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Tch Tch Tch Tch Tg Tg Qcu Qtu Qcu Tg TQg Qcu Qtu Qcm1 TQg TQg TQg Qcl Qm Qal Qtl Qbs Qal Qal Qal Qm TQg TQg Qal Qal Qals Qcu Qcu Tkw Qcu TQg Qcm1 Qtu Tg Qal Qcu Tch Tkw Qm Tkw 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 Qm Qal Qtu Qcl Qal Qcu TQg Tg Tg Tg Qcm1 Qcu Tg Tch Tkw Tg Qcm1 TQg Qal TQg 20 22 21 23 26 27 28 29 30 31 32 33 34 35 36 37 38 25 24 39 40 41 42 43 45 44 309 55 54 56 51 46 47 48 49 50 52 Tg Tch Qm Qbs Tch Tg Tg Qcm1 Tch Qcu Qal Qcu Qtl Qcm1 Qcm1 Qcm1 Qcm2 59 60 58 57 66 65 67 68 70 69 71 72 63 64 Tch Qal Qcm2 Qtl 97 96 104 103 102 101 62 106 105 100 99 107 Qcm2 Qcm2 Qm Qm Qal Qal Qm Qbu Qbe Qbs A’ Qbu Qm Qm Qm Qbs Qbs Qbs Qcm2 Qbu Qbs Qbs Qbs 98 94 93 95 113 112 111 108 109 115 116 119 Qcu Tch Qtl Qal Tg Qcu Qcm2 Qcu Tg Tch Qcm1 Qcm1 Qcm1 78 76 77 91 92 75 73 74 53 88 89 90 86 87 85 175 176 84 110 83 81 80 82 Qtu Qal Qal Qbs Qtl Qbs Tch Tg 174 173 172 171 170 169 Qbs Qm Tkw Qbs Qbs Qm Qbs Qcm2 Tkw Tch Qcm1 177 179 178 166 Qcl Tkw Qbs Qtu Qtl Qtl Qtl Qcm1 Qcm2 Qcm2 Qals Qtl Qtl Qcm1 Qtl Tch Qals Qtl 19 16 17 18 310 184 185 183 182 181 180 Qcm1 Qtl Tch Qtl Tch 186 Qcm1 311 Qcm2 Qals 195 196 194 193 192 190 189 188 191 187 298 299 297 Qcm1 Qcm2 Qals Qtl Qe Qcm2 Tch Qcm1 Qcm1 Qe 197 207 206 208 210 302 167 165 168 138 137 139 Qtl Qals Qbs Qcm2 Qbs Qbs Qcm2 Qbs 136 128 125 127 129 130 131 132 135 134 133 305 140 141 126 211 212 114 117 118 122 123 121 Qals Qals Qcm2 Qbe Qbs Qbu 124 151 150 296 149 152 153 148 Qm Qbu Qcm2 B’ 156 157 158 159 160 Qbe Qbs 146 147 143 142 144 145 162 161 164 163 Qm Qcm2 Qe Qals Qals Qm Qm Qm Qm Tch Qcm2 Qtl 214 306 215 209 213 216 300 218 217 219 221 220 224 Qm Qals Qe Qtl Qtl Qe Qtl Tch Qcm2 Qcm2 Qcm2 Qal Qtl 198 199 200 201 202 203 204 223 222 301 B Qm Qtl Qm 226 227 225 228 Qm Qm Qbs Qbs Qbs Qm Qbs Qm Qbs Qe Qcm2 Qbs 237 238 308 243 307 244 245 304 303 248 247 246 295 Qbs Qbs Qe Qe Qcm2 Qcm2 Qcm2 Qm Qtl Qals Qtl Qm Qm Qe 229 Qcm2 Qbs Qbs Qbs Qbs Qm Qbs Qbs 155 154 231 230 232 234 235 233 Qm Qm 236 Qbu Qbe Qbs Qcm2 Qcm2 Qcm2 Qm 249 250 251 252 253 254 255 256 257 Qm Qcm2 Qbs Qm Qcm2 258 Qe Qe Qe Qcm2 240 241 242 259 261 262 260 Qals Qals Qcm2 Qcm2 Qbs Qm Qbs Qm Qcm2 Qm Qe 263 269 270 271 264 293 265 Qcm2 Qm Qbs Qbs Qbs Qbs Qbs Qm Qbs 276 277 278 280 279 282 281 283 290 291 275 274 284 287 289 285 286 288 272 273 292 Qcm2 Qm Qm Qcm2 Qcm2 Qm Qm Qm Qbu C’ Qm Qbe Qbs 267 268 Qm Tkw Tch Tch Tkw Qm Tkw Tch Tch Tkw Tch Tkw A C Tch Tkw Tch Tkw D’ D 6 3 4 4 9 7 4 7 3 4 5 4 4 5 4 239 Qe8/Qcm2 Qe10/Qcm2 Qe10/Qcm2 Qe15/Qcm2 Qe3/Qcm2 Qe4/Qcm2 Qe4/Qcm2 Qe4/Qcm2 Qe4/Qcm2 Qe4/Qcm2 Qe3/Qcm2 Qbs3/Qm4/Qcm2 Qbs2/Qm Qbs1/Qm figure 3 figure 4 figure 5 figure 6 figure 7 Qe4/Qcm2 Qe5/Qcm2 120 266 79 61 205 Qcm2 294 74 o 07’30” 40 o 07’30” 5’ ASBURY PARK 2’30” 74 o 00’ 40 o 07’30” 5’ 2’30” 40 o 00’ 74 o 00’ 2’30” SEASIDE PARK 5’ 40 o 00’ 74 o 07’30” 2’30” LAKEWOOD 5’ Qm Qals Qtl Qcm2 Qcm1 middle late Holocene Pleistocene Qcm2f Qbs Qtu EXTENSIVE EROSION EXTENSIVE EROSION EROSION EROSION Quaternary TQg early Pliocene Qal Qe Qcl Qbe Qbo Illinoian Sangamonian Wisconsinan PERIOD EPOCH AND AGE NORTH AMERICAN STAGE Qbu Qcu EROSION Tg CORRELATION OF MAP UNITS Miocene UNCONFORMITY Tkw Tch Neogene middle early EXTENSIVE EROSION late Tmq Tvt Tht Krb-ns Kml Kw-mt Ketu Ketl Kwb-mv Kmg Krw UNCONFORMITY UNCONFORMITY UNCONFORMITY UNCONFORMITY UNCONFORMITY UNCONFORMITY UNCONFORMITY UNCONFORMITY Santonian- Coniacian- Turonian Cenomanian Campanian Maastrichtian early late early Late Cretaceous Paleocene Eocene Oligocene Tsr UNCONFORMITY middle Paleogene UNCONFORMITY Tmb Krf Kp3 UNCONFORMITY UNCONFORMITY INTRODUCTION The Point Pleasant quadrangle is in the Barnegat Bay region of the New Jersey Coastal Plain, in the southeastern part of the state. Outcropping geologic materials in the map area are Holocene to upper Miocene surficial deposits that include marine, estuarine, river, wetland, hillslope, and windblown sediments. They overlie the middle to lower Miocene Cohansey and Kirkwood formations, which are shallow-marine and coastal deposits. In the subsurface, unconsolidated Paleogene and Upper Cretaceous sediments underlie the Cohansey and Kirkwood formations. The Paleogene sediments include, from youngest to oldest, the Shark River, Manasquan, Marlboro, Vincentown, and Hornerstown formations, all of which were deposited in continental-shelf settings. The Upper Cretaceous sediments include, from youngest to oldest, the Red Bank, Navesink, Mount Laurel, Wenonah, Marshalltown, Englishtown, Woodbury, and Merchantville formations, all of which were also deposited in continental-shelf settings; and the Magothy, Raritan, and Potomac formations, which were deposited in fluvial and estuarine settings. A summary of the resources provided by the formations, and of the geomorphic history of the map area as recorded by surficial deposits and landforms, is provided below. The age of the deposits and episodes of valley erosion are shown on the correlation chart. Table 1 (in pamphlet) shows the formations penetrated by selected wells and borings as interpreted from drillers’ descriptions and geophysical well logs. These data were used to construct cross sections and to map the elevation of the base of Quaternary deposits. Table 2 (in pamphlet) provides logs for two power-auger holes drilled to a depth of 100 feet. The cross sections (sheet 2) show formations to a maximum depth of about 2200 feet, which is the depth of the deepest well (well 267 in table 1). Although no wells in the quadrangle reached pre-Mesozoic metamorphic basement rock beneath the Coastal Plain formations, wells and seismic data in adjacent areas indicate that basement is probably at a depth of about 1500 feet in the northwest corner of the quadrangle, deepening to about 2500 feet in the southeast (Volkert and others, 1996; Stanford and Sugarman, 2017). Basement rocks in this area are chiefly gneiss and schist. They are commonly weathered to saprolite to thicknesses of as much as 100 feet beneath the basal Cretaceous sediments. RESOURCES Numerous domestic wells, and one public-supply well (well 139 in table 1), tap sands within the Cape May, Cohansey and uppermost Kirkwood formations at depths between 25 and 100 feet. Many of the domestic wells are for lawn irrigation. Many other domestic wells, and eight public-supply wells (wells 102, 103, 104, and three adjacent wells in the same wellfield, a shallow well adjacent to well 97, and well 118) tap deeper sands within the Kirkwood at depths of 90 to 150 feet north of the Metedeconk River and up to 230 feet south of the Metedeconk. Deeper aquifers include sand in the upper member of the Englishtown Formation, which is tapped by six public-supply wells (73, 97, two wells adjacent to well 122, well 153 and another adjacent to it) at depths between 690 and 840 feet; the Magothy Formation, which is tapped by three wells (140, 157, and 255) at depths between 1190 and 1370 feet; and the Potomac Formation, which is tapped by well 267 at a depth interval of 1850 to 1980 feet. The Cohansey and upper Kirkwood formations lack thick, continuous clay beds and so are an unconfined aquifer. The deeper aquifers are confined by fine-grained beds in the lower Kirkwood, Shark River, Manasquan, Hornerstown, Navesink, Wenonah, Marshalltown, Woodbury, Merchantville, and Raritan formations. Additional information on aquifers in the map area is provided by Sugarman and others (2013). Sand and gravel were dug for construction use from the upland gravel, high phase (map unit Tg) and the Cohansey Formation from large pits north of Herbertsville and west of Brielle (former pits are outlined on map). Sand of the Cape May Formation, upper terrace deposits, and windblown deposits on Metedeconk Neck was also dug at smaller pits. No pits were active at the time of mapping, and further extraction is limited by urbanization. Sand for beach replenishment is obtained from offshore sources (Castelli and others, 2015). Clay was mined for brickmaking from the Cohansey Formation at several locations in the Sawmill Creek valley north of Riviera Beach (Ries and others, 1904, and N. J. Geological and Water Survey permanent notes 29-33-723 and 29-33-733). The clay in this area occurred as one or more three- to five-foot thick beds interlaminated with white micaceous fine sand and underlain by iron-cemented sand. SURFICIAL DEPOSITS AND GEOMORPHIC HISTORY After the Cohansey Formation was deposited in the middle Miocene, sea level in the New Jersey region began a long-term decline. As sea level lowered during the middle and late Miocene, between about 15 to 5 million years ago (15-5 Ma, Ma = million years ago), the inner continental shelf emerged as a coastal plain. River drainage was established on this plain. The oldest surficial deposits in the quadrangle are gravels deposited by these rivers. This drainage eroded valleys into an earlier, higher fluvial gravel known as the Beacon Hill Gravel, which formerly covered the map area at an elevation of about 250 to 300 feet (Stanford, 2010). It has been eroded away in the quadrangle but there are remnants farther inland. Groundwater seepage, slope erosion, and channel erosion reworked the Beacon Hill Gravel and deposited it in floodplains, channels, and pediments in valleys that had been cut down between 150 and 200 feet below the level of the former Beacon Hill plain. These deposits are mapped as upland gravel, high phase (unit Tg). They cap the uplands north of Herbertsville and west of Brielle (fig. 1). The base of these deposits declines from an elevation of about 100 feet along the north edge of the quadrangle to about 75 feet to the east in Brielle. North of the quadrangle the base of the gravels continues to rise, to an elevation of 150 feet near Farmingdale, about 8 miles northwest of Brielle (Stanford, 2000a, 2000b). This slope indicates southeasterly stream flow (orange arrows on fig. 1). After a period of higher sea level in the Pliocene, a renewed period of lowering sea level during the early Pleistocene, approximately 2.5 Ma to 800,000 years ago (800 ka, ka = thousand years ago), led to another period of valley incision. Groundwater seepage and channel and slope erosion reworked the upland gravel, high phase and deposited the upland gravel, lower phase (unit TQg) in shallow valleys 20 to 50 feet below the higher gravels. These deposits today cap hilltops and interfluves, and form shallow fills in headwater valleys, between 70 and 85 feet in elevation on the upland north of Herbertsville. They have been removed by later erosion elsewhere in the quadrangle. Continuing incision during the middle Pleistocene (about 800 to 130 ka), primarily during periods of low sea level, formed the modern valley network. The lower reaches of these valleys were submerged during at least two periods of higher-than-present sea level in the middle and late Pleistocene. During these highstands, beach, estuarine, and nearshore deposits were laid down within valleys and in terraces along the bayshore and, north of Bay Head, along the oceanfront (fig. 1). These deposits are grouped into the Cape May Formation. The Cape May includes an older, eroded terrace deposit (Cape May Formation, unit 1, Qcm1) with a maximum surface elevation of 70 feet, and a lower, less eroded terrace deposit with a maximum surface elevation of 35 feet (Cape May Formation, unit 2, Qcm2). Fine-grained clay, silt, and fine sand in the subsurface beneath the outer part of the Cape May 2 terrace (Qcm2f, southeast of dashed purple line on fig. 1) is an estuarine and back-bay deposit laid down as sea level rose during deposition of the Cape May 2. Amino-acid racemization ratios (AAR), optically stimulated luminescence ages, and radiocarbon dates from the Delaware Bay area (Newell and others, 1995; Lacovara, 1997; O’Neal and others, 2000; O’Neal and Dunn, 2003; Sugarman and others, 2007) suggest that the Cape May 1 is of middle Pleistocene age (possibly marine-isotope stage [MIS] 11, 420 ka, or MIS 9, 330 ka; marine isotope stages from Lisiecki and Raymo, 2005) and that the Cape May 2 is of Sangamonian age (MIS 5, 125-80 ka). AAR of shells from vibracores off Long Beach Island, about 30 miles south of Mantoloking, indicate that the Cape May 2 correlate there is of Sangamonian age (Uptegrove and others, 2012). Global sea level during MIS 11 may have reached about 70 feet above present sea level (Olson and Hearty, 2009), about the maximum level of the Cape May 1 terrace, and during MIS 5e it reached about 25 feet above present sea level, about the level of the Cape May 2 terrace. If the age assignments of these terraces are accurate, these elevations suggest that full interglacial sea levels in this region are close to eustatic, as modeled by Potter and Lambeck (2003). Middle Wisconsinan (MIS 3, 65-35 ka) highstand deposits are described from the Delmarva Peninsula and the Virginia-North Carolina coastal plain (Mallinson and others, 2008; Scott and others, 2010; Parham and others, 2013; DeJong and others, 2015) at elevations up to 15 feet, but in New Jersey are apparently restricted to the inner shelf, at elevations of -60 feet or below (Carey and others, 2005; Uptegrove and others, 2012). Seismic and vibracore data show an east-trending middle Wisconsinan shoreline about 20 miles south of Mantoloking, with estuarine clays extending several miles to the north, although the clays do not extend beneath the barrier beaches or Barnegat Bay (Uptegrove and others, 2012). The base of the Cape May 2 deposits (contoured on fig. 1 at 25-foot interval) deepens to the southeast. This pattern implies southerly river flow during the MIS 6 lowstand (200-150 ka) before deposition of the Cape May 2. This southerly routing is also suggested by abandoned valleys between uplands capped by Cape May 1 deposits near Riviera Beach (green arrows on fig. 1), which may mark routes of the Manasquan River and Sawmill Creek, and by less-evident valleys crossing Metedeconk Neck (mostly west of the map area on the Lakewood quadrangle; the lower end of one is shown on fig. 1) that may mark routes of the Metedeconk River into what is now Kettle Creek. These abandoned valleys align with the southward trend of segments of the Manasquan and Metedeconk rivers upstream of the Cape May 2 terrace. They lead southward to the Toms River paleovalley, which exits eastward to the shelf in the Lavalette-Seaside Park area, 4 to 8 miles south of Mantoloking (Stanford and Sugarman, 2017). Southerly paleodrainage of the Manasquan and Metedeconk rivers is also consistent with the distribution of Quaternary sediments offshore on the inner shelf. Seismic surveying shows that, south of the Bay Head area, the base of Pleistocene sediments is at an elevation of -140 to -100 feet along a line parallel to, and two miles east of, the present shoreline (Lugrin, 2016). North of Bay Head the Pleistocene deposits are absent and Holocene deposits lie directly on Miocene formations. Farther offshore, the seismic data show a pre-Wisconsinan shelf valley draining northeastward from the Lavalette area, about 4 miles south of Mantoloking (Lugrin, 2016). This shelf valley may be the drain for the pre-Cape May 2 Manasquan, Metedeconk, and Toms rivers during MIS 6 and, possibly, earlier lowstands (Stanford and Sugarman, 2017). During the Cape May 2 highstand these valleys were filled with estuarine and nearshore deposits. As sea level lowered during the Wisconsinan the lower reaches of the Manasquan and Metedeconk rivers, and their tributaries on the Cape May 2 terrace, adopted new easterly routes on the Cape May 2 deposits. Incision of these streams created the present valleys (outlined by black ticked lines on fig. 1). These incisions reached depths of between -25 and -40 feet along the present coastline, as indicated by the position of lower terrace deposits (see below) beneath the Manasquan and Metedeconk estuaries (section CC’). Fluvial sediments laid down in modern valleys include upper and lower terrace deposits (units Qtu and Qtl) and floodplain (Qal) and wetland deposits (Qals) in valley bottoms. Colluvium deposited at the base of hillslopes in modern valleys includes upper colluvium (Qcu), which grades to the upper terraces and to the Cape May 2 marine terrace, and lower colluvium (Qcl), which grades to the lower terraces and to the modern floodplain. Like the upland gravels, the terrace, hillslope, and floodplain deposits represent erosion, transport, and redeposition of sand and gravel reworked