogra­ arch. They are relatively thin and less readily identi­ phy are vertically exaggerated (1:251) to bring out fied north of the Cape Fear arch. The Paleocene rocks the stratigraphy. The syncline along the coast and in Florida are represented by the Cedar Keys Lime­ the anticline beneath the continental shelf are gentle stone, a light-colored limestone containing Borelis. warps with the steepest dips, found in the Eocene The equivalent formation in Georgia anc1 South rocks, not exceeding 15 feet per mile. These gentle Carolina is the Clayton Formation, which is com­ structures resemble the parallel warps along the coast posed mainly of marl, sandy limestone, and limy at Savannah, Ga., as reported by McCollum and sandstone beds. This correlates with the P^aufort Counts (1964, pi. 1) and McCollum and Herrick Formation in North Carolina, a sequence of gray (1964, p. C63). glauconitic shale interbedded with thin limestone and The test holes on this section and a bottom core chert beds. Farther north, identification of Paleocene (fig. 7) from the Blake Escarpment indicate that rocks is more difficult. The sequence tertatively Paleocene beds probably continue from the Coastal assigned to this age in well NJ-26 at Island Beach, Plain to the edge of the Blake Plateau and may be N.J., is composed mostly of dark-greenish-g-ay fos- exposed as sea bottom along the lower part of the siliferous limy clay and gray glauconitic siltstone. The Florida-Hatteras slope. The Eocene, Oligocene, and underlying Monmouth Formation of Navarro age has Miocene beds appear to be prograded seaward beneath a similar appearance and the two units can be sepa­ the outer Continental Shelf and slope, and are greatly rated only by means of fossils. _____ 253 MILES __ 119(2) 120(5) 121(6) 122(4) BLAKE BLAKE PLATEAU FLORIDA-HATTERAS SLOPEJ* ESCARPMENT r-0'

- 1000'

.AXIS OF MAXIMUM VELOCITY OF GULF STREAM

- 2000'

a j Well or test-hole number in table 1 118(1; I (Joides site number in parentheses) _ 3000' O W 10 10 20 30 MILES Paleoce I I I

EXAGGERATION 1:251

- 4000'

Lower Cretaceous rocks - 5000'

c Woodbine core 5724' L- 6000'

FIGURE 8. JOIDES section across continental shelf and Blake Plateau off Jacksonville, Ma. Core locations projected along Blake Escarpment for diagrammatic purposes. (See flg. 7.)

