39o30'75o22'30"25'CANTON27'30"75o30'32'30"35'39o30'

TAYLORS BRIDGE

39o37'30" 35' 32'30"WILMINGTON SOUTH 75o30' 27'30" PENNS GROVE 25' 75o22'30"39o37'30"

35'

ALL

OW

AY

32'30"

B'

A'

Geology mapped 2006-2007.Cartography by S. Stanford and M. Girard.

B

Base from U. S. Geological Survey Salem (1948, photorevised 1986) and Delaware City (1993) quadrangles. Corner ticks for Salem are on North American Datum of 1927; corner ticks for Delaware City are on North American Datum of 1983. A gap of base information occurs along the boundary of the quadrangles.

Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program, under USGS award number 06HQAG0047. The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U. S. Government.

7000 FEET1000 10000 2000 3000 4000 5000 6000

.5 1 KILOMETER1 0

SCALE 1:24 0001/ 21 0 1 MILE

MA

GN

ETIC

NO

RTH

APPROXIMATE MEANDECLINATION, 1993

TRU

E N

OR

TH

�

LOCATION IN NEW JERSEY

11.5O

CONTOUR INTERVAL 10 FEET (SALEM QUADRANGLE), 5 FEET (DELAWARE CITY QUADRANGLE)

NATIONAL GEODETIC VERTICAL DATUM OF 1929

SURFICIAL GEOLOGY OF THE SALEM AND DELAWARE CITY QUADRANGLES

SALEM COUNTY, NEW JERSEY

byScott D. Stanford

2009

DEPARTMENT OF ENVIRONMENTAL PROTECTIONLAND USE MANAGEMENTNEW JERSEY GEOLOGICAL SURVEY

Prepared in cooperation with theU. S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

SURFICIAL GEOLOGY OF THE SALEM AND DELAWARE CITY QUADRANGLESSALEM COUNTY, NEW JERSEY

OPEN-FILE MAP OFM 76

INTRODUCTION

Surficial deposits are unconsolidated sediments that discontinuously overlie Coastal Plain bedrock formations and that are the parent material for agronomic soils. In the Salem and Delaware City quadrangles, surficial deposits include artificial fill and river, wetland, windblown, hillslope, and estuarine sediments. They are as much as 140 feet thick beneath and adjacent to the Delaware River and as much as 100 feet thick in the lower reaches of the Salem River and Alloway Creek valleys, but are generally less than 40 feet thick elsewhere. They record six main periods of deposition, separated by five episodes of valley erosion. The deposits are described below. The age of the deposits and the episodes of valley erosion are shown on the correlation chart. The underlying Coastal Plain bedrock formations were mapped by Stanford and Sugarman (2009).

DESCRIPTION OF MAP UNITS

ARTIFICIAL FILL--Sand, silt, gravel, clay; gray to brown; demolition debris (concrete, brick, wood, metal, etc.), cinders, ash, slag, glass, trash. Unstratified to weakly stratified. As much as 20 feet thick, generally less than 15 feet thick. In highway and railroad embankments, and filled wetlands and flood plains. Many small areas of fill, particularly along streams in urban areas, are not mapped. The mapped extent of natural deposits beneath fill and dredge spoils is based in part on the position of shorelines and salt marshes shown on topographic map sheet 81 (New Jersey Geological Survey, c. 1880, scale 1:21,120).

DREDGE SPOILS--Fine sand, silt, clay, minor medium-to-coarse sand and gravel; gray to brown. Contain variable amounts of organic matter and mica, and minor amounts of man-made materials. Unstratified to weakly stratified, locally thinly bedded to laminated. In large disposal cell along the Delaware River north of Fort Mott. As much as 50 feet thick.

TRASH FILL--Trash mixed and covered with silt, clay, sand, and minor gravel. As much as 40 feet thick. In solid-waste landfills. Small areas of trash fill may be included in artificial fill and dredge spoils.

ALLUVIUM--Sand, silt, peat, minor clay; brown, yellowish-brown, gray; and pebble gravel. Contains variable amounts of organic matter. Peat and organic silt and clay typically overlie sand and pebble gravel. Sand and silt are unstratified to weakly stratified. Gravel occurs in massive to weakly stratified beds generally less than 2 feet thick. Sand consists chiefly of quartz with some glauconite and mica. Gravel consists of white, gray, and yellow quartz and quartzite, and a trace of gray chert. Beneath the Delaware River (section AA'), the lowermost alluvium may include late Pleistocene glaciofluvial sand and pebble-to-cobble gravel that is the downstream extension of the glaciofluvial gravel that crops out in the Delaware River valley north of the Burlington, New Jersey, area. This gravel was termed the Trenton Gravel by Cook (1880) and Lewis (1880). The same deposit was later named the “Van Sciver Lake” and “Spring Lake” beds by Owens and Minard (1979), although they considered it to be of interglacial age. This glaciofluvial deposit was laid down about 20,000 to 15,000 years ago, during the late Wisconsinan glacial maximum. The glaciofluvial gravel includes much gray sandstone and mudstone, and some red sandstone and mudstone, gray gneiss and schist, black chert, and purple-red conglomerate, in addition to white and gray quartz and quartzite. Alluvium is as much as 30 feet thick beneath the Delaware River, and as much as 15 feet thick elsewhere (estimated). Deposited in modern flood plains and stream channels, and in former flood plains and channels beneath estuarine deposits before Holocene sea-level rise.