from older surficial deposits and the Cohansey Formation by streams, groundwater seepage, and slope processes. Wetland deposits are formed by accumulation of organic matter in swamps and bogs. Upper terrace deposits form terraces and pediments 25 to 40 feet above modern floodplains and estuaries in the Manasquan River and Sawmill Creek valleys. Upper colluvium forms footslope aprons that grade to the upper terrace. The terrace deposits and colluvium were laid down chiefly during periods of cold climate in the middle Pleistocene. During cold periods, permafrost impeded deep infiltration of rainfall and snowmelt. The resulting waterlogged soils accelerated groundwater seepage and slope erosion, increasing the amount of sediment entering valleys, leading to terrace deposition. At their seaward limit, some of the deposits grade to the Cape May 2 marine terrace, and may have been laid down during periods of temperate climate when sea level was high. This topographic equivalence indicates that some of the upper terrace deposits aggraded during the Cape May 2 highstand. Lower terrace deposits (unit Qtl) form terraces with surfaces less than 15 feet above modern valley bottoms. They are of smaller extent than the upper terraces. They formed from stream and seepage erosion of the upper terrace and Cape May 2 deposits, and, in places, older deposits, chiefly during or slightly before the last period of cold climate corresponding to the late Wisconsinan glacial stage. Organic silt at the base of lower terrace deposits upstream of the quadrangle in the Manasquan and Metedeconk river basins yielded radiocarbon dates of 29,050±150 yrs BP (Beta 471459) (33.7-32.8 calibrated ka) from a site near Siloam in the Adelphia quadrangle and a date of 35,570+3180-2270 (GX-24257) (33.4-45.4 calibrated ka) from a site near Farmingdale in the Farmingdale quadrangle (Stanford and others, 2002). (Radiocarbon dates are calibrated using Reimer and others (2013) and the Calib 7.1.0 computer program. Calibrated dates are stated with two-sigma uncertainty.) These dates confirm deposition of the overlying terrace sediments in the middle and late Wisconsinan. Lower colluvium (Qcl) on grade with the lower terraces was also laid down during this time. As permafrost melted beginning around 18 ka, forest regrew and hillslope erosion slowed. The volume of sand washing into valleys was greatly reduced, and streams eroded into the lower terraces to form the modern floodplain (Qal and Qals). This erosion was largely complete by the beginning of the Holocene at 11 ka, based on radiocarbon dates on basal peat in floodplains in the region (Buell, 1970; Florer, 1972; Stanford, 2000c). Inland eolian deposits (unit Qe) form dunes and dune fields. Dune ridges are as much as 15 feet tall, but are more commonly 3 to 6 feet tall, and are as much as 3000 feet long (fig. 2). Their long axes (line symbols on map) are oriented east-west to northeast-southwest. Some of the ridges are closely spaced and parallel, creating a rippled pattern. Some form rims on the southeast side of shallow basins (lower left of fig. 2). These basins may have been created or enlarged by wind erosion (French and Demitroff, 2001). These patterns indicate that the dunes were laid down by winds blowing from the northwest. Most eolian deposits are on the Cape May 2 terrace. One dune near Riviera Beach is on the lower terrace. This distribution indicates that the eolian deposits were laid down after deposition of the Cape May 2, and, in places, also formed after deposition of the lower terraces. This span corresponds to the Wisconsinan Stage, a period of intermittently cold climate between 80 and 11 ka. Another product of cold climate is relict thermokarst basins. These are shallow depressions, circular or oval in plan, that are common on low-lying, flat landsurfaces where the water table is at shallow depth (fig. 2). They are shown by symbols where observed on Metedeconk Neck. Elsewhere they were once equally common but have been destroyed by urbanization. Most formed when ice-rich lenses within permafrost melted. Some may have formed or been enlarged by wind erosion, as discussed above. Modern beach, bay, and salt-marsh deposits were laid down during Holocene sea-level rise, chiefly within the past 6 ka in the map area. As sea level rose, tidal-marsh peat and fine-grained bay deposits (Qm) were covered by advancing flood-tidal delta sand laid down at the landward mouths of inlets, and barrier overwash sand laid down by storm flows washing over the oceanfront dunes (Qbo, Qbu). On the barrier islands, beach (Qbs) and dune (Qbe) sand are laid down atop the delta and overwash sand. The beach and dune deposits are eroded by waves and currents as sea level rises and are rarely preserved in the subsurface. Modern sediments in Barnegat Bay consist of tidal-delta and overwash sands forming flats on the bay side of the barrier spit and extending under the eastern part of the bay. In the bay these sands interfinger with salt-marsh peat and organic mud. The western part of the bay (west of the dashed black line on figure 1), adjacent to the salt marsh, is underlain by fine sand, silt, and clay eroded from mainland sources (Olsen and others, 1980; Psuty, 2004; Andrews and others, 2016; Bernier and others, 2016). Sea level has risen between 1 and 1.3 feet between 1900 and 2017 in the New Jersey region, as measured at tide gauges (https://tidesandcurrents.noaa.gov/sltrends/sltrends.html). This rise has caused the salt marsh and bayshore to advance inland on natural shorelines that are not stabilized by seawalls, bulkheads, and artificial beach replenishment. Inland advance of the salt marsh is indicated by a fringe of dead trees and spread of Phragmites reeds along the advancing front. These features are observed on all the natural inland edges of salt marsh in the quadrangle. DESCRIPTION OF MAP AND SUBSURFACE UNITS Grain-size terms are from the modified Wentworth scale (Ingram, 1982). Color terms are from Munsell Color Company (1975). ARTIFICIAL FILL—Sand, pebble gravel, minor clay and peat; gray, brown, very pale brown, white. In places includes man-made materials such as concrete, asphalt, brick, cinders, trash, and glass. Unstratified to poorly stratified. As much as 15 feet thick. In road and railroad embankments, dams, dikes, infilled pits, filled wetlands, dredge-spoil disposal cells, and land made from dredged material in bayfront residential developments. The extent of fill on salt-marsh deposits is based in part on the extent of the marsh as shown on topographic manuscript maps from the 1880s at a scale of 1:21,120 on file at the N. J. Geological and Water Survey, and aerial photography from the 1930s. WETLAND AND ALLUVIAL DEPOSITS—Fine-to-medium sand and pebble gravel, minor coarse sand and silty clayey sand; light gray, yellowish-brown, brown, dark brown; overlain by brown to black peat and gyttja. Peat is as much as 6 feet thick. Sand and gravel consist chiefly of quartz and are generally less than 3 feet thick. Sand and gravel are stream-channel deposits; peat and gyttja form from the vertical accumulation and decomposition of plant debris in swamps and marshes. In alluvial wetlands on modern valley bottoms. ALLUVIUM—Sediment as in unit Qals except peat and gyttja are thin and discontinuous and may be interbedded with or overlain by sand and gravel. As much as 10 feet thick. Includes small deposits of colluvium as in unit Qcl in places at the foot of steep slopes. TIDAL-MARSH AND ESTUARINE DEPOSITS—Peat, clay, silt, fine sand; brown, dark brown, gray, black; minor thin beds of medium-to-coarse sand and pebble gravel. Contains abundant organic matter and shells. As much as 50 feet thick. Deposited in tidal marshes, tidal flats, tidal channels, and bays and estuaries during Holocene sea-level rise, chiefly within the past 6 ka in the map area. BARRIER-BEACH DEPOSITS—Sand and minor gravel deposited by waves (Qbs), wind (Qbe), and tidal and storm flows (Qbo), and reworked by human activity (Qbu), during the Holocene. BEACH SAND—Fine-to-medium sand with few (1-5%) shells and shell fragments and minor (<1%) to few fine-to-medium quartz pebbles; very pale brown, white, light gray. Bedding is typically planar laminations that dip gently seaward. As much as 15 feet thick. Gravel is more common on mainland bay beaches than on ocean beaches or barrier bay beaches. DUNE SAND—Fine-to-medium sand with a few coarse sand grains and shell fragments; white, light gray, very pale brown. Bedding is typically large-scale trough-planar cross beds; cross beds dip 10-30°, bed sets are 1-5 feet thick. As much as 30 feet thick. Includes artificially constructed dunes that may contain rip-rap, organic debris, and human-made materials like fencing and netting placed to promote stability. OVERWASH AND TIDAL-DELTA SAND—Fine-to-medium sand, few shells and shell fragments, minor coarse sand and fine-to-medium pebble gravel, and a trace (<1%) of rip-up clasts of peat; light gray, very pale brown. Nonstratified to laminated to trough- and planar- cross-bedded. As much as 30 feet thick. Deposited in tidal channels and tidal flats associated with tidal deltas and by storm overwashes of the dune massif. In subsurface only. Underlies units Qbu, Qbe, and Qbs, and interfingers with unit Qm in the eastern part of Barnegat Bay. DUNE AND OVERWASH SAND, UNDIVIDED—Sand as in units Qbe and Qbo, graded and mixed during urban development. May include areas of artificial fill. As much as 10 feet thick. EOLIAN DEPOSITS—Fine-to-medium quartz sand; very pale brown, white, yellowish brown (fig. 3). As much as 15 feet thick. Nonstratified to weakly subhorizontally stratified. Form dune ridges and dune fields. Modern eolian sand on the barrier beaches is mapped separately as unit Qbe. LOWER COLLUVIUM—Fine-to-coarse sand, silty sand, pebble gravel; very pale brown, yellowish-brown, gray. Sand consists chiefly of quartz with a few (1-5%) glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor (<1%) ironstone in places. As much as 15 feet thick (estimated). Nonstratified to weakly subhorizontally stratified. Forms aprons at the base of steep slopes. The aprons grade to lower terraces or the modern floodplain and estuary. LOWER TERRACE DEPOSITS—Fine-to-medium sand, pebble gravel, minor coarse sand; yellowish-brown, light gray, brown, dark brown. As much as 15 feet thick. Sand consists chiefly of quartz with a few to some (5-10%) glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor ironstone in places. Form terraces and pediments in valley bottoms with surfaces 2 to 15 feet above the modern floodplain and estuary. Include stratified and cross-bedded stream-channel deposits and nonstratified to weakly stratified overbank and seepage deposits. UPPER TERRACE DEPOSITS—Fine-to-medium sand, pebble gravel, minor coarse sand; very pale brown, brownish-yellow, yellow. As much as 30 feet thick. Sand consists chiefly of quartz with a few to some glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor ironstone in places. Form terraces and pediments with surfaces 25 to 40 feet above the modern floodplain and estuary. Include stratified and cross-bedded stream-channel deposits and weakly stratified to nonstratified deposits laid down by overbank deposition and groundwater seepage on pediments. UPPER COLLUVIUM—Fine-to-coarse sand, silty sand, pebble gravel; yellowish-brown, very pale brown, gray. As much as 20 feet thick. Sand consists chiefly of quartz with a few to some glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor ironstone. Nonstratified to weakly stratified. CAPE MAY FORMATION—Sand and gravel (Qcm1, Qcm2) and clay, silt, and fine sand (Qcm2f) deposited in beach, nearshore, and estuarine settings during the middle and late Pleistocene. CAPE MAY FORMATION, UNIT 2—Fine-to-medium sand, pebble gravel, minor coarse sand, a few thin beds of silty clay; yellow, very pale brown, yellowish-brown. As much as 50 feet thick. Sand consists chiefly of quartz with few to some glauconite and opaque-mineral grains. Gravel consists of quartz and minor ironstone in places. Nonstratified to horizontally stratified, cross-bedded in places (fig. 4). Forms a terrace with a maximum surface elevation of 35 feet. CAPE MAY FORMATION, UNIT 2, FINE-GRAINED DEPOSITS—Clay, silt, fine sand, minor organic matter; light gray to gray. As much as 50 feet thick. In subsurface only, inferred from well records (fig.1, sections CC’, DD’). CAPE MAY FORMATION, UNIT 1—Fine-to-medium sand, iron-cemented in places, pebble gravel, minor coarse sand, a few thin beds of silty clay; yellow, very pale brown, yellowish-brown, reddish-brown where iron-cemented. As much as 30 feet thick. Sand consists chiefly of quartz with a few glauconite and opaque-mineral grains. Gravel consists of quartz and minor ironstone in places. Nonstratified to horizontally stratified. Forms eroded terraces with a maximum surface elevation of 70 feet. UPLAND GRAVEL, LOWER PHASE—Fine-to-coarse sand, clayey in places, and pebble gravel; yellow, very pale brown, yellowish-brown. As much as 15 feet thick. Sand and gravel consist chiefly of quartz. Nonstratified to weakly horizontally stratified. Occurs as erosional remnants on hilltops and interfluves, and in headwater valleys, between 70 and 85 feet in elevation. UPLAND GRAVEL, HIGH PHASE—Fine-to-coarse sand, clayey in places; pebble gravel; trace small-cobble gravel; yellow, yellowish-brown, reddish-yellow. As much as 25 feet thick. Sand is chiefly quartz with a trace of weathered chert. Gravel is chiefly quartz. Nonstratified to horizontally stratified, cross-bedded in places (fig. 5). Cross-beds are commonly tabular-planar. Occurs as erosional remnants on uplands above 75 to 100 feet in elevation. COHANSEY FORMATION—Fine-to-medium sand, some medium-to-coarse sand, minor very fine sand, minor very coarse sand to very fine pebbles, trace fine-to-medium pebbles; very pale brown, brownish-yellow, white, reddish-yellow, rarely reddish-brown, red, and light red; with thin beds of white, yellow, and red clay and clayey very fine-to-fine sand in places (figs. 6, 7). Clay beds are 0.5 inch to 2 feet thick. Exposure is too limited to map sand and clay beds but in table 1 they are identified from well logs as “Tchs” and “Tchc” respectively. Sand is well-stratified to nonstratified; stratification ranges from thin, planar, subhorizontal beds to large-scale trough and planar cross-bedding. Sand is quartz; coarse-to-very coarse sand may include as much as 5% weathered chert and a trace of weathered feldspar. As much as 20 percent of the sand fraction consists of detrital heavy minerals (Markewicz, 1969), commonly concentrated along bedding planes. In these concentrations, ilmenite dominates the opaque minerals; to a lesser extent zircon and sillimanite dominate the nonopaque minerals. Kaolinite dominates the clay-sized minerals. Coarse-to-very coarse sands commonly are slightly clayey; the clays occur as grain coatings or as interstitial infill. This clay-size material is from weathering of chert and feldspar rather than from primary deposition. Pebbles are chiefly quartz with minor gray chert and rare gray quartzite. Some chert pebbles are light gray, partially weathered, pitted, and partially decomposed; some are fully weathered to white clay. In a few places, typically above or below clayey strata, sand may be hardened or cemented by iron oxide, forming reddish-brown hard sands or ironstone masses. The basal contact of the Cohansey was not observed in the quadrangle. Elsewhere, the Cohansey appears to unconformably overlie the Kirkwood Formation although it may be age-equivalent to younger Kirkwood members downdip to the south. Micaceous fine sand typical of the Kirkwood occurs within the Cohansey in the northwest part of the map area, suggesting a gradational or interfingered contact of the two formations locally. Pollen and dinoflagellates indicate that the Cohansey is of middle to late Miocene age (Rachele, 1976; Greller and Rachele, 1983; Owens and others, 1988; deVerteuil, 1997; Miller and others, 2001). KIRKWOOD FORMATION—Quartz sand, fine-to-medium grained, and clay-silt. Sand is nonstratified to cross-bedded and laminated, light gray, gray, and light-yellow, micaceous, with minor coarse sand and fine gravel. Sand consists chiefly of quartz, with small amounts of feldspar and mica (mostly muscovite). Detrital heavy minerals are concentrated on bedding planes and are chiefly opaques, especially ilmenite, with