CD 50 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Submarine outcrops of Paleocene rocks have not 500 feet in New Jersey. The Eocene rocks are mostly been reported, but considerable thicknesses have been limestone in Florida. In central and northern Florida, drilled or cored by wells on the Blake Plateau and they are subdivided in ascending order into the Olds- Bahama Islands. A Paleocene sequence consisting of mar Limestone of Wilcox (early Eocene) age, the 263 feet of hard, cherty, very fine grained limestone Lake City and Avon Park Limestones of Clriborne interbedded with gray limy clay was penetrated in (middle Eocene) age, and the Ocala Limestone of JOIDES test hole 4 (FL-122), 221 miles east of Jackson (late Eocene) age. In Georgia and South the Georgia coast (figs. 7, 8) Dolomitic limestone and Carolina, the Eocene rocks consist of limestone, marl, limestone beds tentatively assigned to the Paleocene and sandstone beds readily subdivided into rocks of were penetrated at depths of 5,950 to 8,220 feet in Wilcox, Claiborne (Lisbon and Talahatta Forma­ well BA-2 on Andros Island of the Bahamas (pi. 16). tions), and Jackson age. Farther northVard, the Judging by the close proximity of the Northeast Eocene Series exhibits a gradual change from sandy Providence Channel and Tongue of the Ocean (5 to limestone and sandstone beds in North Carolina into 10 miles), which descend to depths of about 10,000 a sequence of shale and sandstone in Maryland and feet, similar thicknesses of Paleocene strata may crop New Jersey. Limestones of middle and late Eocene age out or be thinly mantled along these canyon walls. can be separated from lower Eocene rocks in North Carolina wells, but in Maryland and New Jersey wells CHARACTERISTIC MICRO-FAUNA (pi. 9) the Eocene rocks are neither readily subdivided The foraminiferal species Borelis gunteri Cole and nor easily distinguished from the overlying Miocene Borelis floridanus Cole are key species of the Cedar rocks. Keys Limestone (Cole, 1944, p. 28) in the Florida Rocks of Eocene age probably are not far Hneath Peninsula. These species, and additional ones that the sea bottom where artesian submarine springs issue have been described (Applin and Jordan, 1945), were off the Florida coast. An oceanic spring about 2i/^ present in many Florida wells used on cross sections miles east of Crescent Beach near St. Augustine (pi. 2) herein (table 3). has been described by Rude (1925); others ha^e been The most common species of Paleocene age in reported along the east coast between lat 28° N. and Georgia, South Carolina, Maryland, and New Jer­ 30° N. (V. T. Stringfield, written commun., 1964). sey are Lenticulina pseud omamiUigera (Plummer), Stringfield and Cooper (1951, p. 63) believe that Vaginulina lon,giforma (Plummer) Anomcdina mid­ these submarine springs discharge through sink holes way ensis (Plummer), and Lenticulma midway ensis formed during Pleistocene time when the sea stood (Plummer). The last species has also been reported at lower levels. They conclude that the aquifer is the from the Salt Mountain Limestone and from the Ocala Limestone of late Eocene age and the confining Nanafalia Formation of Paleocene and early Eocene beds are the Hawthorn Formation of Miocene r.ge and age, respectively, in Alabama (Toulmin, 1941, p. 579; younger deposits. Cooke, 1959). The wide distribution of rocks of Eocene age be­ EOCENE ROCKS neath the continental shelf and Blake Plateau has been LITHOLOGY AND DISTRIBUTION established by bottom cores along the continental slope, by test holes drilled offshore from Georgia and Flor­ Eocene rocks crop out in a continuous band on the Coastal Plain from Alabama to the Cape Fear arch. ida, and by a deep well on Andros Island. They are absent from the crest of the arch and are Five short cores of Eocene marl and chalk were somewhat intermittently exposed through a cover of obtained from the continental slope between Georges younger rocks northward to Long Island. Eocene Bank and the Bahama Islands. (See pi. 2.) Tv^o were rocks are present in most of the wells on the cross taken near the middle of the continental slopft about sections. They are thickest in wells off southern Flor­ 90 miles southeast of Martha's Vineyard. One by Stet­ ida (pi. 16), where they range from 2,000 to 4,000 feet son (1949, p. 33) from a depth of 2,886 feet at lat in thickness, and are thinnest in Maryland (pi. 11), 39°50' N., long 70°48' W. consisted of chalk and con­ where they are 100 to 350 feet thick. tained Foraminifera of Jackson age. The second one, Along section A-B (pi. 9), the Eocene rocks range from a depth of 3,280 feet at lat 39° 50' N., long in thickness from 2,328 feet in well FL-86 to 176 70° 50' W. (Northrop and Heezen, 1951, p. 397-398), feet in well NC-58 on the Cape Fear arch and from consisted of Globigerina ooze and contained Forami­ 1,132 feet in well NC-14 at Cape Hatteras to less than nifera most nearly resembling fauna of Jackson age. STRATIGRAPHY 51 Two cores of Eocene marl have been taken near the middle and lower Eocene rocks, composed mainly of base of the continental slope in the vicinity of the limy sand, fine-grained limestone, cheH, and clay. Hudson Canyon. Stetson (19-19, p. 33) reported that About 75 miles north on the outer Blake Plateau, test a core from a small gully southwest of Hudson Can­ hole 4 (FL-122) penetrated 55 feet of lower Eocene yon (lat 38°58' N., long 72°28.5' W.) at a depth of ooze and chert. The lithology and thickness of lower, 5,133 feet contained a late Eocene fauna, rich in middle, and upper Eocene units in the JOIDES test Radiolaria. Ericson, Ewing, and Heezen (1952, p. 502) holes suggest that Eocene rocks became less porous recorded another core of Eocene marl from the base of and thin seaward both internally and by loss of beds the slope near Hudson Canyon (lat 39° 12' N., long at the top. 71°48' W.) at a depth of 7,108 feet, The Bahamas Oil Andros Island 1 (well BA-2) in A single core of foraminiferal chalk has been re­ the Bahama Islands penetrated 4,000 feet of limestone, covered from the escarpment of the Blake Plateau dolomitic limestone, and dolomite bee's tentatively (lat 29°49' N., long 76°35' W.) at a depth of 4,772 assigned to the Eocene. These beds of reef like car­ feet, by Ericson, Ewing, Wollin, and Heezen (1961, bonates are present at depths of 1,950 to 5,950 feet p. 236). They state that the age of the deposit, based and are very likely exposed or are thinly mantled in on H. M. Bolli's examination of the planktonic Foram- the nearby canyon wall of Northeast Providence Chan­ inifera, is late Eocene. nel and the Tongue of the Ocean, both of which The U.S. Coast Guard test hole (well GA-88) off reach depths of 10,000 feet. Georgia penetrated only 5 feet of upper Eocene rocks, the Ocala Limestone (McCollum and Herrick, 1964, CHARACTERISTIC MICROFAUNA p. C61-C62). In onshore wells in Chatham County, Several of the species of Foraminifera that char­ Ga., the Ocala is about 400 feet thick and consists of acterize lower Eocene rocks (Oldsmar Limestone) in gray to buff fossiliferous limestone. It is the principal northern and central Florida are Pseud ophragmina aquifer throughout much of eastern Georgia. No facies cedarkeysensis Cole, Coskinolina elongata Cole, Mis­ change was noted in the Ocala between the coastal cellanea iiassauemis Applin and Jordan, and Helicoste- wells and the offshore test hole. gina gyralis Barker and Grimsdale. The last species The JOIDES test holes (FL-118 through FL-123, is known to occur in the basal part of the middle figs. 7 and 8) off Jacksonville, Fla., penetrated 48 Eocene (Cole and Applin, 1964, p. 14), as well as in to 550 feet of Eocene rocks. Only two test holes, the lower Eocene. Foraminiferal species of early 6 and 4 (FL-121 and FL-122), were drilled com­ Eocene age recovered from samples from wells drilled pletely through the Eocene sequence. Test hole 6 in the Middle Atlantic States (table 3) are Eponides (FL-121), about 136 miles offshore near the middle dorfi Toulmin, Spiroplectammina wilcoxemis Gush- of the Blake Plateau, penetrated 63 feet of lower man and Ponton, Alabamina wilcoxensis Toulmin, and Eocene beds, 35 feet of middle Eocene beds, and 95 Pseudophtwgmina stevemoni (Vaughan). feet of upper Eocene beds. Test hole 4 (FL-122), The middle Eocene rocks in the repor4 area contain about 221 miles offshore near the edge of the Blake many foraminiferal species that are stratigraphically Plateau, found only 53 feet of Eocene beds, all of restricted to the unit but differ in their geographic which were assigned an early Eocene age. distribution. Species that have been reported from Thicknesses in excess of 550 feet were penetrated in wells in both Florida and Georgia are: Astero- test holes 1 and 2 (FL-118 and FL-119), about 27 cyclina monticellensw Cole and Ponton, Discorbis inor- and 64 miles, respectively, offshore on the continental natus Cole, Gyroidina nassauensi-s Cole, Discorinopsis shelf. These thicknesses included otnly beds of late gunteri Cole, Amphi-stegvtia lopeztrigoi D. K. Palmer, and middle Eocene age that were mainly porous Asterigerina texana (Stadnichenko), Cibicides westi medium- to coarse-grained clastic limestones and dolo- Howe, and Lepidocyclina antillea Cushman. The well- mitic limestones. Lower Eocene beds are present in known definitive species Eponides mexwamis Cush­ onshore wells and in test holes 6, 3, and 4 (FL-121, man is widespread; it is present in middle Eocene FL-122, and FL-123) farther out on the Blake Pla­ beds at the depth of 2,572 feet in the Gulf Oil State teau, which suggests that the two test holes on the of Florida Lease 826-G 1 in Florida Bay, Monroe continental shelf would have reached lower Eocene County, Fla., and in middle Eocene beds at the depth rocks if drilling had continued. Test hole 3, (FL-123) of 2,610 feet in the Anchor Gas Dickinson 1 at Cape a*bout 181 miles offshore on the outer Blake Plateau May, N.J. A few species that have been reported opposite Cape Kennedy, Fla., penetrated 85 feet of only from Florida are: Dictyoconus americanus (Cush- 52 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF man), Fdbularia vaughani Cole and Ponton, Lock- Escarpment (lat 29° 12.5' N., long 76°49' W.) at a hartia cushmani Applin and Jordan, Lepidocyclina depth of 7,019 feet. H, M. Bolli (in Ericscn and cedarkeysensis Cole, Dictyoconus floridanus (Cole), others, 1961, p. 236) likened the assemblage of Foram­ Lituonella floridana Cole, Spirolina coryensis Cole, inifera to that of the Globigerina ciperoensis Zone and Flintina avon.parkensis Applin and Jordan. The within the Cipero Formation of Trinidad (middle or recurrence of Dictyoconus floridanus in the middle late Oligocene). Eocene rocks in the Florida Peninsula has been men­ The U.S. Coast Guard test holes (well GA-88) off tioned in the discussion of rocks of late Trinity age. Georgia were drilled through about 76 feet of limy Definitive species reported from upper Eocene rocks sand of Oligocene age between depths of 90 and 166 in Florida and Georgia and found in wells on the cross feet below sea bottom. Oligocene rocks appear to sections of this report are: Lepidocyclina ocalana grade from fossil iferous limestone in inland wells to Cushman, Heterostegina ooalana Cushman, Nummu- sandy limestone in coastal wells and then into limy lites floridensis (Heilprin), Nummulites mariannensis sandstone offshore. This facies change may be related (Vaughan), Nummulites moodysbranchensis (Gravell to the development of the upwarp along shore mapped and Hanna), Amphistegina cosdeni Applin and Jor­ on a Miocene limestone by McCollum and Counts dan, Sphaerogypsina globula (Reuss), Asterocyclina (1964, pi. 1) nassauemsis Cole, and Eponides jacksonensis Cushman Considerable thicknesses of Oligocene rocks were and Applin. BuHmina jacksonensis Cushman and drilled in the six JOIDES test holes off Jacksonville, Uvigerina cocoaensis Cushman are not only found in Fla. (figs. 7, 8). The sequences recorded range from wells of Florida but are also found in the Anchor 30 feet of calcareous clay in test hole 1 (FL-118) on Gas Dickinson 1 (well NJ-25) at Cape May, N.J. the continental shelf to 532 feet of calcareous silt and Additional upper Eocene species in the Anchor Gas limestone in test hole 5 (FL-120) on the slope. Only well are: Marginulina cooperensis Cushman at 1,420 94 feet of foraminiferal sand was found in te?t hole feet, Eponides cocoaensis Cushman at 1,520 feet, and 4 (FL-122) on the outer Blake Plateau. Lenticulina virginiana (Cushman and Cederstrom) at 1,520 feet. Cushman (1948, p. 228, 234, 240) reported CHARACTERISTIC MICROFAUNA the occurrence of M. cooperensis, E. cocoaensis, and B. The Oligocene rocks in Florida and Georgia contain jacksanensis in the Ohio Oil L. G. Hammond 1 well, closely similar faunal populations. Among the larger Wicomico County, Md. Upper Eocene Foraminifera Foraminifera, Heterostegina antillea Cushman, and have been reported from several other wells in Mary­ Miogypsina gunteri Cole are probably the most impor­ land (Anderson, 1948, p. 85-86, 94; Shifflet, 1948, tant faunal elements in southern Florida, and Lepido­ p. 25-26). cyclina (Eulepidina) undosa Cushman and M. gunteri OLIGOGENE ROCKS have also been reported from wells in the Georgia LITHOLOGY AND DISTRIBUTION Coastal Plain. Of the smaller foraminiferal species, Pararotalia mecatepecensls (Nuttall) and Parc.rotalia Oligocene rocks are present both at the surface and byi-amensis (Cushman) are probably the most abun­ in the subsurface from Florida northward to the Cape Fear arch. They are not known at the surface north dant and the most widely distributed. Specimens of of the Cape Fear arch but may be present in the Asterigerina siibacuta Cushman and Nonionella leo- interval marked "Rocks of uncertain age, possibly nenxis Applin and Jordan are common. Oligocene in part" in wells NC-7 and NC-14 in North An unusual but characteristic feature of the Oligo­ Carolina (pis. 9 and 12). The Oligocene rocks are cene rocks in Florida and Georgia is the common composed of limestone beds from 35 to 250 feet thick occurrence of specimens of Dictyoconus ftoridanus south of the Cape Fear arch. The rocks of uncertain (Cole) and Disconnopsis gii-nteri Cole. Both are diag­ age, possibly Oligocene in part, in wells NC-14 and nostic fossils of the upper middle Eocene Avon Park NC-7 in North Carolina include sandy limestone, shale, Limestone in the Florida Peninsula. Their recurrence and sandstone beds. Offshore, the Oligocene rocks have in the Oligocene of Florida and Georgia has been been recovered from the Blake Escarpment and pen­ attributed to secondary deposition by Cole (1941, etrated by test holes on the continental shelf and p. 12-16), although Applin and Applin (1944, p. 1682- Blake Plateau (fig. 7). 1683), among others, suggest that these fossils may Oligocene chalk has been cored by Ericson, Ewing, be indigenous. Because they are generally accorrpanied Wollin, and Heezen (1961, p. 236) on the Blake by many specimens of Pararotalia mecatepecensis and STRATIGRAPHY 53 other typical Oligocene species, the age of the contain­ Lower Miocene rocks are separated from middle ing beds is readily determinable. and upper Miocene rocks in wells NC-14 and NC-7 Cole and Applin (1961, p. 130-131) discussed the in North Carolina on section A-B (pi. 9), but they stratigraphic distribution of some larger Foraminifera are not identified in well MD-14 in I Taryland and in Florida; they showed that certain species of Mio- well NJ-25 in New Jersey. Lower, middle, and upper gypsina are confined to the upper Oligocene, certain Miocene rocks are separated on section G-H (pi. 12) other species are confined to the lower Miocene, in North Carolina. Local formation names Calvert, possibly the basal Tampa Limestone, and some species Choptank, St. Marys, and Yorktown are applied to are common in both the upper Oligocene and lower the shallow subsurface Miocene rocks in Maryland Miocene. Consequently, the occurrence of the genus on section E-F (pi. 11). Miogypsma alone is not indicative of either strati- The sea bottom off the Atlantic coast lias yielded graphic unit. cores and samples of Miocene deposits at many places. Common species of smaller Foraminifera present Miocene strata beneath the continental shelf, Blake from 920 to 1,080 feet in the Anchor Gas well at Plateau, and Bahama Islands have been penetrated Cape May, N.J., are: Cibicides floridanus (Cushman), and sampled by the test holes off Georgia and Florida Nonion mediocostatwn (Cushman), Nonion pizarrense and by wells drilled on the Bahama Islands (BA-2 W. Berry, Spiroplectammina mississippiensis (Cush­ and BA-3). man), Textularia inayorl Cushman, and Uvigerina Miocene rocks have been recovered in 19 tows and subperegn-na Cushman and Kleinpell. cores along the Atlantic coast. These hr.ve come from submarine canyons off Georges Bank, from shoals on MIOCENE ROCKS the Cape Fear arch, and from the top and edge of LITHOLOGY AND DISTRIBUTION the Blake Plateau. Only a few large patches of Miocene deposits are Highly indurated, greenish, fine-grained sandstone exposed on the surface of the Coastal Plain south of of middle to late Miocene age was found in place the Cape Fear arch. These include areas of several along the east wall of Lydonia Canyon (lat 40°23' N., thousand square miles in South Carolina and along long 67°38.5' W.) at a depth of 928 fait. This loca­ the Gulf of Mexico side of Florida. North of the tion is well up the continental slope, just beneath Cape Fear arch, broad flat-lying Miocene deposits the edge of the continental shelf. Similar sandstone blanket the Coastal Plain from North Carolina across has been dredged up as talus in two places along the the Salisbury embayment to the northeastern tip of east side of Hvdrographer Canyon (lat 40°09' N., New Jersey. At Cape Fear, Miocene marl beds form long 69°03'20" W.; depth, 1,319 to 1,53° feet) and in the nearshore shoals termed "Black Rocks" (Pearse one place in Corsair Canyon (lat 40°21'20" N., long and Williams, 1951). 66°08'20" W.; depth, 1,617 to 1,787 feet) (Stetson, Subsurface Miocene rocks along the line of section 1949, p. 11, 33). A-B (pi. 9) are about 800 feet thick in the Florida Stetson and Pratt (Elazar Uchupi, written com- Keys (well FL-104), less than 60 feet thick at the mun., 1963) dredged 10 samples of semiconsolidated Peninsular arch (well FL-57), and about 350 feet and consolidated Ghbigerina and pteropod ooze from thick in the Southeast Georgia embayment (well the top of the Blake Plateau, three samples of which GA-87). They wedge out in South Carolina on the contained fossils. Ruth Todd identified Foraminifera flank of the Cape Fear arch. The lithology changes assemblages that are either fossil (Miocene) or a mix­ gradually from chalky coquinoidal limestone in south­ ture of Miocene and Holocene forms. r^hey are from ern Florida to dark sandy limestone and claystone in lat 31°58' N., long 77°18.5' W., at a depth of 2,427 South Carolina. North of the Cape Fear arch, the feet; lat 31°48' N., long 77°35' W., at a depth of Miocene rocks reach a thickness in excess of 1,300 feet 2,096 feet; and lat 30°58' N., long 7e°31' W., at a at Cape Hatteras (well NC-14) and about 1,400 depth of 2,657 feet. feet in the center of the Salisbury embayment (well Three cores of Miocene rocks have come from the MD-14). Miocene rocks are not delimited in the edge of the Blake Plateau. One from lat 28°35.5' N., Tertiary sequence in well NJ-26 in northeastern New long 77° 10' W., at a depth of 3,296 feet, consisted of Jersey and are not present in well NY-6 on Long clayey sand, and it contained a fauna ranging in age Island. The lithology grades northward from sandy from late Miocene at the bottom to Holocene at the limestone and sandstone in North Carolina to clay, top, through a thickness of only 14.5 feet (Ericson sand, and gravel in New Jersey. and others, 1961, p. ?H5). Because the core bore no 54 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF evidence of slumping, it is assumed that sedimenta­ Middle Miocene deposits are missing at test hole 2 tion from late Miocene time to Holocene is represented (FL-119) on the outer continental shelf, and the in this short core. Another core, at lat 30°04' N., long unconformity is marked by a phosphate pebble zone. 76°57' W., from a depth of 3,542 feet, consisted of Test hole 5 (FL-120) near the top of the continental 21.7 feet of Miocene chalk and 5.1 feet of Pleistocene slope and test hole 6 (FL-121) near the middle of and Holocene ooze (Ericson and others, 1961, p. 236). the Blake Plateau did not record any Miocene rocks The third core,, from lat 30°23' N., long 76°35' W., but went from post-Miocene deposits directly into a at a depth of 6,117 feet, was made up of 10.7 feet thick Oligocene sequence. A Miocene sequence, 260 of pyritic clay of Miocene age and 1.8 feet of Globl- feet thick and composed mainly of calcareou^ ooze gervna and pteropod ooze of Pleistocene and Holocene and some ash beds, was logged in test hole 3 (FL-123) on the outer Blake Plateau. In test hole 4 (FL-122), A single specimen of Miocene marl (Chipola For­ much farther north on the outer Blake Plateau, only mation) has been reported by Bush (1951) from the beds of early Miocene age were recognized; these con­ sea bottom in the western part of the Straits of sisted chiefly of foraminiferal sand. Florida. It was accidently dredged from a depth of A vuggy to cavernous limestone and dolomite se­ 2,250 feet at lat 24°10' N., long 81°31' W., and it quence, 1,420 feet thick, is present in well B./ -2 on is thought to have come from an outcrop. Andros Island in the Bahamas. A water well (BA-3) Numerous samples recovered by Ericson, Ewing, on the nearby Eleuthera Island is reported to have Wollin, and Heezen (1961, p. 234-241) contained a drilled 250 to 300 feet into similar rocks of Miocene mixed assemblage of Miocene and Pliocene micro- age. In general, the Miocene deposits seem to be at fossils. These rocks were assigned a general Neogene or near the top of the continental shelf, the outer age but are thought most likely to be late Miocene Blake Plateau, and the Blake Escarpment. They are in age. Four of these cores were marcasitic silt from absent from the Florida-Hatteras slope and the inner­ the Hudson Canyon near the base of the continental most Blake Plateau where the JOIDES test holes slope at depths of 10,922 to 12,530 feet, and two were drilled off Jacksonville, Fla. cores were Globigerma ooze from the Blake Escarp­ ment (lat 28°42' N., long 76°46' W., and lat 28°26' N., CHARACTERISTIC MICRO-FAUNA long 76°40' W.) at depths of 4,133 feet and 5,674 The foraminiferal faunas of the Miocene recks of feet. Three cores from the walls of Northeast and the Atlantic and eastern Gulf Coastal Plain have been Northwest Providence Channels in the Bahamas found described by Cushman and Cahill (1933) r Puri (1953), Neogene green marcasitic silt, hydrotroilite, and Glo­ Cushman (1948, p. 214-225), and by Dorsey (1948), bigerma ooze beneath 3.6 to 7.1 feet of Pleistocene among others. Only a few of the most common diag­ and Holocene Globigerina ooze. nostic species of Miocene Foraminifera are shown in A Miocene sequence, 80 feet thick, was drilled in table 3, and most of these faunal data relate to wells the U.S. Coast Guard test hole (GA-88) off Georgia. in the southern part of the Florida Peninsula. How­ McCollum and Herrick (1964, p. C63) subdivided this ever, some data are available on Miocene Foraminifera into lithologic units of early, middle, and late Miocene from a well in Maryland and from the Anchor Gas age. They report the lower Miocene unit to be a fossilif- Dickinson 1 well in New Jersey. erous phosphatic sandy conglomeratic limestone, 12 A few of the species of smaller Foraminifera feet thick. Unconformably overlying this limestone are present in wells in Florida are: Globorotalia menardii beds of pale-green phosphatic sandy clay and clayey sand, 50 feet thick, that are considered to be middle ( d'Orbigny), Buccella maiisfieldi ( Cushman), Lentic- Miocene in age. The upper Miocene unit, 18 feet thick, ulina amencana (Cushman), Hanzawaia concentrica consists of sand, clay, and a layer of sandy dolomitic (Cushman), Elpliidmtn cJiipolense (Cushmar), Pe- limestone. The Miocene sequence thins seaward to the neroplis bradyi Cushman, Amphistegina chipolensis test hole, mainly at the expense of the upper Miocene Cushman and Ponton, Textulartella barretti (Jones beds. and Parker), Archaias floridanus (Conrad), and Miocene rocks were drilled and cored in four of Sorites'*, sp. Cushman and Ponton. the six JOIDES test holes off Jacksonville, Fla. (figs. Several important species of larger Foraminifera 7, 8). Test holes 1 (FL-118) and 2 (FL-119), on the are: Miogypsinn antiUea (Cushman), Miogypsina continental shelf, recorded 238 and 258 feet, respec­ stau-fferi Koch, and Lepidoeyclina (Eulepidina) yur- tively, of phosphatic silt and clay of Miocene age. nagunensis Ciishman. STRATIGRAPHY 55 Cole and Applin (1961, p. 130-131) discussed the deposits in this offshore area in post-Miocene time stratigraphic distribution of some larger Foraminifera appear to have been silty limy sand just seaward from in Florida; they showed that certain species of Mio- the edge of the present-day continental shelf. gypsina are confined to the upper Oligocene, certain Stetson (1936, p. 350; 1949, p. 12) dredged a friable other species are confined to the lower Miocene, pos­ very fine grained greensand of probable Pliocene age sibly the basal Tampa Limestone, and some species are from depths of 2,099 to 1,679 feet up the east wall common in both the upper Oligocene and lower of Lydonia Canyon (lat 40°27'00" N., long 67°39' 30" Miocene. Consequently, the occurrence of the genus W.). Cushman (1936, p. 414) thought the green- M iogypsi-na, alone, is not indicative of either strati- sand to be late Tertiary in age because th^ Foraminif­ graphic unit. era are warm-water forms that have not been present Common species of smaller Foraminifera present in the area since the Pleistocene. from 920 to 1,080 feet in the Anchor Gas Dickin- Samples of hard green silt of either late Pliocene son 1 well at Cape May, N.J., are: Cibicides floridanus or Pleistocene age have been dredged by Stetson (1949, (Cushman), Nonion mediocostatum (Cushman), Non- p. 13) from Oceanographer Canyon (lat 40°24'30" N., ion pi&arrcnse W. Berry, Spiroplectamtnina missis- long 68°07'30" W.) at depths of 2,055 to 1,574 sippiensis (Cushman), Textularia mayori Cushman, feet, from Gilbert Canyon (lat 40°29'45" N., long and Uvigerina subperegrina Cushman and Kleinpell. 67°51'15" W.) at depths of 1,968 to 1,738 feet, tod from Lydonia Canyon (lat 40°27'00" N., long TERTIARY AND QUATERNARY ROCKS 67°39W W.) at depths of 2,099 to 1,673 feet. Some POST-MIOCENE ROCKS Foraminifera in these samples had th°, same late Pliocene* resemblances that were found in the green- Pliocene, Pleistocene, and Holocene deposits along sand referred to the Pliocene, but the rest of the the Atlantic coast are represented by beds of marl, assemblage suggested a distinctly colder sea environ­ clay, sand, and gravel that cannot be readily separated ment. In addition, there was a greater proportion of on an age basis in the scattered wells of these cross living species in the green silt than in tl rt, greensand. sections. These are treated as undifferentiated post- Cushman (1936, p. 414) thought the green silt to Miocene rocks. be younger than the greensand and therefore late The thickest sequence of post-Miocene rocks on these Pliocene or Pleistocene. Ericson, Ewing, Wollin, and cross sections is 530 feet thick and is present on Andros Heezen (1961, p. 234) thought it improbable that Island (well BA-2, pi. 16). Thicknesses in excess of the green silts from canyons on George? Bank were 250 feet are present in wells on the Florida Keys Pleistocene because the lithology and fauna differ (wells FL-109 and FL-111, pi. 16). The rocks are strikingly from sediments of known Pleistocene age predominantly marl in Florida and the Bahamas. found elsewhere in the Atlantic. Along section A-B (pi. 9), the thickness exceeds 200 feet only in the Salisbury embayment (well NC-7 and QUATERNARY BOTTOM DEPOSITS well MD-14). £>and and gravel beds predominate in this area. Bottom deposits along the Atlantic co^st were first- The U.S. Coast Guard test holes (GA-88) off known from ship soundings, storm deposits on the Georgia revealed very thin undifferentiated post- beaches, and sediments accidently dredg°d in fishing Miocene deposits 011 the shelf there. Fossiliferous sand, and anchoring operations. Pebbles and boulders of only 10 feet thick and possibly all Holocene in age, granite, gneiss, and schist found in nets and lobster was logged above the Miocene rocks. The six JOIDES traps gave early evidence of glacial debris on bottom in the fishing grounds. Pourtales (1850, 1854, 1871, test holes off Jacksonville, Fla., (fig. 7) penetrated 1872) and Bailey (1851, 1854) produced much of the thicknesses of post-Miocene deposits ranging from 220 early information about the sea bottom along the feet in test hole 5 (FL-120), 76 miles offshore Atlantic coast. As early as 1879, the U.S. Coast and beneath the Florida-Hatteras slope (fig. 7), to 20 Geodetic Survey (Mitchell, 1879) published bottom feet in test hole 6 (FL-121), 136 miles offshore near studies of the Gulf of Maine pointing out the presence the middle of the Blake Plateau (fig. 8). The litholo- of pebbles and small stones on the top of Georges gies ranged from silty fine- to medium-grained quartz- Bank. Agassiz (1888, p. 260-293) discussed submarine ose partly shelly sand beneath the continental shelf deposits and presented a map (1888, fig. 191) of bot­ to foraminiferal-pteropod limy sand and silty forami- tom sediments in the Gulf of Mexico, Caribbean Sea, niferal ooze beneath the Blake Plateau. The thickest and western Atlantic Ocean. Later publications con- 56 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF cerning bottom sediments along the Atlantic coast are ooze composed largely of tests of planktonic Foram­ numerous and detailed. Uchupi (1963) has summarized inifera and pteropods and reef detritus (Miami those published prior to 1963. More recent ones include University Marine Laboratory, 1958; Nestercff and Moore and Curray (1963), Schlee (1964), Gorsline Rusnak, 1962; Athearn, 1962a,b; Busby, 1962a,b,c). (1963), Pilkey (1964), Uchupi (1964), Stewart and Radiocarbon measurements of samples gave age? rang­ Jordan (1964), Emery, Merrill, and Trumbull (1965), ing from 300±70 years to 29,120±850 years (Ostlund Emery, Wigley, and Rubin (1965), Nota and Loring and others, 1962; Rusnak and others, 1963). More (1964), Merrill, Emery, and Rubin (1965), and Pratt than 50 percent of the sediment column sampled in and McFarlin (1966). the central and cul-de-sac areas of the Tongue of the Numerous samples of Pleistocene and Holocene Ocean gave evidence of turbidity current deposition, materials have been dredged by Stetson (1949, p. whereas samples from the flanks of the platform sug­ 15-21) from Corsair Canyon on the north to Norfolk gested that the sediment particles there settled from Canyon on the south, (See pi. 2 and fig. 2.) F. B. the overlying water. Apparently turbidity currents Phleger, Jr. (in Stetson, 1949, p. 53), reported a sub­ originate on the upper flanks of the platform, flow arctic foraminiferal fauna beneath the Holocene tem­ down gullies at relatively high velocities, and spread perate fauna and assigned a Wisconsin age to the the sediment locally on the lower channel flocr. lower sediments in the cores. Stetson (1949, p. 15) The areal distribution of bottom sediments of Qua­ pointed out that these glacial sediments are mainly ternary age on the continental margin off the Eastern pink and gray clay (color when damp) and that the United States has been compiled on a map and dis­ overlying Holocene sediments are mainly coarser grades cussed in a report by Uchupi (1963). The complete of greenish silt. list of references dating from 1850 through 1962 Ericson, Ewing, Wollin, and Heezen (1961, p. 202- attached to the report can be useful for anyone seeking 228) have presented much later information on the more detailed information. Uchupi (1963, p. C132) lithology, particle-size distribution, and areal distribu­ summarizes the areal distribution as follows: tion of Pleistocene and Holocene sediments in both "Relict glacial sediments blanket most of the conti­ the Atlantic and Caribbean regions. They concluded nental shelf north of Hudson Canyon, and relict fluvial from variations in the planktonic Foraminifera in 108 or nearshore quartzose sands occur throughout most of cores and by extrapolation of rates of sediment accu­ the shelf from Hudson Canyon to Cape Hatteras. Cal­ mulation determined by 37 radiocarbon dates in 10 careous organic and authigenic sediments p.re the cores that the last period of climate comparable with dominant sediment types on the continental margin the present ended about 60,000 years ago and that a farther south. Present-day detrital sediments are re­ faunal change caused by a wanning climate, and stricted to a narrow zone near shore, to the outer edge probably corresponding to the beginning of post­ of the shelf off Long Island, and to the continental glacial time, began about 11,000 years ago. slope of Cape Hatteras. The predominance of relict In addition to the Pleistocene silts and clays found and calcareous sediments indicates that present rate in cores, patches of Pleistocene gravel are present on of deposition of detritus derived from land is very the continental shelf from Cape Hatteras northward low over most of the continental shelf/' to Nova Scotia (Uchupi, 1963, fig. 94.1). Shepard, Trefethen, and Cohee (1934, p. 294) reported that PETROLEUM POTENTIAL pebbles and granules of granite and gneiss pre­ dominate in the gravels on Georges Bank and that quartzite and felsite are common. Wigley (1961, p. 183, Oil and gas have not been discovered in commercial figs. 2, 8) showed the bottom sediments of Georges quantities in the Atlantic Coastal Plain and Conti­ Bank to be mainly well-sorted sands on much of the nental Shelf, but three accumulations have been found bank and less well-sorted gravel in the channels and along the eastern edge of the Gulf Coastal Plain in on the northern and eastern parts of the bank. Schlee the southwestern part of the Florida Peninsulr, These (1964) recently pointed out the possible economic are the Sunniland field in Collier County, the Forty- value of extensive fluvial gravel deposits off New Mile Bend field in Dade County, and the Felda field Jersey that were first noted by Shepard (1932, fig. 1, in Hendry County (pi. 1). p. 1020). Sunniland field, Collier County, Fla., was discovered Holocene sediment on the channel floor in the Tongue in 1943 after intensive exploration with seismograph, of the Ocean (see fig. 2) is poorly sorted unconsolidated gravity meter, and core drilling (Hughes : 1944, PETROLEUM POTENTIAL 57 p. 804). The early history of this field has been de­ Felda field, Hendry County, Fla., about 15 miles scribed by Gimter (1946, 1950), Puri and Banks northwest of the Sunniland field, was discovered in (1959), and Roberts and Vernon (1961, p. 218). The 1964 near the Town of Felda. The discovery well was discovery well, the Humble Oil and Refining Gulf the Sun Oil Red Cattle 2 in sec. 32, T. 45 S., R. 29 E. Coast Realties 1, in sec, 29, T. 48 S., R. 30 E., produced Its initial flow was 111 barrels of 24.5° API. gravity 110 barrels of 20° API. gravity oil and 475 barrels of oil from the interval of 11,471 to 11,485 feet in the salt water a day by pumping from depths of 11,613 to Sunniland Limestone (Gardner, 1964). A second pro­ 11,626 feet in the Sunnlland Limestone of Trinity ducing well was drilled to a total depth of 11,495 (Lower Cretaceous) age. The field was developed by feet about 1*4 miles southeast of the discovery, and a drilling a total of 20 wells between 1943 and 1950. third successful well was drilled about 14 mile south­ Thirteen wells were successful, with initial production east of the first well. The third well, which is the most tests ranging from 97 to 527 barrels of oil a day. productive so far, had an initial pumping potential The reservoir, the Sunniland Limestone, lies "above of 336 barrels of oil and one barrel of salt water. The the thick anhydrite bed in the Trinity, which is equiva­ cumulative production of Felda field reached 42,903 lent to some part of the Glenrose formation of Texas'1 barrels of oil on March 1, 1965 (Kc-nfeld, 1965, (Jordan, 1954, p. 375). Puri and Banks (1959, p. 123) p. 173). state that the trap is formed by a small fold not evi­ Although petroleum has been produced in three dent in the rocks above 5,000 feet. They ascribe 150 countries of southern Florida, little evidence of hydro­ feet of relief to the structure at a depth of 11,500 carbons has been found in the many wells drilled in feet, but they explain that tilting to the northeast by northern Florida. The St. Mary's Rive- Oil Hilliard 50 feet per mile has reduced the fold closure to only Turpentine 1 (well FL-51, table 1) in Nassau County 36 feet. was reported to have asphaltic staining in the Cedar According to Roberts and Vernon (1961, p. 218), Keys Limestone of Paleocene (Tertiary) age, in lime­ two of the producing wells had been abandoned by stones of Taylor (Upper Cretaceous) age, and in the 1960, and the remaining 11 wells pumped an average lower part of the Atkinson or Tuscaloosa Formation of of 96 barrels per day. They state that the cumulative Woodbine (Upper Cretaceous) age (Cole, 1944, p. 97- production for the Sunniland field was 6,089,470 bar­ 100). However, these shows must be regarded as doubt­ rels at the close of 1960 and that the best well had ful in view of the State Geologist's statement (Vernon, produced more than 800,000 barrels and the average 1951, p. 238) that "shows of oil and gas are unknown well, more than 400,000 barrels. On March 1, 1965, throughout the northern Peninsula." Sunniland field was producing 1,800 barrels of oil and Indications of hydrocarbons in two wells in south­ 3,600 barrels of salt water per day by pumping, and western Georgia have been reported tc the Georgia the cumulative production reached 8,475,830 barrels Department of Mines, Mining, and Geology. Oil and of oil (Kornfeld, 1965, p. 173). Pumping costs have gas shows at unspecified depths in the J. R. Sealy been relatively low because of an efficient water drive. Spindle Top 3, Seminole County (well GA-65, table 1), Forty-Mile Bend field, Dade County, Fla., was dis­ were recorded without confirmation. This well was covered in 1954 about 50 miles southeast of the Sunni­ abandoned in Lower Cretaceous rocks at a total depth land field after both reflection and refraction seismic of 7,620 feet. State records of the second well, the J. R. Sealy Fee 1 (well GA-67, table 1), Decatur County, surveys had been made in the area (Powell and Culli- show that an unknown quantity of gas and hot water gan, 1955, p. 1008). The discovery well, the Gulf flowed from an Upper Cretaceous sandstone at a depth Refining Wiseheart-State of Florida 1, sec. 16, T. 54 S., of 3,005 feet. The calculated heating value for this gas R.. 35 E., reached a total depth of 11,557 feet and was was only 754 Btu (British thermal units) per cubic completed in the Sunniland Limestone of Trinity foot. The analysis of the gas is: (Lower Cretaceous) age. The initial production was Percent 76 barrels of 20° API. gravity oil and 96 barrels of Methane-.--..---_.___._.--_-.___.___... 74. 2 salt water from depths of 11,322 to 11,339 feet. A Nitrogen_ . ______24. 1 Carbon dioxide- ______.6 second producing well completed with an initial pro­ Argon.______. 4 duction of 112 barrels per day was followed by three Helium.______. 3 dry holes that delimited the small field. The field pro­ Oxygen______-______-__--____-- . 2 duced a total of 32,888 barrels of oil before being Hydrogen.. ______. 1 Ethane-______--____-___------_------' - 1 abandoned (Roberts and Vernon, 1961, p. 218). Cyclopentane______---___--- Trace 58 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Seeps and shows of oil have been reported in central near Cape May was reported to him by an oil com­ Georgia. The seeps occur in the vicinity of Scotland, pany geologist. Telfair County, where oil of about 30° API. gravity Source beds for hydrocarbons, generally regarded and gas come to the surface in a swampy area (Hull to be marine shales, marls, and limestones ir about and Teas, 1919). The surface beds are sands and clays that order of importance, are scattered throughout the of probable Oligocene age in an area that may be stratigraphic sequence beneath the Coastal Pkin, but structurally high, according to Hull and Teas (1919, they only reach considerable thicknesses beneath the p. 11). The oil shows in wells in Coffee and Telfair Florida Peninsula and in a narrow band along the Counties have been recorded, without confirmation, in coast from New Jersey to North Carolina. Thick lime­ the files of the Georgia Department of Mines, Mining, stone, marl, and dolomite beds make up most of the and Geology. A show of oil in a sandstone of Taylor Cretaceous and Tertiary rocks in Florida and southern age was reported in a Carpenter Oil Co. well about Georgia; shale, marl, and limestone beds m<\ke up 20 miles north of Douglas in Coffee County, and fluo­ more than half of the sequence at Cape Hatteras and rescence and staining was reported in sidewall cores in coastal Maryland. Offshore, much thicker marine taken from sandstones of Lower Cretaceous(?), Wood­ deposits, particularly in the Lower Cretaceous and bine, and Austin age in the Parsons and Hoke Henry older rocks, may be expected beneath the continental Spurlin 1 (well GA-33, table 1) in Telfair County. shelf. Inland, the rocks with more continental aspects A few oil seeps and surface indications of gas in probably are more likely to be sources of dry gas North Carolina have been reported to the North Caro­ than of oil. lina Department of Conservation and Development Emery (1963, p. 6; 1965c, p. C159-C160) has sug­ but none have been substantiated. Subsurface evidence gested that fine-grained organic-rich source be^s may for the presence of hydrocarbons is also very meager. be interbedded with coarse-grained turbidites at the Scattered shows of oil were reported by the driller in base of the continental slopes of the world and that cuttings and sidewall cores of the F. L. Karsten possibly large reserves of petroleum will be found Laughton 1 (well NC-47, table 1) located near the there when cheap and effective methods of drilling coastline in Carteret County, but these were not con­ and extraction at such water depths are developed. firmed by later studies of the samples and cores. If this is established, a band of sedimentary rocks "Showings of a gas" of unspecified composition in along the slope and rise from Newfoundland to Florida Lower Cretaceous or possibly Triassic rocks between will deserve consideration for petroleum exploration. depths of 3,170 and 4,050 feet in the DuGrandlee Exploration Foreman 1 (well NC-4, table 1) in Cam- RESERVOIRS AND FLUIDS den County were reported to Richards (1954, p. 2565). Reservoirs are thick and numerous beneath the A minor amount of gas was produced from shal­ Atlantic Coastal Plain. Sandstones of Late Cretaceous low wells in the Coastal Plain of Maryland and age and sandstones and limestones of Tertipry age used as fuel for a period of 2 years near the turn of supply fresh water to most of the communitier on the the century (Clark, Matthews, and Berry, 1918, p. Coastal Plain. The Upper Cretaceous sandstones, 320). These wells, located in the vicinity of Parson- especially those of Woodbine and Austin age that are burg and Pittsville in Wicomico County, were less several hundred feet thick, yield large quantities of than 100 feet deep. The gas produced had a high potable water for several tens of miles downdip from nitrogen content (77.96 percent) and a low methane their outcrops. Sandstones of the Raritan (Woodbine content (19.86 percent). It was concluded that this age) and Magothy (Austin age) Formations cropping gas was marsh gas and had its origin in -a buried out along the Fall Line in New Jersey have porosities swamp. No gas was reported below these shallow as large as 46 and 40 percent respectively (Br.rksdale depths. Reference to well MD-12 on section E-F and others, 1958, p. 98). Generally, the Upper Creta­ (pi. 11) of this report suggests that the gas came ceous sandstones contain salt water near the, coast, from Pleistocene or Pliocene alluvium. although fresh-to-brackish water is present in the Rari­ Traces of hydrocarbons were detected at a deptli tan Formation along the New Jersey coast (Gill and of 300 feet in a water well at Cape May, N.J., and others, 1963, p. 20) and the southern shore of Long in another water well at Atlantic City, by F. J. Island (Perlmutter and Crandell, 1959, p. 1068). The Markewicz, of the New Jersey Geological Survey, Raritan sands yield from 200 to 2,000 gallons a minute according to M. E. Johnson (Petroleum Week, 1958, in wells on Long Island (Perlmutter and Crandell, p. 23). A similar occurrence in another water well 1959, p. 1069, 1072), which suggests excellent porosity PETROLEUM POTENTIAL 59 and permeability. The shallow Tertiary sandstones consists mainly of light-gray, fine- to coarse-grained and limestones, particularly those of late Eocene, sandstone interbedded with some thin bed^ of light-gray, Oligocene, and Miocene age, yield potable water from fine-grained, silty sandstone and white, slightly oolitic, their outcrops to the seacoast. The Ocala Limestone finely crystalline limestone. In the upper part, porosities (upper Eocene) is an especially extensive fresh-water range from 12.8 to 32.6 percent and permeabilities from artesian aquifer in Florida and Georgia and is known 2.1 to 2,080 millidarcys (table 4). A drill-stem test to discharge fresh water in submarine springs off (test 2, pi. 12) taken opposite the interval between Florida, where indicated on plate 2 (Stringfield and 7,018 and 7,027 feet with the tool open 10 minutes Cooper, 1951, p. 61). recorded a bottom-hole pressure of 3,100 psi (pounds At present, no deep wells have been drilled on the per square inch) and yielded 7 barrelr of mud and Atlantic Continental Shelf, so the probability of ade­ muddy salt water and 51 barrels of gs.lt water. The quate reservoirs for petroleum accumulations can be analysis (Spangler, 1950, p. 106) of water from this test judged only from the wells drilled along the coast is: and in the Bahama Islands. Two wells, the Standard Parts per million Sodium_____--____.-______-._____-___. 42, 858 Oil of New Jersey Hatteras Light 1 at Cape Hatteras, Calcium..______5, 856 N.C., and the Bahamas Oil Andros Island 1 on Andros Magnesium.______---__-___----_.______1, 258 Island, Bahama Islands, are particularly significant. Sulphate______---_-__-_-___-_--__-_ 840 The first penetrated 9,878 feet of predominantly marine Chloride..______79,460 elastics and some thick limestone sequences; the latter Bicarbonates______47 Carbonates-______--______---_-__--_--_ 0 penetrated 14,585 feet of marine limestone and dolo­ mite beds. Thick sandstone reservoirs are present in The principal reservoir of Washita age, 6,487 to the Cape Hatteras well, whereas thick porous-to- 6,585 feet in depth, is a 98-foot sequence of sandstone cavernous limestone and dolomite beds are reservoirs beds grading from medium grained at the top to fine in the Andros Island well. grained and silty at the bottom. The porosities of these beds range from 2.5 to 33.9 percent and the permeabili­ HATTERAS LIGHT WELL ties from 0 to 2,103 millidarcys. A drill-stem test (test 1, The drilling and testing of the Standard Oil of pi. 12) with packers set at 6,474 and 6,483 feet and the New Jersey Hatteras Light 1 (well NC-14, table 1) tool open 10 minutes recovered 6 barrels of mud and has been reported by Spangler (1950, p. 104-108). muddy salt water, and 55 barrels of salt water. Total This well penetrated ten major sandstone bodies, nu­ depth was 6,512 feet during the test and the bottom-hole merous thin sandstone beds, and a few porous lime­ pressure was recorded as 2,900 psi. The analysis stone and dolomite beds. The major sandstone bodies, (Spangler, 1950, p. 106) of water from this test is: ranging from 93 to 728 feet in thickness, are present Parts per million at depths of (1) 9,150 to 9,878 feet [earliest Late Sodium______---____-_-__---__-_-. 36, 097 Jurassic or Early Cretaceous (Neocomian) age], (2) Calcium..______7, 100 8,585 to 8,750 feet [Early Cretaceous (Trinity?) age], Magnesium. ______1, 302 Sulphate_-__-----__---_-_ ------840 (3) 8,240 to 8,500 feet [Early Cretaceous (Trinity?) Chloride..-__--_-__--__-_--_------71, 335 age], (4) 7,665 to 7,758 feet [Early Cretaceous (Trin­ Bicarbonates. ______--_____-_--__-_--_-_--- 99 ity?) age], (5) 7,018 to 7,360 feet [Early Cretaceous Carbonates- ______0 (Fredericksburg?) age], (6) 6,475 to 6,585 feet [Early Rocks of Woodbine age, which include the more or and Late Cretaceous (Washita?) age], (7) 4,800 to less equivalent Atkinson, Tuscaloosa, and Raritan 5,580 feet [Late Cretaceous (Woodbine) age], (8) fresh-water aquifers of the Coastal Plain, have poor 3,660 to 4,288 feet [Late Cretaceous (Austin) age], (9) reservoir characteristics in the Hatter^s Light well. 2,385 to 2,755 feet [Tertiary (early Eocene) age], and (10) 575 feet to 995 feet [Tertiary (Miocene) age]. This interval is made up of thin, silty, fine-grained The three most promising reservoirs for petroleum sandstones interbedded with sandy shale and a few sandstones of Fredericksburg (?), Washita (?), and fossiliferous limestone layers. Updip in the Standard Austin age were cored and tested. The porosity and Oil North Carolina Esso 2 (well NC-7) in Panllico permeability determinations are given in table 4, which Sound, the interval is about the s^me thickness, is adapted from Spangler (1950). roughly 1,300 feet, but it consists of thick sandstone The principal potential petroleum reservoir of beds interbedded with thin layers of gray shale and Fredericksburg age, 7,018 to 7,360 feet in depth, some limestone lenses. Generally, the sandstone beds 60 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 4. Porosity and permeability determinations for reservoirs in the Standard Oil of New Jersey Hatteras Light 1 [Adapted from Spangler, 1950, p. 107] Age of sandstone rocks Core No. Depth (feet) Recovery Porosity ]Permeability (feet) (percent) (jnillidarcys)