BEACH SAND--Fine-to-medium quartz sand with minor glauconite, very pale brown to yellowish-brown. Contains few (1-5%) quartz pebbles and shells. As much as 5 feet thick. Overlies salt-marsh deposits in small beaches along the Delaware River.

SALT-MARSH AND ESTUARINE DEPOSITS--Silt, fine sand, peat, clay; brown, dark-brown, gray, black; and minor medium sand and pebble gravel. Contain abundant organic matter and some mica and shells. As much as 100 feet thick beneath and adjacent to the Delaware River; as much as 80 feet thick in the lower Salem River and Alloway Creek valleys. Deposited in tidal wetlands, salt marshes, tidal flats, and tidal channels during Holocene sea-level rise, within the past 10,000 years.

SWAMP DEPOSITS--Peat and organic silt and fine sand, minor organic clay; brown to black. As much as 10 feet thick (estimated). Deposited in non-tidal wetlands.

LOWER COLLUVIUM--Fine-to-medium sand, minor silt and clay; light gray, very pale brown; minor pebble gravel. Sand consists chiefly of quartz and is unstratified to weakly stratified. Gravel is scattered within the sand, and occurs as a sparse lag at the base of the deposit. Gravel consists of white, gray, and yellow quartz and quartzite, and minor gray chert. As much as 10 feet thick (estimated). Forms foot-slope aprons that grade to the modern flood plain. Deposited by mass movement and unchanneled washing of material on hillslopes.

LOWER TERRACE DEPOSITS--Fine-to-medium sand, minor silt and clay; yellow, brown, olive-yellow; and pebble gravel. Sand is unstratified to well-stratified. Gravel occurs in thin beds (generally less than 6 inches thick) within and at the base of the deposit. Sand consists chiefly of quartz and glauconite. Gravel consists of white, gray, and yellow quartz and quartzite, and a trace of gray chert. In deposits beneath the Delaware River and its fringing marshes, gravel also includes gray and red sandstone and mudstone, gray gneiss and schist, and purple-red conglomerate. As much as 30 feet thick beneath the Delaware River, 10 feet thick (estimated) elsewhere. In tributary valleys, form stream terraces with surfaces 2 to 10 feet above modern estuaries and flood plains. Beneath the Delaware River and its fringing marshes, form eroded stream-terrace remnants, now covered by estuarine deposits, with top surfaces rising to about -30 feet in elevation.

Both the tributary-valley terraces and the terrace deposits in the main Delaware River valley were laid down in valleys cut into the Cape May Formation, units 2 and 3. After the lower terrace sediments were deposited, the Delaware River eroded as much as 100 feet into and through the lower terrace before depositing glaciofluvial gravel, and then postglacial alluvium and estuarine sediment. These relationships indicate that the lower terrace deposits beneath the river were laid down during the period of lower-than-present sea level known as the early and middle Wisconsinan in North American stage terminology. This period was between the interglacial highstand of sea level about 125,000 years ago (the Sangamon interglacial) and the last glacial maximum about 20,000 years ago (the late Wisconsinan glacial), when sea level was at its lowest late Pleistocene level of about 350 feet below that at present. Radiocarbon dates of 31,380+4530-2880 (GX 22966) and 29,330+/-600 (Beta 190911) radiocarbon years before present on wood within the lower terrace deposits in Marcus Hook, Pennsylvania, about 18 miles northeast of Salem, confirm this age range (Jengo, 2006). Older, higher stream-terrace deposits (known as "Upper Terrace Deposits") occur in the upper Salem River and Alloway Creek valleys but do not extend into the map area.

UPPER COLLUVIUM--Fine-to-medium sand, minor silt, very pale brown, yellow, reddish-yellow; and pebble gravel. Sand consists chiefly of quartz and is unstratified to weakly stratified. Gravel is scattered within the sand and occurs as thin layers within, and at the base of, the deposit. Gravel consists of white, gray, and yellow quartz and quartzite and minor gray to white chert. As much as 10 feet thick. Forms foot-slope aprons that grade to the Cape May Formation, unit 1. Deposited by mass movement and unchanneled washing of material on hillslopes.