lesser amount of nonopaques including zircon, staurolite, garnet, rutile, and tourmaline. Clay and silt are dark gray to brown. Finely dispersed clay minerals include kaolinite, illite, and illite/smectite. The lowermost Kirkwood (below tielines on sections), termed the Asbury clay (Ries and others, 1904), or the Asbury Park Member (Isphording, 1970), is a dark gray to dark brown, peaty, laminated clay-silt with lenses of massive to locally cross-bedded fine sand. Pyrite is common in the clayey, organic-rich beds. At the base of the Kirkwood a bed of coarse glauconite-quartz sand, with granules and scattered shark teeth, typically 2 to 3 feet thick, rests unconformably on the Shark River Formation. Maximum thickness 150 feet. The Kirkwood Formation, as revised by Owens and others (1998), includes the following members, in ascending order: (1) an unnamed lower member (equivalent to the Brigantine Member of Miller and others, 1997 or sequence Kw1a of Sugarman and others, 1993); (2) the Shiloh Marl Member (equivalent to sequence Kw1b of Sugarman and others, 1993); (3) the Wildwood Member (equivalent to sequence Kw2 of Sugarman and others, 1993); and (4) the Belleplain Member (equivalent to sequence Kw3 of Sugarman and others, 1993). Both the unnamed lower member and the Shiloh Marl Member are clayey at the base and sandy at the top, a pattern that is evident on gamma-ray geophysical logs. The unnamed lower member and Shiloh Marl Member are approximately 21-19 million years old, the Wildwood Member is 18-15 million years old, and the Belleplain Member is 13 million years old (Miller and others, 1997). Previous mapping indicates that the lower member and Shiloh Marl Member are present in the quadrangle, while the Wildwood and Belleplain members are present only south of the quadrangle (Sugarman and others, 1993). In the Sea Girt corehole (well 107), the lower member and Shiloh Marl Member were tentatively identified, as was a thin upper clay-silt possibly correlative to the Wildwood Member, although no datable material was found in the Kirkwood to substantiate this correlation (Miller and others, 2006). SHARK RIVER FORMATION—Very fine-to-fine, slightly glauconitic and micaceous quartz sand, which thins to the northwest (above upper tielines on sections) grading downward into clay-silt, very fossiliferous, glauconitic (up to 15%), slightly micaceous, greenish-gray to very dark greenish-gray; nonstratified to thick-bedded and extensively burrowed (below upper tielines). Thin porcellanitic zones are present in places. There is less glauconite is the lower 40 feet of the formation (below lower tielines on sections), although glauconite is locally abundant in the basal 10 feet. Calcareous microfossils are abundant in the lower clay-silt; small, broken mollusk shells are present in the upper fine sand. Clay minerals include illite, illite/smectite, kaolinite, and minor amounts of clinoptilolite. The upper sand is also known as the Toms River Member and the lower clay-silt as the Squankum Member (Enright, 1969). Maximum thickness of the Shark River Formation in the map area is 230 feet. The contact with the underlying Manasquan Formation is unconformable and is placed at the top of the pale-olive clay-silt of the Manasquan. It is marked by a sharp positive gamma-ray response on geophysical logs. Calcareous nannofossils in samples from the Allaire State Park corehole (Sugarman and others, 1991) and in the Sea Girt corehole (Miller and others, 2006) indicate the Shark River is of middle Eocene age (nannozones NP 14-17). MANASQUAN FORMATION—Clay-silt, dusky-yellow-green to pale-olive and grayish-green, extensively burrowed, nonstratified to thick-bedded, calcareous, minor very fine quartz sand. Cross-bedded laminae of very fine sand are present locally. Fine glauconite sand is commonly dispersed throughout the dominantly clayey matrix. Clay minerals include illite, illite/smectite, and minor clinoptilolite. In the Sea Girt corehole, silica-cemented porcellanite zones are common (Miller and others, 2006). The contact with the underlying Marlboro or Vincentown formations is marked by a sharp positive response on gamma-ray logs. Otherwise the formation, in general, has a neutral response on gamma-ray logs, not reflecting the dominant clay-silt lithology. Maximum thickness is 150 feet. Calcareous nannofossils and planktonic foraminifers in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Manasquan is of early Eocene age (nannozones NP 11-12, foraminifer zones P 7-8). MARLBORO FORMATION—Clay to sandy silty clay, greenish-gray, brown, reddish-brown, with glauconite, pyrite, and phosphate nodules. Maximum thickness is 35 feet, and the formation pinches out to south (section CC’). The Marlboro Formation was named by Glaser (1971) in Maryland and identified in the subsurface in New Jersey by Miller and others (2017). Calcareous nannofossils in samples from the Sea Girt corehole indicate that the Marlboro Formation (identified as “unnamed clay” in Miller and others, 2006) is of earliest Eocene age (nannozone NP 9b). VINCENTOWN FORMATION—Clayey silt and silt, extensively burrowed, slightly micaceous, finely laminated where not burrowed, dark greenish-gray to very dark gray, with thin beds of very fine quartz and glauconite sand and silt. Grades downward to a massive, slightly quartzose, glauconitic silt and glauconite sand with shell material at the base. The contact with the underlying Hornerstown Formation is marked by a sharp positive response on gamma-ray logs. Maximum thickness is 110 feet. Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Vincentown is of late Paleocene age (nannozones NP 8 and 9a). HORNERSTOWN FORMATION—Glauconite, clayey, massive- bedded, very dark greenish-gray to very dark grayish-brown, with scattered shells and shell fragments. Glauconite grains are mainly medium to coarse sand in size and botryoidal. Contains 1 to 2 percent fine-to-very coarse-grained quartz sand, phosphate fragments, pyrite, and lignite. Matrix contains minor glauconite clay. Locally cemented by iron oxides and siderite. Unconformably overlies the Red Bank Formation. Maximum thickness is 40 feet. Calcareous nannofossils and planktonic foraminifers in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Hornerstown is of early Paleocene age (nannozones NP 2-4, foraminifer zones P1-P3). NAVESINK-RED BANK FORMATIONS (UNDIVIDED)— Glauconite, slightly quartzose, clayey, greenish-black, with calcareous shells. Glauconite grains are mainly medium to coarse sand in size. Unconformably overlies the Mount Laurel Formation. This contact is easily distinguished in the subsurface by a sharp positive gamma-ray response. Maximum thickness is 70 feet. In outcrop in northern Monmouth County the Navesink Formation and the Red Bank Formation form an unconformity-bounded, coarsening-upward sequence consisting of a basal glauconite sand (Navesink Formation), a middle silt (lower Red Bank Formation), and an upper quartz sand (upper Red Bank Formation). Downdip from outcrop, the sand pinches out and the silt changes facies to glauconite. Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Navesink is of Late Cretaceous (Maastrichtian) age (nannozones CC 23a, 25, 26). MOUNT LAUREL FORMATION—Quartz sand, fine- to coarse-grained, slightly glauconitic, extensively burrowed, slightly micaceous and feldspathic, commonly interbedded with thin layers of dark clay and silt, and intervals of scattered shells. Olive-gray to dark greenish-gray. Conformably overlies the Wenonah Formation. The transition from the Wenonah to the Mount Laurel is generally marked by an increase in grain size, a decrease in mica (Owens and Sohl, 1969), and the appearance of alternating thin beds of clay and sand in the Mount Laurel (Minard, 1969). Maximum thickness is 70 feet. Calcareous nannofossils, and a strontium stable-isotope age of 74.5 Ma, in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Mount Laurel is of Late Cretaceous (late Campanian) age (nannozones CC21-22). MARSHALLTOWN–WENONAH FORMATIONS (UNDIVID- ED)—Glauconite, greenish-black, extensively burrowed, with silt and pyrite and rare shell fragments (Marshalltown), grading upward into a micaceous, lignitic, burrowed clayey fine sand to silt with traces of glauconite and pyrite (Wenonah). The Marshalltown- Wenonah is recognized in the subsurface by a gamma spike at the base of the Marshalltown passing into a relatively flat, high-intensity pattern above. The two formations are undivided due to the thinness of the Marshalltown Formation (approximately 10 feet) and its lithologic similarity to the lower Wenonah Formation. Unconformably overlies the Englishtown Formation. The lower contact is extensively burrowed; wood and locally coarse sand from the underlying Englishtown Formation are reworked into the basal Marshalltown. Maximum thickness is 60 feet. Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Marshalltown is of Late Cretaceous (late Campanian) age (nannozone CC20). ENGLISHTOWN FORMATION—Informally divided into the upper Englishtown and lower Englishtown members. The upper member consists of fine- to coarse-grained sand interbedded with thin, dark-gray, micaceous, woody, clay-silt that grades downward to glauconitic, dark greenish-gray, micaceous, and lignitic clay-silt to very fine quartz sand. The sand is dominantly quartz; less than 10 percent consists of feldspar, rock fragments, and glauconite. The upper member is defined on gamma-ray logs by a thick, low-intensity sand at its top (above tielines on sections) and a thick, high-intensity clayey unit (below tielines) at its base. The upper member unconformably overlies the lower Englishtown member. In the Sea Girt corehole, a 1.5-foot indurated zone marks the contact. Maximum thickness of the upper member is 150 feet. The lower member is quartz sand, feldspathic, micaceous and lignitic, fine- to medium-grained, medium-to dark-gray. Sand is typically cross-bedded. The contact of the lower member with the underlying Woodbury Formation is gradational. Maximum thickness of the lower member is 40 feet. Calcareous nannofossils and strontium stable-isotope ages of 74-78 Ma in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Englishtown Formation is of Late Cretaceous (middle-late Campanian) age (nannozones CC19-20). MERCHANTVILLE-WOODBURY FORMATIONS (UNDIVID- ED)—Clay and silt, some very fine sand with mica, and a few lenses of finely disseminated pyrite, lignite, and siderite (Woodbury Formation). Color ranges from dark gray to olive black. Bedding is nonstratified to finely laminated with alternating beds of very fine sand and clay-silt. Grades downward into an intercalated, thick-bedded sequence of glauconitic sand and silt and micaceous clayey silt (Merchantville Formation). Quartz and glauconite are the major sand components; feldspar, mica (colorless and green), and pyrite are minor constituents. Siderite-cemented beds are common. The Merchantville contains zones of broken calcareous mollusk shells. Unconformably overlies the Magothy Formation. Maximum thickness is 200 feet. Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Merchantville and Woodbury formations are of Late Cretaceous (Santonian to mid-Campanian) age based on (nannozones CC16-18). MAGOTHY FORMATION—Quartz sand and clay, thin- to thick-bedded. Sand is light- to medium-gray or brownish-gray; clay is olive-black to grayish-black. Bedding is horizontally laminated to cross-bedded. The sand is fine to very coarse, well sorted within each bed, predominantly quartz, and includes minor feldspar and mica. Pyrite-cemented and pyrite-coated sand concretions are common. Lignite is abundant in beds as much as 0.5 feet thick. Recognized on gamma logs as a series of thick sands and interbedded clay-silts. Unconformably overlies the Raritan Formation. Maximum thickness is 250 feet. Pollen in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Magothy is of Late Cretaceous (Turonian-Coniacian) age (pollen zones V-VII). RARITAN FORMATION—Includes two members: the Woodbridge Clay Member (Krw) and the underlying Farrington Sand Member (Krf). The Woodbridge Clay Member is clay and silt, dark gray, nonstratified, with mica, pyrite, lignite, and siderite. Siderite forms layers 0.25 to 0.5 inches thick. Maximum thickness is 250 feet. The Farrington Sand Member is fine-to-medium quartz sand, white, yellow, red, light gray, commonly interbedded with thin coarse sand and fine gravel beds and thin to thick dark gray silt beds. Maximum thickness is 40 feet. Pollen and calcareous nannofossils in samples from the Sea Girt corehole indicate that the Raritan is of Late Cretaceous (Cenomanian-Turonian) age (Miller and others, 2006). The Woodbridge Clay Member yielded zone IV pollen and nannozones CC 10-11. The Farrington Sand Member yielded zone III pollen. In the Sea Girt corehole the Raritan Formation is identified as the Bass River Formation based on downdip correlation to subsurface marine sediments in southern Burlington County (Petters, 1976). It is identified as Raritan Formation here because of its lithologic continuity with the outcropping updip Raritan in Middlesex County. POTOMAC FORMATION—Fine-to-coarse quartz sand with beds of clay and silty clay; white, yellow, red where weathered, gray where unweathered. Sands are nonstratified to horizontally bedded to cross-bedded, clays are in beds as much as 10 feet thick. More than 400 feet thick; full thickness is not penetrated by drillholes in the quadrangle. Pollen in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the uppermost Potomac in the quadrangle is of Late Cretaceous (Cenomanian) age (pollen zone III), indicating it is within the Potomac Formation, unit 3, of Doyle and Robbins (1977). REFERENCES Andrews, B. D., Miselis, J. L., Danforth, W. W., Irwin, B. J., Worley, C. R., Bergeron, E. M., and Blackwood, D. S., 2016, Marine geophysical data collected in a shallow back-barrier estuary, Barnegat Bay, New Jersey: U. S. Geological Survey Data Series 937, version 1.1, 15 p. Bernier, J. C., Stalk, C. A., Kelso, K. W., Miselis, J. L., and Tunsted, R., 2016, Sediment data collected in 2014 from Barnegat Bay, New Jersey: U. S. Geological Survey Data Series 985. Buell, M. F., 1970, Time of origin of New Jersey Pine Barrens bogs: Bulletin of the Torrey Botanical Club, v. 97, p. 105-108. Carey, J. S., Sheridan, R. E., Ashley, G. M., and Uptegrove, J., 2005, Glacially influenced late Pleistocene stratigraphy of a passive margin: New Jersey’s record of the North American ice sheet: Marine Geology, v. 218, p. 153-173. Castelli, M. V., Latini, D., Uptegrove, J., Waldner, J. S., Hall, D. W., and Friedman, A. L., 2015, Significant sand resource areas in state and federal waters offshore Monmouth County, New Jersey: N. J. Geological and Water Survey Geologic Map Series GMS 15-3, scale 1:80,000. DeJong, B. D., Bierman, P. R., Newell, W. L., Rittenour, T. M., Mahan, S. A., Balco, G., Rood, D. H., 2015, Pleistocene relative sea levels in the Chesapeake Bay region and their implications for the next century: GSA Today, v. 25, p. 4-10. deVerteuil, Laurent, 1997, Palynological delineation and regional correlation of lower through upper Miocene sequences in the Cape May and Atlantic City boreholes, New Jersey Coastal Plain, in Miller, K.G., and Snyder, S. W., eds., Proceeding of the Ocean Drilling Program, Scientific Results, v. 150X: College Station, Texas, Ocean Drilling Program, p. 129-145. Doyle, J. A., and Robbins, E. I., 1977, Angiosperm pollen zonation of the Cretaceous of the Atlantic coastal plain and its application to deep wells in the Salisbury embayment: Palynology, v. 1, p. 43-78. Florer, L. E., 1972, Palynology of a postglacial bog in the New Jersey Pine Barrens: Bulletin of the Torrey Botanical Club, v. 99, p. 135-138. French, H. M., and Demitroff, M., 2001, Cold-climate origin of the enclosed depressions and wetlands (“spungs”) of the Pine Barrens, southern New Jersey, USA: Permafrost and Periglacial Processes, v. 12, p. 337-350. Glaser, J. D., 1971, Geology and mineral resources of southern Maryland: Maryland Geological Survey, Report of Investigations 15, 85 p. Greller, A. M., and Rachele, L. D., 1983, Climatic limits of exotic genera in the Legler palynoflora, Miocene, New Jersey, USA: Review of Palaeobotany and Palynology, v. 40, p. 149-163. Ingram, R. L., 1982, Modified Wentworth scale, in Dutro, J. T., Dietrich, R. V., and Foose, R. M., eds., AGI data sheets for geology in the field, laboratory, and office, 2nd edition: American Geological Institute, Washington, D. C. Isphording, W. C., 1970, Petrology, stratigraphy, and redefinition of the Kirkwood Formation (Miocene) of New Jersey: Journal of Sedimentary Petrology, v. 40, p. 986-997. 