Late Cretaceous (Austin) 51 3, 657-3, 666 1.5 41.2 . 52 3, 693-3, 703 3 27.6 5.7 53t 3, 827-3, 837 3 31.8 4.5 53b 3, 827-3, 837 3 15. 9 5.7 54 3, 930-3, 940 0. 8 39.2 . 55 4, 042-4, 052 4.5 32.2 5.0 56 4, 152-4, 162 10 40.9 _ 57 4, 275-4, 285 4 28.0 5.4 Late and Early Cretaceous 77 6, 487-6, 497 10 27. 0 65. 0 (Washita?) 77 6, 487-6, 497 10 33.7 73.6 77 6, 487-6, 497 10 33.2 70.0 78 6, 497-6, 507 9 24.7 _ 78 6, 497-6, 507 9 30.2 184 78 6, 497-6, 507 9 3. 1 0 79 6, 507-6, 512 5 27. 2 58.3 79 6, 507-6, 512 5 26. 9 _ 80 6, 512-6, 522 7. 5 29.3 . 80 6, 512-6, 522 7.5 27.8 . 80 6, 512-6, 522 7.5 32. 1 . 81 6, 522-6, 532 4 19.8 118 81 6, 522-6, 532 4 25.9 191 82 6, 532-6, 542 3 27.8 247 83 6, 542-6, 552 7 28.9 1,546 84 6, 552-6, 562 10 26.4 999 84 6, 552-6, 562 10 33.6 . 84 6, 552-6, 562 10 33.9 2, 103 85 6, 562-6, 572 10 28.0 142 85 6, 562-6, 572 10 31.4 1,024 86 6, 572-6, 581 7 30.8 605 86 6, 572-6, 581 7 2.5 0 Early Cretaceous (Frederieksburg?) 91 7, 021-7, 026 2.1 32.6 2,080 92 7, 034-7, 039 2.7 31.4 _ 93 7, 076-7, 081 4 22.0 58.3 94 7, 081-7, 091 4 19.3 391 94 7, 081-7, 091 4 16.5 11.7 95 7, 091-7, 096 2.5 24. 1 _ 96 7, 096-7, 106 10 27.3 301 96 7, 096-7, 106 10 29. 1 537 97 7, 106-7, 113 7 28.4 386 98 7, 113-7, 123 9 29.0 810 98 7, 113-7, 123 9 31. 5 943 99 7, 123-7, 133 10 26.8 205 99 7, 123-7, 133 10 12.8 2. 1 100 7, 191-7, 201 10 25.4 . 100 7, 191-7, 201 10 26. 1 _ are very fine to medium grained and are limy and Coastal Plain. Such a condition is not necessarily a slightly carbonaceous with scattered conglomeratic negative factor in the evaluation of the petroleum layers composed mostly of chert and pebbles. Exami­ potential of the continental shelf, as clean, well-sorted nation of a core between depths of 4,377 and 4,387 sandstones are not common among the oil reservoirs in feet revealed a fine- to medium-grained, slightly limy, the United States. glauconitic sandstone that is extremely porous. This The principal potential petroleum reservoir cf Aus­ comparison suggests that rocks of Woodbine age may tin age, 3,660 to 4,288 feet in depth, is competed of be considerably less porous and permeable a short fine- to coarse-grained, calcareous glauconitic sand­ distance offshore than they are beneath the Atlantic stone with thin conglomeratic layers. Some coarse PETROLEUM POTENTIAL 61 sandstones are very loosely cemented and the indi­ TRAPS vidual sand grains break free in the drilling. Porosi­ ties range from 15.9 to 41.2 percent and permeabilities Traps for petroleum have been grouped by Levor- from 4.5 to 5.7 millidarcys (table 4). Drill-stem tests sen (1954, p. 142-143) into three basic types: struc­ were not made in this interval. tural traps, stratigraphic traps, and combination traps. The possibility of carbonate reservoirs beneath the 1. Structural traps are those that have been formed continental shelf in the vicinity of the Hatteras Light primarily by local deformation of the reservoir well is suggested by porous zones in limestone and and sealing beds. The deformation may involve dolomite beds in pre-Upper Cretaceous rocks. The either folding or faulting, or both, and some­ upper part of a 100-foot carbonate sequence at the times produces fracturing of the reservoir as an top of rocks of Late Jurassic or Early Cretaceous important element of the trap. (Neocomian) age (8,750 feet) contains oolitic lime­ 2. Stratigraphic traps are those that have been stone, conglomeratic limestone, dolomitic limestone, formed primarily by stratigraphic variations and porous granular dolomite, and anhydrite. The porosity discontinuities. Primary stratigraphic traps are of these beds is slight compared to the sandstones dis­ those that are effective mainly because of origi­ cussed previously, but it bears on the probability that nal depositional characteristics, such as compo­ thicker units of porous dolomite and oolitic limestone sition, shape, and attitude of the reservoir. These beds may be expected offshore. Another porous car­ are related mainly to lateral variations of lithol- bonate bed was drilled in the lower part of rocks of ogy, or lithofacies in the broadest sense of that Trinity (?) age between depths of 8,500 and 8,585 term. Secondary stratigraphic traps are those feet. This one is composed of light-brown, sandy, that are effective primarily because of discon­ coarsely crystalline dolomite and dolomitic limestone. tinuities in stratigraphic succession. Such traps The upper part was described as cavernous by Swain may be associated with either local unconformi­ (1952, p. 66). No drill-stem tests or porosity tests ties present in a few townships or regional were made for this interval. unconformities present throughout a sedimentary basin or province. ANDROS ISLAND WELL 3. Combination traps are those that combine both structural and stratigraphic elements of subequal The Bahamas Oil Andros Island 1 (well BA-2) in '"importance. Combinations of unconformities and the Bahama Islands penetrated 14,585 feet of carbonate anticlines with modifications due tc faults, litho­ rocks ranging from Early Cretaceous to Tertiary in facies, and hydrodynamic conditions are prob­ age. This sequence included many porous, fragmental ably the most common trap. and fossiliferous limestones in differing stages of The principal components of traps are sealing beds, recrystallization and <|olomitization. Circulation of folds and faults, unconformities, lithofr.cies, and hy­ drilling mud was lost at depths of 70, 540, 2,689, drodynamic conditions. The following discussion at­ 9,604, 10,020, 12,965, 13,230, and 13,383 feet before tempts to identify each component in the Mesozoic the drill pipe was lost in the hole at a depth of rocks along the Atlantic coast and suggests areas in 14,585 feet. The well was abandoned at that depth which certain combinations of components may have with 11,960 feet of drill pipe not recovered. Especially formed traps for petroleum. viscous muds with fibre added were used to regain circulation. Cavities were reported by the driller at SEALING BEDS 10,663-10,685; 10,687-10,696; 12,963-12,965; 13,202- Sealing beds of some kind are necessary for the en­ 13,206; 13,208-13,210; 13,214-13,215; 13,225-13,230; trapment of petroleum, except in trap-' sealed with and 13,312-13,313 feet. All of these cavities are in lower asphaltic residue and in any traps that were possibly Upper Cretaceous and upper Lower Cretaceous rocks. created by hydrodynamic conditions alone. The sealing Sample and core studies indicate considerable fracture beds are usually the more plastic beds of clay, shale, and intergranular porosity in the rocks as well as and salt, but they also may be anhydrite, limestone, cavernous porosity. Carbonate reservoirs are so thick and dolomite beds that have escaped fracturing or and open as to create drilling problems in this area, whose fractures have been closed by chemical but more suitable conditions may be present at other precipitates. places beneath the continental shelf in the Bahama Clay and shale beds act as aquicludes in the artesian Banks and Blake Plateau regions. system of the Coastal Plain north of Florida and 62 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF could readily serve as sealing beds over petroleum ac­ younger rocks. These gentle folds and faults, along cumulations. Some that extend seaward an unknown with stratigraphic components, may be sufficient to distance beneath the continental shelf, judging by the provide combination traps. Hatteras Light well (NC-14) in North Carolina, The major positive features are the Cape Fe^.r arch, include shale beds of Cretaceous (Trinity or Freder- the Peninsular arch, the Bahama uplift, and a long icksburg, Eagle Ford, Taylor and Navarro) and Pale- basement ridge at the edge of the continental shelf ocene age. off New England. (See pi. 4.) Both the Cape Fear Anhydrite, which is not only a cap rock in salt- arch and the Peninsular arch (including tin offset dome fields but also a common seal throughout the Ocala arch) show evidence of recurrent movement world in oil fields with carbonate reservoirs, overlies along older lines of weakness and an overlap of the oil-producing Sunniland Limestone of Early Cre­ Lower Cretaceous beds by Upper Cretaceous beds. The taceous (Trinity?) age in the oil fields of southern Bahama uplift appears to be mainly structural. If it Florida. This unit has been informally named the is, a thick marine sequence possibly containing reefs "upper anhydrite" by oil geologists of this area. A may have the traps necessary for the accumulation of short distance below the oil-producing beds is a mas­ petroleum. The long ridge at the edge of th°, conti­ sive anhydrite bed once referred to as the "lower mas­ nental shelf off New England (pi. 4) is completely sive anhydrite" and now known as the Punta Gorda unknown except for its expression in the basement Anhydrite (Applin and Applin, 1965, p. 39). Thinner rocks as recorded by seismic surveys. Whether or not beds of anhydrite are interspersed with limestone and this basement ridge is reflected in sedimentary rocks shale in other parts of the Lower Cretaceous rocks, in of suitable character for petroleum accumulation is the upper Upper Cretaceous rocks, and in the lower unknown at present. Tertiary rocks (Cedar Keys Limestone of Paleocene Several long faults or fault zones along the edge age and Oldsmar Limestone of Eocene age). Similar of the continental shelf and along the continental lithologies are present in southern Florida wells and margin at the eastern edge of the Blake Plateau have have been reported orally for the deep well on Cay been suggested by Pressler (1947, p. 1858, fig. 1). The Sal (well 1, table 1) about 80 miles southeast of the presence and placement of these faults, inferred from Florida Keys. bottom topography, are highly speculative, as little Massive anhydrite beds were not found in the An- seismic evidence for or against their existence has dros Island well (well BA-2, table 1) in the Bahamas, been presented. In a preliminary statement of results and only a few thin anhydrite beds have been reported from seismic-refraction investigations off Florida and along the Atlantic coast in the vicinity of Cape Hat­ Georgia, Sheridan, Drake, Nafe, and Hennior (1964) teras (Spangler, 1950, p. 123; Swain, 1952, p. 66 and suggested some faulting at the edge of the shelf. In 67). This suggests that conditions suitable for depo­ their complete report (Sheridan and others< 1966), sition of evaporites may have been more prevalent they concluded that anomalous seismic record"1 at the in the eastern Gulf of Mexico than northward along shelf edge were primarily a result of bottom topog­ the Atlantic coast. In general, however, it seems that raphy and sedimentary facies change. Ewing, Ewing, sealing beds of clay, shale, and impervious chemical and Leyden (1966) in a companion report lased on precipitates may be common enough beneath the At­ continuous seismic-reflection profiles reached the same lantic Continental Shelf to provide the vertical dis­ conclusion. Test holes in Tertiary strata off Jackson­ continuities necessary for trapping petroleum. ville, Fla. (Bunce and others, 1965), do not indicate FOLDS AND FAULTS the presence of a post-Cretaceous fault along the shelf edge there but provide no information on the older Although the Coastal Plain deposits flank the much-folded and faulted Appalachian Mountains, beds. they have not been involved in any major tectonic A transcurrent fault in the basement beneath the movements. As a result, they do not exhibit the abrupt shelf has been postulated along the 40th parallel about folds and numerous faults commonly associated with 50 miles south of New York by Drake, Heirtzler, and the flanks of mountain systems. This suggests that few Hirshman (1963, p. 5270) on the basis of a linear traps of a purely structural nature should be expected. magnetic anomaly. (See fig. 6.) Emery (1965c, p. Nevertheless, the basement structural features buried C159 and fig. 1) has suggested that suitable petroleum- by Coastal Plain deposits are reflected to different bearing structures may be associated with this "major degrees by gentle warping and normal faulting in the strike-slip fault." No data suggesting the time of the PETROLEUM POTENTIAL 63 major fault movements or the presence of smaller taceous (Woodbine) reservoirs as indicated in plates associated structures has been published. 9, 11, and 12. One of the places where this uncon­ formity and pthers within Lower Cretaceous and LITHOFACIES older beds may supply the component necessary for Lateral variations in lithology within a strati- a combination trap is on the seaward nose of the Cape graphic unit that may form primary stratigraphic or Fear arch. combination traps are difficult to predict in relatively The unconformity at the top of the Cretaceous rocks unexplored regions such as the Atlantic Coastal Plain probably is less important as a trapping component and Continental Shelf. Such traps may include off­ than the deeper major ones. Thinning of Upper Cre­ shore bars, channel fillings, reefs, and porosity changes taceous rocks and overlap of Tertiary b°ds as exem­ between two carbonate facies or carbonate and clastic plified in Georgia on plate 13 takes place at relatively facies. Offshore bars and channel fillings might be shallow depths and rather close to the outcrops. Pos­ expected in predominantly shale and marl sequences sibly it could be a more important factor on structures of Late Cretaceous age along the Coastal Plain north beneath the continental shelf. of Florida. Reefs and porosity changes at dolomite- limestone transitions may be present in Florida and HYDRODYNAMIC CONDITION0 along the continental shelf, particularly beneath the The accumulation of petroleum in all traps may Bahama and Blake Plateau platforms. Limestone- be modified considerably by the hydrostatic or hydro- shale and sandstone-limestone transitions probably are dynamic forces of the water in the reservoir (Hub- present beneath the shelf at many places. One of the bert, 1953). Under hydrostatic conditions, the water likely places is the Southeast Georgia embayment. is essentially at rest and the impelling force on the There well data are adequate to show a clastic- petroleum is upward. The boundaries of the trap carbonate transition in Cretaceous rocks trending alone determine the location and shape of the accumu­ northeastward across the inner shelf. This in conjunc­ lation. Under hydrodynamic conditions, a potential tion with faults or folds offers possibilities for combi­ exists from areas of higher pressure to those of lower nation traps. pressure and this force modifies the location and shape UNCONFORMITIES of the accumulation by inclining it in the direction Numerous unconformities subdivide the Coastal of flow. The effect of hydrodynamics may be sufficient Plain deposits, but only a few extend far enough to cause trapping in or near lithologic, depositional, downdip and laterally to be important as avenues of and structural features that would be ineffective under migration or loci of hydrocarbon traps. However, hydrostatic conditions. these few may have provided excellent opportunities Fresh-water reservoirs beneath the Coastal Plain for the accumulation of petroleum in both secondary alluvium are under artesian pressure downdip from stratigraphic and combination traps. their outcrops, and flowing wells are not uncommon Little is known of the nature of possible uncon­ in lower areas. The artesian head of f^esh water in formities separating sequences assigned to Late Juras­ the Ocala Limestone (Eocene) beneath the continen­ sic or Early Cretaceous (Neocomian), Trinity(?), tal shelf is as much as 30 feet above f°,a level at a Fredericksburg(?), and Washita(?) ages, as only a distance of 27 miles off Jacksonville, Fir,, (Bunce and few wells at the coastal extremities have been drilled others, 1965, p. 710; Schlee and Gerard, 1965, p. 37). this deep. These rocks do wedge out against the Penin­ Submarine springs of large volume is?ue from the sular arch (pis. 9, 15), the Cape Fear arch (pis. 9, 12), Ocala Limestone through sink holes near the shore and northward from iMew Jersey (pi. 9). They may in the same area (Stringfield and Cooper, 1951; wedge out landward beneath the continental shelf all Stringfield, written commun., 1964). along the coast similar to the way they do west of the Although water-level and pressure records are Hatteras Light well (well NC-14, pi. 12). available for many wells in the fresh-water part of Probably the most important unconformity occurs the reservoirs, little is known about pressures where at the top of the beds of Washita (?) age, essentially the waters become brackish or salty at d°.pth. The one the top of the Lower Cretaceous rocks. The structure deep well for which drill-stem test pressures have of the Lower Cretaceous rocks is somewhat different been published is the Hatteras Light well (well NC- from that of the overlying beds. The marine Lower 14, pi. 12) in North Carolina. In this well, drill-stem Cretaceous rocks not only lap out landward against tests opposite intervals at 6,474 to 6,583 feet and 7,018 the basement rocks but are overlapped by Upper Cre­ to 7,027 feet in depth recorded bottom-hole pressures 64 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF of 2,900 and 3,100 psi, respectively. The reservoirs ferent from that of the Upper Cretaceous (Woodbine) tested are Lower Cretaceous sandstones of Washita (?) rocks that overlap them. Important unconformities and Fredericksburg( ?) age that do not crop out along are present not only at the top but within the se­ the Fall Line in North Carolina because of Upper Cre­ quence. These suggest the possibility of not only taceous and Tertiary overlap. These recorded bottom- structural but combined structural and stratigraphic hole pressures, which may not, be very accurate traps. because of the difficulties in setting packers tightly Upper Cretaceous rocks have good possibilities for above and below the interval tested, are equivalent oil and gas production beneath the continental shelf, to a head of 6,670 and 7,130 feet, respectively. They but they have only fair possibilities, chiefly for gas, approximate the hydrostatic head of reservoirs at in the Coastal Plain. Although the thickness of these depths of 6,583 and 7,027 feet plus the land elevation rocks does not exceed 3,500 feet onshore and may be (80 feet) at the Cretaceous outcrop more than 100 only a few thousand feet more beneath the si ^lf (pi. miles westward, and they suggest that only gentle 17#), the beds are buried sufficiently beneath the Ter­ pressure gradients exist in these reservoirs in this tiary rocks to provide ample opportunity for the ac­ area. Until many more drill-stem tests are available, cumulation of petroleum. Reservoir rocks are thick little can be done to determine the regional effects of and numerous in the Upper Cretaceous rocki? of the hydrodynamics. Coastal Plain and seem to extend beneath the shelf where thick marine source rocks may be expected. SUMMATION OF PETROLEUM POTENTIAL Rocks of Woodbine and Eagle Ford age appear to Pre-Cretaceous rocks have few characteristics of be a favorable reservoir-source rock combination petroleum-producing beds. Paleozoic rocks in the pre- whose thickness probably exceeds 2,000 feet offshore Mesozoic basement are highly metamorphosed except (pi. 17(7). Unconformities at the top and base are in southwestern Georgia (pi. 14) and central Florida extensive; the basal unconformity may be the more (pis. 9 and 15), where they are not metamorphosed important from the standpoint of petroleum accumu­ but are so highly indurated and folded as to have lation, as it permits the basal Upper Cretaceous doubtful reservoir characteristics. Triassic(?) rocks sandstones of Woodbine age to overlap the underly­ (pis. 11 and 14) exhibit many continental aspects, ing, more marine Lower Cretaceous rocks. Defending such as red beds and conglomerate, and numerous ig­ upon the juxtaposition of lithologies, this uncon­ neous intrusions; such rocks may contain good reser­ formity may be either a trap or an avenue, of mi­ voirs, but they are not generally regarded as good gration in different places. It appears to mark an source rocks. extremely porous zone in the carbonates of the Andros Lower Cretaceous rocks and those classed tenta­ Island well. tively as Upper Jurassic or Lower Cretaceous (Neo- Tertiary rocks exhibit very good reservoir and fair comian) in this report (pis. 12 and 16) offer the most source rock characteristics. They are less promising promising prospects for oil and gas production in the than Cretaceous rocks for a number of reasonr: Atlantic coastal region. Their combined thickness 1. They probably are less than 4,000 feet thick in probably exceeds 5,000 feet beneath the continental most of the area north of southern Florida and shelf in the Baltimore Canyon trough and in the the Bahama Islands (pi. 17Z>), and they contain Southeast Georgia embayment. Even greater thick­ fresh-to-brackish artesian water in much of that nesses may exist beneath the Blake Plateau and Ba­ area. hama Islands. These rocks, where penetrated along 2. They crop out in part along the continental shelf the coastal extremities, exhibit many characteristics and Blake Plateau (see pi. 2 and figs. 7 and 8), of petroleum-producing beds. Marine beds generally and in other places they give rise to submarine regarded as potential sources of petroleum are pre­ springs in sink holes (Stringfield and Cooper, dominant, and the enviroment of their deposition, at 1951, p. 61). least in the southern areas, probably favored reef 3. Structural features are reflected less distinctly in growth. Thick, very porous, salt-water-bearing res­ the Tertiary rocks than in the older rocks, as ervoirs, both sandstone and carbonate, are numerous. they have been subject to less tectonic adjustment. Although not many thick shale beds have been drilled 4. Unconformities within the Tertiary rocks are less in the sequence as yet, adequate sealing beds may be significant regionally than those in older rocks. provided by dense limestone and anhydrite beds. The Tertiary (Paleocene and lower Eocene) beds at the, structural attitude of these rocks is considerably dif­ basal unconformity wedge out against Upper Greta- REFERENCES CITED 65 ceous rocks in places (pi. 13). However, this wedgeout Richards (1963, p. 151, 152) in discus-sing the oil occurs at depths too shallow to offer much hope for prospects off the New Jersey shore mentioned Five trapping commercial quantities of petroleum. Fathom Bank, about 10 miles off Cape May, and The continental shelf offers more promise as a several landward shoals as likely places for an oil potential petroleum province than the Coastal Plain test. These locations were selected for their conven­ because it has a thicker sedimentary column with ience in drilling operations rather than for geological better source beds and trapping possibilities. Thick­ considerations of a local nature. nesses of 10,000 feet and more are present beneath the Most recently, Emery (1965c, p. C159 ard fig. 1) has Coastal Plain only in southern Florida, whereas stated that suitable petroleum-bearing structures may thicknesses beneath the continental shelf exceed 10,000 be associated with the seaward extension of the Cape feet in the Southeast Georgia embayment and Georges Fear arch, the basement ridge at the edge of the Bank trough, 12,500 feet in the Emerald Bank trough, continental shelf off New England, and a "major and 15,000 feet in the Baltimore Canyon trough strike-slip fault" just southeast of New York City. (pi. 4). Comparable thicknesses may be present beyond The latter is the transverse fault deduced by Drake, the continental shelf beneath the Blake Plateau and Heirtzler, and Hirshman (1963, p. 5270) from mag­ Bahama platform. Extreme thicknesses of 25,000 feet netic anomalies in the basement rocks. (Se*j pi. 8.) underlie the continental slope in water 5,000 to 10,000 All the published suggestions for areas in which to feet deep; this is not within present economic limits conduct exploration operations for petroleum seem to for commercial exploration. have merit. However, the Bahama platfcrm, the sea­ Different views as to the most favorable areas of ward extension of the Cape Fear arch, tH long base­ the continental shelf for petroleum exploration have ment ridge at the edge of the continental shelf off been expressed by J. F. Pepper (in Trumbull and New England, and the Southeast Georgia embayment others, 1958, p. 51, 52, and 55), Johnston, Trumbull, appear to this writer to be the areas most favorable and Eaton (1959, p. 439-441), Richards (1963, p. 150, for initial operations in waters controlled by the 151), and Emery (1965b, fig. 6). These are based United States. The outer shelf in Canadian waters off mainly on considerations of basement structure and Nova Scotia and Newfoundland offers equally good gross thickness of sediments without regard to age or possibilities, but with the exception of the possible unconformities. extension of the outer shelf basement ridge near Sable According to J. F. Pepper (in Trumball and others, Island, no basis exists for comparing different parts 1958, p. 55), the results of an airborne magnetometer of this huge area that includes the Grand Banks survey of the Bahamas "are said to indicate that struc­ extending 120 miles from land. tures are present which may be favorable for the In summary, more stratigraphic and seismic data accumulation of oil." He points out favorable thick­ on the older rocks are needed before add;tional areas nesses of sediments at places only 60 miles offshore on for exploration can be suggested. Howeve", the proba­ the continental shelf between Florida and New Jersey, bilities for discovery of commercial accumulations of but he states (in Trumbull and others, 1958, p. 51, 52) petroleum in the Atlantic coastal region s?-em to favor that "the possibility of finding oil in commercial quan­ rocks classed herein as Upper Jurassic or Lower Creta­ tities in any of the shelf areas between New Jersey ceous (Neocomian) and Lower Cretaceons in strati- and Newfoundland is not considered to be favorable." graphic or combination traps beneath the continental In discussing structural factors related to petroleum shelf. possibilities, Johnston, Trumbull, and Eaton (1959, p. 440, 441) give favorable mention to the Cape Fear REFERENCES CITED arch and its seaward extension, a high at Fort Munroe, Adkins, W. S., 1928, Handbook of Cretaceous fossils: Texas Va., and the basement ridge mapped at the edge of Univ. Bur. Econ. Geology Bull. 2838, 385 p. the continental shelf off New England by Drake, 1933, The Mesozoic systems in Texas, Part 2 in The geology of Texas: Texas Univ. Bur. Econ. Geology Bull. Ewing, and Sutton (1959, p. 176, fig. 29). Somewhat 3232, p. 239-518. earlier, a brackish ground-water anomaly on the Cape Agassiz, Alexander, 1888, Three cruises of the U.S. Coast and Fear arch, a few miles inland from Wilmington, N.C., Geodetic Survey steamer Blake, Volume I: Boston and had been cited by LeGrand (1955, p. 2020) as deserv­ New York, Houghton, Mifflin and Co., 314 p. Alexander, A. E., 1934, A petrographic and petr?logic study of ing attention "if oil-prospecting becomes more active some continental shelf sediments: Jour. F°d. Petrology, on the Atlantic Coast." v. 4, p. 12-22. 66 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF American Geographical Society, 1948, Atlas of the Americas: Bartlett, J. R., 1883, Deep-sea soundings and temperatures in New York, Am. Geog. Soc. atlas sheet IE, scale 1: 5,000,000. the Gulf Stream off the Atlantic coast, taken under direc­ Anderson, J. L., 1948, Cretaceous and Tertiary subsurface tion of the U.S. Coast and Geodetic Survey [18f2] ; Am. geology [Maryland] with appendix, Description of well Assoc. Adv. Sci. Proc., v. 31, p. 349-352. samples: Maryland Dept. Geology, Mines and Water Bassler, R. S., 1936, Cretaceous bryozoan from Georges Bank, Resources Bull. 2, p. 1-113; app., p. 385-441. Part 3, Geology and paleontology of the Georf«?s Bank Antoine, J. W., and Harding, J. L., 1963, Structure of the con­ canyons: Geol. Soc. America Bull., v. 47, no. 3, p, 411-412. tinental shelf, northeastern Gulf of Mexico: Texas Agr. Bayley, R. W., and Muehlberger, W. R., compilers, 1£^8, Base­ and Mech. Coll. Dept. Oceanography and Meteorology ment rock map of the United States, exclusive of Alaska Prelim. Kept, May 1963, 18 p. and Hawaii: Washington, D. C., U.S. Geol. Survey, 2 Antoine, J. W., and Henry, V. J., Jr., 1965, Seismic refraction sheets, scale 1:2,500,000. study of shallow part of continental shelf off Georgia Bentley, C. R., and Worzel, J. L., 1956, Continental slope and coast: Am. Assoc. Petroleum Geologists Bull., v. 49, no. 5, continental rise south of the Grand Banks, Part 10, p. 601-609. Geophysical investigations in the emerged and submerged Applin, E. R., 1955, A biofacies of Woodbine age in south­ Atlantic Coastal Plain: Geol. Soc. America Bu''., v. 67, eastern gulf coast region: U.S. Geol. Survey Prof. Paper no. 1, p. 1-18. 264-1, p. 187-197. Berger, J., Blanchard, J. E., Keen, M. J., McAllistC'-, R. E., Applin, E. R., and Jordan, Louise, 1945, Diagnostic Foraminif- and Tsong, C. F., 1965, Geophysical observations- on sedi­ era from subsurface formations in Florida: Jour. Paleon­ ments and basement structure underlying Sabl^ Island, tology, v. 19, no. 2, p. 129-148. Nova Scotia: Am. Assoc. Petroleum Geologists Bull., v. Applin, P. L., 1951, Preliminary report on buried pre- 49, no. 7, p. 959-965. Mesozoic rocks in Florida and adjacent states: U.S. Geol. Birch, W. B., and Dietz, F. T., 1962, Seismic refract'on inves­ Survey Circ. 91, 28 p. tigations in selected areas of Narragansett Bay, Rhode 1960, Significance of changes in thickness and lithofacies Island: Jour. Geophys. Research, v. 67, no. 7, p. 2813- of 'the Sunniland limestone, Collier County, Fla., in Short 2821. papers in the geological sciences: U.S. Geol. Survey Prof. Blaik, Maurice, Northrop, John, and Clay, C. S., 1^59, Some Paper 400-B, p. B209-B211. seismic profiles onshore and offshore Long Island, New Applin, P. L., and Applin, E. R., 1944, Regional subsurface York: Jour. Geophys. Research, v. 64, no. 2, p. 231-239. stratigraphy and structure of Florida and southern Geor­ Bonini, W. E., 1955, Seismic-refraction studies of geologic gia: Am. Assoc. Petroleum Geologists Bull., v. 28, no. 12, structure in North Carolina and South Carolina [abs.] : p. 1673-1753. Geol. Soc. America Bull., v. 66, no. 12, pt. 2, p. 1532-1533. 1947, Regional subsurface stratigraphy, structure and correlation of middle and early Upper Cretaceous rocks in 1957, Subsurface geology in the area of the Cape Fear Alabama, Georgia, and north Florida: U.S. Geol. Survey arch as determined by seismic-refraction measurements: Oil and Gas Inv. (Prelim.) Chart 26. Madison, Wisconsin- Univ. Ph.D. thesis, 218 p.; Ann Arbor, 1965, The Conianche Series and associated rocks in the Mich., Univ. Microfilms, Inc., Pub. 20,225. subsurface in central and south Florida: U.S. Geol. Survey Bonini, W. E., and Woollard, G. P., 1960, Subsurface geology of Prof. Paper 447, 86 p. North Carolina-South Carolina Coastal Plain fnm seismic Athearn, W. D., 1962a, Bathymetry and sediments, Part 1 of data: Am. Assoc. Petroleum Geologists Bull., v. 44, no. Bathymetric and sediment survey of the Tongue of the 3, p. 298-315. Ocean, Bahamas: Woods Hole Oceanog. Inst., Final Rept. Bower, M. E., 1962, Sea magnetometer surveys off southwestern to U.S. Naval Underwater Ordnance Sta., Newport, R.I., Nova Scotia, from Sable Island to St. Pierre Bank, and July 1962, Reference 62-25. over Scatari Bank: Canada Geol. Survey Paper C9-6, 13 p. 1962b, Bottom photographs, Part 2 of Bathymetric and Bridge, Josiah, and Berdan, J. M., 1951, Preliminary correla­ sediment survey of the Tongue of the Ocean, Bahamas: tion of the Paleozoic rocks from test wells in Florida and Woods Hole Oceanog. Inst., Final Rept. to U.S. Naval adjacent parts of Georgia and Alabama: U.S. Geol. Sur­ Underwater Ordnance Sta., Newport, R.I., July 1962, Ref­ vey open-file rept, Jan., 1951, 8 p.; Also in FloHLda Geol. erence 62-27. Survey Guidebook, Assoc. Am. State Geologists 44th Bailey, J. W., 1851, Microscopical examination of soundings, Ann. Mtg. Field Trip, 1952, p. 29-38 [1952]. made off the coast of the United States by the Coast Brown, M. V., Northrop, John, Frasetto, Roberto, and1 Grabner, Survey: Smithsonian Contr. Knowledge, v. 2, art. 2, 15 p. L. H., 1961, Seismic refraction profiles on the c?ntinental 1854, Examination of some soundings from the Atlantic shelf south of Bellport, Long Island, New York: Geol. Soc. Ocean: Am. Jour. Sci., 5th sen, v. 17, p. 176-178. America Bull., v. 72, no. 11, p. 1693-1706. Ball, Douglas, and Winer, A. S., 1958, Brandywine structure [Maryland] and underground natural gas storage for Brown. P. M., 1958, Well logs from the Coastal Plait of North Washington, D.C. [abs.]: Washington Acad. Sci. Jour., Carolina: North Carolina Dept. Conserv. ar«l Devel. v. 48, no. 4, p. 133. Div. Mineral Resources Bull. 72, 68 p. Barksdale, H. C., and others, 1958, Ground-water resources in Bucher, W. H., 1940, Submarine valleys and related geologic the tri-state region adjacent to the lower Delaware River problems of the North Atlantic: Geol. Soc. America Bull., [Delaware-New Jersey-Pennsylvania]: New Jersey Dept. v. 51, no. 4, p. 489-511. Conserv., Div. Water Policy and Supply Spec. Rept. 13, Bunce, E. T., and others, 1965, Ocean drilling on the continental 190 p. margin: Science, v. 150, no. 3697, p. 709-716. REFERENCES CITED 67