CAPE MAY FORMATION (Salisbury and Knapp, 1917)--Estuarine and fluvial-estuarine deposits of middle and late Pleistocene age. Divided into three units (Qcm1, Qcm2, Qcm3) based on surface elevation and age (Newell and others, 1995). Fossils, pollen, and amino-acid racemization ratios in shells from unit Qcm2 elsewhere in the Delaware estuary and Delaware Bay area indicate that it is of Sangamon age (about 125,000 years ago), when sea level was approximately 20-30 feet higher than at present in this region (Newell and others, 1995; Lacovara, 1997; Wehmiller, 1997). Unit Qcm1 is an older estuarine deposit laid down during a pre-Sangamon interglacial sea-level highstand and is of early or middle Pleistocene age (Lacovara, 1997; O’Neal and McGeary, 2002). Unit Qcm3 was deposited during sea-level fall from the highstand represented by the Qcm2 deposits and is of Sangamon or early Wisconsinan age. Unit Qcm2 is equivalent to the Lynch Heights Formation in Delaware and unit Qcm3 is equivalent to the Scotts Corners Formation in Delaware (Ramsey, 2005).

CAPE MAY FORMATION, UNIT 3--Fine-to-medium sand, minor coarse sand, silt, clay, and peat; yellow, brownish-yellow, very pale brown, light gray; and pebble gravel, minor cobble gravel. Unstratified to laminated; sand and pebble gravel may be cross-bedded. Sand consists of quartz with a little glauconite and a trace of mica, feldspar, and chert. Feldspar and chert grains may be partially or completely weathered. Gravel consists of white, gray, and yellow quartz and quartzite, with minor gray chert, gray gneiss and schist, gray to red sandstone and mudstone, and white to gray clay rip-up clasts. Schist, gneiss, sandstone, and mudstone, and a few chert, pebbles are partially to completely weathered. As much as 40 feet thick. Forms a terrace with a maximum surface elevation of about 15 feet.

CAPE MAY FORMATION, UNIT 2--Fine-to-medium sand, minor coarse sand, silt, clay, and peat; yellow, brownish-yellow, very pale brown, light gray; and pebble gravel, minor cobble gravel. Unstratified to laminated; sand and pebble gravel may be cross-bedded. Sand consists of quartz with a little glauconite and a trace of mica, feldspar, and chert. Feldspar and chert grains may be partially or completely weathered. Gravel consists of white, gray, and yellow quartz and quartzite; minor gray chert; and a trace of gray gneiss, gray schist, and gray to red sandstone and mudstone. Schist, gneiss, sandstone, and mudstone, and a few chert, pebbles are partially to completely weathered. As much as 50 feet thick. In the subsurface in the Pennsville paleovalley beneath Supawna Meadows, and in a paleovalley in the Oakwood Beach area, logs of wells and borings record gray to dark-gray silt, clayey silt, and sandy silt, with some peat and wood, as much as 70 feet thick. These fine-grained sediments are mapped separately as unit Qmc2l on sections AA' and BB'. Qcm2 forms a terrace with a maximum surface elevation of about 35 feet.

CAPE MAY FORMATION, UNIT 1--Fine-to-medium sand, some silt and very fine sand; very pale brown, yellow; and pebble gravel. Unstratified to weakly stratified. Sand consists of quartz with a little glauconite. Gravel consists of white and yellow quartz with minor gray chert. As much as 15 feet thick. In eroded remnants of a terrace with a maximum surface elevation of 65 feet. "Qcm1/Tg" indicates areas where the Cape May Formation, unit 1, is generally less than 6 feet thick over Upland Gravel.

PENSAUKEN FORMATION (Salisbury and Knapp, 1917)--Fine-to-coarse sand, clayey sand, minor silt and very coarse sand; reddish-yellow to yellow; pebble gravel. Unstratified to well-stratified; tabular, planar cross-beds are common in sand. Pebble gravel occurs in thin layers (generally less than 3 inches thick) within the sand and in thicker, massive beds in places at the base of the formation, where it may include some cobble gravel. Sand consists chiefly of quartz with some feldspar, rock fragments (chert and shale), mica, and glauconite. The feldspar and chert grains are partially or completely weathered to a white clay. Gravel consists of yellow, reddish-yellow (from iron-staining), white, or gray quartz and quartzite; a little brown to gray chert; and a trace of brown, reddish-brown, and gray sandstone and shale, and white-to-gray gneiss. The chert, sandstone, shale, and gneiss pebbles are partially weathered or fully decomposed. As much as 30 feet thick (estimated). Crops out in the Mannington Creek valley, with a maximum surface elevation of about 65 feet. The base of the deposit descends from an elevation of about 30 feet northeast of Mannington Creek to about -30 feet on the east edge of the Pennsville paleovalley, where it is

covered by the Cape May Formation and was penetrated in boring SL-12. This pattern records thickening of the deposit towards the main Delaware River valley and indicates that the Pensauken was deposited as an aggraded valley fill. This geometry, regional paleoflow data (Owens and Minard, 1979; Martino, 1981), and the provenance of the sand and gravel in the formation, indicate that the Pensauken was deposited by a large river flowing southwesterly from the New York City area to the Delmarva Peninsula. The map area is on the southeastern edge of the former river valley.