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. Lisiecki, L. E., and Raymo, M. E., 2005, Pliocene-Pleistocene stack of 57 globally distributed benthic d 18 O records: Paleoceanography, v. 20, PA 1003. Lugrin, L., 2016, Delta progradation and channel drainage systems from the early Miocene to the present day between Barnegat and Manasquan inlets, New Jersey: unpublished M. S. thesis, Rutgers University, New Brunswick, N. J., 165 p. Mallinson, D., Burdette, K., Mahan, S., and Brook, G., 2008, Optically stimulated luminescence age controls on late Pleistocene and Holocene coastal lithosomes, North Carolina, USA: Quaternary Research, v. 69, p. 97-109. Markewicz, F. J., 1969, Ilmenite deposits of the New Jersey coastal plain, in Subitzky, S., ed., Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions: Rutgers University Press, New Brunswick, N. J., p. 363-382. Miller, K. G., Browning, J. V., Aubry, M.-P., Babila, T., Baluyot, R. D., Esmeray-Senlet, S., Feigenson, M. D., Karakaya, S., Lombardi, C. J., Makarova, M., McCreary, S., McLaughlin, P. P., Jr., Monteverde, D. H., Olsson, R. K., Smith, C. T., Sugarman, P. J., Wright, J. D., 2017, Wilson Lake site, in Miller, K. G., Sugarman, P. J., Browning, J. V., and others, eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174 AX (Supplement): College Station, Texas, Ocean Drilling Program, p. 1-31. Miller, K. G., Rufolo, S., Sugarman, P. J., Pekar, S. F., Browning, J. V., and Gwynn, D. W., 1997, Early to middle Miocene sequences, systems tracts, and benthic foraminiferal biofacies, New Jersey coastal plain, in Miller, K. G., and Snyder, S. W., eds, Proceedings of the Ocean Drilling Program, Scientific Results, Volume 150X: College Station, Texas, Ocean Drilling Program, p. 169-186. Miller, K. G., Sugarman, P. J., Browning, J. V., Pekar, S. F., Katz, M. E., Cramer, B. S., Monteverde, D., Uptegrove, J., McLaughlin, P. P., Jr., Baxter, S. J., Aubry, M.-P., Olsson, R. K., Van Sickel, B., Metzger, K., Feigenson, M. D., Tiffin, S., and McCarthy, F., 2001, Ocean View site, in Miller, K. G., Sugarman, P. J., Browning, J. V., and others, eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174AX (Supplement 2): College Station, Texas, Ocean Drilling Program, p. 1-72. Miller, K. G., Sugarman, P. J., Browning, J. V., Aubry, M.-P., Brenner, G. J., Cobbs, G. III, de Romero, L., Feigenson, M. D., Harris, A., Katz, M. E., Kulpecz, A., McLaughlin, P.P., Jr., Misintseva, S., Monteverde, D. H., Olsson, R. K., Patrick, L., Pekar, S. J., and Uptegrove, J., 2006, Sea Girt Site, in Miller, K. G., Sugarman, P. J., Browning, J. V. eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174AX (Supplement): College Station, Texas, Ocean Drilling Program, p. 1-104. Minard, J. P., 1969, Geology of the Sandy Hook quadrangle in Monmouth County, New Jersey: U. S. Geological Survey Bulletin 1276, 43 p. Munsell Color Company, 1975, Munsell soil color charts: Baltimore, Maryland, Kollmorgen Corporation, MacBeth Division. Newell, W. L., Powars, D. S., Owens, J. P., and 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. Olsen, C. R., Biscaye, P. E., Simpson, H. J., Trier, R. M., Kostyk, N., Bopp, R. F., Li, Y.-H., and Feely, H. W., 1980, Reactor-released radionuclides and fine-grained sediment transport and accumulation patterns in Barnegat Bay, New Jersey, and adjacent shelf waters: Estuarine and Coastal Marine Science, v. 10, p. 119-142. Olson, S. L., and Hearty, P. J., 2009, A sustained +21 m sea-level highstand during MIS 11 (400 ka): direct fossil and sedimentary evidence from Bermuda: Quaternary Science Reviews, v. 28, p. 271-285. O’Neal, M. L., and Dunn, R. K., 2003, GPR investigation of multiple stage-5 sea level fluctuations on a siliclastic estuarine shoreline, Delaware Bay, southern New Jersey, U. S. A., in Bristow, C. S., and Jol, H. M., eds., Ground penetrating radar in sediments: Geological Society of London, Special Publication, v. 211, p. 67-77. O’Neal, M. L., Wehmiller, J. F., and Newell, W. L., 2000, Amino acid geochronology of Quaternary coastal terraces on the northern margin of Delaware Bay, southern New Jersey, U. S. A., in Goodfriend, G. A., Collins, M. J., Fogel, M. L., Macko, S. A., Wehmiller, J. F., eds., Perspectives in Amino Acid and Protein Geochemistry: Oxford University Press, p. 301-319. Owens, J. P., Bybell, L. M., Paulachok, G., Ager, T. A., Gonzalez, V. M., and Sugarman, P. J., 1988, Stratigraphy of the Tertiary sediments in a 945-foot-deep corehole near Mays Landing in the southeastern New Jersey Coastal Plain: U. S. Geological Survey Professional Paper 1484, 39 p. Owens, J. P., and Sohl, N. F., 1969, Shelf and deltaic paleoenvironments in the Cretaceous-Tertiary formations of the New Jersey Coastal Plain, Field Trip 2, in Subitzky, S., ed., Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions: New Brunswick, N. J., Rutgers University Press, p. 235-278. Owens, J. P., Sugarman, P. J., Sohl, N. F., Parker, R. A., Houghton, H. F., Volkert, R. A., Drake, A. A., Jr., and Orndorff, R. C., 1998, Bedrock geologic map of central and southern New Jersey: U. S. Geological Survey Miscellaneous Investigations Series Map I-2540-B, scale 1:100,000. Parham, P. R., Riggs, S. R., Culver, S. J., Mallinson, D. J., Jack Rink, W., Burdette, K., 2013, Quaternary coastal lithofacies, sequence development, and stratigraphy in a passive margin setting, North Carolina and Virginia, USA: Sedimentology, v. 60, p. 503-547. Petters, S. W., 1976, Upper Cretaceous subsurface stratigraphy of Atlantic coastal plain of New Jersey: AAPG Bulletin, v. 60, p. 87-107. Potter, E.-K., and Lambeck, K., 2003, Reconciliation of sea-level observations in the western North Atlantic during the last glacial cycle: Earth and Planetary Science Letters, v. 217, p. 171-181. Psuty, N. P., 2004, Morpho-sedimentological characterisitics of the Barnegat Bay-Little Egg Harbor estuary, in Davis, D. W., and Richardson, M., eds., The Coastal Zone: Papers in Honor of H. Jesse Walker: Lousiana State University, Geoscience and Man Series no. 38, Baton Rouge, Louisiana, p. 81-92. Rachele, L. D., 1976, Palynology of the Legler lignite: a deposit in the Tertiary Cohansey Formation of New Jersey, USA: Review of Palaeobotany and Palynology, v. 22, p. 225-252. Reimer, P. J., Bard, E., Bayliss, A., Beck, J. W., Blackwell, P. G., Bronk Ramsey, C., Buck, C. E., Cheng, H., Edwards, R. L., Friedrich, M., Grootes, P. M., Guilderson, T. P., Haflidason, H., Hajdas, I., Hatte, C., Heaton, T. J., Hoffmann, D. L., Hogg, A. G., Hughen, K. A., Kaiser, K. F., Kromer, B., Manning, S. W., Niu, M., Reimer, R. W., Richards, D. A., Scott, E. M., Southon, J. R., Staff, R. A., Turney, C. S. M., and van der Plicht, J., 2013, IntCal13 and Marine13 radiocarbon age calibration curves 0-50,000 years cal BP: Radiocarbon, v. 55, p. 1869-1887. Ries, H., Kummel, H. B., and Knapp, G. N., 1904, The clays and clay industry of New Jersey: N. J. Geological Survey, Final Report of the State Geologist, v. 6, 548 p. Scott, T. W., Swift, D. J. P., Whittecar, G. R., and Brook, G. A., 2010, Glacioisostatic influences on Virginia’s late Pleistocene coastal plain deposits: Geomorphology, v. 116, p. 175-188. Stanford, S. D., 2000a, Surficial geology of the Asbury Park quadrangle, Monmouth and Ocean counties, New Jersey: N. J. Geological Survey Open File Map OFM 40, scale 1:24,000. Stanford, S. D., 2000b, Surficial geology of the Farmingdale quadrangle, Monmouth and Ocean counties, New Jersey: N. J. Geological Survey Open File Map 35, scale 1:24,000. Stanford, S. D., 2000c, Geomorphology of selected Pine Barrens savannas: report prepared for the N. J. Department of Environmental Protection, Division of Parks and Forestry, Office of Natural Lands Management, 10 p. and appendices. Stanford, S. D., 2010, Onshore record of Hudson River drainage to the continental shelf from the late Miocene through the late Wisconsinan deglaciation, USA: synthesis and revision: Boreas, v. 39, p. 1-17. Stanford, S. D., Ashley, G. M., Russell, E. W. B., and 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., 2017, Geology of the Toms River and Seaside Park quadrangles, Ocean County, New Jersey: N. J. Geological and Water Survey Open File Map OFM 116, scale 1:24,000. Sugarman, P. J., Miller, K. G., Browning, J. V., Monteverde, D. H., Uptegrove, J., McLaughlin, P. P., Jr., Stanley, A. M., Wehmiller, J., Kulpecz, A., Harris, A., Pusz, A., Kahn, A., Friedman, A., Feigenson, M. D., Barron, J., and McCarthy, F. M. G., 2007, Cape May Zoo site, in Miller, K. G., Sugarman, P. J., Browning, J. V., and others, eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174AX (Supplement 7), p. 1-66. Sugarman, P. J., Miller, K. G., Owens, J. P., and Feigenson, M. D., 1993, Strontium-isotope and sequence stratigraphy of the Miocene Kirkwood formation, southern New Jersey: Geological Society of America Bulletin, v. 105, p. 423-436. Sugarman, P. J., Monteverde, D. H., Boyle, J. T., and Domber, S. E., 2013, Aquifer correlation map of Monmouth and Ocean counties, New Jersey: N. J. Geological and Water Survey Geologic Map Series GMS 13-1. Sugarman, P. J., Owens, J. P., and Bybell, L. M., 1991, Geologic map of the Adelphia and Farmingdale quadrangles, Monmouth and Ocean counties, New Jersey, New Jersey Geological Survey Geologic Map Series 91-1, scale 1:24,000. Uptegrove, J., Waldner, J. S., Stanford, S. D., Monteverde, D. H., Sheridan, R. E., and Hall, D. W., 2012, Geology of the New Jersey offshore in the vicinity of Barnegat Inlet and Long Beach Island: N. J. Geological Survey Geologic Map Series GMS 12-3, scale 1:80,000. Volkert, R. A., Drake, A. A., Jr., and Sugarman, P. J., 1996, Geology, geochemistry, and tectonostratigraphic relations of the crystalline basement beneath the coastal plain of New Jersey and contiguous areas: U. S. Geological Survey Professional Paper 1565-B, 48 p. MAP SYMBOLS Contact of surficial deposits—Solid where well-defined by landforms as visible on 1:12,000 stereo airphotos and LiDAR imagery; long-dashed where approximately located; short-dashed where gradational or featheredged; dotted where exposed in excavations. Contact of bedrock formations—Approximately located. Dotted where concealed by surficial deposits. Concealed bedrock formation—Covered by surficial deposits. Material penetrated by hand-auger hole, or observed in exposure or excavation. Number indicates thickness of surficial material, in feet, where penetrated. Symbols within surficial deposits without a thickness value indicate that surficial material is more than 5 feet thick. Where more than one unit was penetrated, the thickness (in feet) of the upper unit is indicated next to its symbol and the lower unit is indicated following the slash. Photograph location Well or test boring showing formations penetrated—Location accurate to within 200 feet. List of formations penetrated is provided in table 1. Well or test boring showing formations penetrated—Location accurate to within 500 feet. List of formations penetrated is provided in table 1. Dune ridge—Line on crest. Shallow topographic basin—Line at rim; pattern in basin. Includes thermokarst basins formed from melting of permafrost and a few deflation basins, adjacent to eolian deposits, formed from wind erosion. Excavation perimeter—Line encloses excavated area. Sand and gravel pit—Inactive in 2018. Dominant grain size of bay-bottom sediment in 6-foot vibracore—Data on file at N. J. Geological and Water Survey. sand sand and clay-silt clay-silt Dominant grain size of bay-bottom sediment in shallow grab sample—Data from Andrews and others (2016). sand sand and clay-silt clay-silt Dominant grain size of bay-bottom sediment in 6-foot vibracore—Data from Bernier and others (2016). sand sand and clay-silt clay-silt GEOLOGY OF THE POINT PLEASANT QUADRANGLE MONMOUTH AND OCEAN COUNTIES, NEW JERSEY by Scott D. Stanford, Peter J. Sugarman, Michael V. Castelli, and Alexandra R. Carone 2018 7000 FEET 1000 1000 0 2000 3000 4000 5000 6000 .5 1 KILOMETER 1 0 SCALE 1:24 000 1/ 2 1 0 1 MILE MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1999 TRUE NORTH LOCATION IN NEW JERSEY 13 O CONTOUR INTERVAL 5 FEET BATHYMETRIC CONTOURS IN FEET NATIONAL GEODETIC VERTICAL DATUM OF 1929 Base map from U. S. Geological Survey Point Pleasant quadrangle, 1995. Topography compiled 1986. Planimetry derived from imagery taken 1995. Survey control current as of 1984. North American Datum of 1983. Bedrock geology mapped by P. J. Sugarman, M. V. Castelli, A. R. Carone, and S. D. Stanford, 2016-2018 Surficial geology by S. D. Stanford, 2018 Drilling by B. Buttari Drilling assistance by M. Castelli, I. Snook, G. Steidl, N. Thistle Geophysical logging by M. Gagliano and M. Spencer Cartography by S. D. Stanford and A. R. Carone Reviewed by J. W. Jengo and C. S. Swezey Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program, under USGS award numbers G16AC00284 (bedrock) and G17AC00256 (surficial). 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. DEPARTMENT OF ENVIRONMENTAL PROTECTION WATER RESOURCES MANAGEMENT NEW JERSEY GEOLOGICAL AND WATER SURVEY GEOLOGY OF THE POINT PLEASANT QUADRANGLE MONMOUTH AND OCEAN COUNTIES, NEW JERSEY GEOLOGIC MAP SERIES GMS 18-5 SHEET 1 OF 2 Pamphlet containing tables 1 and 2 accompanies map Prepared in cooperation with the U. S. GEOLOGICAL SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM Manasquan River Sawmill Creek Metedeconk River Beaverdam Ck Barnegat Bay Kettle Creek -25 -50 -75 -25 -50 0 0 0 -25 -25 0 0 -25 -25 Metedeconk Neck Mantoloking Bay Head Point Pleasant Brielle Herbertsville Riviera Beach Wardells Neck figure 2 Atlantic Ocean fine-grained bay deposits tidal-delta and overwash sand 0 1 2 miles Holocene features salt marsh ocean beach beach dunes overwash plain and urbanized barrier Pleistocene and older features inland limit of Cape May Formation, unit 2, dashed where eroded inland limit of Cape May Formation, unit 1, dashed where eroded limit of Wisconsinan valley incision (ticks point into valley) inland limit of Cape May Formation, unit 2, fine-grained facies well penetrating Cape May Formation, unit 2, fine-grained facies stream drainage during deposition of upland gravel possible routes of the Manasquan and Metedeconk rivers before deposition of Cape May Formation, unit 2 eolian deposits paleodune ridge elevation of base of Quaternary deposits, contour interval 25 feet, shown only at and below sea level -25 approximate boundary of overwash sand and fine bay deposits Figure 1. Geomorphic and surficial geologic features of the Point Pleasant quadrangle. dune ridges thermokarst basins 0 1000 feet blow-out dunes Figure 2. LiDAR hillshade image showing paleodune ridges and relict thermokarst basins on Metedeconk Neck. Dune orientation indicates winds blowing from the north and northwest. Easternmost thermokarst basin is partially covered by tidal-marsh deposits. Blow-out dunes rim basins that may have formed or been enlarged by wind erosion. Location shown on figure 1. Tch ! ! Qe5/Qcm2 4 ! figure 5 ! 47 . 247 ! ! ! # # # ! Qals Qal Qm Qbs Qbe Qbo Qbu Qe Qcl Qtl Qtu Qcu Qcm1 Qcm2 Qcm2f TQg Tg Tch Tkw Tsr Tmq Tmb Tvt Tht Krb-ns Kml Kw-mt Ketu Ketl Kwb-mv Kmg Krw Krf Kp3 Figure 3. Eolian sand (unit Qe) exposed in former sand pit in dune ridge on Metedeconk Neck. Location shown on map and inset. MAP AREA Figure 4. Cape May Formation, unit 2 (unit Qcm2), exposed in bank along Manasquan River. Thin horizontal bedding visible in upper part of bank is typical of tidally influenced deposition. Location shown on map and inset. MAP AREA Figure 5. Upland gravel, high phase (unit Tg), exposed in former gravel pit west of Brielle. Cross bedding indicates former stream flow to east (right on photo). Photo by Meredith Johnson, N. J. Geological Survey, April 1936. Location shown on map and inset. MAP AREA Figure 6. Interbedded clay (white beds) and sand (yellow and red beds) of the Cohansey Formation (unit Tch). Red color in sand above clay marks iron deposition where drainage is impeded. Location shown on map and inset. MAP AREA Figure 7. Alluvial sand (unit Qal, above shovel head) over clay of the Cohansey Formation. Subvertical features highlighted by orange color (arrows) below yellow bed may be burrows. Location shown on map and inset. MAP AREA