Burbank, W. S., 1929, The petrology of the sediment of the 1939, Scenery of Florida interpreted by a geologist: Gulf of Maine and Bay of Fundy: U.S. Geol. Survey Florida Geol. Survey Bull. 17, 118 p. open-file rept., 74 p. 1945, Geology of Florida: Florida Geol. Svrvey Bull. 29, Busby, R. F., 1962a, Preliminary data reports of bottom sedi­ 339 p. ments from the Tongue of the Ocean, Bahamas: U.S. 1959, Cenozoic echinoids of Eastern United States: U.S. Navy Hydrog. Office unpub. ms. 0-31-62, 21 p. [duplicated]. Geol. Survey Prof. Paper 321, 106 p. 1962b, Subaerial features on the floor of the Tongue of Cooke, C. W., and Munyan, A. C., 1938, Stratigraphy of Coastal the Ocean, Bahamas: U.S. Navy Hydrog. Office unpub. ms. Plain of Georgia: Am. Assoc. Petroleum Geologists Bull., 0-48-62, 13 p. v. 22, no. 7, p. 789-793. 1962c, Submarine geology of the Tongue of the Ocean, Cushman, J. A., 1936, Cretaceous and Late Tertiary Foraminif­ Bahamas: U.S. Navy Oceanog. Office Tech. Rept. 108, era, Part 4 of Geology and paleontology of the Georges 84 p. Bank canyons: Geol. Soc. America Bull., v. 47, no. 3, p. Bush, James, 1951, Rock from straits of Florida: Am. Assoc. 413-440. Petroleum Geologists Bull., v. 35, no. 1, p. 102-107. 1939, Eocene Foraminifera from the submarine cores off Carlson, R. O., and Brown, M. V., 1955, Seismic-refraction pro- the easteni coast of North America: Cushman Lab. Foram. flies in the submerged Atlantic Coastal Plain near Ambrose Research Contr., v. 15, pt. 3, no. 210, p. 49-7 . Lightship: Geol. Soc. America Bull., v. 66, no. 8, p. 969- 1946, Upper Cretaceous Foraminifera of tl^ Gulf coastal 976. region of the United States and adjacent areas: U.S. Geol. Carroll, Dorothy, 1963, Petrography of some sandstones and shales of Paleozoic age from borings in Florida: U.S. Survey Prof. Paper 206, 241 p. Geol. Survey Prof. Paper 454-A, p. A1-A15. 1948, Foraminifera from the Hammond weJl [Maryland] : Cederstrom, D. J., 1943, Deep wells in the Coastal Plain of Maryland Dept. Geology, Mines and Water P^sources Bull. Virginia: Virginia Geol. Survey Reprint Ser. 6,13 p. [Apr.]. 2, p. 213-267. 1945, Selected well logs in the Virginia Coastal Plain Cushman, J. A., and Cahill, E. D., 1933, Miocene Foraminifera north of James River: Virginia Geol. Survey Circ. 3, 82 p. of the Coastal Plain of the Eastern United States: U.S. Chadwick, G. H., 1949, Glacial molding of the Gulf of Maine Geol. Survey Prof. Paper 175, p. 1-50. [abs.] : Geol. Soc. America Bull., v. 60, no. 12, pt. 2, p. Dall, W. H., 1925, Tertiary fossils dredged off th« northeastern 1967; Also in Earth Sci. Digest, v. 4, no. 6, p. 15 [1950]. coast of North America: Am. Jour. Sci., 5th ser., v. 10, Charm, W. B., 1965, JOIDES, new inner space probe: Sea no. 57, p. 213-218. Frontiers, v. 11, no. 6, p. 368-378. Daly, R. A., 1936, Origin of submarine canyons: Am. Jour. Sci., Clark, W. B., Matthews, E. B., and Berry, E. W., 1918, The 5th ser., v. 31, no. 186, p. 401-420. surface and underground water resources of Maryland, Davis, C. H., 1849, A memoir upon the geological action of the including Delaware and the District of Columbia: Mary­ tidal and other currents of the ocean: Am. Acad. Arts and land Dept. Geology, Mines, and Water Resources Bull. Sci. Mem., new series, v. 4, pt 1, p. 117-156. 10, p. 169-564. Davis, W. M., 1896, The outline of Cape Cod: Am. Acad. Art.s Cloud, P. E., Jr., 1962, Environment of calcium carbonate and Sci. Proc., v. 31, p. 303-332. deposition west of Andros Island, Bahamas: U.S. Geol. 1934, Submarine mock valleys: Geog. Rev., v. 24, no. 2, Survey Prof. Paper 350, 138 p. p. 297-308. Cohee, G. V., chm., 1962, Tectonic map of the United States, deLaguna, Wallace, 1963, Geology of Brookhaven National exclusive of Alaska and Hawaii, by the United States Geo­ Laboratory and vicinity, Suffolk County, New York: U.S. logical Survey and the American Association of Petroleum Geol. Survey Bull. 1156-A, p. A1-A35. Geologists: U.S. Geol. Survey, scale 1:2,500,000. Cole, W. S., 1941, Stratigraphic and paleontologic studies of Dietz, R. S., 1963a, Origin of continental sloper preprint for wells in Florida; [No. 1] United Brotherhood of Carpenters presentation at American Association of Petroleum Geolo­ and Joiners of America, Power House well No. 2; Penin­ gists symposium, "Composition, structure, and history of sular Oil and Refining Company's J. W. Gory No. 1, with a continental shelves and slopes." Houston, Texas, March 2.1, description of a species of Foraminifera from another well: 1963: U.S. Navy Electronics Lab. Preprint, 23 p. Florida Geol. Survey Bull. 19, 91 p. 1963b, Collapsing continental rises an jrctualistic con­ 1944, Stratigraphic and paleontological studies of wells cept of geosynclines and mountain building: Jour. Geology, in Florida No. 3: Florida Geol. Survey Bull. 26, 168 p. v. 71, no. 3, p. 314-333. Cole, W. S., and Applin, E. R., 1961, Stratigraphic and geo­ Dorsey, A. L., 1948, Miocene Foraminifera from the Chesapeake graphic distribution of larger Foraminifera occurring in a group of southern Maryland: Maryland Dept. Geology, well in Coffee County, Georgia: Cushman Found. Foram. Mines, and Water Resources Bull. 2, p. 268-321. Research Contr., v. 12, pt. 4, p. 127-135. Douglass, R. C., 1960a, The foraminiferal genus Orbitolina in 1964, Problems of the geographic and Stratigraphic dis­ North America: U.S. Geol. Survey Prof. Pfper 333, 52 p. tribution of American middle Eocene larger Foraminifera: 19GOb, Revision of the family Orbitolinidae: Micropaleon- Am. Paleontology Bull., v. 47, no. 212, 48 p. tology, v. 6, no. 3, p. 249-270. Conkin, J. E., and Conkin, B. M., 1956, Nummoloculina in Drake, C. L., Ewing, Maurice, and Sutton, G. H., 1959, Con­ Lower Cretaceous of Texas and Louisiana: Am. Assoc. tinental margins and geosynclines the east coast of North Petroleum Geologists Bull., v. 40, no. 5, p. 890-896. America north of Cape Hatteras, in Ahems, L. H., and Cooke, C. W., 1936, Geology of the Coastal Plain of South others, eds., Physics and chemistry of th* earth: New Carolina: U.S. Geol. Survey Bull. 867, 196 p. York, Pergamon Press, v. 3, p. 110-199. 68 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Drake, C. L., Heirtzler, J., and Hirshman, Julius, 1963, Mag­ in the west Atlantic basins: Jour. Geophys. Research, v. netic anomalies off eastern North America: Jour. Geophys. 65, no. 9, p. 2849-2859. Research, v. 68, no. 18, p. 5259-5275. Ewing, W. M., Crary, A. P., and Rutherford, H. M., 1937, Drake, C. L., Worzel, J. L., and Beckmann, W. C., 1954, Gulf of Methods and results, Part 1 of Geophysical investigations Maine, Part 9 of Geophysical investigations in the emerged in the emerged and submerged Atlantic Coast? I Plain: and submerged Atlantic Coastal Plain: Geol. Soc. America Geol. Soc. America Bull., v. 48, no. 6, p. 753-802. Bull., v. 65, no. 10, p. 957-970. Ewing, W. M., Woollard, G. P., and Vine, A. C., 1939, Barneget Du Toit, A. L., 1940, An hypothesis of submarine canyons: Bay, New Jersey, section, Part 3 of Geophysical investiga­ Geol. Mag. [Great Britain], v. 77, no. 5, p. 395-404. tions in the emerged and submerged Atlantic Coastal Bardley, A. J., 1951, Structural geology of North America: Plain: Geol. Soc. America Bull., v. 50, no. 2, p.* 2f 7-296. New York, Harper and Row, 624 p. 1940, Cape May, New Jersey, section, Part 4 of Geophysi­ 1962, Structural geology of North America [2d ed.] : cal investigations in the emerged and submerged Atlantic New York, Harper and Row, 743 p. Coastal Plain: Geol. Soc. America Bull., v. 51, no. 12, pt. Bllis, C. H., and Tschudy, R. H., 1964, The Cretaceous mega- 1, p. 1821-1840. spore genus ArcelUtes Miner: Micropaleontology, v. 10, Ewing, W. M., Worzel, J. L., Steenland, N. C., and Press, Frank, 1950, Woods Hole, New York, and Cape May sec­ no. 1, p. 73-[79]. tions, Part 5 of Geophysical investigations in the emerged Emery, K. O., 1950, A suggested origin of continental slopes and submerged Atlantic Coastal Plain: Geol. Soc. America and of submarine canyons: Geol. Mag. [Great Britain], Bull., v. 61, no. 9, p. 877-892. v. 87, p. 102-104. Fenneman, N. M., 1938, Physiography of the Eastern United 1963, Oceanographic factors in accumulation of petro­ States: New York, McGraw-Hill Book Co., 714 p leum: World Petroleum Cong., 6th, Frankfort 1963, Proc., Field, R. M., and others, 1931, Geology of the Bahamas: Geol. sec. 1, p. 1-7. Soc. America Bull., v. 42, no. 3, p. 759-784. 1965a, Geology of the continental margin of Eastern Fuller, M. L., 1914, The geology of Long Island, New York: United States, in Whittard, W. F., and Bradshaw, R., eds., U.S. Geol. Survey Prof. Paper 82, 231 p. Submarine geology and geophysics: London, Butterworth's Gardner, F. J., 1964, Sun enhances Florida chances: Oil and Sci. Pub., Colston Papers 17, p. 1-17. Gas Jour., v. 62, no. 43, p. 175. 1965b, Characteristics of continental shelves and slopes: Gill, H. E., Seaber, P. R., Vecchioli, John, and Anderson, H. R., Am. Assoc. Petroleum Geologists Bull., v. 49, no. 9, p. 1963, Evaluation of geologic and hydrologic data from the 1379-1384. test-drilling program at Island Beach State P.^rk, New -1965c, Some potential mineral resources of the Atlantic Jersey: New Jersey Dept. Conserv. and Econ. Devel. and continental margin, in Geological Survey research 1965: U.S. Geol. Survey open-file rept, 55 p. U.S. Geol. Survey Prof. Paper 525-C, p. C157-C160. Gilluly, James, 1964, Atlantic sediments erosion ratef and the Emery, K. O., Merrill, A. S., and Trumbull, J. V. A., 1965, evolution of the continental shelf some speculations: Geology and biology of the sea floor as deduced from Geol. Soc. America Bull., v. 75, no. 6, p. 483-492. simultaneous photographs and samples: Limnology and Gorsline, D. S., 1963, Bottom sediments off the Southern United Oceanography, v. 10, no. 1, p. 1-21. States: Jour. Geology, v. 71, no. 4, p. 422-440. Emery, K. O., and Uchupi, Elazar, 1965, Structure of Georges Groot, C. R., and Groot, J. J., 1964, The pollen flora of Quater­ Bank: Marine Geology, v. 3, no. 5, p. 349-358. nary sediments beneath Nantucket Shoals: Am. Jour. Sci., Emery, K. O., Wigley, R. L., and Rubin, Meyer, 1965, A sub­ v. 262, no. 3, p. 488-493. merged peat deposit off the Atlantic coast of the United Gunter, Herman, 1946, Prospecting for petroleum ir Florida: States: Limnology and Oceanography, supp., v. 10, [no. 4], Florida Univ. Bur. Econ. and Business Research Econ. p. R97-R102. Leaflet, v. 5, no. 7, 4 p. Engelen, G. B., 1963, Indications for large scale graben forma­ 1950, Oil exploration in Florida during 1949: Oil and tion along the continental margin of Eastern United Gas Jour., v. 49, no. 7, p. 310-312. States: Geologie en Mijnbouw, v. 42, no. 3, p. 65-75. Heezen, B. C., 1962, The deep sea floor, in Runcorn, S. K., ed., Ericson, D. B., Ewing, Maurice, and Heezen, B. C., 1951, Deep- Continental drift: New York, Academic Press, p. 235-288. sea sands and submarine canyons [Atlantic Ocean]: Geol. Heezen, B. C., and Sheridan, R. E., 1966, Lower Cretaceous Soc. America Bull., v. 62, no. 8, p. 961-965. rocks (Neocomian-Albian) dredged from Blal'^ escarp­ 1952, Turbidity currents and sediments in North Atlan­ ment: Science, v. 154, no. 3757, p. 1644-1647. tic: Am. Assoc. Petroleum Geologists Bull., v. 36, no. 3, Heezen, B. C., Tharp, Marie, and Ewing, W. M., 1959, The p. 489-511. North Atlantic text to accompany the physiographic dia­ Ericson, D. B., Ewing, Maurice, Wollin, Goesta, and Heezen, gram of the North Atlantic, Part 1 of The floors of the B. C., 1961, Atlantic deep-sea sediment cores: Geol. Soc. oceans: Geol. Soc. America Spec. Paper 65, 122 p America Bull., v. 72, no. 2, p. 193-286. Herrick, S. M., 1961, Well logs of the Coastal Plain of Georgia: Ewing, John, Ewing, Maurice, and Leyden, Robert, 1966, Georgia Geol. Survey Bull. 70, 462 p. Seismic-profiler survey of Blake Plateau: Am. Assoc. Herrick, S. M., and Vorhis, R. C., 1963, Subsurface geology Petroleum Geologists Bull., v. 50, no. 9, p. 1948-1971. of the Georgia Coastal Plain: Georgia Geol. Survey Inf. Ewing, John, Luskin, Bernard, Roberts, A. C., and Hirshman, Circ. 25, 78 p. Julius, 1960, Sub-bottom reflection measurements on the Hersey, J. B., Bunce, E. T., Wyrick, R. F., and Dietz, F. T., Continental Shelf, Bermuda Banks, West Indies arc, and 1959, Geophysical investigation of the continental margin REFERENCES CITED 69