The age of the Pensauken is not firmly established. Berry and Hawkins (1935) describe plant fossils from the Pensauken near New Brunswick, New Jersey that they consider to be of early Pleistocene age. Owens and Minard (1979) assign a late Miocene age based on correlation to units in the Delmarva Peninsula. In Delaware, the Columbia Formation, which is a fluvial sand similar in lithology and topographic position to the Pensauken, contains pollen indicating a Pleistocene age (Groot and Jordan, 1999). Pollen from a black clay bed within the Pensauken near Princeton, New Jersey, includes cool-temperate species and a few pre-Pleistocene taxa. This assemblage suggests a Pliocene age (Stanford and others, 2002). The Pensauken is overlain by late Pliocene or early Pleistocene till in Somerset County, New Jersey, and lies in a valley deeply eroded into middle and late Miocene marine and fluvial deposits (Stanford, 1993). These relationships indicate a Pliocene to early Pleistocene age.

UPLAND GRAVEL--Fine-to-medium sand, minor silt and coarse sand, very pale brown, yellow, brownish-yellow; pebble gravel. Sand consists of quartz with minor glauconite, feldspar, and chert. Feldspar and chert grains are partially or fully weathered. Gravel consists of white, yellow, and gray quartz and quartzite with minor gray chert. Most chert pebbles are partially or fully weathered. As much as 20 feet thick. Occurs as erosional remnants of deposits capping interfluves and ridgetops along the western edge of the map area. Elevation of the base of the deposits ranges from 90 to about 40 feet. The upland gravel is thus younger than the Bridgeton Formation, which is at higher elevation, and is partly on grade with, and so of the same age as, the Pensauken Formation. The deposit was, in part, laid down by slope wash and stream deposition in valleys that were tributary to the Pensauken river. Post-Pensauken stream erosion resulted in a topographic inversion, with the former valley-bottom deposits now capping interfluves.

BRIDGETON FORMATION (Salisbury and Knapp, 1917)--Fine-to-coarse sand to clayey sand, reddish-yellow, brownish-yellow, reddish-brown; pebble gravel. Unstratified to well stratified, with some cross-beds in sand. Cemented by iron in places. Sand consists of quartz with some weathered feldspar and a little weathered chert. Gravel consists of quartz and quartzite with some chert. Most chert pebbles are weathered to white and yellow clay. As much as 20 feet thick. Occurs as erosional remnants atop Burden Hill east of Quinton, above 90 to 120 feet in elevation. These are the westernmost remnants of a large river-plain deposit that extend across southern New Jersey. This plain was laid down by an easterly to southeasterly flowing river system (Owens and Minard, 1979; Martino, 1981). Stratigraphic position and petrologic correlations with marine deposits in the Delmarva Peninsula indicate a late Miocene age (Owens and Minard, 1979; Pazzaglia, 1993).

COASTAL PLAIN FORMATIONS--Exposed formations of Cretaceous and Tertiary age, oxidized and weathered to varied depths. Upper several feet generally include some quartz pebbles from eroded surficial deposits, mixed into the formation by bioturbation and cryoturbation. Map unit includes thin, patchy colluvial or alluvial sediments less than 3 feet thick. Not shown on sections owing to varied depth of weathering.

MAP SYMBOLS

Contact--Solid where well-defined by landforms; dashed where approximately located; short-dashed where featheredged or gradational; dotted where covered by water or where artificially exposed within excavated areas.

Thickness and stratigraphy of surficial material in well or boring--Location accurate to within 200 feet. Upper number is identifier; lower number is thickness in feet of surficial material, inferred from driller’s log. Where multiple surficial units were penetrated, the depth of the base of the unit (in feet below land or water surface) is indicated next to the unit symbol. A ">" indicates that the base of the unit was not reached at depth shown. A "<" indicates that thickness of surficial material is less than depth shown. Identifiers of the form 30-xxxx and 34-xxxx are well permits issued by the N. J. Department of Environmental Protection, Bureau of Water Allocation. Identifiers of the form SL-x and DC-x are auger borings drilled by J. P. Owens and D. S. Powars of the U. S. Geological Survey. Identifiers of the form Dcxx-xx and Ddxx-xx are from Talley (1985). Identifiers of the form 33-xxx are U. S. Geological Survey Ground Water Site Inventory numbers and are shown only for wells without N.J. Department of Environmental Protection permit numbers.

Thickness of surficial material in well or boring--Location accurate to within 500 feet. Identifiers and thickness values as above.

Material observed in exposure or excavation, or penetrated in hand-auger hole--Number next to symbol indicates thickness of surficial material, in feet. No number indicates thickness is greater than 5 feet.

Windblown deposits overlying map unit--Windblown very fine sand and silt (indicated by symbol "Qe") observed in hand-auger hole or exposure. Number following symbol is thickness of windblown deposit, in feet. These deposits are discontinuous and lack distinctive morphology and so are not mapped separately from the underlying surficial unit.