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296

149

152153

148

Qm

Qbu

Qcm2

B’156

157

158159 160

Qbe

Qbs

146147

143142

144

145

162

161

164

163

Qm

Qcm2Qe

Qals

QalsQm

Qm

Qm

QmTch

Qcm2

Qtl

214

306

215

209

213

216

300

218

217219

221 220

224Qm

Qals

Qe

Qtl

Qtl Qe

Qtl

Tch

Qcm2

Qcm2

Qcm2

Qal

Qtl

198 199200

201

202203

204

223222

301

B

Qm

Qtl

Qm

226

227

225

228

Qm

Qm

Qbs Qbs

QbsQm

Qbs

Qm

Qbs

Qe

Qcm2

Qbs

237

238

308

243

307 244 245

304

303

248247

246

295

Qbs Qbs

QeQe

Qcm2

Qcm2Qcm2

Qm Qtl QalsQtl

Qm Qm

Qe

229

Qcm2

Qbs

Qbs

QbsQbs

Qm

Qbs

Qbs

155154

231230

232234

235233

Qm

Qm

236

Qbu

Qbe

Qbs

Qcm2

Qcm2

Qcm2

Qm

249

250251

252253

254

255256

257

Qm

Qcm2Qbs

Qm

Qcm2

258

Qe

Qe

Qe

Qcm2

240

241

242

259

261

262 260

Qals

Qals

Qcm2

Qcm2

Qbs

Qm

Qbs

QmQcm2

Qm

Qe

263

269

270271

264293

265

Qcm2

QmQbs

QbsQbs

Qbs Qbs

Qm

Qbs

276277

278

280279

282281

283290

291

275274284

287

289

285286

288

272273

292

Qcm2Qm

Qm

Qcm2

Qcm2

Qm Qm

QmQbu

C’

QmQbe

Qbs

267268

Qm

TkwTch

Tch

Tkw

Qm

TkwTch

TchTkw

Tch

Tkw

A

C

TchTkw

Tch

Tkw

D’

D

6 3

4

49

74

7

3

45

4

4

5

4

239

Qe8/Qcm2

Qe10/Qcm2

Qe10/Qcm2Qe15/Qcm2

Qe3/Qcm2

Qe4/Qcm2Qe4/Qcm2

Qe4/Qcm2

Qe4/Qcm2Qe4/Qcm2

Qe3/Qcm2

Qbs3/Qm4/Qcm2Qbs2/Qm

Qbs1/Qm

figure 3

figure 4

figure 5figure 6

figure 7

Qe4/Qcm2

Qe5/Qcm2

120

266

79

61

205

Qcm2

294

74o07’30”40o07’30”

5’ ASBURY PARK 2’30” 74o00’40o07’30”

5’

2’30”

40o00’74o00’2’30”SEASIDE PARK5’40o00’

74o07’30”

2’30”

LAK

EWO

OD

5’

QmQals

Qtl

Qcm2

Qcm1middle

late

Holocene

PleistoceneQcm2f

Qbs

Qtu

EXTENSIVE EROSION

EXTENSIVE EROSION

EROSION

EROSION

Quaternary

TQg

early

Pliocene

Qal

Qe Qcl

Qbe Qbo

Illinoian

Sangamonian

Wisconsinan

PERIODEPOCH

AND AGE

NORTH AMERICAN

STAGE

Qbu

Qcu

EROSION

Tg

CORRELATION OF MAP UNITS

Miocene

UNCONFORMITY

Tkw

TchNeogene

middle

early

EXTENSIVE EROSIONlate

Tmq

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Krw

UNCONFORMITY

UNCONFORMITY

UNCONFORMITY

UNCONFORMITY

UNCONFORMITY

UNCONFORMITY

UNCONFORMITY

UNCONFORMITY

Santonian-Coniacian-Turonian

Cenomanian

Campanian

Maastrichtian

early

late

early

Late Cretaceous

Paleocene

Eocene

Oligocene

Tsr

UNCONFORMITY

middle

PaleogeneUNCONFORMITY

Tmb

Krf

Kp3

UNCONFORMITY

UNCONFORMITY

INTRODUCTION

The Point Pleasant quadrangle is in the Barnegat Bay region of the New Jersey Coastal Plain, in the southeastern part of the state. Outcropping geologic materials in the map area are Holocene to upper Miocene surficial deposits that include marine, estuarine, river, wetland, hillslope, and windblown sediments. They overlie the middle to lower Miocene Cohansey and Kirkwood formations, which are shallow-marine and coastal deposits. In the subsurface, unconsolidated Paleogene and Upper Cretaceous sediments underlie the Cohansey and Kirkwood formations. The Paleogene sediments include, from youngest to oldest, the Shark River, Manasquan, Marlboro, Vincentown, and Hornerstown formations, all of which were deposited in continental-shelf settings. The Upper Cretaceous sediments include, from youngest to oldest, the Red Bank, Navesink, Mount Laurel, Wenonah, Marshalltown, Englishtown, Woodbury, and Merchantville formations, all of which were also deposited in continental-shelf settings; and the Magothy, Raritan, and Potomac formations, which were deposited in fluvial and estuarine settings.

A summary of the resources provided by the formations, and of the geomorphic history of the map area as recorded by surficial deposits and landforms, is provided below. The age of the deposits and episodes of valley erosion are shown on the correlation chart. Table 1 (in pamphlet) shows the formations penetrated by selected wells and borings as interpreted from drillers’ descriptions and geophysical well logs. These data were used to construct cross sections and to map the elevation of the base of Quaternary deposits. Table 2 (in pamphlet) provides logs for two power-auger holes drilled to a depth of 100 feet. The cross sections (sheet 2) show formations to a maximum depth of about 2200 feet, which is the depth of the deepest well (well 267 in table 1). Although no wells in the quadrangle reached pre-Mesozoic metamorphic basement rock beneath the Coastal Plain formations, wells and seismic data in adjacent areas indicate that basement is probably at a depth of about 1500 feet in the northwest corner of the quadrangle, deepening to about 2500 feet in the southeast (Volkert and others, 1996; Stanford and Sugarman, 2017). Basement rocks in this area are chiefly gneiss and schist. They are commonly weathered to saprolite to thicknesses of as much as 100 feet beneath the basal Cretaceous sediments.

RESOURCES

Numerous domestic wells, and one public-supply well (well 139 in table 1), tap sands within the Cape May, Cohansey and uppermost Kirkwood formations at depths between 25 and 100 feet. Many of the domestic wells are for lawn irrigation. Many other domestic wells, and eight public-supply wells (wells 102, 103, 104, and three adjacent wells in the same wellfield, a shallow well adjacent to well 97, and well 118) tap deeper sands within the Kirkwood at depths of 90 to 150 feet north of the Metedeconk River and up to 230 feet south of the Metedeconk. Deeper aquifers include sand in the upper member of the Englishtown Formation, which is tapped by six public-supply wells (73, 97, two wells adjacent to well 122, well 153 and another adjacent to it) at depths between 690 and 840 feet; the Magothy Formation, which is tapped by three wells (140, 157, and 255) at depths between 1190 and 1370 feet; and the Potomac Formation, which is tapped by well 267 at a depth interval of 1850 to 1980 feet. The Cohansey and upper Kirkwood formations lack thick, continuous clay beds and so are an unconfined aquifer. The deeper aquifers are confined by fine-grained beds in the lower Kirkwood, Shark River, Manasquan, Hornerstown, Navesink, Wenonah, Marshalltown, Woodbury, Merchantville, and Raritan formations. Additional information on aquifers in the map area is provided by Sugarman and others (2013).