between Cape Henry, Virginia, and Jacksonville, Florida: Kay, Marshall, 1951, North American geosynclines: Geol. Soc. Geol. Soc. America Bull., v. 70, no. 4, p. 437-466. America Mem. 48, 193 p. Hess, H. H., 1933, Interpretation of geological and geophysical Kaye, C. A., 1964a, Outline of Pleistocene geolory of Martha's observations: U.S. Navy Hydrog. Office, Navy-Princeton Vineyard, Massachusetts, in Geological Survey research gravity expedition to the West Indies in 1932, p. 27-54. 1964: U.S. Geol. Survey Prof. Paper 501-C. p. C134-C139. 1960, The origin of the Tongue of the Ocean and other 1964b, Illinoian and early Wisconsin moraines of great valleys of the Bahama Bank, in Talwani, Manik, Martha's Vineyard, Massachusetts, in Geological Survey Worzel, L. J., and Ewing, Maurice, Gravity anomalies and research 1964: U.S. Geol. Survey Prof. P^oer 501-C, p. structure of the Bahamas: Caribbean Geol. Conf., 2d, C140-C143. Mayagiiez, Puerto Rico, 1959, Trans., p. 160-161. 1964e, Upper Cretaceous to Recent stratigraphy of Hoskins, Hartley, and Knott, S. T., 1961, Geophysical investi­ Martha's Vineyard, Massachusetts [abs.]: G-eol. Soc. Amer­ gation of Cape Cod Bay, Massachusetts, using the continu­ ica Spec. Paper 76, p. 91. ous seismic profiler: Jour. Geology, v. 69, no. 3, p. 330-340. Keller, Fred, Jr., Meuschke, J. L., and Alldredge, L. R., 1954, Hubbert, M. K., 1953, Entrapment of petroleum under hydro- Aeromagnetic surveys in the Aleutian, Marshall, and Ber­ dynamic conditions: Am. Assoc. Petroleum Geologists Bull., muda Islands: Am. Geophys. Union Tranr., v. 35, no. 4, v. 37, no. 8, p. 1954-2026. p. 558-572. Hughes, U. B., 1944, Developments in Southeastern United King, E. R., 1959, Regional magnetic map of Florida: Am. States in 1943: Am. Assoc. Petroleum Geologists Bull., v. Assoc. Petroleum Geologists Bull., v. 43, DO. 12, p. 2844- 28, no. 6, p. 801-805. 2854. Hull, J. P. D., and Teas, L. P., 1919, A preliminary report on King, E. R., Zietz, Isidore, and Dempsey, W. J., 1961, The the oil prospect near Scotland, Telfair County, Georgia: significance of a group of aeromagnetic profiles off the Georgia Geol. Survey, 23 p. eastern coast of North America, m Short papers in the Imlay, R. W., 1944, Correlation of Lower Cretaceous formations geologic and hydrologic sciences: U.S. GeoV Survey Prof. of the Coastal Plain of Texas, Louisiana, and Arkansas, Paper 424-D, p. D299-D303. 1944: U.S. Geol. Survey Oil and Gas Inv. (Prelim.) King, P. B., 1950, Tectonic framework of Soutl eastern United Chart 3. States: Am. Assoc. Petroleum Geologists Brll., v. 34, no. 4, International Hydrographic Bureau, 1958, Carte bathymetrique p. 635-671. des oceans: Internat. Hydrog. Bur. Map, 4th ed., sheet Al; 1959, The evolution of North America: F rinceton, N. J., 3d ed. [1937], sheet Bl. Princeton Univ. Press, 190 p. Jenny, W. P., 1934, Ergebnisse der. magnetischen vektoren- 1964, Further thoughts on tectonic framework of the methode in den Staaten Alabama und Florida, U.S.A.: Southeastern United States, in Lowry, C. D., ed., Tectonics Gerlands Beitrage zur Geophysik, v. 42, no. 4, p. 413-422. of the southern Appalachians: Virginia Polytech. Inst. Johnson, D. W., 1925, The New England-Acadian shoreline: Dept. Geol. Sci. Mem. 1, p. 5-31. New York, John Wiley and Sons, 608 p. Kornfeld, J. A., 1965, Sunoco-Felda discovery puts South 1938, Origin of submarine canyons: Jour. Geomorphol- Florida in the spotlight: World Oil, v. 160, no. 6, p. 172- ogy, v. 1, no. 2, p. 111-129; v. 1, no. 3, p. 230-243; v. 1, [176]. no. 4, p. 324-340; v. 2, no. 1, p. 42-68 [1939] ; v. 2, no. 2, Kuenen, P. H., 1950, Marine geology: New Yo~k, John Wiley p. 133-156 and 234-236 [1939]. and Sons, 568 p. 1939, The origin of submarine canyons, a critical review La Forge, Laurence, 1932, Geology of the Boston area, Massa­ of hypotheses: New York, Columbia Univ. Press, 126 p. chusetts: U.S. Geol. Survey Bull. 839, 105 p. Johnson, M. E., 1961, Thirty-one selected deep wells logs and Lee, C. S., 1951, Geophysical surveys on the I^hama Banks: map: New Jersey Geol. Survey Geol. Rept Ser., no. 2, Inst. Petroleum Jour., v. 37, no. 334, p. 633-657. 110 p. Lee, F. W., Swartz, J. H., and Hemburger, S. J., 1945, Magnetic Johnson, W. R., Jr., and Straley, H. M., 3d, 1935, An attempt survey of the Florida Peninsula: U.S. Bur. Mines Rept. to locate the boundaries of the Durham [North Carolina] Inv. 3810, 49 p. Triassic basin with a magnetometer: Am. Geophys. Union LeGrand, H. E., 1955, Brackish water and its structural im­ Trans., pt 1, p. 176-181. plications in the Great Carolina Ridge: Am. Assoc. Pe­ Johnston, J. E., Trumbull, J. V., and Eaton, G. P., 1959, The troleum Geologists Bull., v. 39, no. 10, p. 2020-2037. petroleum potential of the emerged and submerged Atlantic 1961, Summary of geology of Atlantic Coastal Plain: Coastal Plain of the United States: World Petroleum Am. Assoc. Petroleum Geologists Bull., v. 45, no. 9, p, Cong., 5th, New York 1959, Proc., sec. 1, p. 435-445. 1557-1571. Jordan, Louise, 1954, A critical appraisal of oil possibilities in Levorsen, A. I., 1954, Geology of petroleum: San Francisco, Florida: Oil and Gas Jour., v. 53, no. 28, p. 370-375. Calif., W. H. Freeman and Co., 703 p. Kasabach, H. F., and Scudder, R. J., 1961, Deep wells of the New Jersey Coastal Plain: New Jersey Geol. Survey Livingstone, D. A., 1964, The pollen flora of submarine sedi­ Geol. Rept. Ser., no. 3, 61 p. ments from Nantucket Shoals: Am. Jour. Sci., v. 262, no. 3, Katz, Samuel, and Ewing, Maurice, 1956, Atlantic Ocean basin, p. 479-487. west of Bermuda, Part 7 of Seismic refraction measure­ MacCarthy, G. R., 1936, Magnetic anomalies an

eastern Queens Counties, Long Island, New York: U.S. Rasmussen, W. C., and Slaughter, T. H., 1957, Ground-w.ater Geol. Survey Water-Supply Paper 1613-A, p. A1-A205. resources, in Water resources of Caroline, Ii>rchester, and Perlmutter, N. M., and Todd, Ruth, 1965, Correlation and Fo- Talbot Counties: Maryland Dept Geologr, Mines, and raminifera of the Monmouth Group (Upper Cretaceous), Water Resources Bull. 18, p. 447-465. Long Island, New York: U.S. Geol. Survey Prof. Paper Richards, H. G., 1945, Subsurface stratigraphy of Atlantic 483-1, 24 p. Coastal Plain between New Jersey and Georgia: Am. Petroleum Week, 1958, Will offshore drilling come to the At­ Assoc. Petroleum Geologists Bull., v. 29, no 7, p. 885-995. lantic coast?: Petroleum Week, v. 6, no. 6, p. 22-23. 1948, Studies of the subsurface geology and paleontology Pilkey, O. H., 1964, The size distribution and mineralogy of the of the Atlantic Coastal Plain: Acad. Nat Sci. Philadel­ carbonate fraction of the United States South Atlantic phia Proc., v. 100, p. 39-76. Shelf and upper slope sediments: Marine Geology, v. 2, 1950, Geology of the Coastal Plain of North Carolina: nos. 1-2, p. 121-136. Am. Philos. Soc. Trans., v. 40, pt 1, 83 p. Pooley, R. N., 1960, Basement configuration and subsurface 1954, Subsurface Triassic in eastern North Carolina: geology of eastern Georgia and southern South Carolina Am. Assoc. Petroleum Geologists Bull., v. 38, no. 12, p. as determined by seismic refraction measurements: Madi­ 2564-2565. son, Wisconsin Univ. M.S. thesis, 47 p. 1963, How good are New Jersey offshore oil prospects?: Pourtales, L. F., 1850, On the distribution of the foraminifera World Oil, v. 156, no. 6, p. 149-152. on the coast of New Jersey, as shown by the off-shore Roberson, M. I., 1964, Continuous seismic prowler survey of soundings of the Coast Survey: Am. Assoc. Adv. Sci. Proc., Oceanographer, Gilbert, and Lydonia subrrarine canyons, 2d Mtg., Charleston, S.C., p. 84-88. Georges Bank: Jour. Geophys. Research, v. 69, p. 4779- 1854, Extracts from letters of assistant L. F. Pourtales 4789. upon examination of specimens of bottom obtained in the Roberts, W. L., and Vernon, R. O., 1961, Florida more ex­ Gulf Stream by Lieutenants Commander Craven and Maf- tensive drilling might uncover big oil and gas-producing fit: U.S. Coast Survey Rept. of Superintendent, 1853, p. areas: Oil and Gas Jour., v. 59, no. 11, p. 215-219. 82-83. Rona, P. A., and Clay, C. S., 1966, Continuous seismic profiles 1871, Constitution of the bottom of the ocean off Cape of the continental terrace off southeast Florida: Geol. Soc. Hatteras: Boston Soc. Nat History Proc., v. 14, p. 58-59. America Bull., v. 77, no. 1, p. 31-43. 1872, The characteristics of the Atlantic sea bottom off Rude, G. T., 1925, St. Augustine [Florida] and its' oceanic the coast of the United States: U.S. Coast Survey Rept of spring: Geog. Soc. Philadelphia Bull., v. 23, no. 3, p. 85-91. Superintendent, 1869, App. 11, p. 220-225. Rusnak, G. A., Bowman, A. L., and Ostlund, H. G., 1963, Miami Powell, L. C., and Culligan, L. B., 1955, Developments in south­ natural radiocarbon measurements II: Radiocarbon, v. 5, eastern states in 1954: Am. Assoc. Petroleum Geologists p. 23-33. Bull., v. 39, no. 6, p. 1004-1014. Rusnak, G. A., and Nesteroff, W. D., 1964, Modem turbidltes Pratt, R. M., 1963, Bottom currents on the Blake Plateau: terrigenous abyssal plain versus bioclastic 1 7 sin, in Miller, Deep-Sea Research, v. 10, p. 245-249. R. L., ed., Papers in marine geology, Shepard commemora­ 1966, The Gulf Stream as a graded river: Limnology and tive volume: New York, MacMillan Co., p. 488-507. Oceanography, v. 11, no. 1, p. 60-67. Schlee, John, 1964, New Jersey offshore grav»l deposit: Pit Pratt, R. M., and Heezen, B. C., 1964, Topography of the Blake and Quarry, v. 57, no. 6, p. 80-81, 95. Plateau: Deep-Sea Research, v. 11, p. 721-728. Schlee, John, and Gerard, Robert, 1965, Cruise report and Pratt, R. M., and McFarlin, P. F., 1966, Manganese pavements preliminary core log M/V Caldrill I, 17 April to 17 May, on the Blake Plateau: Science, v. 151, no. 3714, p. 1080- 1965: JOIDES Blake Panel Rept, 64 p. [duplicated]. 1082. Schuchert, Charles, 1935, Historical geology of the Antillean- Press, Frank, and Beckmann, W. C., 1954, Grand Banks and Caribbean region: New York, John Wile^ and Sons, p. adjacent shelves, Part 8 of Geophysical investigations in 26-27, 243-248, 528-540. the emerged and submerged Atlantic Coastal Plain: Geol. Seaber, P. R., and Vecchioli, John, 1963, Stratigraphic section Soc. America Bull., v. 65, no. 3, p. 299-314. at Island Beach State Park, New Jersey, in Short papers Pressler, E. D., 1947, Geology and occurrence of oil in Florida: in geology and hydrology: U.S. Geol. Survey Prof. Paper Am. Assoc. Petroleum Geologists Bull., v. 31, no. 10, p. 475-B, p. B102-B105. 1851-1862. Shafer, J. P., and Hartshorn, J. H., 1965, The Quaternary of Prouty, W. F., 1946, Atlantic Coastal Plain floor and con­ New England, in Wright, H. E., Jr., and F ey, D. G., eds., tinental slope of North Carolina: Am. Assoc. Petroleum The Quaternary of the United States a review volume Geologists Bull., v. 30, no. 11, p. 1917-1920. for the VII Congress of the International Association for Purl, H. S., 1953, Cenozoic Ostracoda, Part 1 of Ostracoda Quaternary Research: Princeton, N. J., Princeton Univ. from wells in North Carolina taxomic comment: Jour. Press, p. 113-128. Paleontology, v. 27, no. 5, p. 750-752. Shaler, N. S., 1885, Report on the geology of Martha's Vine­ Puri, H. S., and Banks, J. E., 1959, Structural features of the yard: U.S. Geol. Survey 7th Ann. Rept, 1885-1886, p. Sunniland oil field, Collier County, Florida: Gulf Coast 304-306, 325-330, 340-347, 352-353. Assoc. Geol. Socs. Trans., v. 9, p. 121-130. 1889, The geology of Nantucket: U.S. Ge->l. Survey Bull. Puri, H. S., and Vernon, R. O., 1959, Summary of the geology 52, p. 28-47. of Florida and a guidebook to the classic exposures: Flor­ 1898, Geology of the Cape Cod district: U.S. Geol. Survey ida Geol. Survey Spec. Pub. no. 5, 255 p. '18th Ann. Rept., pt "2, p.- 497-593. 72 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF Shepard, F. P., 1932, Sediments of the continental shelves: Stetson, H. C., 1936, Geology, Part 1 of Geology and paleon­ Geol. Soc. America Bull., v. 43, no. 4, p. 1017-1039. tology of the Georges Bank canyons: Geol. Soc. America 1933, Submarine valleys: Geog. Rev., v. 23, no. 1, p. Bull., v. 47, no. 3, p. 339-366. 77-89. 1938, The sediments of the continental shelf off the east 1934, Canyons off the New England coast: Am. Jour. coast of the United States: Massachusetts Inst Technology Sci., 5th ser., v. 27, p. 24-36. and Woods Hole Oceanog. Inst., Papers of physical ocean­ 1948, Submarine geology [1st ed.] : New York, Harper ography and meteorology, v. 5, no. 4, 48 p. and Brothers, 348 p. -1949, The sediments and stratigraphy of the e«st coast 1951a, Composite origin of submarine canyons: Jour. continental margin, Georges Bank to Norfolk Canyon: Geology, v. 60, no. 1, p. 84-96. Massachusetts Inst. Technology and Woods Hole Oceanog. 1931b, Submarine canyons a joint product of rivers and Inst., Papers on physical oceanography and meteorology, submarine processes: Science, v. 114, no. 2949, p. 7-9. v. 11, no. 2, 60 p. 1963, Submarine geology [2d ed.] : New York, Harper Stetson, T. R., Squires, D. F., and Pratt, R. M., 19^, Coral and Row, 557 p. banks in deep water on the Blake Plateau: Am. Mus. Shepard, F. P., and Cohee, G. V., 1936, Continental shelf sedi­ Novitates, no. 2114, p. 1-39. ments off the mid-Atlantic states: Geol. Soc. America Bull., Stewart, H. B., Jr., and Jordan, G. F., 1964, Underwater sand v. 47, no. 3, p. 441-457. ridges on Georges Shoal, in Miller, R. L., ed., Papers in Shepard, F. P., Trefethen, J. M., and Cohee, G. V., 1934, Origin marine geology, Shepard commemorative volume: New of Georges Bank: Geol. Soc. America Bull., v. 45, no. 2, York, MacMillan Co., p. 102-114. p. 281-302. Stose, G. W., compiler, 1932, Geologic map of tb<> United Sheridan, R. E., Drake, C. L., Nafe, J. E., and Hennion, J., States: U.S. Geol. Survey Map, scale 1:2,500,000 1964, Seismic refraction measurements of the continental Stringfield, V. T., and Cooper, H. H., Jr., 1951, Geologic and margin east of Florida: Geol. Soc. America Program, 1964 hydrologic features of an artesian submarine sr^ng east Ann. Mtg., p. 183. of Florida: Florida Geol. Survey Inv. Rept 7, pt 2, p. 1966, Seismic-refraction study of continental margin east [61]-72. of Florida: Am. Assoc. Petroleum Geologists Bull., v. 50, Suter, Russell, deLaguna, Wallace, and Perlmutter, N. M., 1949, no. 9, p. 1972-1991. Mapping of geologic formations and aquifers of Long Is­ Shifliett, F. E., 1948, Eocene stratigraphy and Foraminifera of land, New York: New York Water Power and Control the Aquia Formation [Maryland and Virginia] : Maryland Comm. Bull. GW-18, 212 p. Dept. Geology, Mines, and Water Resources Bull. 3, 93 p. Swain, F. M., Jr., 1947, Two recent wells in Coastal Plain of Siple, G. E., 1946, Progress report on ground-water investiga­ North Carolina: Am. Assoc. Petroleum Geologists Bull., tions in South Carolina: South Carolina Resources, Plan­ v. 31, no. 11, p. 2054-2060. ning and Devel. Board Bull. 15, 116 p. 1951, Cenozoic Ostracoda, Part 1 of Ostracoda f^om wells Skeels, D. C., 1950, Geophysical data on the North Carolina in North Carolina: U.S. Geol. Survey Prof. Paper 234-A, Coastal Plain: Geophysics, v. 15, no. 3, p. 409-425; Oil and p. 1-58. Gas Jour., v. 48, no. 51, p. 120. 1952, Mesozoic Ostracoda, Part 2 of Ostracoda from wells Southeastern Geological Society, Mesozoic Committee, 1949, in North Carolina: U.S. Geol. Survey Prof. Paper 234-B, Mesozoic cross section A-A', Walton County to Monroe p. 59-93. County, Florida; B-B', Beaufort County, South Carolina, Swick, C. H., 1937, Gravity in southwestern Virginia: Am. to Highlands County, Florida; C-C', Toombs County, Assoc. Petroleum Geologists Bull., v. 21, no. 3, p. 333-339. Georgia, to Volusia County, Florida; D-D', Dixie County Tahvani, M. J., Worzel, J. L., and Ewing, Maurice, 10*50, Grav­ to Nassau County, Florida; E-E', Bullock County, Ala­ ity anomalies and structure of the Bahamas: Pr^rto Rico bama, to Franklin County, Florida: Southeastern Geol. Univ. Caribbean Geol. Conf., 2d, Trans., p. 156-161. Soc. Mesozoic Comm., cross sections, scale 1 inch to 10 Torphy, S. R., and Zeigler. J. M., 1957, Submarine topography miles. of eastern channel, Gulf of Maine: Jour. Geokrr, v. 65, Spangler, W. B., 1950, Subsurface geology of Atlantic Coastal p. 433-441. Plain of North Carolina: Am. Assoc. Petroleum Geologists Toulmin, L. D., 1941, Eocene smaller Foraminifera from Salt Bull., v. 34, no. 1, p. 100-132. Mountain Limestone of Alabama: Jour. Paleontology, v. Spangler, W. B., and Peterson, J. J., 1950, Geology of Atlantic 15, no. 6, p. 567-611. Coastal Plain in New Jersey, Delaware, Maryland, and 1955, Cenozoic geology of southeastern Alabamr, Florida, Virginia: Am. Assoc. Petroleum Geologists Bull., v. 34, and Georgia: Am. Assoc. Petroleum Geologists Bull., v. no. 1, p. 1-99. 39, no. 2, p. 207-235. Stephenson, L. W., 1926, Major features in the Atlantic and 1957, Notes on a peralkaline granite from Casl °s Ledge, Gulf Coastal Plain: Washington Acad. Sci. Jour., v. 16, Gulf of Maine: Am. Mineralogist, v. 42, nos. 11-12, p. no. 17, p. 460-480. 912-915. 1928, Structural features of the Atlantic and Gulf Trumbull, J. V., Lyman, John, Pepper, J. F., and T' omasson, Coastal Plain: Geol. Soc. America Bull., v. 39, no. 4, p. E. M., 1958, An introduction to the geology and mineral 887-899. resources of the continental shelves of the Amer'cas: U.S. 1936, Upper Cretaceous fossils from Georges Bank, Part Geol. Survey Bull. 1067, 92 p. 2 of Geology and paleontology of the Georges Bank can­ Tuttle, C. R., Alien, W. B., and Hahn, G. W., 1961, A seismic yons : Geol. Soc. America Bull., v. 47, no. 3, p. 367-^10. record of Mesozoic rocks on Block Island, Rhode Island, in REFERENCES CITED 73

Short papers in the geologic and hydrologic sciences: U.S. Van Bemmelen, R. W., 1956, The geochemical control of tec­ Geol. Survey Prof. Paper 424-C, p. C254-C256. tonic activity: Geologic en Mijnbouw, new series, v. 18, Uchupi, Elazar, 1963, Sediments on the continental margin off no. 4, p. 113-144. eastern United States, in Short papers on geology and Veatch, A. C., 1906, Outlines of the geology of Long Island, in hydrology: U.S. Geol. Survey Prof. Paper 475-C, p. C132- Veatch, A. C., Slichter, C. S., Bowman, Isaiah, Crosby, C137. W. O., and Horton, R. E., Underground water resources of 1964, Unusual hauls from Georges Bank: Oceanus, v. 10, Long Island, New York: U.S. Geol. Survey Prof. Paper 44, no. 4, p. 20-22. p. 15-52. 1965a, Map showing relation of land and submarine Veatch, A. C., and Smith, P. A., 1939, Atlantic submarine val­ topography, Nova Scotia to Florida: U.S. Geol. Survey leys of the United States and Congo submarine valley: Misc. Geol. Inv. Map 1-451, scale 1:1,000,000. Geol. Soc. America Spec. Paper 7, 101 p. 1965b, Basins of the Gulf of Maine, in Geological Survey Vernon, R. O., 1951, Geology of Citrus and Levy Counties, research 1965: U.S. Geol. Survey Prof. Paper 525-D, p. Florida: Florida Geol. Survey Bull. 33, 256 p. D175-D177. Verrill, A. E., 1878, Occurrence of fossiliferous Tertiary rocks 1966, Topography and structure of northeast channel, on the Grand Banks and Georges Bank: Am. Jour. Sci., Gulf of Maine: Am. Assoc. Petroleum Geologists Bull., v. 3d ser., v. 16, p. 323-324. 50, no. 1, p. 165-167. Vokes, H. E., 1948, Cretaceous mollusca from depths of 4,875 Uchupi, Elazar, and Tagg, A. R., 1966, Microrelief of the con­ to 4,885 feet in the Maryland Esso well, in Cretaceous and tinental margin south of Cape Lookout, North Carolina: Tertiary subsurface geology: Maryland Dept. Geology, Geol. Soc. America Bull., v. 77, no. 4, p. 427-430. Mines, and Water Resources Bull. 2, p. 126-151. Umbgrove, J. H. F., 1946, Origin of continental shelves: Am. Watkins, J. S., and Geddes, W. H., 1965, Magnetic anomaly Assoc. Petroleum Geologists Bull., v. 30, no. 2, p. 249-253. and possible erogenic significance of geologic structure of 1947, The pulse of the earth: The Hague, Martinus the Atlantic Shelf: Jour. Geophys. Research, v. 70, no. 6, Nijhoff, 2d ed., p. 97-143. p. 1357-1361. U.S. Coast and Geodetic Survey, 1945, Nautical chart: U.S. Wegener, Alfred, 1924, The origin of continents and oceans: Coast and Geod. Survey Chart 1107. New York, E. P. Button and Co., 212 p. 1957, Nautical chart: U.S. Coast and Geod. Survey Chart 5617. White, W. A., 1958, Some geomorphic features of central peninsular Florida: Florida Geol. Survey Geol. Bull. 41, 1959, Nautical chart: U.S. Coast and Geod. Survey Chart 92 p. 1113. 1961, Nautical charts: U.S. Coast and Geod. Survey Wigglesworth, Edward, 1934, Geology of Marthas Vineyard, in Charts 1000, 1003, 1109, and 1111. Woodworth, J. B., and Wigglesworth, Edward, Geography 1962, Nautical charts: U.S. Coast and Geod. Survey and geology of the region including Cape Cod, the Eliza­ Charts 1001, 1002, 1108, 1110, and 1112. beth Islands, Nantucket, Marthas Vineyard, No Mans U.S. Geological Survey, 1957, United States contour map: Land, and Block Island: Harvard Coll. Mus. Comp. Washington, D.C., U.S. Geol. Survey, scale 1:7,000,000. Zoology Mem., v. 52, p. 117-209. U.S. Navy Hydrographic"Office, 1948, Nautical chart: U.S. Navy Wigley, R. L., 1961, Bottom sediments of George Bank: Jour. Hydrog. Office Chart 1411. Sed. Petrology, v. 31, 110. 2, p. 165-188. 1949, Nautical chart: U.S. Navy Hydrog. Office Chart Willmore, P. L., and Tolmie, R., 1956, Geophysical observations 6610. on the history and structure of Sable Is1 and in Ocean 1951, Contoured position plotting sheets: U.S. Navy floors around Canada: Royal Soc. Canada Trans., 3d ser., Hydrog. Office Sheets BC-0510N, BC-0608N, BC-0609N. v. 50, p. 13-20. BC-0610N, BC-0706N, BC-0707N, BC-0708N, BC-0805N, Woodworth, J. B., 1934a, Geology of Cape Cod, in Woodworth, BC-0806N, and BC-0807N. J. B., and Wigglesworth, Edward, Geography and geology 1952a, Nautical chart: U.S. Navy Hydrog. Office Chart of the region including Cape Cod, the Elizabeth Islands, 5617. Nantucket, Marthas Vineyard, No Mans Lpnd, and Block 1952b, Contoured position plotting sheets: U.S. Navy Island: Harvard Coll. Mus. Comp. Zoology Mem., v. 52, Hydrog. Office Sheets BC-0611N and BC-0612N. p. 237-306. 1955, Contoured position plotting sheet: U.S. Navy 1934b, Geology of Block Island, in Wocdworth, J. B., Hydrog. Office Sheet BC-0804N. and Wigglesworth, Edward, Geography and geology of the 1962a, Contoured position plotting sheets: U.S. Navy region including Cape Cod, the Elizabeth Islands, Nan­ Hydrog. Office Sheets BC-0904N and BC-0905N. tucket, Marthas Vineyard, No Mans Land, and Block Is­ 1962b, Catalog of nautical charts and publications: land: Harvard Coll. Mus. Comp. Zoology Mem., v. 52, p. Washington, D.C., U.S. Navy Hydrog. Office Pub. I-X, pt. 1, 20 p.; pt. 2, 52 p. 209-219. 1934c, Geology of Nantucket and adjacent islands, in U.S. Navy Oceanographic Office, 1962, A marine magnetic sur­ vey off the east coast of the United States: U.S. Navy Woodworth, J. B., and Wigglesworth, Edward, Geography Oceanog. Office Tech. Rept. Proj. N-20, 29 p. and geology of the region including Cape Cod, the Eliza­ Upham, Warren, 1894, The fishing banks between Cape Cod beth Islands, Nantucket, Marthas Vineyard, No Mans and Newfoundland: Am. Jour. Sci., 3d ser., v. 47, p. 123- Land, and Block Island: Harvard Coll, Mus. Comp. 129. Zoology Mem., v. 52, p. 93-116. 74 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

Woodworth, J. B., and Wigglesworth, Edward, 1934, Geography Virginia and Florida: Madison, Wisconsin Univ. Dept. and geology of the region including Cape Cod, the Eliza­ Geology Tech. Rept, Office Naval Research Contract beth Islands, Nantucket, Marthas Vineyard, No Mans N70NR-2851a, 95 p. Land, and Block Island: Harvard Coll. Mus. Comp. Woollard, G. P., Ewing, Maurice, and Johnson, M., If38, Geo­ Zoology Mem., v. 52, 338 p. physical investigations of the geologic structure of the Woollard, G. P., 1939, The geological significance of gravity Coastal Plain: Am. Geophys. Union Trans., v. ]

Well Total Notes No. Name (feet)

Alabama

Sec. 18, T. 14 N., R. 22 310 1,725 Pre-Mesozoic_ Electric log available. Gholston 1. E., Bullock County. Top of pre-Mesozoic granite 1,700 ft. 2 __ ___ Capital Oil & Gas, Sec. 22, T. 13 N., R. 21 430 2, 523 Electric log available. Pickett 1. E., Bullock County. Top of pre-Mesozoic granite 2,495 ft. 3 ____ W. B. Hinton, Sec. 14, T. 9 N., R. 26 504 5,556 Triassic or pre- Electric log available. Creel 1. E., Barbour County. Mesozoic. Top of pre-Cretaceous rocks 4,395 ft.