Dune ridge--Line along crest of ridge. Dune formed by wind-shaping of underlying Cape May Formation.

Paleocurrent measurement--Observation at "x", arrow indicates paleoflow direction. Measured on cross-beds in the Bridgeton Formation. Observations with cross-bar are reported by J. P. Owens of the U. S. Geological Survey (undated field notes on file at the N. J. Geological Survey). Excavation perimeter--Marks limit of sand pit or other large excavation. Topography within these areas may differ from that on the base map. Contacts within excavated areas show the approximate distribution of surficial materials in 2007.

Sand and gravel pit--Inactive in 2007.

Sand and gravel pit--Active in 2007.

Shallow topographic basin--Line at rim, pattern in basin. Marks shallow surface depressions generally less than 5 feet deep, as seen on stereo aerial photographs taken in 1979 and color infrared planimetric aerial photographs taken in 1995. Most basins are on the Cape May Formation, a few are on the Pensauken Formation, Upland Gravel, or weathered Coastal Plain formations. They are most abundant on flat surfaces where the water table is at shallow depth. They do not occur on lower terraces or modern flood plains and tidal marshes. A few basins are visible beneath thin tidal marsh deposits; these are mapped within unit Qm although they are developed on the underlying Cape May 3. May contain peat or organic silt less than 3 feet thick; basins with thicker organic sediment are mapped as unit Qs. Basins were likely formed by melting of permafrost 18,000 to 15,000 years ago; some may have been formed by wind erosion or groundwater processes.

Elevation of base of surficial deposits--Contour interval 25 feet. Shown only where thickness of surficial deposits exceeds 20 feet. Shows topography of erosional surface at top of Cretaceous through middle Miocene Coastal Plain formations. Refer to Woodruff (1986) for information on the thickness of surficial deposits in the Delaware part of the map area.

REFERENCES

Berry, E. W., and Hawkins, A. C., 1935, Flora of the Pensauken Formation in New Jersey: Geological Society of America Bulletin, v. 46, p. 245-252.

Cook, G. H., 1880, Surface geology--report of progress: N. J. Geological Survey Annual Report for 1880, p. 14-97.

Groot, J. J., and Jordan, R. R., 1999, The Pliocene and Quaternary deposits of Delaware: palynology, ages, and paleoenvironments: Delaware Geological Survey Report of Investigations 58, 36 p.

Jengo, J. W., 2006, Stratigraphy and radiocarbon dates of Pleistocene and Holocene-age deposits, Delaware County, Pennsylvania--rectifying the presence of the Cape May Formation and the Trenton Gravel in the Delaware valley: Northeastern Geology and Environmental Sciences, v. 28, no. 1, p. 45-76.

Lacovara, K. J., 1997, Definition and evolution of the Cape May and Fishing Creek formations in the middle Atlantic Coastal Plain of southern New Jersey: unpublished Ph.D. dissertation, University of Delaware, Newark, Delaware, 245 p.

Lewis, H. C., 1880, The Trenton Gravel and its relation to the antiquity of man: Proceedings of the Academy of Natural Sciences of Philadelphia, Part 2, April to September 1880, p. 296-309.

Martino, R. L., 1981, The sedimentology of the late Tertiary Bridgeton and Pensauken formations in southern New Jersey: unpublished Ph. D. dissertation, Rutgers University, New Brunswick, N. J., 299 p.

Newell, W. L., Powars, D. S., Owens, J. P., Schindler, J. S., 1995, Surficial geologic map of New Jersey: southern sheet: U. S. Geological Survey Open File Map 95-272, scale 1:100,000.

O’Neal, M. L., and McGeary, S., 2002, Late Quaternary stratigraphy and sea-level history of the northern Delaware Bay margin, southern New Jersey, USA: a ground-penetrating radar analysis of composite Quaternary coastal terraces: Quaternary Science Reviews, v. 21, p. 929-940.

Owens, J. P., and Minard, J. P., 1979, Upper Cenozoic sediments of the lower Delaware valley and northern Delmarva Peninsula, New Jersey, Pennsylvania, Delaware, and Maryland: U. S. Geological Survey Professional Paper 1067D, 47 p.

Pazzaglia, F. J., 1993, Stratigraphy, petrography, and correlation of late Cenozoic middle Atlantic Coastal Plain deposits: implications for late-stage passive margin geologic evolution: Geological Society of America Bulletin, v. 105, p. 1617-1634.

Ramsey, K. W., 2005, Geologic map of New Castle county, Delaware: Delaware Geological Survey Geologic Map Series 13, scale 1:100,000.

Salisbury, R. D., and Knapp, G. N., 1917, The Quaternary formations of southern New Jersey: N. J. Geological Survey Final Report, v. 8, 218 p.

Stanford, S. D., 1993, Late Cenozoic surficial deposits and valley evolution of unglaciated northern New Jersey: Geomorphology, v. 7, p. 267-288.