Sand and gravel were dug for construction use from the upland gravel, high phase (map unit Tg) and the Cohansey Formation from large pits north of Herbertsville and west of Brielle (former pits are outlined on map). Sand of the Cape May Formation, upper terrace deposits, and windblown deposits on Metedeconk Neck was also dug at smaller pits. No pits were active at the time of mapping, and further extraction is limited by urbanization. Sand for beach replenishment is obtained from offshore sources (Castelli and others, 2015). Clay was mined for brickmaking from the Cohansey Formation at several locations in the Sawmill Creek valley north of Riviera Beach (Ries and others, 1904, and N. J. Geological and Water Survey permanent notes 29-33-723 and 29-33-733). The clay in this area occurred as one or more three- to five-foot thick beds interlaminated with white micaceous fine sand and underlain by iron-cemented sand.

SURFICIAL DEPOSITS AND GEOMORPHIC HISTORY

After the Cohansey Formation was deposited in the middle Miocene, sea level in the New Jersey region began a long-term decline. As sea level lowered during the middle and late Miocene, between about 15 to 5 million years ago (15-5 Ma, Ma = million years ago), the inner continental shelf emerged as a coastal plain. River drainage was established on this plain. The oldest surficial deposits in the quadrangle are gravels deposited by these rivers. This drainage eroded valleys into an earlier, higher fluvial gravel known as the Beacon Hill Gravel, which formerly covered the map area at an elevation of about 250 to 300 feet (Stanford, 2010). It has been eroded away in the quadrangle but there are remnants farther inland. Groundwater seepage, slope erosion, and channel erosion reworked the Beacon Hill Gravel and deposited it in floodplains, channels, and pediments in valleys that had been cut down between 150 and 200 feet below the level of the former Beacon Hill plain. These deposits are mapped as upland gravel, high phase (unit Tg). They cap the uplands north of Herbertsville and west of Brielle (fig. 1). The base of these deposits declines from an elevation of about 100 feet along the north edge of the quadrangle to about 75 feet to the east in Brielle. North of the quadrangle the base of the gravels continues to rise, to an elevation of 150 feet near Farmingdale, about 8 miles northwest of Brielle (Stanford, 2000a, 2000b). This slope indicates southeasterly stream flow (orange arrows on fig. 1). After a period of higher sea level in the Pliocene, a renewed period of lowering sea level during the early Pleistocene, approximately 2.5 Ma to 800,000 years ago (800 ka, ka = thousand years ago), led to another period of valley incision. Groundwater seepage and channel and slope erosion reworked the upland gravel, high phase and deposited the upland gravel, lower phase (unit TQg) in shallow valleys 20 to 50 feet below the higher gravels. These deposits today cap hilltops and interfluves, and form shallow fills in headwater valleys, between 70 and 85 feet in elevation on the upland north of Herbertsville. They have been removed by later erosion elsewhere in the quadrangle.

Continuing incision during the middle Pleistocene (about 800 to 130 ka), primarily during periods of low sea level, formed the modern valley network. The lower reaches of these valleys were submerged during at least two periods of higher-than-present sea level in the middle and late Pleistocene. During these highstands, beach, estuarine, and nearshore deposits were laid down within valleys and in terraces along the bayshore and, north of Bay Head, along the oceanfront (fig. 1). These deposits are grouped into the Cape May Formation. The Cape May includes an older, eroded terrace deposit (Cape May Formation, unit 1, Qcm1) with a maximum surface elevation of 70 feet, and a lower, less eroded terrace deposit with a maximum surface elevation of 35 feet (Cape May Formation, unit 2, Qcm2). Fine-grained clay, silt, and fine sand in the subsurface beneath the outer part of the Cape May 2 terrace (Qcm2f, southeast of dashed purple line on fig. 1) is an estuarine and back-bay deposit laid down as sea level rose during deposition of the Cape May 2.

Amino-acid racemization ratios (AAR), optically stimulated luminescence ages, and radiocarbon dates from the Delaware Bay area (Newell and others, 1995; Lacovara, 1997; O’Neal and others, 2000; O’Neal and Dunn, 2003; Sugarman and others, 2007) suggest that the Cape May 1 is of middle Pleistocene age (possibly marine-isotope stage [MIS] 11, 420 ka, or MIS 9, 330 ka; marine isotope stages from Lisiecki and Raymo, 2005) and that the Cape May 2 is of Sangamonian age (MIS 5, 125-80 ka). AAR of shells from vibracores off Long Beach Island, about 30 miles south of Mantoloking, indicate that the Cape May 2 correlate there is of Sangamonian age (Uptegrove and others, 2012). Global sea level during MIS 11 may have reached about 70 feet above present sea level (Olson and Hearty, 2009), about the maximum level of the Cape May 1 terrace, and during MIS 5e it reached about 25 feet above present sea level, about the level of the Cape May 2 terrace. If the age assignments of these terraces are accurate, these elevations suggest that full interglacial sea levels in this region are close to eustatic, as modeled by Potter and Lambeck (2003). Middle Wisconsinan (MIS 3, 65-35 ka) highstand deposits are described from the Delmarva Peninsula and the Virginia-North Carolina coastal plain (Mallinson and others, 2008; Scott and others, 2010; Parham and others, 2013; DeJong and others, 2015) at elevations up to 15 feet, but in New Jersey are apparently restricted to the inner shelf, at elevations of -60 feet or below (Carey and others, 2005; Uptegrove and others, 2012). Seismic and vibracore data show an east-trending middle Wisconsinan shoreline about 20 miles south of Mantoloking, with estuarine clays extending several miles to the north, although the clays do not extend beneath the barrier beaches or Barnegat Bay (Uptegrove and others, 2012).

The base of the Cape May 2 deposits (contoured on fig. 1 at 25-foot interval) deepens to the southeast. This pattern implies southerly river flow during the MIS 6 lowstand (200-150 ka) before deposition of the Cape May 2. This southerly routing is also suggested by abandoned valleys between uplands capped by Cape May 1 deposits near Riviera Beach (green arrows on fig. 1), which may mark routes of the Manasquan River and Sawmill Creek, and by less-evident valleys crossing Metedeconk Neck (mostly west of the map area on the Lakewood quadrangle; the lower end of one is shown on fig. 1) that may mark routes of the Metedeconk River into what is now Kettle Creek. These abandoned valleys align with the southward trend of segments of the Manasquan and Metedeconk rivers upstream of the Cape May 2 terrace. They lead southward to the Toms River paleovalley, which exits eastward to the shelf in the Lavalette-Seaside Park area, 4 to 8 miles south of Mantoloking (Stanford and Sugarman, 2017).

Southerly paleodrainage of the Manasquan and Metedeconk rivers is also consistent with the distribution of Quaternary sediments offshore on the inner shelf. Seismic surveying shows that, south of the Bay Head area, the base of Pleistocene sediments is at an elevation of -140 to -100 feet along a line parallel to, and two miles east of, the present shoreline (Lugrin, 2016). North of Bay Head the Pleistocene deposits are absent and Holocene deposits lie directly on Miocene formations. Farther offshore, the seismic data show a pre-Wisconsinan shelf valley draining northeastward from the Lavalette area, about 4 miles south of Mantoloking (Lugrin, 2016). This shelf valley may be the drain for the pre-Cape May 2

Manasquan, Metedeconk, and Toms rivers during MIS 6 and, possibly, earlier lowstands (Stanford and Sugarman, 2017).

During the Cape May 2 highstand these valleys were filled with estuarine and nearshore deposits. As sea level lowered during the Wisconsinan the lower reaches of the Manasquan and Metedeconk rivers, and their tributaries on the Cape May 2 terrace, adopted new easterly routes on the Cape May 2 deposits. Incision of these streams created the present valleys (outlined by black ticked lines on fig. 1). These incisions reached depths of between -25 and -40 feet along the present coastline, as indicated by the position of lower terrace deposits (see below) beneath the Manasquan and Metedeconk estuaries (section CC’).

Fluvial sediments laid down in modern valleys include upper and lower terrace deposits (units Qtu and Qtl) and floodplain (Qal) and wetland deposits (Qals) in valley bottoms. Colluvium deposited at the base of hillslopes in modern valleys includes upper colluvium (Qcu), which grades to the upper terraces and to the Cape May 2 marine terrace, and lower colluvium (Qcl), which grades to the lower terraces and to the modern floodplain. Like the upland gravels, the terrace, hillslope, and floodplain deposits represent erosion, transport, and redeposition of sand and gravel reworked from older surficial deposits and the Cohansey Formation by streams, groundwater seepage, and slope processes. Wetland deposits are formed by accumulation of organic matter in swamps and bogs.

Upper terrace deposits form terraces and pediments 25 to 40 feet above modern floodplains and estuaries in the Manasquan River and Sawmill Creek valleys. Upper colluvium forms footslope aprons that grade to the upper terrace. The terrace deposits and colluvium were laid down chiefly during periods of cold climate in the middle Pleistocene. During cold periods, permafrost impeded deep infiltration of rainfall and snowmelt. The resulting waterlogged soils accelerated groundwater seepage and slope erosion, increasing the amount of sediment entering valleys, leading to terrace deposition. At their seaward limit, some of the deposits grade to the Cape May 2 marine terrace, and may have been laid down during periods of temperate climate when sea level was high. This topographic equivalence indicates that some of the upper terrace deposits aggraded during the Cape May 2 highstand.

Lower terrace deposits (unit Qtl) form terraces with surfaces less than 15 feet above modern valley bottoms. They are of smaller extent than the upper terraces. They formed from stream and seepage erosion of the upper terrace and Cape May 2 deposits, and, in places, older deposits, chiefly during or slightly before the last period of cold climate corresponding to the late Wisconsinan glacial stage. Organic silt at the base of lower terrace deposits upstream of the quadrangle in the Manasquan and Metedeconk river basins yielded radiocarbon dates of 29,050±150 yrs BP (Beta 471459) (33.7-32.8 calibrated ka) from a site near Siloam in the Adelphia quadrangle and a date of 35,570+3180-2270 (GX-24257) (33.4-45.4 calibrated ka) from a site near Farmingdale in the Farmingdale quadrangle (Stanford and others, 2002). (Radiocarbon dates are calibrated using Reimer and others (2013) and the Calib 7.1.0 computer program. Calibrated dates are stated with two-sigma uncertainty.) These dates confirm deposition of the overlying terrace sediments in the middle and late Wisconsinan. Lower colluvium (Qcl) on grade with the lower terraces was also laid down during this time. As permafrost melted beginning around 18 ka, forest regrew and hillslope erosion slowed. The volume of sand washing into valleys was greatly reduced, and streams eroded into the lower terraces to form the modern floodplain (Qal and Qals). This erosion was largely complete by the beginning of the Holocene at 11 ka, based on radiocarbon dates on basal peat in floodplains in the region (Buell, 1970; Florer, 1972; Stanford, 2000c).

Inland eolian deposits (unit Qe) form dunes and dune fields. Dune ridges are as much as 15 feet tall, but are more commonly 3 to 6 feet tall, and are as much as 3000 feet long (fig. 2). Their long axes (line symbols on map) are oriented east-west to northeast-southwest. Some of the ridges are closely spaced and parallel, creating a rippled pattern. Some form rims on the southeast side of shallow basins (lower left of fig. 2). These basins may have been created or enlarged by wind erosion (French and Demitroff, 2001). These patterns indicate that the dunes were laid down by winds blowing from the northwest. Most eolian deposits are on the Cape May 2 terrace. One dune near Riviera Beach is on the lower terrace. This distribution indicates that the eolian deposits were laid down after deposition of the Cape May 2, and, in places, also formed after deposition of the lower terraces. This span corresponds to the Wisconsinan Stage, a period of intermittently cold climate between 80 and 11 ka.

Another product of cold climate is relict thermokarst basins. These are shallow depressions, circular or oval in plan, that are common on low-lying, flat landsurfaces where the water table is at shallow depth (fig. 2). They are shown by symbols where observed on Metedeconk Neck. Elsewhere they were once equally common but have been destroyed by urbanization. Most formed when ice-rich lenses within permafrost melted. Some may have formed or been enlarged by wind erosion, as discussed above.

Modern beach, bay, and salt-marsh deposits were laid down during Holocene sea-level rise, chiefly within the past 6 ka in the map area. As sea level rose, tidal-marsh peat and fine-grained bay deposits (Qm) were covered by advancing flood-tidal delta sand laid down at the landward mouths of inlets, and barrier overwash sand laid down by storm flows washing over the oceanfront dunes (Qbo, Qbu). On the barrier islands, beach (Qbs) and dune (Qbe) sand are laid down atop the delta and overwash sand. The beach and dune deposits are eroded by waves and currents as sea level rises and are rarely preserved in the subsurface.

Modern sediments in Barnegat Bay consist of tidal-delta and overwash sands forming flats on the bay side of the barrier spit and extending under the eastern part of the bay. In the bay these sands interfinger with salt-marsh peat and organic mud. The western part of the bay (west of the dashed black line on figure 1), adjacent to the salt marsh, is underlain by fine sand, silt, and clay eroded from mainland sources (Olsen and others, 1980; Psuty, 2004; Andrews and others, 2016; Bernier and others, 2016).

Sea level has risen between 1 and 1.3 feet between 1900 and 2017 in the New Jersey region, as measured at tide gauges (https://tidesandcurrents.noaa.gov/sltrends/sltrends.html). This rise has caused the salt marsh and bayshore to advance inland on natural shorelines that are not stabilized by seawalls, bulkheads, and artificial beach replenishment. Inland advance of the salt marsh is indicated by a fringe of dead trees and spread of Phragmites reeds along the advancing front. These features are observed on all the natural inland edges of salt marsh in the quadrangle.

DESCRIPTION OF MAP AND SUBSURFACE UNITS

Grain-size terms are from the modified Wentworth scale (Ingram, 1982).Color terms are from Munsell Color Company (1975).

ARTIFICIAL FILL—Sand, pebble gravel, minor clay and peat; gray, brown, very pale brown, white. In places includes man-made materials such as concrete, asphalt, brick, cinders, trash, and glass. Unstratified to poorly stratified. As much as 15 feet thick. In road and railroad embankments, dams, dikes, infilled pits, filled wetlands, dredge-spoil disposal cells, and land made from dredged material in bayfront residential developments. The extent of fill on salt-marsh deposits is based in part on the extent of the marsh as shown on topographic manuscript maps from the 1880s at a scale of 1:21,120 on file at the N. J. Geological and Water Survey, and aerial photography from the 1930s.

WETLAND AND ALLUVIAL DEPOSITS—Fine-to-medium sand and pebble gravel, minor coarse sand and silty clayey sand; light gray, yellowish-brown, brown, dark brown; overlain by brown to black peat and gyttja. Peat is as much as 6 feet thick. Sand and gravel consist chiefly of quartz and are generally less than 3 feet thick. Sand and gravel are stream-channel deposits; peat and gyttja form from the vertical accumulation and decomposition of plant debris in swamps and marshes. In alluvial wetlands on modern valley bottoms.

ALLUVIUM—Sediment as in unit Qals except peat and gyttja are thin and discontinuous and may be interbedded with or overlain by sand and gravel. As much as 10 feet thick. Includes small deposits of colluvium as in unit Qcl in places at the foot of steep slopes.

TIDAL-MARSH AND ESTUARINE DEPOSITS—Peat, clay, silt, fine sand; brown, dark brown, gray, black; minor thin beds of medium-to-coarse sand and pebble gravel. Contains abundant organic matter and shells. As much as 50 feet thick. Deposited in tidal marshes, tidal flats, tidal channels, and bays and estuaries during Holocene sea-level rise, chiefly within the past 6 ka in the map area.