Bahama Islands

BA-1 ______Bahama California Lat 23°49'24" N., long ______18, 906 Offshore. No data re­ Oil Cay Sal 4 80°12'24" W. leased, May 19C<5. well 1. 2______Bahamas Oil Lat 24°52'37.2" N., long 20 14, 585 Lower Cretaceous Electric log from 6,503 Andros Island 1. 78°01'54.7" W., to 10,670 ft only. Stafford Creek, Andros Island. 3______Harrisville Eleu- Hatchet Bay, approx 123 730 Miocene(?) ______No electric log available. thera Island 2. lat 25°20'45' rN., long Tested salt water 200 76°28'30" W., to 490 ft in Miocene. Eleuthera Island. Water level 123 ft below surface.

Delaware

About 4.5 miles north- 65 365 water well 1. west of Newcastle on 352 ft. State Highway 41, Newcastle County. 2 ____ U.S. Army Fort Near Delaware City, 10 762 Lower Cretaceous _ Dupont water Newcastle County. well. 3___._- Town of Middle- Middletown, Newcastle 65 1,478 Probably reached bed­ town water well. County. rock at total depth, 2,312 well 1. east of Smyrna, rocks 2,290 ft. Newcastle County. 5______U.S. Air Force Base Near Dover, Kent 27 1,422 test well JE 32-4. County. 6______Town of Lewes Lewes, Sussex County __ 10 1,080 water well. 7______Sun Oil Townsend 4 miles southeast of 43 2,600 Upper Cretaceous (Apple Orchard) Bridgeville, Sussex D-6. County. 8______Continental Oil 4 miles southeast of 42 3,012 Townsend 1. Bridgeville, Sussex County. 9 _____ Sun Oil R. Russell 5.2 miles southeast of 36 2,674 1. Bridgeville, Sussex County.

Florida

Jeffreys Abbott !____ Sec. 19, T. 3 N., R. 32 202 7, 513 Lower Cretaceous. Electric log avail?ble. W., Escambia County. Zach Brooks_Drilling Sec. 31, T. 2 S., R. 31 33 12,512 _____do__----__._- Do. Cald"" well- Gar vin W., Escambia County. unit 1. Mobil Oil, St. Sec. 35, T. 4 N., R. 30 120 12,523 Do. Regis Paper 1. W., Santa Rosa County. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 77 TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported 1 Totes No. Name (feet)

Florida Continued

FL-4 _____ Sunnyland Oil, Sec. 24, T. 5 N., R. 29 250 6,665 Lower Cre­ Electric log' available. Nowling 1. W., Santa Rosa taceous (?). County. 5 ____ Humble Oil & Re­ Sec. 17, T. 2 S., R. 28 26 7,505 Lower Cretaceous. Do. fining, State of W., Pensacola Bay, Florida lease 833 Santa Rosa County. well 1. 6. _ _ _ _ Sinclair Oil & Gas Sec. 7, T. 1 N., R. 27 35 6,950 Lower Cre­ Do. Boland 1. W., Santa Rosa taceous (?). County, 7 _ _._ Haden McCort !__-_ Sec. 30?, T. 4 N., R. 24 254(?) 6,326 Lower Cretaceous, Do. W., Okaloosa County. 8_ _ __ Hawkins Kelly 1 _ Sec. 18, T. 2 S., R. 22 27 6,250 do No electric log available. W., Cobbs Point, Okaloosa County. 9 __ _ _ Hawkins Coffeein 1__ Sec. 12, T. 2 S., R. 21 W. 14 6,010 do Do. Fourmile Point, Walton County. 10 __ __ Sun Oil Belcher 4 __ Sec. 25, T. 4 N., R. 21 244 5,220 Lower Cretaceous. Electric log- available. W., Walton County. 11 _ __ Pan American Sec. 9, T. 1 S., R. 18 111 11, 947 Electric log available. Petroleum W., Walton County. Top of p~e-Mesozoie Sealy 1. rhyolite, 11,930ft. 12______Byers Oil Sealy 1__ Sec. 12, T. 2 S., R. 18 W., 37 5, 475 Lower Cretaceous. Electric lof available. Walton County. 13_____ Hunt Oil Linton 1_ Sec. 30, T. 3 N., R. 17 104 6,503 Do. W., Walton County. 14______Southeastern Ex- Sec. 18, T. 6 N., R. 17 159 8,521 Do. pi oration Hobbs- W., Holmes County. Gillis 1. 15______Breeding Coats !____ Sec. 25, T. 7 N., R. 15 202 4, 107 Do. W., Holmes County. 16__--__ Magnolia Petroleum Sec. 21, T. 3 S., R. 15 7 7,003 Do. State block 4-B W., Bay County. well 1. 17______Temple Oil Moore 1_ Sec. 27, T. 1 S., R. 15 60 6,021 _____do_--_-____ Do. W., Bay County. 18---_-_ Chipley Oil & Gas Sec. 27, T. 4 N., R. 13 198 4,912 _____do___-______No electric log run. Dekle 1. W., Washington County. 19____ Humble Oil & Sec. 8, T. 5 N., R. 11 W., 128 9,245 Paleozoic.-______Electric log available. Refining Tindel 1. Jackson County. Top of Paleozoic sandstone and shale 8,440 ft. 20______Hammond Gran- Sec. 15, T. 5 N., R. 9 W., 107 5,022 Triassic(?)____ No electric log run. berry 1. Jackson County. 21 ______Pure Oil Interna­ Sec. 31, T. 1 S., R. 10 107 5, 096 Lower Cretaceous. Electric log available. tional Paper 2. W., Calhoun County. 21A___ Gulf Coast Drilling Sec. 4, T. 5 S., R. 7 W., 49 10,011 ___._do--__-__._- Do. and Exploration Liberty County. U.S.A. 1. 22-_-_._ Pure Oil Hopkins 1_. Sec. 22, T. 6 S., R. 9 W., 32 8,708 ..-..do. Do. Gulf County. 23 ______Magnolia Petroleum Lat 29°41'18* N., long 10 7,021 _--._do. Do. State block 5-B 85°07'13* W., Franklin well 1-A. County. 24______California State of Sec. 7, T. 9 S., R. 5 W., 26 7,031 -__-_do-______Offshore. E'metric log Florida lease St. George Sound, available. 224-A well 1. Franklin County. 25__-___ California State of Lat 29°47'03* N., long 35 10,566 ...-.do. Do. Florida lease 84°22'51* W., Franklin 224-A well 2. County. 26______Pure Oil St. Joe Sec. 34, T. 6 S., R. 4 W., 21 4, 787 ___-_do______Electric log available. Paper 2. Franklin County. 27______Hughes Oil Sec. 6, T. 2 N., R. 5 W., 296 4,222 _---_do__-.--_-_._ Do. McDonald 1. Gadsden County. 28_ _ _ _ . _ Oles-Nayler Florida Sec. 35, T. 2 N., R. 3 W., 177 4,240 __--_do-_-__.__-__ Do. Power 1. Gadsden County. 29_ _ _ _ . _ Central Florida Oil Sec. 11, T. 2 S., R. 1 E., 50 3, 755 Upper Cretaceous. No electric log run. & Gas Rhodes 1. Leon County. 78 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Florida Continued

FL-30___.... Ravelin-Brown Sec. 14, T. 3 S., R. 1 E., 28 5,766 Triassic (?) ______Electric log available. Philips 1. Wakulla County. 31___.._ Coastal Petroleum Sec. 1, T. 2 S., R. 3 E., 51 7,913 _ __do______Electric log available. Larsh 1. Jefferson County. Top of Triass'r;(?) red beds and sills 7,909 ft. 32_.__ __ South State Oil Sec. 17, T. 2 N., R. 5 E., 220 3,838 Upper Cretaceous No electric log available. Miller & Gossard Jefferson County. 1. 33.__- __ Hunt Oil Gibson 2___ Sec. 6, T. 1 S., R. 10 E., 107 5,385 Paleozoic______Electric log available. Madison County. Top of igneous rock 4,589 ft. Top of Pale­ ozoic black shale 4,628 ft. 34. Humble Oil & Re­ Sec. 12, T. 5 S., R. 6 E., 36 6,254 Triassic(?). Electric log available. fining Hodges 1. Taylor County. Top of Triass^(?) diabase gabbro 6,153 ft. 35. Gulf Oil Brooks- Sec. 18, T. 4 S., R. 9 E., 96 5,243 _-.-_do.-_. Electric log available. Scanlon, State Taylor County. Top of Triass'X?) block 33 well 1. diabase gabbro 5,200 ft. 36. Gulf Oil Brooks- Sec. 9, T. 8 S., R. 9 E., 41 5,517 _--__do _ Electric log available. Scanlon, State Taylor County. Top of Triass^f?) block 42 well 1. diabase gabbro 5,438 ft. 37. Gulf Oil Brooks- Sec. 36, T. 5 S., R. 10 87 4,512 Paleozoic_. Electric log available. Scanlon, State E., Lafayette County. Top of Paleozoic block 49 well 1. quartzitic sandstone 4,505 ft. 38____ Sun Oil Crapps !____ Sec. 25, T. 6 S., R. 12 70 4,133 _--__do- Electric log available. E., Lafayette County. Top of Paleoroic quartzitic sandstone and shale 4,030 ft. 39. Stanolind Oil & Gas Sec. 5, T. 11 S., R. 11 33 7, 510 ___do. Electric log available. Perpetual Forest E., Dixie County. Top of Paleoroic 1. quartzitic sandstone 5,228 ft. 40. Sun Oil Adams 1_ _ Sec. 15, T. 9 S., R. 15 93 3,753 _..do. Electric log available. E., Gilchrist County. Top of Paleoroic quartzitic sandstone and shale 3,588 ft. 41____ Sun Oil Odom 1. . Sec. 31, T. 5 S., R. 15 73 3,161 ___do. Electric log available. E., Suwannee County. Top of Paleozoic black shale 3,040 ft 42. Fields-Randall Sec. 6, T. 2 S., R. 13 119 3,833 _____do- Electric log available. Crawley 1. E., Suwannee County. 43. Sun Oil Tillis 1. . Sec. 28, T. 2 S., R. 15 162 3,572 ___do. Electric log available. E., Suwannee County. Top of Paleoroic black shale 3,500 ft. 44. Sun Oil Sapp 1-A Sec. 24, T. 2 S., R. 16 138 3,311 ___do. Electric log available. E., Columbia County. Top of Paleozoic black shale 3,303 ft. 45. Humble Oil & Re­ Sec. 22, T. 1 N., R. 17 141 4,444 ___do_ Electric log available. fining Cone 1. E., Columbia County. Top of Paleozoic black shale 3,482 ft 46. Hunt Oil Hunt 1_ _ Sec. 21, T. 1 N., R. 20 130 3,349 __--_do. Electric log available. E., Baker County. Top of Paleoroic quartzitic sandstone 3,342 ft. 47. Tidewater Associ­ Sec. 15, T. 6 S., R. 20 141 3, 167 .-_do. Electric log available. ated Oil Wiggins E., Bradford County. Top of Paleoroic 1. quartzitic sandstone and shale 3,167 ft. 48_ Tidewater Associ­ Sec. 33, T. 7 S., R. 19 168 3,220 ___do. Electric log available. ated Oil Parker 1. E., Alachua County. Top of Paleozoic quartzitic sandstone and shale 3,1?') ft. 49. The Texas Co. Sec. 16, T. 11 S., R. 19 77 3, 527 Lower Cretaceous Electric log available. Creighton 1. E., Alachua County. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 79 TABLE 1. Records of selected wells along the Atlantic coast Continued

WeU Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Florida Continued

FL-50. Tidewater-Associ- Sec. 24, T. 9 S., R. 21 132 3,228 Paleozoic. Electric log available. ated Oil Phifer 1. E., Alachua County. Top of Paleozoic quartflitic sandstone and shale 3,217 ft. St. Mary's River Oil Sec. 19, T. 4 N., R. 24 110 4,824 _____do.._ No electric l->g run. Top Hilliard Turpen- E., Nassau County, of Paleozoic black tine 1. shale and diabase 4,636 ft. 52. Humble Oil & Refin- Sec. 4, T. 6 S., R. 25 E., 115 5,862 _.__.do___ Electric log available. ing Foremost Clay County. Top of Paleozoic Properties 1. quartzitic sandstone and shale 3,725 ft. 53. Sun Oil Roberts 1-A. Sec. 19, T. 9 S., R. 25 E., 206 3, 328 _-_._do__. Electric log available. Putnam County. Top of Paleozoic quartzitic sandstone 3,320 ft. 54__ __ Sun Oil Westbury 1. Sec. 37, T. 11 S., R. 26 32 3,892 Pre-Mesozoic. Electric log available. E., Putnam County. Top of pre-Mesozoic volcanic rocks 3,873 ft. Humble Oil & Re­ Sec. 8, T. 11 S., R. 28 31 4,632 _____do__... Electric log available. fining Campbell 1. E., Flagler County. Top of pre-Mesozoic volcanic rocks 4,588 ft. Grace Drilling Retail Sec. 2, T. 15 S., R. 30 45 5, 424 -....do...... Electric log available. Lumber 1. E., Volusia Country. Top of pre-Mesozoic rhyolite 5,403 ft. Sun Oil Powell Sec. 11, T. 17 S., R. 31 48 5, 958 -__-_do___-._ Electric log available. Land 1. E. Volusia County. Top of pre-Mesozoic hornblend-s diorite 5,910 ft. Coastal Petroleum Sec. 16, T. 15 S., R. 13 14 5,850 Paleozoic. Electric log available. Ragland 1. E., Levy County. Top of Paleozoic black shale 5,810 ft. 59. Sun Oil Goethe 1_. Sec. 31, T. 14 S., R. 17 34 3,997 ___do... Electric log available. E., Levy County. Top of Paleozoic quartzitic sandstone 3,960 ft. Humble Oil & Re­ Sec. 19, T. 16 S., R. 17 58 4, 609 Lower Cretaceous. Electric log available. fining Robinson 1. E., Levy County. 61. J. S. Cosden Lawson Sec. 25, T. 13 S., R. 20 195 4,334 Paleozoic______No electric log run. Top 1. E., Marion County. of Paleozoic quartzitic sandstone 3,660(?) ft. 62. OcalaOil York 1. _ Sec. 10, T. 16 S., R. 20 80 6, 180 No electric log run. Top E., Marion County. of Paleozoic quartzitic sandstone 4,100(?) ft. Sun Oil Parker !___. Sec. 24, T. 14 S., R. 22 79 3, 845 Lower Ordovi- Electric log available. E., Marion County. cian(?). Sun Oil Camp !__._. Sec. 16, T. 16 S., R. 23 74 4, 637 Pre-Mesozoic _. Electric log available. E., Marion County. Top of pre-Mesozoic volcanic neks 4,615 ft. Dundee Petroleum Sec. 24, T. 20 S., R. 22 77 3, 090 Upper Cretaceous. No electric log available. Bushnell 1. E., Sumter County. Ohio Oil Hernasco 1. Sec. 19, T. 23 S., R. 18 47 8,472 Electric log available. E., Hernando County. Top of Paleozoic quartzitic sandstone 7,720 ft. Oil Development of Sec. 17, T. 24 S., R. 25 120 6, 120 Pre-Mesozoic. Electric log available. Florida Arnold 1. E., Lake County. Top of pre-Mesozoic granite 6, 103 ft. Warren Petroleum Sec. 21, T. 23 S., R. 31 100 6, 589 _____do_... Electric log available. Terry 1. E., Orange County. 69 Hill Oldsmar !_____ Sec. 19, T. 28 S., R. 17 8 3,255 Paleocene. No electric log run. E., Hillsborough County. Coastal Petroleum Sec. 7, T. 30 S., R. 17 13 11, 507 Lower Cretaceous. Electric log available. Wright 1. E., Pinellas County. Humble Oil & Sec. 7, T. 31 S., R. 22 112 10,129 Pre-Mesozoic_-__- Electric log available. Refining Jameson E., Hillsborough Top of pre-Mesozoic 1. County. volcanic rocks 10,010 ft. 80 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

TABLE 1. Records of selected wetts along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Florida Continued

FL-72___ _ Pioneer Oil Sec. 28, T. 30 S., R. 25 88 4, 540 Upper Cretaceous- No electric log a vailable. Herscher- Yarnell E., Polk County. 1. 73____ Humble Oil & Sec. 10, T. 27 S., R. 34 62 8,049 Pre-Mesozoic___-_ Electric log available. Refining Carroll E., Osceola County. Top of pre-Mesozoic 1. biotite granite 8,035 ft. 74....._ Humble Oil & Sec. 12, T. 31 S., R. 33 86 8, 798 ___do______Electric log available. Refining Hay man E., Osceola County. Top of pre-Mesozoic 1. rhyolite 8,740 ft. 75__ _ Amerada Petroleum Sec. 28, T. 31 S., R. 35 60 9, 488 _____do.______Electric log available. Mitchell 1. E., Indian River County. 76____ Magnolia Petroleum Sec. 11, T. 35 S., R. 19 70 11,228 Lower Cretaceous. Do. Schroeder- E., Manatee County. Manatee 1. 77_... Humble Oil & Sec. 23, T. 35 S., R. 23 83 11,934 Pre-Mesozoic.. ____ Electric log available. Refining Keen 1. E., Hardee County. Top of pre-Mesozoic volcanic rocks 11,828ft. 78_____. Amerada Petroleum Sec. 5, T. 36 S., R. 34 54 10, 838 _ _ _ _ _do______Electric log available. Swenson 1. E., Okeechobee County. 79____ Amerada Petroleum Sec. 19, T. 36 S., R. 40 32 12, 748 _ _ .do___ _. _ _ Electric log available. Cowles Magazine E., St. Lucie County. Top of pre-Mesozoic 2. igneous rocks 12,680 ft. Top of Fort Fr3rce Formation of Late Jurassic or Early Cretaceous ajre 10,460 ft. 80___ Humble Oil & Sec. 34, T. 38 S., R. 29 114 12,985 __.__do. ______Electric log available. Refining Carlton E., Highlands County. Top pre-Mesozoic Estate 1. rhyolite and I ^.salt 12,618 ft. 81 _ ___ Gulf Oil Vanderbilt Sec. 35, T. 41 S., R. 21 22 12, 725 Lower Cretaceous. Electric log available. 1. E., Charlotte County. 82______Humble Oil & Sec. 17, T. 42 S., R. 23 20 13,304 _____do. Do. Refining Lowndes- E., Charlotte County. Treadwell 1-A. 83 ______Amerada Petroleum Sec. 1, T. 41 S., R. 30 (?) 10,993 _____do. Do. Lykes Bros. 1. E., Glades County. 84__ __ Coastal Petroleum Sec. 25, T; 42 S., R. 33 14 13, 440 Upper Jurassic or Electric log available. Tiedke 1. E., Glades County. Lower Top of Fort Pierce Cretaceous. Formation of Late Jurassic or Early Cretaceous age 12,933 ft. 85_ _ _ _ Amerada Petroleum Sec. 34, T. 41 S., R. 39 E., 36 11,030 Lower Cretaceous _ Electric log ava''able. Southern States Palm Beach County. lease 3 4 well 1. 86_ _ _ _ Humble Oil & Re­ Sec. 35, T.43S..R. 40 E., 34 13, 375 Upper Jurassic or Electric log available. fining Tucson 1. Palm Beach County. Lower cretace­ Top of Upper Jurassic ous. or Lower Cretaceous rocks 13,180 ft. 87. _ _ _ _ _ Humble Oil & Refin­ Sec. 2, T. 48 S., R. 35 E., 31 12,800 Lower Cretaceous _ Oil staining in upper part ing State of Florida Palm Beach County. of Lower Cretaceous. lease 1004 well 1. 88- _ _ _ _ California, State of Lat26°4l'07"N.,long 39 13,975 __._.do. Electric log run. Florida lease 224- 82°19'02" W., Boca Bwelll. Grande area, Lee County. 89_ _ _ _ California, State of Lat 26°43'06" N., long 12,600 _____do. Do. Florida lease 224- 82°17'12" W., Boca B well 2. Grande area, Lee County. 90__ _ _ Humble Oil & Refin­ Sec. 23, T. 45 S., R. 24 24 12,877 _.___do_ Electric log available. Oil ing Kirchoff 1. E., Lee County. show at 11,819 to 11,928ft. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 81 TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported No*<« No. Name (feet)

Florida Continued

FL-91. Gulf Refining Con­ Sec. 27, T. 45 S., R. 26 E., 45 12, 865 Lower Cretaceous _ Electric log available. solidated Naval Lee County. Tested 28° API gravity Stores 1. oil at 11,748 to 11,799 ft. 92.. Humble Oil & Refin­ Sec. 16, T. 46 S., R. 27 E., _--_ 11,893 ____-do.-___-_____ Electric log available. ing Consolidated Lee County. Naval Stores 1. 93- Sun Oil Red Cattle Sec.32, T.45S., R.29E., 11,485 _.__-do. ______Electric log r>n. Oil pro­ 2. Felda field, Hendry duced from 11,471 to County. 11,485ft. 94.. Humble Oil & Refin­ Sec. 30, T. 48 S., R. 30 E., 34 13,512 _.__.do. ______Electric log available. Oil ing Gulf Coast Sunniland field, Collier produced f~om 11,613 Realties 2. County. to 11,626 fi. 95. Humble Oil & Refin­ Sec. 27, T. 50 S., R. 26 E., 25 12,516 _____do__.__.___ Electric log available. ing Collier 1. Collier County. 96. McCord Oil Damoco Sec. 31, T. 53 S., R 35 E., 17 11,885 _-._.do. ______Do. 1. Dade County. 97. Commonwealth Oil, SE^ Sec. 16, T. 54 S., R. 24 11,557 _____do______Electric log available. Oil Wiseheart 1. 35 E., Forty-Mile Bend produced from 11,322 to field, Dade County. 11,339ft. Abandoned 1955. 98.. Humble Oil & Refin­ Sec. 30, T. 55 S., R. 36 E., 15 11,794 ___do.___.____ Electric log available. ing 1.1. P.I. Dade County. 99.. Coastal Petroleum Sec. 25, T. 55 S., R. 37 E., 25 11,520 _____do.--_-_.____ Do. I. I. F. 1. Dade County. 100. East Coast Oil & Sec. 12, T. 55 S., R. 40 E., 13 5, 535 Paleocene.__.____ No electric Hg. Natural Gas War- Dade County. nrjf»lr 1 101. Gulf Oil State Model Lat25°13'35",long 12 6, 030 Upper Cretaceous _ Electric log available. Land "C" 1. 80°40'55", T.60S., R. 35 E., Dade County. 102. Peninsular Oil & Re­ Sec. 6, T. 55 S., R. 34 E., 14 10,006 Lower Cretaceous '.* Do. fining Gory 1. Monroe County. 103. Republic Oil-Robin­ Sec. 29, T. 59 S., R. 40 E., 23 12,051 Upper Jurassic or Electric log available. Top son State 1. Mpnroe County. Lower Creta­ of Fort Pierce Forma­ ceous. tion of Late Jurassic or Early Cretaceous age 11,878ft. 104. Sinclair Oil & Gas Sec. 24, T. 59 S., R. 40 20 11,968 Upper Jurassic or Electric log available. H. R. Williams 1. E., Key Largo, Lower Monroe County. Cretaceous. 105. Gulf Oil State of Lat 25°0'53" N., long 21 12,631 Lower Cretaceous. Offshore. Electric log Florida lease 826- 8r5'54" W., Oxfoot available. G well 1. Bank, Monroe County. 106. Coastal Petroleum Sec. 32, T. 62 S., R. 38 15 7,559 _.--_do_.__--_ Electric log available. State of Florida E., Plantation Key, Live oil shows at lease 363 well 1. Monroe County. 6,702 ft. 107. Florida East Coast Sec. 10, T. 66 S., R. 32 .-__ 2,310 Lower Eocene. No electric log run. Railway, E., Key Vaca, Monroe Marathon 1. County. 108. California, State of Sec. 1, T. 67 S., R. 29 E. 24 6,033 Upper Electric log rot released, Florida lease 1011 E., Big Pine Key, Cretaceous. May 1963 tract 2 well 1. Monroe County. 109. Gulf Oil State of Sec. 2, T. 67 S., R. 29 23 15, 455 Upper Jurassic or Electric log available. Florida lease 373 E., Big Pine Key, Lower Top of Fo~t Pierce well 1. Monroe County. Cretaceous. Formation of Late Jurassic or Early Cretaceous age 14,340 ft. 110. Gulf Refining State Sec. 15, T. 67 S., R. 27 23 6, 100 Upper Cretaceous. Electric log available. of Florida lease E., Sugar Loaf Key, 374 well 1. Monroe County. 111. Gulf Oil State of Lat 24036'59" N., long 52 15, 475 Upper Jurassic or Offshore. Electric log Florida lease 82002'21" W., Lower available. 826-Y well 1. Marquesas Keys, Cretaceous. Monroe County. 112-A__ California State of Lat24032'10/r N., long 7,723 Upper Offshore. No data Florida lease 1011 82°06'40" W., Cretaceous (?). released, May 1963. tract 1 well 2. Marquesas Keys, Monroe County. 82 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total No. Name (feet)

Florida Continued

FL-112-B__ California State of Lat 24°32'lw N., long ______12, 850 Florida lease 1011 82°06'31W W., Cretaceous (?). released. May 1963. tract 1 well 3. Marquesas Keys, Monroe County. 113 ___ Gulf Oil O.C.S. Lat 24°27'00W N., long ______15, 294 ______Offshore. No data State block 28 82°21'45W W., released, March 1966. well 1. Marquesas Keys, Monroe County. 114 __ _ California O.C.S. Lat 24°26'10" N., long ______7,871 Upper Cretaceous. Offshore. Twisted off State block 46 82°29'37" W., 7,871 ft abandoned. well 1. Marquesas Keys, Monroe County. 115_ _ California O.C.S. Lat 24°25'17" N., long ______4,687 Eocene _ - ______Offshore. Twisted off State block 44 12°36'02" W., 4,687 ft abandoned. well 1. Marquesas Keys, No data released, May Monroe County. 1963. Lat 28°05'31. 5" N., ______10, 524 Lower Cretaceous. Offshore. State lease 224.-B long 82°52'49.9" W., well 3. Honeymoon Island, Pinellas County. 117. ___ Fernandina Beach Fernandina Beach, 10 2, 130 Middle Eocene. _ _ water well 1. Nassau County. 118. __ JOIDES group site Lat 30°33.2' N./long -90 910 ____ do______Composite of offshore 1. 80°59.5' W., 27 miles core holes. Gamma log offshore from run. Artesiar head of Jacksonville, Fla. 30 to 35 ft. reported in Eocene aquifers. 119 ___ JOIDES group site Lat 30°20.5' N., long -136 1,050 _____do______. Offshore core h'lle. 2. 80°20' W., 63.5 miles Gamma and velocity offshore Jacksonville, log run. Fla. 120 _ _ JOIDES group site Lat 30°22.7' N., long -581 804 Upper Eocene _ __ Composite of offshore 5. 80°07.5' W., 76.5 miles core holes. G i,mma offshore Jacksonville, log run. Fla. 121. ___ JOIDES group site Lat 30°04.8' N., long -2, 710 393 Paleocene ______Offshore core hole. No 6. 79°14.5 W., 136 miles geophysical l"»g run. offshore Jacksonville, Fla. 122__ __ JOIDES group site Lat 31°02.5' N., long 2, 945 585 ___ _do______Composite of offshore 4. 77°43' W., 221 miles core holes. No geo­ offshore from physical log run. Brunswick, Ga. 123 ___ JOIDES group site Lat 28°30' N., long 3, 886 585 Middle Eocene.. _ Composite of offshore 3. 77°30.o' W., 181 miles core holes. Gamma log offshore Cape run. Kennedy, Fla.