Stanford, S. D., Ashley, G. M., Russell, E. W. B., Brenner, G. J., 2002, Rates and patterns of late Cenozoic denudation in the northernmost Atlantic Coastal Plain and Piedmont: Geological Society of America Bulletin, v. 114, p. 1422-1437.

Stanford, S. D., and Sugarman, P. J., 2009, Bedrock geology of the Salem and Delaware City quadrangles, Salem County, New Jersey: N. J. Geological Survey Open File Map OFM 75, scale 1:24,000.

Talley, J. H., 1985, Geologic cross-section of Delaware River, Red Lion Creek to Kilcohook National Wildlife Refuge: Delaware Geological Survey, Miscellaneous Map 3, 1 pl.

Wehmiller, J. F., 1997, Data report: aminostratigraphic analysis of mollusk specimens: Cape May Coast Guard station borehole, in Miller, K. G., and Snyder, S. W., eds., Proceedings of the Ocean Drilling Program: Scientific Results, v. 150x, p. 355-357.

Woodruff, K. D., 1986, Geohydrology of the Chesapeake and Delaware Canal area, Delaware: Delaware Geological Survey, Hydrologic Map Series 6, scale 1:24,000.

afd

aft

Qal

Qm

Qs

Qcl

Qtl

Qcu

Qcm3

Qcm2

Qcm2l

Qcm1

Qcm1/Tg

Tp

Tg

Tb

Qwcp

!

!

.

!

-25

!

!

4

Qe3

30-806515

34-364130

D

xx

30-981640 Qcm3>53 Qcm2l

Qbs

QmQal

aft

5-40 feet of tributary stream incision;up to 100 feet of incision in main Delaware valley

Qtl

modern Delaware channel established,10-20 feet of tributary stream incision,up to 50 feet of incision in main Delaware valley

Qcu

Qcm2

Qcm1

weathering and extensive erosion,new drainage established

Tp

CORRELATION OF MAP UNITS

Pliocene

early

middle

late

Holocene

Pleistocene

Qcl

Qcm3

erosion and up to 50 feet of tributary stream incision, Pennsville paleovalley eroded by Delaware River, up to 150 feet of incision in main Delaware valley

Qsafd

Qcm2l

weathering and extensive erosion,new drainage established

Tb

Tg

late Miocene

Qbs

Qe2

.

.

.

.

.

.

.

..

..

.

.

.

.

.

.

.

.

.

.

.

.

..

.

.

.

.

.

.

.

.

.

.

.

.

.

.

.

..

.

.

.

.

.

.

.

.

!

!!

!

! !

!! !

!

!

!

!

!

!

!

!!

!!

!

!!!

!!

!

!

!!

!

!

!

!

! !

!

!

!

!

!!

!!!

!

!!!

!

!

!

!

!

!

!

!

! !!

!

!!!

!!!

!!!!

!! !

!!

!!

!

!

!

!

!

!

!

!

!

!

! !

!

!

!!!

!

!

!

!

!

!

!

!

!

!!!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!! !

!

!

!

!

!

!

!

!

!

!

!

!! !

!

!

!

!

!

!

!

!

!

!

!

!

!

!

! !

!

!

!

!

!

!

!

!

!

!

!

!!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!!

!

!

!

!

!

!! !

!

!!

!

!

!!

!!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!

!

!!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!

!

!

!

!

!

!

!

!

!

!

!!

!

!

!

!!

!

!

!

! !

!