Georgia

GA-1______Town of Groveton 1 mile north of State 500 300 Pre-Cretaceous _ _ No electric log run. Top water well 1. Highway 12, of pre-Cretaceous Groveton, Columbia rocks 135 ft. County. Georgia Training Near Gracewood, 136 1, 200 _____do_-______--. No electric log run. Top School water Richmond County. of pre-Cretaceous well 1. schist 305 ft U.S. Geological 0.25 mile east of 129 620 _____do__--_------No electric log available. Survey test hole 1. McBean-Waynesboro Top of pre-Oetaeeous Rd., Burke County. rocks 602 ft. 4______Three Creeks Oil 2__ 2.5 miles east of Greens ______1, 033 _____do_-_-__---_- No electric log run. Top Cut, Burke County. of pre-Cretaceous crystalline rocks 1,002 ft. U.S. Geological Wrens, Jefferson County. 445 549 Upper No electric log available. Survey test hole 2. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 83

TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported No*»;s No. Name (feet)

Georgia Continued

GA-6. A. F. Lucas & 3.5 miles southwest of _____ 1,143 Pre-Cretaceous___. No electric Ic^ run. Georgia Louisville, Jefferson Petroleum. County. 7. Middle Georgia 12 miles northwest of _____ 395 _____do_----_-____ No electric lent run. Top Oil & Gas Sandersville, of pre-Cretaceous Lillian-B 1. Washington County. rocks 395 f<-. Town of Sandersville 1.4 miles southwest of 465 872 _-_-_do_---______No electric lc«c run. Top water well 51. junction of State of pre-Cretaceous Highways 15 and 24 quartzite and gneiss in Sandersville, rocks 871 ft. Washington County. Strietmann Biscuit 1.5 miles east of State 364 303 ___do_ No electric log available. water well 1. Highway 11 in Top of pre-Cretaceous southwest Macon, rocks 301 ft. Bibb County. 10. U.S. Government Avondale, 8 miles south 358 509 _.___do___---__ No electric log available. Cochran Flying of Macon, Bibb Top of pre-Cretaceous Field 2. County. rocks 496 ft. 11. Town of Swainsboro 0.9 mile southwest of 330 873 Middle Eocene. No electric log available. water well 3. courthouse, Swainsboro, Emanuel County. 12. Town of Sylvania Sylvania, Screven 202 490 ___-_do_-_-__ Do. water well 3. County. 13. Gray Drilling 0.2 mile northwest of 250 445 Pre-Cretaceous. No electric log available. W. M. McRae 1. junction of State Top of pre-Cretaceous Highways 1 and 85, rocks 439 ft. 0.5 mile north of main gate, Fort Benning, Muscogee County. 14. Town of Cusseta 0.25 mile south of 550 1,205 _____do_ No electric log available. water well 1. junction of State Top of pre-Cretaceous Highways 26 and 280, rocks 1,185 ft. Chattahoochee County. 15 Lee Oil & Natural Land lot 207, land dist. 600 1, 770 ___do. No electric log available. Gas Burgin 1. 31, 4 miles southeast Top of pre-Cretaceous of Buena Vista, rocks 1,590 ft. Marion County. Lee Oil & Natural 7 miles southwest of 3, 990 Lower Electric log run but not Gas Winkler 2. Putnam, Marion Cretaceous (?) available. County. Merica Oil Land lot 182, land dist. 290 2,140 Pre-Cretaceous__._ Electric log r.vailable. Forhand 1. 1, 3 miles northeast Top of pre-Cretaceous of Ideal, Macon schist 2,139 ft. County. 18. Tricon Minerals Land lot 44, land dist. 419 1,494 ___do______No electric log available. Duke 1. 14, 5 miles southwest Top of pro-Cretaceous of Perry, Houston gneiss 1,4?0 ft. County. 19. Tricon Minerals Land lot 266, land dist. 367 1,698 _____do_ -. Electric log available. Gilbert 1. 13, 7 miles southwest Top of pre-Cretaceous of Elko, Houston gneiss 1,685 ft. County. 20__.__ Merica Oil Hill !____ Land lot 74, land dist. 1, 371 2,319 ___do. Electric log available. 1 mile northwest of Top of pre-Cretaceous Byromville, Dooly quartzite 2,317 ft. County. 21--..- Georgia-Florida Land lot 163, land dist. 442 3,748 _____do_ No electric log available. Drilling Walton 1. 6, 9 miles southeast of Top of pre-Cretaceous Vienna, Dooly County. metamorpMc rocks 3,512 ft. 22_____ Ainsworth Tripp 1_ Land lot 306, land dist. 280 2, 710 Pre-Cretaceous (?) _ Electric log run to 2,457 21, 4 miles south of ft availabh. Top of Pulaski-Beckley serpentinisred diabase County line, near 2,488 ft. Hawkinsville, Pulaski County. 84 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Georgia Continued

GA-23--. __ R. O. Leighton Land lot 280, land dist. 290 6,035 Pre- Cretaceous. _ Electric log avr'lable. Dana 1. 12, near Hawkins- ville, Pulaski County. 24_._ __ Calaphor Manufac- 0.5 mile South of Minter, 280 2,548 Triassic(?) _ _ __ Electric log available. .turing McCain 1. Laurens County. Top of Triasf=>ic(?) diabase 2,53? ft. 25__- ._ Glen Rose Oil Land lot 221, Georgia 291 2, 125 Upper Cretaceous- No electric log available. Fowler 1. Military Dist. 1386, 6 miles west of Soper­ ton, Treutlen County. 26- McCain & Nicholson 3 miles east of Soperton, 351 3, 168 Pre-Cretaceous__ Electric log available. J. Gillis & H. Georgia Military Top of pre-O-jtaceous Gillis 1. Dist. 1386, Treutlen granite 3,158 ft. County. 27- Barnwell Drilling 3 miles east of Soperton, 3,239 -__do. Electric log available. J. L. Gillis. Georgia Military Top of pre-Cretaceous Dist. 1386, Treutlen rocks 3,053 f*. County. 28. Town of Statesboro Southwest part of States­ 219 921 Middle Eocene.... No electric log available. water well 3. boro, Bulloch County. 29. Flynn-Austin Land lot 210, land dist. 431 5, 240 Lower Creta­ Do. Stephens 1. 17, 9.5 miles southwest ceous (?). of Americus, Sumter County. 30. Town of Dawson East side of Main St., 347 1,028 Upper Cretaceous. Do. water well 3. Dawson, Terrell County. 31. Kerr-McGee Pate 1_. Land lot 144, land dist. 364 5, 008 Lower Cretaceous- Electric log available. 13, 3 miles northwest of Arabi, Crisp County. 32. Dixie Oil Wilcox 1_ 7.5 miles southwest of 240 3, 384 _____do___----_-__ No electric log run. Alamo, Wheeler County. 33. Parsons & Hoke Land lot 260, land dist. 242 4, 008 _ _ _ ^ _ do.__-__--_ Electric log available. Spurlin 1. 7, 1 mile south of Scotland, Telfair County. 34. Paul Parsons Land lot 288, land dist. 205 3,630 Triassic or lower Do. Hinson 1. 10, 4 miles northeast Cretaceous. of Lumber City, Wheeler County. 35. Meadows Develop­ Near Uvalda, Georgia 199 1,619 Eocene. Do. ment Moses 2. Military Dist. 1810, Montgomery County. 36. J. E. Weatherford 1 mile north of Higgston, 293 3, 433 Triassic(?) ______Electric log available. Wilkes 1. Georgia Military Dist. Top of Triassic (?) 1567, Montgomery diabase 3,415 ft. County. 37. Tropic Oil & Gas 6.5 miles southwest of 198 3,681 ___-_do--_-__----- Electric log available. Gibson 1. Lyons, Toombs Top of Triassic(?) County. arkosic sandstone 3,663 ft. 38. Felsenthal-Weather- Land lot 522, land dist. 229 4, 106 __-__do______Electric log available. ford Bradley 1. 2, 6 miles northeast Top of Triable basalt of Pine Grove, 4,095 ft. Appling County. 39. Savannah Oil Cher- 2}_ miles southwest of 21 2,131 Upper Cretaceous. No electric loft run. okee Hill 1. Port Wentworth, Chatham County. 40. U.S. Geological Fort Pulaski on Cock- 8 1, 435 Paleocene______No electric lop available. Survey test well 1. spur Island, Chatham County. 41. U.S. Army Camp 1.6 miles northwest of 91 816 Upper Eocene...- Do. Stewart water Hinesville Liberty well. County. 42. E. B. LaRue Jelks 6 miles southeast of 26 4,264 Pre-Cretaceous-___ Electric log available. & Rodgers 1. Riceboro, Liberty Top of pre-Cretaceous County. rhyolite pomhyry 4,250 ft. TABLE 1 RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 85 TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Georgia Continued

GA-43. Sowega Minerals Land lot 328, land dist. 345 5,275 Triassic(?).______Electric log available. Exploration West 4, 4.2 miles northwest Top of Triassic(?) 1. of Edison, Calhoun diabase 5,190 ft. County. 44. Sealy Reynolds Land lot 2, land dist. 209 5, 012 Lower Cretaceous. Electric log available. Lumber 1. 116, 6 miles northeast of Pretoria, Dougherty County. 45. J. R. Sealy Reynolds Land lot 374, land dist. 192 5,310 .....do- Do. Lumber 2. 2, 5.4 miles southwest of Pretoria, Dougherty County. 46. Carpenter Oil Nina Land lot 275, land dist. 193 1, 903 Upper Cretaceous. No electric log available. McLean 1-A. 1, Coffee County. 47. Carpenter Oil Thur- Land lot 189, land dist. 1, 317 4,130 Lower Cretaceous. Electric log available. man 1. 1, 3.8 miles southeast of Relee, Coffee County. 48. Carpenter Oil Land lot 144, land dist. _____ 4,151 Pre-Cretaceous(?)_ Electric log available. Knight 1. 1, 5 miles northeast of Top of pr>Createeous Broxton, Coffee County rocks 4,1?8 ft. 49. Rowland L. Taylor Land lot 327, land dist. 238 1,210 Eocene...____ Knight 1. 6, 6 miles northeast of Douglas, Coffee County. 50. Operator unknown, 7 miles northwest of 175 1, 965 __---do.-_--__-_ No electric log available. Byars 1. Jesup, Wayne County. 51. Humble Oil Union 12.5 miles southeast of 65 4,554 Pre-Cretaceous.___ Electric log available. Bag-Camp Paper Jesup, land lot 54, Top of pre-Cretaceous 1. Georgia Military dist. metamorphic rocks 333, Wayne County. 4,358 ft. 52. California Bruns­ Land lot 7, Georgia 73 4, 620 _____do.-.______Electric log available. wick Peninsular 1. Military dist. 333, 7.5 Top of pre-Cretaceous miles east of McKin- quartzite 4,570 ft. non, Wayne County. 53. U.S. Biological Sur­ Boat landing, west side 9 711 Upper Eocene. _ _ _ No electric log available. vey water well 4. Blackbeard Island, Mclntosh County. 54. Pan-American Land lot 329, land dist. 75 4,376 Pre-Cretaceous____ Electric log available. Products Adam- 4, 2 miles southeast of Top of pre-Cretaceous McCaskill 1. Offerman, Pierce granite 4,348 ft. County. 55. W. B. Hinton Land lot 332, land dist. 75 4, 355 _____do_____--____ Electric log available. (Clark) Adams- 4, 3 miles northeast of Top of pre-Cretaceous McCaskill 1. Offerman, Pierce granite 4,345 ft. County. 56. Humble Oil W. F. Land lot 95, land dist. 2, 52 4, 512 Lower Cretaceous. Electric log available. Hellem 1. 5.3 miles north of Nahunta, Brantley county. 57_ Humble Oil W. C. Georgia Military Dist. 25 4, 737 Pre-Cretaceous- _ _ _ Electric log available. McDonald 1. 1499, southwest of Top of pre-Cretaceous Brunswick, Glynn granite 4,737 ft. County. 58_ Humble Oil Union Georgia Military Dist. 24 4, 632 Lower Cretaceous.. Electric log available. Bag-Camp Paper 27, Spring Bluff area, ST-1. Glynn County. 59_ E. B. LaRue Colonels Island, 5 miles 20 4,614 _____do__ _ Do. Massey 1. southwest of Bruns­ wick, Glynn County. 60_ State of Georgia About middle of Jekyii 12 706 Upper Eocene..___ No electric log available. Jekyll Island water Island, Glynn County. well 1. 61. Mont Warren Land lot 406, land dist. 186 7,320 Pre-Cretaceous-_ _ _ Electric log available. Chandler 1. 26, 3.5 miles west of Top of Triassic (?) Cedar Springs, Early rocks 5,677 ft. Top of County. Paleozoic black shale 6,600 ft. 62_____ Sun OilEllis 1. Land lot 341, land dist. 163 3,175 Up >er Cretaceous. No electric log available. 26, Early County. 86 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 1. Records of selected wetts along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Georgia Continued.

GA-63. Mont Warren Land lot 82, land dist. 145 3, 572 Lower Cretaceous- Electric log avaiHble. Harlow 1. 27, 5 miles east of Donalsonville, Seminole County. 64. Mont Warren Grady Land lot 61, land dist. 114 3,810 _._..do. Do. Bell 1. 27, 12 miles southeast of Donalsonville, Seminole County. 65. J. R. Sealy Spindle Land lot 142, land dist. 7,620 __--_do---_-_- Electric log run. Top 3 (Seminole 21, 16 miles southeast Naval Stores). of Donalsonville, Seminole County. 66. Humble Oil J. R. Land lot 42, land dist. 96 4, 500 Lower Cretaceous Electric log available. Sealy 1. 14, 18 miles west of Bainbridge, Seminole County. 67. J. R. Sealy Fee 1__. 6.5 miles west of Recov- . .____ 3, 007 Upper Cretaceous- No electric log available. ery, Decatur County. Slight gas sho^v reported. 68. Hunt Oil Metcalf 1. Land lot 260, land dist. 104 6, 152 Lower Cretaceous- Electric log available. 21,5 miles east of Recov­ ery, Decatur County. 69. Hughes and others Land lot 189, land dist. 132 3,718 _..-.do. Do. Martin 1. 15, 4.8 miles north of Bainbridge, Decatur County. 70. Renwar Oil G. E. Land lot 111, land dist. 129 4,995 ___do_____- Do. Dollar 1. 15, Decatur County. 71. Calvary Develop­ Land lot 25, Land dist. 277 4,195 _--._do__-_. Do. ment Scott 1. 22, 2H miles south­ east of Amsterdam, Decatur County. 72. Stanolind Oil & Gas Land lot 133, land dist. 338 7,490 Triassic (?). ._. Electric log available. Pullen 1. 10, 1 mile south of Top of Triass;c(?) Cotton, Mitchell diabase 5,677 ft. Top County. of Paleozoic rocks 7,486ft. 73. Adams Drilling Land lot 270, land dist. 270 4, 910 Lower Creta­ Electric log available. Arrington 1. 8, 2 miles southwest ceous. of Funston, Colquitt County. 74. D. E. Hughes Land lot 154, land dist. 136 3,850 Upper Cretaceous. Do. Rodgers 1-B. 12, 7 miles west of Morven, Brooks County. 75. Sun Oil Doster- Land lot 71, land dist. 222 4,296 Pre-Cretaceous__ Electric log available. Ladson 1. 7, 5 miles southwest Top of pre-C^taceous of Kirkland, Atkinson volcanic rock" 4,282 ft. County. 76. Wiley P. Ballard, Land lot 306, land dist. 215 4,232 _..do ______Electric log available. Jr., Timber Prod­ 7, 8.5 miles northwest Top of Ordovician(?) ucts 1-B. of Homerville, Clinch rocks 4,010 ft County. 77. Hunt Oil Musgrove Land lot 523, land dist. 171 3, 513 Upper Cretaceous. 2. 12, 5.5 miles southeast of Homerville, Clinch County. 78_ Sun Oil Barlow 1__ Land lot 373, land dist. 177 3,847 Pre-Cretaceous----- Electric log available. 12, 9 miles southwest of Top of pre-C^taceous of Homerville, Clinch quartzitic sar*istone County. 3,840 ft. 79. Hunt Oil Musgrove Land lot 198, land dist. 147 4,088 ..---do-__-___ Electric log available. 12. 15 miles south of Top of Paleozoic (?) Homerville, Clinch black shale 3 953 ft. County. 80. Luke Grace Drilling Land lot 36, land dist. 176 4,588 _.-..do__..... Electric log ava;'able. Griffis 1. 13. 8.4 miles north­ Top of Paleozoic rocks east of Fargo, Clinch 3,843 ft. County. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST

TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported No*«ss No. Name (feet)

Georgia Continued

GA-81.._ _. Humble Oil & Re­ Land lot 146, land dist. 181 4,185 Pre-Cretaceous _ _ _ _ Electric log available. fining Bennett & 12, 4 miles northwest Top of Paleozoic rocks Langsdale 1. of Haylow, Echols 4,108 ft. County. 82... _ _ Hunt Oil Superior Land lot 219, land dist. 156 3,916 .... _do___ ._..._. . Electric log available. Pine Products 4. 13, 5 miles northeast Top of Pa'eozoic(?) of Statenville, Echols red silty shale 3,911 ft. County. 83. ...._ Hunt Oil Superior Land lot 364, land dist. 148 3,865 ...-.do...... Electric log available. Pine Products 1. 13, 5 miles east of Staten­ Top of Paleozoic (?) ville, Echols County. black shah 3,782 ft. 84. ._ __ Hunt Oil Superior Land lot 532, land dist. 143 4,003 ...-. do.. __..._.._ Electric log available. Pine Products 3. 13, 13 miles southeast Top of Paleozoic (?) of Statenville, Echols black shale 3,657 ft. County. 85. ._ __ Hunt Oil Superior Land lot 317, land dist. 142 4,062 .....do... __.__._. Electric log available. Pine Products 2. 13, 10 miles southwest Top of Paleozoic (?) of Colon, Echols quartzitic sandstone County. 3,710 ft. 86... __ Waycross well W-7__ 6 miles southeast of 130 3,045 Upper Cretaceous. No electric l->g. Ruskin, Ware County. 87... __ California Buie 1___. 4.5 miles northwest of 65 4,955 Pre-Cretaceous. ... Electric log available. Tarboro, Camden Top of pro- Cretaceous County. volcanic rocks 4,674 ft. 88... _ U.S. Coast Guard Lat. 31°56'53.5" N., long -54 161 Upper Eocene....- Penetrated 5 ft of Ocala tower site 1. 41°00'00" W. 10 miles Limestone. Composite offshore from Savan­ of two offrhore core nah, Ga. holes.

Maryland

MD-1- __ Anne Arundel 1 mile north of Glen 35 530 *Pt*A_ TV/TAflnTni t* Top of pre-Mesozoie County Sanitary Burnie, Anne Arundel granite 52" ft. Commission County. water well. 2____ _- Bethlehem Steel Near Sparrows Point, 10 711 .---.do.... _.-.._- Top of pre-Hesozoic water well 10. Baltimore County. granite 65S ft. 3__._ ._ Chestertown Water Chestertown, Kent 22 1,135 Lower Cretaceous. _ Board water well County. 1. 4___. _ _ City of Centerville Centerville, Queen Annes 59 655 Upper Cretaceous.. water well. County. 5 _ . _ _ Maryland Oil and Andrews Air Force Base, 240 1,511 Lower Cretaceous. _ Development oil Prince Georges test Ed-9. County. 6. ... _. Washington Gas Near Brandywine, 124 1,727 Triassic(?) _ ._ .. Electric log run. Top of Light Mudd 3. Prince Georges Triassic(?) rocks 1,492 County. ft. 7 ._ Washington Gas Near Brandywine, 65 1,478 "Pl*A TVTAQrtTrtl/* Electric log run. Top of Light Thorne 2. Prince Georges pre-Mesoroic gneiss County. 1,430 ft. 8 _ _ _. Washington Gas Near Brandywine, 178 1,523 Upper Cretaceous. Electric log run. Light Moore 2. Prince Georges County. 9 __ Coastal Petroleum ... Near Pomonkey, Charles .. 492 ..-..do----...--. County. 10 _ __ Pan American Re­ Wades Point, Talbot 13 1,520 ... ..do... .--_.- fining water well. County. 11 _ _ Dorchester Water Cambridge, Dorchester 15 977 . _.__do._-_ ..---. Cambridge CE-3. County. 12_._ 6 miles east of Salisbury, 70 5,568 Pre-Mesozoic. Electric log available. 1. Wicomico County. Top of proMesozoic quartzite or gneiss 5,498 ft. 13 ... __ Socony-Vacuum Oil 4.5 miles southwest of 45 7,178 Triassic(?> __ _... Electric log available. Bethards 1. Berlin, Worcester Top of Triassic(?) County. gabbro 7,130 ft. PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF

TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Maryland Continued

MD-14. Standard Oil of New 4.5 miles north of Ocean 13 7, 710 Lower Cretaceous.. Electric log available. Jersey Maryland City, Worcester Esso 1. County. 15. City of Crisfield Crisfield, Somerset . _ _ _ 1, 302 Upper Cretaceous. water well. County. 16. Washington Su­ Near Forest Heights, 22 630 Lower Cretaceous.. burban Sanitary Prince Georges District water County. well EB-2.

Massachusetts

W. Manning, water Gays Head on Martha's 125 175 Probably Pleisto­ Tertiary and Cretaceous well 1. Vineyard, Dukes cene. rocks crop out along County. coast. Town of Tisbury Northeast part of 115 262 _____do______water well 1. Martha's Vineyard, Dukes County. U.S. Coast Guard Northern tip of Nan- 10 301 Pleistocene ______Coskata Life tucket Island, Nan- Saving Station 1. tucket County. U.S. Air Force 8,500 ft N. 86° W. 25 1,000 Pre-Mesozoic Top of pre-Mes^zoic schist Harwich 1. of South and Main 435 ft. Sts., Harwich, Barn- stable County. Operator unknown._ Holden Pond near Prov- 264 Eocene- Tertiary rockr also re­ incetown, Barnstable ported in shallow wells County. at Duxbury on main­ land.