ADc 44-043 water112 Qm142 Qal

Dc 45-0212 water95 Qm128 Qal

Dc 45-0511 water99 Qm115 Qal

Dd 41-0328 water35 Qm60 Qtl

Dd 41-0717 water27 Qm76 Qtl-Qcm3

Dd 41-0931 afd47 Qm>75 Qcm3

Dd 42-0229 afd41 Qm>75 Qcm3

30-1490428

30-111143

afdafd

-100

-75

-50

-25

-25

-50

-75

-100

-100

-75

Qm

Qm

Qm

Qbs

Qcm3

Qs

DC-146

Qcm3

30-9480>30

Qbs

Qm

Qcm3

Qcm3Qcm3

Qcm3

30-52, 33-10838

Qcm3

Qcm3Qcm3

Qm

Qal

Qal

Qcm3

30-981640 Qcm3>53 Qcm2l

30-204941 Qcm372 Qcm2l

30-433124

30-843930

30-720920

30-935316

30-711645SL-12

11 Qcm336 Tp

30-802730

-50

-25

-25

-50

PENN

SVIL

LE

PALE

OVA

LLEY

Qcm3

Qcm3

Qm

Qcm3

Qcm3

Qm

Qm

Qcm3

Qcm3

Qm

30-235925

30-653130

30-429537

Qm

-75

-75

-50

-25

-50

-25

Qcm2

Qal Qal

Qal

Qm

Qcm2

Qcm2

Qal

QalQal

Tp

Qtl

Qm

Qal

Qal

Tp

Tp

Qal

Qal

Qm

Qm

Qtl

Qtl

Qtl

Tp

Qcm2Qcm2 Qal

30-912124

30-1082935

30-75233

30-563130

30-78640

30-141832

30-94232

30-649127

30-742811

30-74244

30-742511

30-763815

30-2287

Qwcp

30-5838

30-74266

30-74276

30-74170

30-74180

30-54160

30-64110

30-74690

30-50450

30-78180

30-7040

Qcm1

Qwcp

Qwcp

Qal

QalQcm2

Qcm2

Qcm2

Qcm2

Qwcp

Qe2

Qe2

Qwcp

Tg

Tg

Qwcp

30-74200

30-74430

30-74380

30-74390

30-74220

Tg

QtlQwcp

Qwcp30-47480

Qe2

Qcm2

Qal

Qal

Qtl

Qcm2

Qwcp

Tp

Qal30-525930

30-100660

30-104554 fill>25 Qm

30-104545 fill45 Qm

30-104525 fill39 Qm

30-276221

Qtl

Qal

Qal

0-25

0

0

-25

-25

0

0

-25

-25

Qcm2

Qbs

Qbs

Qcm3

Qcm3

Qcm3

Qm

Qcm3

Qs30-847612 fill27 Qm>60 Qcm3-Qcm2

30-709210

30-55>25

30-570524

33-10625

30-509810 fill25 Qm

30-337785 Qm

Qcm3

Qm-25

-50

-75

-75-50

-25

30-150113

30-73511

30-103612

30-115317

30-991528Qe2

Qm

Qcm2

QalQal

Qm

Qm

Qal

30-19530

30-22017

30-906419

30-127920

30-1105240

0

-25

-25

Qtl

QalQal

Qcm2

Qal

Qal

SL-714

Qal

QalQcm2

30-99160

30-46920

30-46080

Qwcp

Qm

Qm

Qm

Qm

Qbs

Qs

Qs

Qm

Qcm3

Qm

Qm

Qcm3

Qm

Qal

Qcm3

-100

-75

-50-25

30-796431 Qcm372 Qcm2l

30-934635 Qcm377 Qcm2l

30-367660

30-793733 Qcm374 Qcm2l

30-799425 Qcm381 Qcm2l

30-541425 Qcm365 Qcm2l

30-585633 Qcm375 Qcm2l

30-1022028 Qcm380 Qcm2l30-8121

35 Qcm395 Qcm2l

30-985122 Qcm390 Qcm2l

30-1022542 Qcm388 Qcm2l

30-333035 Qcm375 Qcm2l

30-814837 Qcm3108 Qcm2l

30-256545

SL-13>21

30-980950 Qm

30-1045839

30-975017

30-82317

30-3660>52 Qm

30-664530

30-635625 30-7807

12

30-1069920

30-794314

30-1028629

30-1063417

30-806515

30-460614

30-818912

SL-1119

30-65672630-6047

38

Qe4

Qe2

Qe2

Qe4

Qe2

Qe2

Qe3

Qe4Qe2 Qe2

30-964023

SL-96 30-1044

31

30-87721

30-1486727

30-82225

30-82123

30-558832

Qm

Qm

Qcm3

Qal

Qal

30-768685 Qm30-7927

66 Qm

30-103292 fill13 Qm30-10312

7 fill18 Qm

30-1032516

30-1032710 fill20 Qm

30-335728

30-461612

30-1066435

30-420331

30-818746

30-752536

30-13240

30-254930

30-530532

Qcm2

Qcm3

Qm

Qal

Qal

Qal

Qal

Qal

Qal

Qwcp

Qwcp

SL-103

30-161012

30-98267

30-42399

Qe2

Qe24

45

30-94059

30-56654

30-86458

30-343130

30-176330

30-9482930-878627

Qcm2

Qcm2

Qcm2

Qcm2

Qcm1

Qm

Qm

Qtl

Qal

Qal

Qal

Qal

Qal

Qal

Qal

Qcm2

Qal

Qwcp

Qwcp

Qwcp

Qwcp

QwcpQwcp

7

5

Qe2

Qe4

30-958425

34-354410

30-85634 30-10471

1130-594715

Qcm1/Tg