New*srsey

NJ-1______Harold Kuhn water Near Fords, Middlesex 175 235 Triassic. ______Top of Triassic red shale well 1. County. 160 ft. 2___ _ _ Clifford Stultz water Cranbury, Middlesex 95 263 Pre-Mesozoic. _ _ __ Top of Wissahnkon Schist well 1. County. 200 ft. 3 __ ___ Van Horn Oil Com- Millstone, Somerset 100 2, 382 Triassic. ______Well started in Triassic pany oil test 1. County. red shale. 4 ____ New Jersey Highway Telegraph Hill, Holmdel 215 1, 039 Pre-Mesozoic. ... Top of Wissahnkon Schist Authority test hole Township, Monmouth 965 ft. 1. County. 5 __ _ Monmouth Consoli- Long Branch, Monmouth __..-_._-__ 981 Upper Cretaceous. Electric log rur. dated Water West County. End Station water well. 6______Monmouth Consoli- Asbury Park, Monmouth 30 1, 053 dated Water County. Whitesville Sta­ tion water well #1. 7 _ _ _ New Jersey Oil & Prospertown, Ocean .____.__ 1,100 Gas Fields Com- County, pany. 8 _ ___ Hamilton Square About 4 miles east of inn 9^n Water well 1. Trenton, Mercer 215 ft. County. Maguire Air Force Fort Dix, near Wrights- 160 1, 139 ___do __-______- Top of Wissahhkon Schist Base water well 2. town, Burlington 1,100ft. County. N.J. Oil & Gas Jacksons Mills, Ocean 110 5,022 _ do ______Top of pre-Mefozoie schist Fields and W & K County. 1,336 ft. Oil Mathews 2. 11 American Water Lakewood, Ocean 638 Upper Cretaceous. Electric log run. Works water well. County. Ocean County Mantoloking, Ocean 1,052 _.___do______. Do. Water Dept. County. water well 6. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 89 TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) No. Name (feet)

New Jersey Continued

NJ-13 ___ Transcontinental About 2 miles north- 39 1,805 Upper Cretaceous. Gas Pipeline west of Garden State test hole 19. Parkway, State Highway 530, Ocean County. 14_..._. Trans continental About 6 miles north- 156 1,741 __-__do_-______Do. Gas Pipeline west of Garden State test hole 17. Parkway, State Highway 72, Ocean County. 14A_-__ Trans continental About 2.5 miles east of 90 1,519 __.._do ._ __ . Do. Gas Pipeline Speedwell, Burlington test hole 13. County. 15 _- Town of Beach Beach Haven, Ocean 5 575 Middle Miocene. __ Haven water County. well. 16 - Trans continental Near Harris ville, 19 1,701 Upper Cretaceous. Electric log run. Gas Pipeline Burlington County. test hole 15. 17 __ New Jersey water Near Barrington, ______634 _____do ._ _ _. Do. well 15. Camden County. 18 - Borough of Berlin, Berlin, Camden ______955 Lower(?) Do. water well. County. Cretaceous. 19 - Atlantic City, Atlantic 15 860 Do. water well 2. County. 20 - Borough of Clayton Clayton, Gloucester ______._ 1,010 Do. water well 2. County. 2l.._. ._ Town of Salem Near Standpipe in 12 1 440 water well 1. Salem, Salem County. granite l,f 76 ft. 22 - Town of Bridgeton On Cumberland Ave. in 85 1,651 See Kasabach and water well 1. Northern Bridgeton, Scudder (1961, p. 54). Cumberland County. 23 __ East Coast Oil.. _ .. 1.5 miles east of 15 1,200 __.__do.______-__ Newport, Cumberland County. 24 ..- Town of Sea Isle Sea Isle City, Cape May ______897 Electric log run. City water well. County. 25 - Anchor Gas Higbee Beach Road on 22 6,408 Pre-Mesozoic _____ Dickinson 1. Cape May, Cape May pre-Mesoyoic gneiss County. 6,344 ft. 26 __ U.S. Geological South end of Island 13 3,891 _-.__do______.____ Electric log run. Top of Survey Island Beach. pre-Mesoyoic biotite Beach 1. gneiss 3,798 ft. 27 -. U.S. Geological Lat 39° 42' N., long 110 2,080 _-___do._-___.___. Electric log run. Top of Survey New 74°57' W., Camden Paleozoic metamorphic Brooklyn Park 1. County. rocks 1,94^ ft.

New York

NY-1. City of New York Emmett and Hylan 10 319 Precambrian. Top of Prec^mbrian Boulevard Station Blvd., Richmond soapstone 319 ft. 7. County, Staten Island. 2. Water well K514___. Near East New York 26 560 Pre-Mesozoic. Top of pre-Mesozoic Kings County, Long gneiss or fohist 466 ft. Island. 3. City of New York Rockway Park Pumping 10 1,049 _-__.do----_- Top of pre-I lesozoic Rockaway Beach Station, Rockaway granite ro"k 991 ft. 2. Beach, Borough of Queens. U.S. Naval Receiv­ Long Beach, Nassau 10 1,471 _____do. Top of pre-Mesozoic ing Station water County. rocks 1,46° ft. well 1. Port Washington Port Washington, Nassau 24 369 ____.do. Top of pre-Mesozoic Water District County. rocks 365 ft. water well 2. 90 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total depth Oldest rocks reported Notes No. Name (feet) ^

New York Continued

NY-6 ______Columbia Univer­ Lat 40°49' N., Long 1,956 Pre-Mesozoic. Electric log available. , sity (Bellport 72°56' W., on Fire Top of pre-Mesozoic Coast Guard Sta­ Island opposite Bell- rocks 1,915 ft. tion) Schwenke port, Suffolk County. Estate 1-B. 7______Brookhaven Na­ Lat 40°51.5' N., long 113 1,568 Electric log run. Top of tional Laboratory. 72°53.9' W., Suffolk weathered pre-Mesozoic County, Long Island. igneous rock about 1,540 ft. Brookhaven Na­ Lat40°52.4' N.,long 85 1,600 Electric log run. Top of tional Laboratory 72°52.3' W., Suffolk pre-Mesozoic igneous water well 6434. County, Long Island. rock about 1,493 ft. Water well 189__._- Near Orient, Suffolk 5 668 Top of pre-Mesozoic County, Long Island. gneiss or schist 668 ft.

North Carolina

City of Murfrees- Murfreesboro, Hert- 64 432 Upper Cretaceous _ boro water well. ford County. Pam-Beau Drilling 2 miles northwest of Har- ______1, 278 Pre-Cretaceous__ No electric log available. Basnight 1. rellsville, Hertford County. State Highway Gates County Prison 29 615 Upper Cretaceous. Commission water Camp, Gates County. well. DuGrandlee Ex­ 10 miles northeast of 16 6,421 Pre-Mesozoic Top of Triassic^?) rocks ploration Fore­ Elizabeth City, Cam- 3,520 ft. Top of pre- man 1. den County. Mesozoic rocks 4,900 ft. Gas show 3,170 to 4,050 ft. 5_-____ U.S. Navy Harvey Harvey Point, Perqui- 8 77 Upper Mi Point Seaplane mans County. Base 1. 6 ______Town of Windsor Windsor, Bertie County. _ 46 405 Upper Cretaceous. water well. 7_ ___ Standard Oil of Pamlico Sound, Dare 21 6, 410 , Lower Cretaceous. Electric log available. New Jersey, County North Carolina 2. 8 _ _ _ _ Town of Tarboro Tarboro, Edgecombe 50 349 Pre-Cretaceous_. Top of pre-Creti%ceous water well. County. rocks 328 ft. 9 ______Town of Williams- Williamston, Martin 60 500 Upper Cretaceous. ton water well. County. 10______Operator unknown, 4 miles northwest of ______2, 223 Lower Cretaceous. Roper 1. Wenona, Washington County. 11 _---._ Davidson Oil & 2 miles northeast of 36 2,660 ___do____. Electric log avr'lable. Development Wenona, Washington Furbee 1. County. 12______Davidson Oil & 1 mile north of Ponzer, 9 3,123 _____do_.______Development Hyde County. Rhem 1. ___ Coastal Plains Oil 5.9 miles east of State l 10 2, 005 Upper Cretaceous . No electric log run. J. M. Ballance 1. Highway 94 on north side of Lake Matta- muskeet, Hyde County. 13B___ Coastal Plains Oil 2.4 miles east of State 1 10 1, 635 Do. F. F. Spencer, Jr., Highway 94 on north side of Lake Matta- muskeet, Hyde County. 13C.___1 Coastal Plains Oil 0.4 mile north of Fair- 1 10 2,005 ___do. Do. David Q. Holton field Post Office, Hyde County. .__ Coastal Plains Oil 4.5 miles west of State l 10 1,685 __ _do- Do. J. L. Simmons, Highway 94 along Jr., 1. north side of Lake Mattamuskeet, Hyde County. 1 Estimate. RECORDS OP SELECTED WELLS ALONG THE ATLANTIC COAST 91 TABLE 1. Records of selected wetts along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Tites No. Name (feet)

North Carolina Continued

NC-13E____ Coastal Plains Oil 8.3 miles west of State '10 2,005 Upper Cretaceous No electric log run. J. L. Simmons, Highway 94 along Jr., 2. north side of Lake Mattamuskeet, Hyde County. 13F____ Coastal Plains Oil 2.3 miles northwest of 1 10 2,005 ___._do_ Do. Walton Williams, Swindell Fork and 1. State Highway 264 on southwest side of Lake Mattamuskeet, Hyde County. 13 G__ Coastal Plains Oil 2.4 miles northwest of 1 10 2,005 ___do. Do. M. M. Swindell, 1. Swindell Fork and State Highway 264 on southeast side of Lake Mattamuskeet, Hyde County. 14. _. Standard Oil of New Cape Hatteras, Dare 24 10,054 Pre-Cretaceous____ Electric log* available. Jersey Hatteras County. Top of p~e-Cretaceous Light 1. granite 9 878 ft. 15...__ A. B. Williams 9 miles east of Wilson, 123 335 _____do______Top of pre-Cretaceous water well. Wilson County. rocks 330 ft. 16 _.. _ _ Town of Farmville Farmville, Pitt County. _. 80 472 ___do_-_____._ Top of pre-Cretaceous water well. granite 470 ft. 17.____ Don Langston 2 miles north of Winter- 63 378 Upper Cretaceous _ water well. ville, Pitt County. 18 _____ American Metal 2.4 miles northeast of 30 310 .do. test hole. Washington, Beaufort County. 19 _____ Town of La Grange La Grange, Lenoir 105 404 Pre-Cretaceous___. Top of pre-Cretaceous water well. County. granite 3?2 ft. 20 _ _ _ _ _ Owner unknown, 5 miles west of Loftins, 64 120 Upper Cretaceous. water well. Lenoir County. 21_____ Carlton Ward 2 miles northwest of 46 180 .do. water well. Cove City, Craven County. 22 _____ Carolina Petroleum 2 miles east of Merritt, 11 3, 425 Pre-Cretaceous..__ Electric lop available. Atlas Plywood 1. Pamlico County. Top of p'e-Cretaceous granite 3,414ft. 23 _____ Carolina Petroleum 1 mile southwest of 11 3, 667 _ _ _ _ _do.--.__- __ Electric lor available. North Carolina Pamlico, Pamlico Top of p-e-Cretaceous Pulp Wood 1. County. granite 3,657 ft. 24 _____ Carolina Petroleum 1 mile east of Merritt, 16 2, 897 Lower Cretaceous. Electric lof available. Linley 1. Pamlico County. 25_ _ _ _ _ Seymour Johnson Goldsboro, Wayne 64 180 Pre-Cretaceous..__ Top of pre-Cretaceous Air Field water County. rocks 180 ft. well. 26_____ Town of Mount Mount Olive, Wayne 155 310 Upper Cretaceous. Olive water well. County. 27_.___ Town of Calypso Calypso, Duplin County. 157 215 ___do-______water well. 28_____ Warsaw Dress Warsaw, Duplin County. 158 153 _____do.______water well. 29. J. O. Smith water 6 miles southwest of 85 111 ___do.______well. Kornegay, Duplin County. Henry Vann water 5 miles west of Faison, 166 271 Pre-Cretaceous.. _ _ Top of pre-Cretaceous well 1. Sampson County. schist 24* ft. Town of Roseboro Roseboro, Sampson 134 470 __--_do--.____ Top of pre-Cretaceous water well. County. granite gneiss 353 ft. 32 Town of Garland Garland, Sampson 139 348 Upper Cretaceous. water well 2. County. American Mining & 2 miles southeast of 23 765 Pre-Cretaceous.._. Radioactivity log avail­ Development Kelly, Bladen County. able. Top of pre- Corbett 1. Cretaceous rocks 690 ft. American Mining & 7 miles north of Acme 23 730 _ do.______Top of pre-Cretaceous Development and 8 miles southwest rocks 695 ft. Keith 1. of Currie, Pender County. 1 Estimate. 92 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 1. Records of selected wells along the Atlantic coast Continued

WeU Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

North Carolina Continued

NC-35-.--- Mueller Farms Rocky Point, Pender 35 580 Upper Cretaceous. water well. County. 36_ _ _ _ _ Town of Richlands Richlands, Onslow 50 535 __.__do.______water well. County. 37 ----- Peter Henderson Sec. 21, block 4, Hoff­ 1,232 Pre-Cretaceous(?) _ Well 2, 2.5 milep to the H off man Forest 1. man Forest, Onslow north, drilled to 1,239 County. ft. Well 3, 2 miles southeast, drilled to 1,328 ft. . Gilbert and Seay 10 miles north of Jack­ 1,430 ._.__do.______Well 2 nearby d-illed Hoffman Forest 1. sonville, Onslow to pre-Cretacpous County. rocks at 1,335 ft. 39. . Burton Drilling Sec. 8, block 10, Hoff­ 44 1,570 -____do.______Electric log available. Hofmann Forest man Forest, 5 miles Top of basement 1. south of Belgrade, 1,562 ft. Onslow County. 40. . U.S. Government 1 mile southeast of 30 567 Upper Cretaceous. Camp Lejeune Jacksonville, Onslow water well 1. County. 41. . Operator unknown, 4 miles southwest of 1, 493 Pre-Cretaceous. Top of pre-Cret-'ceous Cadco 2. Verona, Onslow rocks 1,343 ft County. 42_ _ _ _ _ Operator unknown, Hollyridge, Onslow 30 1,497 Top of pre-Cretaceous Cadco 1. County. rocks 1,422 ft. 43 _____ Carolina Petroleum 2 miles east of Ellis 15 2,435 Electric log available. Bryan 1. Lake, Craven County. Top of pre-Ci^taceous granite 2,408 ft. 44___._ Great Lakes Drilling 5 miles west of Have- 30 2,351 Top of pre-Creti-ceous Havelock 1. lock, Craven County. granite 2,318 ft. 45 _____ Carolina Petroleum Merrimon, Carteret 15 4,069 Electric log available. G. Carraway 1. County. Top of pre-Ci-etaceous granite 4,054 ft. 46A.. _ _ Carolina Petroleum 2 miles south of Mer­ 15 4, 126 Electric log ava^able. N. Carraway 1. rimon, Carteret Top of pre-Ci etaceous County. granite 4,120 ft. 46B -. _ _ Carolina Petroleum 2 miles south of Mer­ 20 4, 097 Lower Creta­ Electric log ava-'able. G. Yeatman 1. rimon, Carteret ceous (?). County. 47 F. L, Karsten 3 miles northwest of 17 4,044 Pre-Cretaceous.... Electric log ava^able. Laughton 1. Morehead City, Slight oil shows (?). Carteret County. Top of pre-Cretaceous granite 4,030 ft. 48 Coastal Plains Oil 0.5 mile north of Markers . _ _ _ 4, 975 Pre-Cretaceous Electric log ava*'able. Huntley-Davis 1. Island Bridge, Top of pre-Cntaeeous Carteret County. rocks 4,954 ft. 49 Coastal Plains Oil 2.5 miles north of Atlan­ .___ 5, 607 ___do.______Electric log available. Baylands 1. tic, Carteret County. Top of pre-Cretaceous rocks 5,561 ft. 50A..__ Carolina Petroleum 1 mile north of Mer­ 13 3,963 Pre-Cretaceous. Electric log ava;'able. Salter 1. rimon, Carteret Top of pre-Cretaceous County. rocks 3,954 ft. 50B.-_ Carolina Petroleum 1.5 miles north of Mer­ 10 3,964 ___do______Electric log available. Phillips-State 1. rimon, Carteret Top of pre-Cr»,taceous County. rocks 3,930 ft. 50C- Carolina Petroleum West side Jerry Creek, 11 4, 020 Pre-Creta­ Electric log available. Wallace 1. Merrimon Township, ceous (?). Top of pre-Cretaceous Carteret County. (?) 4,016 ft. 51 North Carolina 2 miles east of McCain, 510 401 Pre-Cretaceous. Top of pre-Cret

WeU Total Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

North Carolina Continued

NC-55_._ . Town of Whiteville Whiteville, Columbus 59 260 Upper Cretaceous. . water well. County. EC _ _ Brunswick County Leland, Brunswick 25 300 .....do... _...... Leland Colored County. High School. 57_-_ _ _ U.S. Army Ammu- Sunny Point, Bjrunswick 35 198 do . nition Depot County. water well 6. 58. U.S. Army Fort Fort Caswell, Brunswick 11 1,543 Pre-Cretaceous-___ Top of pre-C^taceous Caswell water County. metamorpl '

Rhode Island

RI-1.. _ . _ Block Island Water Central southern part 80 Pre-Mesozoic(?)... Pleistocene en pre- well 33. Block Island, Town of Mesozoic granite (?); New Shoreham. "Rotten granite" re­ ported by Drake, Ewing, an-* Sutton (1959, p. 152) at 80 ft below sea level in this or nearby well. 2____ U.S. Army Corps of Fort Greene, Ocean 28 109 Pre-Mesozoic. . Pleistocene en pre- Engineers test Road and Old Point Mesozic g-anite well 46. Judith Road. at 95 ft. 1 Estimate. 94 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notes No. Name (feet)

Sornth Ckr«lin»

SC-1- - __ Town of Harts- Hartsville, Darlington 170 432 Pre-Cretaceous . _ Top of pre-Crr*.»ceous ville water well. County. schist 428 ft. 2..___ .. Town of Dillon Dillon, Dillon County ..._ 114 595 ____do. ______Top of pre-Cretaceous water well. rhyolite breccia 594 ft. 3---_ Florence, Florence 142 715 Triassic(?).. _ ... Top of Triassio'?) oli- water well. County. vine diabase 710 ft. 4 _ _ Town of Marion Marion, Marion County . . 68 1,244 Pre-Cretaceous .... No electric log available. water well. Top of pre-C^taceous schist 700 ft. 5.. _ ._ Palmetto Drilling 1 mile north of Alls- 107 1, 150 _.___do. .____.__.. No electric log available. Allsbrook 1. brook, Horry County. Top if pre-C'^taceous rocks l,160f+. 6--... 12 miles southwest of 31 1,429 _.___do. ______Electric log available. Smart 1. Conway, Horry Top of pre-C^taceous County. rocks 1,400 f . 7.-__.._ A. B. Cruse Drilling 12 miles southwest of 15 1,440 Upper Cretaceous ... Fannie Collins 1. Conway, Horry County. 8.-.__ . _ Southern States 28 miles north of George­ 46 1,397 _____do-______No electric log available. Drilling Williams 1. town, Georgetown County. 9...... _ Town of George­ Georgetown, Georgetown 15 1,870 _____do..____.____ Do. town water well. County. 10.-- __ Southern States Near Rhems, Williams- 40 825 _____do-_. _..____ Do. Drilling oil test. burg County. 11 ._ Town of Sumter Sumter, Sumter County. 162 784 Pre-Cretaceous. _ _ _ No electric log available. water well. Top of pre-Cretaceous granite 782 ft. 12 .._ Survey Drilling oil 5 miles southwest of 315 492 __--.do______-__. Top of pre-Cretaceous test. Aiken, Aiken County. granite 450 ft. 13... _ __ Town of Aiken 1 mile south of center of 480 519 -____do___. ______Top of pre-Crctaceous water well 266. Aiken, Aiken County. rocks 519 ft. Electric* log run. 14-.. .. Oil test ______Between Perry and 450 1,000 __-_.do.______._ Top of pre-Cretaceous Wagner, Aiken County. granite 642 ft. 15-.. __ U.S. Government Savannah River area, 1,185 ._ _ do.... _._-.__ Top of pre-Cretaceous Savannah River Aiken County. schist 999 ft. Project water well. 16.... _ Town of Vance 26 miles southeast of 131 839 Upper Cretaceous. No electric log available. water well. Orangeburg, Orange- burg County. 17.... _ U.S. Government Moncks Corners, 53 177 Eocene. ____.____- Do. Intransit Depot Berkeley County. water well. 18... _ ... Oil test.... ___ ,__. Near Summerville, 71 2,470 Pre-Cretaceous- _ Top of pre-Cretaceous Dorchester County. diabase 2,4fO ft. 19-.. _ _ Town of Walterboro Walterboro, Colleton 65 1,500 Upper Cretaceous. water well 3. County. 20.... __ Charleston Con­ Charleston, Charleston 10 2,015 ___ do ______solidated Railway County. & Lighting water well 1. 21.... _ U.S. Government Parris Island Marine 18 3,450 Lower Cretaceous. Electric log available. water well 2. Base, Beaufort County.

Virginia

VA-1_.___ __ Spotsylvania 263 Pre-Mesozoic- Top of pre-Mesozoic County water well. Fredericksburg Spot­ granite 229 ft. sylvania County. 2_____ ._ U.S. Navy Proving Dahlgren, King George 20 780 Upper Cretaceous. Ground water well. County. 3 __ Town of Dogue Dogue King, George 385 _____do... ______water well. County. 4..... _ _ Town of Colonial Colonial Beach, West- 654 _____do______-_-_. Beach water well. moreland County. RECORDS OF SELECTED WELLS ALONG THE ATLANTIC COAST 95 TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total Location Alt (feet) depth Oldest rocks reported Notow No. Name (feet)

Virginik Continued

VA *> . . Westmoreland State Westmoreland State _._....._. 631 Upper Cretaceous.. Park water well. Park, Westmoreland County. E. Henneson water Oak Grove, Westmore­ 180 530 _____do_____ ...... well. land County. 7.... Port Royal Tomato Port Royal, Caroline .._-.--._. 240 Lower Eocene __ _ Cannery water County. well. ... Town of Bowling Bowling Green, Caroline 215 1, 550 Pre-Mesozoic. Top of pre-Mesozoic Green water well County. granite 1,160ft. 23. ... Town of Warsaw Warsaw, Richmond ._-.__..__ 653 Upper Cretaceous.. water well. County. 10 HonfnrH TVif»o nrflt.Ai* St. Stephens Church, _...__..__ 470 ..._.do.. ______well. King and Queen County. 11 _ _ A. R. Beane water Lancaster, Lancaster _ .__ 438 Lower Eocene _ __ well. County. 19 .___ T. A. Treakle water Palmer, Lancaster ....---.__ 740 Upper Cretaceous _ well. County. 10 .___ Peaks Industrial 1 mile southeast of 190 240 Lower Eocene __ _ School water well. Peaks, Hanover County. 14__..___ V. E. Portwood 6 miles northeast of __....-... 350 Lower Cretaceous . water well. Mechanicsville, Hanover County. 15__ .___ Roberts Drilling 18 miles northeast of 37 3, 278 Pre-Mesozoic. Red clastic rocks 834- Hugh Townsend Richmond and 3 miles 2,609 ft. Igneous and 1. southwest of Man- metam orphic frag­ quin, King William ments abur dant County. 2,083-2,60. ft. Schist, quartzite and gneiss below 2,60r ft (top of pre-Mesozoic rocks). 16 .... W. S. Reynolds Cohoke, King William _____- . 555 Upper Cretaceous _ water well. County. IT- West Point, King Wil­ 30 1, 689 Triassic(?) ______Top of Triassic(?) rocks Point 1. liam County. 1,284 ft. IS... _. Elkins Oil & Gas Mathews, Mathews 15 2, 325 Pre-Mesozoic _____ Top of pre-Mesozoic Marchant and County. granite 2,307 ft. Minter 1. 19 _ _ Tidewater Oil & Gas Approx. lat 37°30' N., 145 860(?) Johr 1. long 77° 15' W., Henrico County. 20 _ V. R. Shepherd 5 miles southeast High­ __ __- 236 Lower Eocene. water well. land Springs, Henrico County. 21... ___ Riverview Farm Malvern Hill, Charles 42 204 ___._do~------water well. City County. 22... _._ Charles City School Charles City, Charles __..._..._ 205 Upper Cretaceous. water well. City County. 23... ___ U.S. Navy Mine 2 miles northwest of 80 620 _____do~_------Depot water well. Yorktown, York County. 24... ___ Pennsylvania Rail­ Cape Charles, North­ 20 1, 810 Lower Cretaceous. road Co. water ampton County. well. 25... ___ Disputanta School Disputanta, Prince 114 219 _____do~_------for Colored water George County. well. 26 ... City of Newport 3 miles south of Bacons 97 1, 060 ___..do------News water sup­ Castle, Surry County. ply well 1. 27 .-- Newport News Gas_. Newport News, Warwick _-_----_.. 1,065 Upper Cretaceous. County. 28 .. U.S. Army Fort Fort Monroe, Elizabeth 10 3, 255 Pre-Mesozoic... . Top of pre-Mesozoic Monroe water County. granite 2,246 ft. well. 96 PETROLEUM POTENTIAL, ATLANTIC COASTAL PLAIN AND CONTINENTAL SHELF TABLE 1. Records of selected wells along the Atlantic coast Continued

Well Total No. Name (feet)

Virginia Continued

VA-29 ... Town of Wakefield Wakefield, Sussex ______399 Upper Cretaceous- water well. County. 3(L_____ Monogram Farm Driver, Nansemond 20 540 Lower Cretaceous water well. County. 31 ____ Nestle Company 1 mile north of Suffolk, ______1,006 _-_-_do--_--_--_- water well. Nansemond County. 32___ _ _ Town of Whaley ville Whaleyville, Nansemond ______320 water well. County. 33_._ _ Town of Franklin Franklin, Southampton ______601 Lower Cretaceous water well. County. 34... _-_ Town of Norfolk 5 miles east of Norfolk, 12 1,740 _____do--_-_--__- water well. Princess Anne County.