Tg

TbTg

Qcl

Qwcp

Qwcp

Qwcp

Qwcp

Qwcp

Qal

Qal

Qwcp

Qcm2

Qcm2

Qcm2

Qwcp

Qwcp

Qal

Qal

Qal

Qal

Qwcp

Qwcp

Qcm2 Qcm1

Qcu

Tb

Tb

QclQwcp

30-604913

30-52640

30-2820

34-8170

Qcm1

Qal

Qcm2

Qm

Qal

Qal

Qal

30-53126

30-86898

30-608417

30-536515

30-70018

30-164628

34-320530

SL-1626

30-1039812

30-823512

30-484114

30-30119

30-432715

30-677025

30-360027

30-182120

30-29619

30-239110

30-477018

30-218

30-30319

30-70618

30-17514

30-709517

30-636313 fill33 Qm

30-636110 fill26 Qm

30-638617

30-636410 fill35 Qm30-6387

33 30-636531

30-636814

30-1009121

Qal

Qal

Qal

Qcm2

Qcm3

Qcm3

Qcm3

Qal

Qal

Qal

Qm

30-345627

30-820827

30-291417

Qe2

Qe330-978430

SL-1424

34-37076

34-29093534-3641

30

30-836435

Qe4

Qe2

Qe2

QsQal

Qcm3Qm

Qbs

Qcm3

Qcm3

Qcm3

Qcm3Qbs

Qm

Qcm3

30-971714

30-71801530-3740

4 Qbs25 Qm

Qcm3

Qbs

Qcm3Qcm3

Qm

Qm

Qcm3Qcm3

Qcm3

Qm

Qm

Qe4

Qe4

Qe2

Qe2

Qe2

Qs

Qcm3

30-752931

34-374420

34-362935

34-312126

30-543332

34-313325

34-43540

34-21044 fill28 Qcm3

Qm

Qcm3

Qcm3

SL-174 fill21 Qcm3

34-360017

Qcm3

Qcm3

Qal

Qal34-347238

34-111317

34-97228

34-243130

34-323012

34-352511

Qm

Qcm2

Qcm2

Qal

Qal

Qal

QmQal

Qal

34-32516 34-3324

<35SL-158

34-3459834-47220

34-317515

34-345815 34-2680

15

Qal

34-239610

4

4

Qcm2

Qcm1

Qcm1

Qwcp

Tg

Qcu

QalQcl

Tg

Qwcp

QwcpQwcp Qcm2

Qal

Qcm1

Qwcp

34-38035

34-203719

D

D

-25

-25

-50

-75

-25

-75

-25

-50

-50

-25

-25

-25

0

0

0

0

-25

0

0

0

0

Qwcp

aft

aft

x

xx

Qal

Qcm2

Qe>5

Qe2

Qe3

Qe4

Qe5Qe3

Qe6Qe3

Qe4

30-91062 fill35 Qm

30-275510 fill>30 Qm

12

Qe2

DEL

AWA

RE

CIT

Y

SALE

M

-25

-25

Qal

30-764625

100

50

0

-50

-100

-150VERTICAL EXAGGERATION 40X

ELEV

ATIO

N (fe

et)

Qm

Qal

Qtl

water

Dc 4

4-04

Dc 4

5-02

Dc 4

5-05

Dd 4

1-02

Dd 4

1-07

DEL

AWA

RE

RIV

ER

A

afd

Qm

Qcm3

Coastal Plain Formations

Dd 4

1-09

Dd 4

2-02

BEND

INSE

CTIO

NDC

-1

30-9

480

MIL

L C

REE

K

FORT

MO

TT R

OA

D

Qcm3

Qcm2l

Qm

Qm

Qm Qm 30-9

816

Qcm3Tp

Qm Qm

Qm

Qcm3

Coastal Plain Formations

BEND

INSE

CTIO

NSL

-12

30-7

116

SALE

M R

IVER

MA

NN

ING

TON

MEA

DO

WNJ

RO

UTE

49

NJ

RO

UTE

45

NJ

RO

UTE

45

NJ

RO

UTE

45

BEND

INSE

CTIO

N

BEND

IN

SECT

ION

30-9

155

30-1

9530

-220

30-9

064

30-6

491

30-1

418

30-9

121

30-7

8630

-108

29

Qcm3

Qcm2Qcm2

Coastal Plain Formations

Tp

Qm

QtlQal

Tg

30-1

0485

30-1

0454

30-1

0455

MA

NN

ING

TON

CR

EEK

100

50

0

A'

-50

-100

-150

Qal

150

100

50

0

-50

-100VERTICAL EXAGGERATION 40X

ELEV

ATIO

N (fe

et)

30-9

851

Qm

Qcm3

Qcm2l

Qm SL-1

3

30-6

047

30-6

567

SL-1

1

BEND

INSE

CTIO

N

AM

WEL

LBU

RY R

OA

D

Qm Qm

Qcm3

Coastal Plain Formations

30-9

640

Qcm3

30-8

7730

-14,

867

BEND

INSE

CTIO

N

MIL

L ST

REE

T

NEW

BR

IDG

E R

OA

DQm

30-7

525

30-8

187

30-4

203

Qcm2

HA

NC

OC

KS

BR

IDG

E-Q

UIN

TON

RO

AD

ALL

OW

AY C

REE

K BEND

INSE

CTIO

N

30-6

361

30-6

363

30-6

368

30-7

095

30-2

Qm

30-4

770

30-2

391

Qcm2

Qal

Coastal Plain Formations

30-9

584

NJ

RO

UTE

49

Qcm1

Qcu

34-3

544

Tb

Qcl

150

100

50

B'

0

-50

-100

B