BARRIER-BEACH DEPOSITS—Sand and minor gravel deposited by waves (Qbs), wind (Qbe), and tidal and storm flows (Qbo), and reworked by human activity (Qbu), during the Holocene.

BEACH SAND—Fine-to-medium sand with few (1-5%) shells and shell fragments and minor (<1%) to few fine-to-medium quartz pebbles; very pale brown, white, light gray. Bedding is typically planar laminations that dip gently seaward. As much as 15 feet thick. Gravel is more common on mainland bay beaches than on ocean beaches or barrier bay beaches.

DUNE SAND—Fine-to-medium sand with a few coarse sand grains and shell fragments; white, light gray, very pale brown. Bedding is typically large-scale trough-planar cross beds; cross beds dip 10-30°, bed sets are 1-5 feet thick. As much as 30 feet thick. Includes artificially constructed dunes that may contain rip-rap, organic debris, and human-made materials like fencing and netting placed to promote stability.

OVERWASH AND TIDAL-DELTA SAND—Fine-to-medium sand, few shells and shell fragments, minor coarse sand and fine-to-medium pebble gravel, and a trace (<1%) of rip-up clasts of peat; light gray, very pale brown. Nonstratified to laminated to trough- and planar- cross-bedded. As much as 30 feet thick. Deposited in tidal channels and tidal flats associated with tidal

deltas and by storm overwashes of the dune massif. In subsurface only. Underlies units Qbu, Qbe, and Qbs, and interfingers with unit Qm in the eastern part of Barnegat Bay.

DUNE AND OVERWASH SAND, UNDIVIDED—Sand as in units Qbe and Qbo, graded and mixed during urban development. May include areas of artificial fill. As much as 10 feet thick.

EOLIAN DEPOSITS—Fine-to-medium quartz sand; very pale brown, white, yellowish brown (fig. 3). As much as 15 feet thick. Nonstratified to weakly subhorizontally stratified. Form dune ridges and dune fields. Modern eolian sand on the barrier beaches is mapped separately as unit Qbe.

LOWER COLLUVIUM—Fine-to-coarse sand, silty sand, pebble gravel; very pale brown, yellowish-brown, gray. Sand consists chiefly of quartz with a few (1-5%) glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor (<1%) ironstone in places. As much as 15 feet thick (estimated). Nonstratified to weakly subhorizontally stratified. Forms aprons at the base of steep slopes. The aprons grade to lower terraces or the modern floodplain and estuary.

LOWER TERRACE DEPOSITS—Fine-to-medium sand, pebble gravel, minor coarse sand; yellowish-brown, light gray, brown, dark brown. As much as 15 feet thick. Sand consists chiefly of quartz with a few to some (5-10%) glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor ironstone in places. Form terraces and pediments in valley bottoms with surfaces 2 to 15 feet above the modern floodplain and estuary. Include stratified and cross-bedded stream-channel deposits and nonstratified to weakly stratified overbank and seepage deposits.

UPPER TERRACE DEPOSITS—Fine-to-medium sand, pebble gravel, minor coarse sand; very pale brown, brownish-yellow, yellow. As much as 30 feet thick. Sand consists chiefly of quartz with a few to some glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor ironstone in places. Form terraces and pediments with surfaces 25 to 40 feet above the modern floodplain and estuary. Include stratified and cross-bedded stream-channel deposits and weakly stratified to nonstratified deposits laid down by overbank deposition and groundwater seepage on pediments.

UPPER COLLUVIUM—Fine-to-coarse sand, silty sand, pebble gravel; yellowish-brown, very pale brown, gray. As much as 20 feet thick. Sand consists chiefly of quartz with a few to some glauconite and opaque-mineral grains and a trace of mica. Gravel consists of quartz and minor ironstone. Nonstratified to weakly stratified.

CAPE MAY FORMATION—Sand and gravel (Qcm1, Qcm2) and clay, silt, and fine sand (Qcm2f) deposited in beach, nearshore, and estuarine settings during the middle and late Pleistocene.

CAPE MAY FORMATION, UNIT 2—Fine-to-medium sand, pebble gravel, minor coarse sand, a few thin beds of silty clay; yellow, very pale brown, yellowish-brown. As much as 50 feet thick. Sand consists chiefly of quartz with few to some glauconite and opaque-mineral grains. Gravel consists of quartz and minor ironstone in places. Nonstratified to horizontally stratified, cross-bedded in places (fig. 4). Forms a terrace with a maximum surface elevation of 35 feet.

CAPE MAY FORMATION, UNIT 2, FINE-GRAINED DEPOSITS—Clay, silt, fine sand, minor organic matter; light gray to gray. As much as 50 feet thick. In subsurface only, inferred from well records (fig.1, sections CC’, DD’).

CAPE MAY FORMATION, UNIT 1—Fine-to-medium sand, iron-cemented in places, pebble gravel, minor coarse sand, a few thin beds of silty clay; yellow, very pale brown, yellowish-brown, reddish-brown where iron-cemented. As much as 30 feet thick. Sand consists chiefly of quartz with a few glauconite and opaque-mineral grains. Gravel consists of quartz and minor ironstone in places. Nonstratified to horizontally stratified. Forms eroded terraces with a maximum surface elevation of 70 feet.

UPLAND GRAVEL, LOWER PHASE—Fine-to-coarse sand, clayey in places, and pebble gravel; yellow, very pale brown, yellowish-brown. As much as 15 feet thick. Sand and gravel consist chiefly of quartz. Nonstratified to weakly horizontally stratified. Occurs as erosional remnants on hilltops and interfluves, and in headwater valleys, between 70 and 85 feet in elevation.

UPLAND GRAVEL, HIGH PHASE—Fine-to-coarse sand, clayey in places; pebble gravel; trace small-cobble gravel; yellow, yellowish-brown, reddish-yellow. As much as 25 feet thick. Sand is chiefly quartz with a trace of weathered chert. Gravel is chiefly quartz. Nonstratified to horizontally stratified, cross-bedded in places (fig. 5). Cross-beds are commonly tabular-planar. Occurs as erosional remnants on uplands above 75 to 100 feet in elevation.

COHANSEY FORMATION—Fine-to-medium sand, some medium-to-coarse sand, minor very fine sand, minor very coarse sand to very fine pebbles, trace fine-to-medium pebbles; very pale brown, brownish-yellow, white, reddish-yellow, rarely reddish-brown, red, and light red; with thin beds of white, yellow, and red clay and clayey very fine-to-fine sand in places (figs. 6, 7). Clay beds are 0.5 inch to 2 feet thick. Exposure is too limited to map sand and clay beds but in table 1 they are identified from well logs as “Tchs” and “Tchc” respectively. Sand is well-stratified to nonstratified; stratification ranges from thin, planar, subhorizontal beds to large-scale trough and planar cross-bedding. Sand is quartz; coarse-to-very coarse sand may include as much as 5% weathered chert and a trace of weathered feldspar. As much as 20 percent of the sand fraction consists of detrital heavy minerals (Markewicz, 1969), commonly concentrated along bedding planes. In these concentrations, ilmenite dominates the opaque minerals; to a lesser extent zircon and sillimanite dominate the nonopaque minerals. Kaolinite dominates the clay-sized minerals. Coarse-to-very coarse sands commonly are slightly clayey; the clays occur as grain coatings or as interstitial infill. This clay-size material is from weathering of chert and feldspar rather than from primary deposition. Pebbles are chiefly quartz with minor gray chert and rare gray quartzite. Some chert pebbles are light gray, partially weathered, pitted, and partially decomposed; some are fully weathered to white clay. In a few places, typically above or below clayey strata, sand may be hardened or cemented by iron oxide, forming reddish-brown hard sands or ironstone masses.

The basal contact of the Cohansey was not observed in the quadrangle. Elsewhere, the Cohansey appears to unconformably overlie the Kirkwood Formation although it may be age-equivalent to younger Kirkwood members downdip to the south. Micaceous fine sand typical of the Kirkwood occurs within the Cohansey in the northwest part of the map area, suggesting a gradational or interfingered contact of the two formations locally. Pollen and dinoflagellates indicate that the Cohansey is of middle to late Miocene age (Rachele, 1976; Greller and Rachele, 1983; Owens and others, 1988; deVerteuil, 1997; Miller and others, 2001).

KIRKWOOD FORMATION—Quartz sand, fine-to-medium grained, and clay-silt. Sand is nonstratified to cross-bedded and laminated, light gray, gray, and light-yellow, micaceous, with minor coarse sand and fine gravel. Sand consists chiefly of quartz, with small amounts of feldspar and mica (mostly muscovite). Detrital heavy minerals are concentrated on bedding planes and are chiefly opaques, especially ilmenite, with lesser amount of nonopaques including zircon, staurolite, garnet, rutile, and tourmaline. Clay and silt are dark gray to brown. Finely dispersed clay minerals include kaolinite, illite, and illite/smectite. The lowermost Kirkwood (below tielines on sections), termed the Asbury clay (Ries and others, 1904), or the Asbury Park Member (Isphording, 1970), is a dark gray to dark brown, peaty, laminated clay-silt with lenses of massive to locally cross-bedded fine sand. Pyrite is common in the clayey, organic-rich beds. At the base of the Kirkwood a bed of coarse glauconite-quartz sand, with granules and scattered shark teeth, typically 2 to 3 feet thick, rests unconformably on the Shark River Formation. Maximum thickness 150 feet.

The Kirkwood Formation, as revised by Owens and others (1998), includes the following members, in ascending order: (1) an unnamed lower member (equivalent to the Brigantine Member of Miller and others, 1997 or sequence Kw1a of Sugarman and others, 1993); (2) the Shiloh Marl Member (equivalent to sequence Kw1b of Sugarman and others, 1993); (3) the Wildwood Member (equivalent to sequence Kw2 of Sugarman and others, 1993); and (4) the Belleplain Member (equivalent to sequence Kw3 of Sugarman and others, 1993). Both the unnamed lower member and the Shiloh Marl Member are clayey at the base and sandy at the top, a pattern that is evident on gamma-ray geophysical logs. The unnamed lower member and Shiloh Marl Member are approximately 21-19 million years old, the Wildwood Member is 18-15 million years old, and the Belleplain Member is 13 million years old (Miller and others, 1997). Previous mapping indicates that the lower member and Shiloh Marl Member are present in the quadrangle, while the Wildwood and Belleplain members are present only south of the quadrangle (Sugarman and others, 1993). In the Sea Girt corehole (well 107), the lower member and Shiloh Marl Member were tentatively identified, as was a thin upper clay-silt possibly correlative to the Wildwood Member, although no datable material was found in the Kirkwood to substantiate this correlation (Miller and others, 2006).

SHARK RIVER FORMATION—Very fine-to-fine, slightly glauconitic and micaceous quartz sand, which thins to the northwest (above upper tielines on sections) grading downward into clay-silt, very fossiliferous, glauconitic (up to 15%), slightly micaceous, greenish-gray to very dark greenish-gray; nonstratified to

thick-bedded and extensively burrowed (below upper tielines). Thin porcellanitic zones are present in places. There is less glauconite is the lower 40 feet of the formation (below lower tielines on sections), although glauconite is locally abundant in the basal 10 feet. Calcareous microfossils are abundant in the lower clay-silt; small, broken mollusk shells are present in the upper fine sand. Clay minerals include illite, illite/smectite, kaolinite, and minor amounts of clinoptilolite. The upper sand is also known as the Toms River Member and the lower clay-silt as the Squankum Member (Enright, 1969). Maximum thickness of the Shark River Formation in the map area is 230 feet.

The contact with the underlying Manasquan Formation is unconformable and is placed at the top of the pale-olive clay-silt of the Manasquan. It is marked by a sharp positive gamma-ray response on geophysical logs.

Calcareous nannofossils in samples from the Allaire State Park corehole (Sugarman and others, 1991) and in the Sea Girt corehole (Miller and others, 2006) indicate the Shark River is of middle Eocene age (nannozones NP 14-17).

MANASQUAN FORMATION—Clay-silt, dusky-yellow-green to pale-olive and grayish-green, extensively burrowed, nonstratified to thick-bedded, calcareous, minor very fine quartz sand. Cross-bedded laminae of very fine sand are present locally. Fine glauconite sand is commonly dispersed throughout the dominantly clayey matrix. Clay minerals include illite, illite/smectite, and minor clinoptilolite. In the Sea Girt corehole, silica-cemented porcellanite zones are common (Miller and others, 2006). The contact with the underlying Marlboro or Vincentown formations is marked by a sharp positive response on gamma-ray logs. Otherwise the formation, in general, has a neutral response on gamma-ray logs, not reflecting the dominant clay-silt lithology. Maximum thickness is 150 feet.

Calcareous nannofossils and planktonic foraminifers in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Manasquan is of early Eocene age (nannozones NP 11-12, foraminifer zones P 7-8).

MARLBORO FORMATION—Clay to sandy silty clay, greenish-gray, brown, reddish-brown, with glauconite, pyrite, and phosphate nodules. Maximum thickness is 35 feet, and the formation pinches out to south (section CC’). The Marlboro Formation was named by Glaser (1971) in Maryland and identified in the subsurface in New Jersey by Miller and others (2017).

Calcareous nannofossils in samples from the Sea Girt corehole indicate that the Marlboro Formation (identified as “unnamed clay” in Miller and others, 2006) is of earliest Eocene age (nannozone NP 9b).

VINCENTOWN FORMATION—Clayey silt and silt, extensively burrowed, slightly micaceous, finely laminated where not burrowed, dark greenish-gray to very dark gray, with thin beds of very fine quartz and glauconite sand and silt. Grades downward to a massive, slightly quartzose, glauconitic silt and glauconite sand with shell material at the base. The contact with the underlying Hornerstown Formation is marked by a sharp positive response on gamma-ray logs. Maximum thickness is 110 feet.

Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Vincentown is of late Paleocene age (nannozones NP 8 and 9a).

HORNERSTOWN FORMATION—Glauconite, clayey, massive- bedded, very dark greenish-gray to very dark grayish-brown, with scattered shells and shell fragments. Glauconite grains are mainly medium to coarse sand in size and botryoidal. Contains 1 to 2 percent fine-to-very coarse-grained quartz sand, phosphate fragments, pyrite, and lignite. Matrix contains minor glauconite clay. Locally cemented by iron oxides and siderite. Unconformably overlies the Red Bank Formation. Maximum thickness is 40 feet.

Calcareous nannofossils and planktonic foraminifers in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Hornerstown is of early Paleocene age (nannozones NP 2-4, foraminifer zones P1-P3).

NAVESINK-RED BANK FORMATIONS (UNDIVIDED)— Glauconite, slightly quartzose, clayey, greenish-black, with calcareous shells. Glauconite grains are mainly medium to coarse sand in size. Unconformably overlies the Mount Laurel Formation. This contact is easily distinguished in the subsurface by a sharp positive gamma-ray response. Maximum thickness is 70 feet.

In outcrop in northern Monmouth County the Navesink Formation and the Red Bank Formation form an unconformity-bounded, coarsening-upward sequence consisting of a basal glauconite sand (Navesink Formation), a middle silt (lower Red Bank Formation), and an upper quartz sand (upper Red Bank Formation). Downdip from outcrop, the sand pinches out and the silt changes facies to glauconite.

Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Navesink is of Late Cretaceous (Maastrichtian) age (nannozones CC 23a, 25, 26).

MOUNT LAUREL FORMATION—Quartz sand, fine- to coarse-grained, slightly glauconitic, extensively burrowed, slightly micaceous and feldspathic, commonly interbedded with thin layers of dark clay and silt, and intervals of scattered shells. Olive-gray to dark greenish-gray. Conformably overlies the Wenonah Formation. The transition from the Wenonah to the Mount Laurel is generally marked by an increase in grain size, a decrease in mica (Owens and Sohl, 1969), and the appearance of alternating thin beds of clay and sand in the Mount Laurel (Minard, 1969). Maximum thickness is 70 feet.

Calcareous nannofossils, and a strontium stable-isotope age of 74.5 Ma, in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Mount Laurel is of Late Cretaceous (late Campanian) age (nannozones CC21-22).

MARSHALLTOWN–WENONAH FORMATIONS (UNDIVID- ED)—Glauconite, greenish-black, extensively burrowed, with silt and pyrite and rare shell fragments (Marshalltown), grading upward into a micaceous, lignitic, burrowed clayey fine sand to silt with traces of glauconite and pyrite (Wenonah). The Marshalltown- Wenonah is recognized in the subsurface by a gamma spike at the base of the Marshalltown passing into a relatively flat, high-intensity pattern above. The two formations are undivided due to the thinness of the Marshalltown Formation (approximately 10 feet) and its lithologic similarity to the lower Wenonah Formation. Unconformably overlies the Englishtown Formation. The lower contact is extensively burrowed; wood and locally coarse sand from the underlying Englishtown Formation are reworked into the basal Marshalltown. Maximum thickness is 60 feet.

Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Marshalltown is of Late Cretaceous (late Campanian) age (nannozone CC20).

ENGLISHTOWN FORMATION—Informally divided into the upper Englishtown and lower Englishtown members. The upper member consists of fine- to coarse-grained sand interbedded with thin, dark-gray, micaceous, woody, clay-silt that grades downward to glauconitic, dark greenish-gray, micaceous, and lignitic clay-silt to very fine quartz sand. The sand is dominantly quartz; less than 10 percent consists of feldspar, rock fragments, and glauconite. The upper member is defined on gamma-ray logs by a thick, low-intensity sand at its top (above tielines on sections) and a thick, high-intensity clayey unit (below tielines) at its base. The upper member unconformably overlies the lower Englishtown member. In the Sea Girt corehole, a 1.5-foot indurated zone marks the contact. Maximum thickness of the upper member is 150 feet. The lower member is quartz sand, feldspathic, micaceous and lignitic, fine- to medium-grained, medium-to dark-gray. Sand is typically cross-bedded. The contact of the lower member with the underlying Woodbury Formation is gradational. Maximum thickness of the lower member is 40 feet.

Calcareous nannofossils and strontium stable-isotope ages of 74-78 Ma in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Englishtown Formation is of Late Cretaceous (middle-late Campanian) age (nannozones CC19-20).

MERCHANTVILLE-WOODBURY FORMATIONS (UNDIVID- ED)—Clay and silt, some very fine sand with mica, and a few lenses of finely disseminated pyrite, lignite, and siderite (Woodbury Formation). Color ranges from dark gray to olive black. Bedding is nonstratified to finely laminated with alternating beds of very fine sand and clay-silt. Grades downward into an intercalated, thick-bedded sequence of glauconitic sand and silt and micaceous clayey silt (Merchantville Formation). Quartz and glauconite are the major sand components; feldspar, mica (colorless and green), and pyrite are minor constituents. Siderite-cemented beds are common. The Merchantville contains zones of broken calcareous mollusk shells. Unconformably overlies the Magothy Formation. Maximum thickness is 200 feet. Calcareous nannofossils in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Merchantville and Woodbury formations are of Late Cretaceous (Santonian to mid-Campanian) age based on (nannozones CC16-18).

MAGOTHY FORMATION—Quartz sand and clay, thin- to thick-bedded. Sand is light- to medium-gray or brownish-gray; clay is olive-black to grayish-black. Bedding is horizontally laminated to cross-bedded. The sand is fine to very coarse, well sorted within each bed, predominantly quartz, and includes minor feldspar and mica. Pyrite-cemented and pyrite-coated sand concretions are common. Lignite is abundant in beds as much as 0.5 feet thick. Recognized on gamma logs as a series of thick sands and interbedded clay-silts. Unconformably overlies the Raritan Formation. Maximum thickness is 250 feet.

Pollen in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the Magothy is of Late Cretaceous (Turonian-Coniacian) age (pollen zones V-VII).

RARITAN FORMATION—Includes two members: the Woodbridge Clay Member (Krw) and the underlying Farrington Sand Member (Krf). The Woodbridge Clay Member is clay and silt, dark gray, nonstratified, with mica, pyrite, lignite, and siderite. Siderite forms layers 0.25 to 0.5 inches thick. Maximum thickness is 250 feet. The Farrington Sand Member is fine-to-medium quartz sand, white, yellow, red, light gray, commonly interbedded with thin coarse sand and fine gravel beds and thin to thick dark gray silt beds. Maximum thickness is 40 feet.

Pollen and calcareous nannofossils in samples from the Sea Girt corehole indicate that the Raritan is of Late Cretaceous (Cenomanian-Turonian) age (Miller and others, 2006). The Woodbridge Clay Member yielded zone IV pollen and nannozones CC 10-11. The Farrington Sand Member yielded zone III pollen. In the Sea Girt corehole the Raritan Formation is identified as the Bass River Formation based on downdip correlation to subsurface marine sediments in southern Burlington County (Petters, 1976). It is identified as Raritan Formation here because of its lithologic continuity with the outcropping updip Raritan in Middlesex County.

POTOMAC FORMATION—Fine-to-coarse quartz sand with beds of clay and silty clay; white, yellow, red where weathered, gray where unweathered. Sands are nonstratified to horizontally bedded to cross-bedded, clays are in beds as much as 10 feet thick. More than 400 feet thick; full thickness is not penetrated by drillholes in the quadrangle.

Pollen in samples from the Sea Girt corehole (Miller and others, 2006) indicate that the uppermost Potomac in the quadrangle is of Late Cretaceous (Cenomanian) age (pollen zone III), indicating it is within the Potomac Formation, unit 3, of Doyle and Robbins (1977).

REFERENCES

Andrews, B. D., Miselis, J. L., Danforth, W. W., Irwin, B. J., Worley, C. R., Bergeron, E. M., and Blackwood, D. S., 2016, Marine geophysical data collected in a shallow back-barrier estuary, Barnegat Bay, New Jersey: U. S. Geological Survey Data Series 937, version 1.1, 15 p.

Bernier, J. C., Stalk, C. A., Kelso, K. W., Miselis, J. L., and Tunsted, R., 2016, Sediment data collected in 2014 from Barnegat Bay, New Jersey: U. S. Geological Survey Data Series 985.

Buell, M. F., 1970, Time of origin of New Jersey Pine Barrens bogs: Bulletin of the Torrey Botanical Club, v. 97, p. 105-108.

Carey, J. S., Sheridan, R. E., Ashley, G. M., and Uptegrove, J., 2005, Glacially influenced late Pleistocene stratigraphy of a passive margin: New Jersey’s record of the North American ice sheet: Marine Geology, v. 218, p. 153-173.

Castelli, M. V., Latini, D., Uptegrove, J., Waldner, J. S., Hall, D. W., and Friedman, A. L., 2015, Significant sand resource areas in state and federal waters offshore Monmouth County, New Jersey: N. J. Geological and Water Survey Geologic Map Series GMS 15-3, scale 1:80,000.

DeJong, B. D., Bierman, P. R., Newell, W. L., Rittenour, T. M., Mahan, S. A., Balco, G., Rood, D. H., 2015, Pleistocene relative sea levels in the Chesapeake Bay region and their implications for the next century: GSA Today, v. 25, p. 4-10.

deVerteuil, Laurent, 1997, Palynological delineation and regional correlation of lower through upper Miocene sequences in the Cape May and Atlantic City boreholes, New Jersey Coastal Plain, in Miller, K.G., and Snyder, S. W., eds., Proceeding of the Ocean Drilling Program, Scientific Results, v. 150X: College Station, Texas, Ocean Drilling Program, p. 129-145.

Doyle, J. A., and Robbins, E. I., 1977, Angiosperm pollen zonation of the Cretaceous of the Atlantic coastal plain and its application to deep wells in the Salisbury embayment: Palynology, v. 1, p. 43-78.

Florer, L. E., 1972, Palynology of a postglacial bog in the New Jersey Pine Barrens: Bulletin of the Torrey Botanical Club, v. 99, p. 135-138.

French, H. M., and Demitroff, M., 2001, Cold-climate origin of the enclosed depressions and wetlands (“spungs”) of the Pine Barrens, southern New Jersey, USA: Permafrost and Periglacial Processes, v. 12, p. 337-350.

Glaser, J. D., 1971, Geology and mineral resources of southern Maryland: Maryland Geological Survey, Report of Investigations 15, 85 p.

Greller, A. M., and Rachele, L. D., 1983, Climatic limits of exotic genera in the Legler palynoflora, Miocene, New Jersey, USA: Review of Palaeobotany and Palynology, v. 40, p. 149-163.

Ingram, R. L., 1982, Modified Wentworth scale, in Dutro, J. T., Dietrich, R. V., and Foose, R. M., eds., AGI data sheets for geology in the field, laboratory, and office, 2nd edition: American Geological Institute, Washington, D. C.

Isphording, W. C., 1970, Petrology, stratigraphy, and redefinition of the Kirkwood Formation (Miocene) of New Jersey: Journal of Sedimentary Petrology, v. 40, p. 986-997.

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.

Lisiecki, L. E., and Raymo, M. E., 2005, Pliocene-Pleistocene stack of 57 globally distributed benthic d18O records: Paleoceanography, v. 20, PA 1003.

Lugrin, L., 2016, Delta progradation and channel drainage systems from the early Miocene to the present day between Barnegat and Manasquan inlets, New Jersey: unpublished M. S. thesis, Rutgers University, New Brunswick, N. J., 165 p.

Mallinson, D., Burdette, K., Mahan, S., and Brook, G., 2008, Optically stimulated luminescence age controls on late Pleistocene and Holocene coastal lithosomes, North Carolina, USA: Quaternary Research, v. 69, p. 97-109.

Markewicz, F. J., 1969, Ilmenite deposits of the New Jersey coastal plain, in Subitzky, S., ed., Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions: Rutgers University Press, New Brunswick, N. J., p. 363-382.

Miller, K. G., Browning, J. V., Aubry, M.-P., Babila, T., Baluyot, R. D., Esmeray-Senlet, S., Feigenson, M. D., Karakaya, S., Lombardi, C. J., Makarova, M., McCreary, S., McLaughlin, P. P., Jr., Monteverde, D. H., Olsson, R. K., Smith, C. T., Sugarman, P. J., Wright, J. D., 2017, Wilson Lake site, in Miller, K. G., Sugarman, P. J., Browning, J. V., and others, eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174 AX (Supplement): College Station, Texas, Ocean Drilling Program, p. 1-31.

Miller, K. G., Rufolo, S., Sugarman, P. J., Pekar, S. F., Browning, J. V., and Gwynn, D. W., 1997, Early to middle Miocene sequences, systems tracts, and benthic foraminiferal biofacies, New Jersey coastal plain, in Miller, K. G., and Snyder, S. W., eds, Proceedings of the Ocean Drilling Program, Scientific Results, Volume 150X: College Station, Texas, Ocean Drilling Program, p. 169-186.

Miller, K. G., Sugarman, P. J., Browning, J. V., Pekar, S. F., Katz, M. E., Cramer, B. S., Monteverde, D., Uptegrove, J., McLaughlin, P. P., Jr., Baxter, S. J., Aubry, M.-P., Olsson, R. K., Van Sickel, B., Metzger, K., Feigenson, M. D., Tiffin, S., and McCarthy, F., 2001, Ocean View site, in Miller, K. G., Sugarman, P. J., Browning, J. V., and others, eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174AX (Supplement 2): College Station, Texas, Ocean Drilling Program, p. 1-72.

Miller, K. G., Sugarman, P. J., Browning, J. V., Aubry, M.-P., Brenner, G. J., Cobbs, G. III, de Romero, L., Feigenson, M. D., Harris, A., Katz, M. E., Kulpecz, A., McLaughlin, P.P., Jr., Misintseva, S., Monteverde, D. H., Olsson, R. K., Patrick, L., Pekar, S. J., and Uptegrove, J., 2006, Sea Girt Site, in Miller, K. G., Sugarman, P. J., Browning, J. V. eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174AX (Supplement): College Station, Texas, Ocean Drilling Program, p. 1-104.

Minard, J. P., 1969, Geology of the Sandy Hook quadrangle in Monmouth County, New Jersey: U. S. Geological Survey Bulletin 1276, 43 p.

Munsell Color Company, 1975, Munsell soil color charts: Baltimore, Maryland, Kollmorgen Corporation, MacBeth Division.

Newell, W. L., Powars, D. S., Owens, J. P., and 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.

Olsen, C. R., Biscaye, P. E., Simpson, H. J., Trier, R. M., Kostyk, N., Bopp, R. F., Li, Y.-H., and Feely, H. W., 1980, Reactor-released radionuclides and fine-grained sediment transport and accumulation patterns in Barnegat Bay, New Jersey, and adjacent shelf waters: Estuarine and Coastal Marine Science, v. 10, p. 119-142.

Olson, S. L., and Hearty, P. J., 2009, A sustained +21 m sea-level highstand during MIS 11 (400 ka): direct fossil and sedimentary evidence from Bermuda: Quaternary Science Reviews, v. 28, p. 271-285.

O’Neal, M. L., and Dunn, R. K., 2003, GPR investigation of multiple stage-5 sea level fluctuations on a siliclastic estuarine shoreline, Delaware Bay, southern New Jersey, U. S. A., in Bristow, C. S., and Jol, H. M., eds., Ground penetrating radar in sediments: Geological Society of London, Special Publication, v. 211, p. 67-77.

O’Neal, M. L., Wehmiller, J. F., and Newell, W. L., 2000, Amino acid geochronology of Quaternary coastal terraces on the northern margin of Delaware Bay, southern New Jersey, U. S. A., in Goodfriend, G. A., Collins, M. J., Fogel, M. L., Macko, S. A., Wehmiller, J. F., eds., Perspectives in Amino Acid and Protein Geochemistry: Oxford University Press, p. 301-319.

Owens, J. P., Bybell, L. M., Paulachok, G., Ager, T. A., Gonzalez, V. M., and Sugarman, P. J., 1988, Stratigraphy of the Tertiary sediments in a 945-foot-deep corehole near Mays Landing in the southeastern New Jersey Coastal Plain: U. S. Geological Survey Professional Paper 1484, 39 p.

Owens, J. P., and Sohl, N. F., 1969, Shelf and deltaic paleoenvironments in the Cretaceous-Tertiary formations of the New Jersey Coastal Plain, Field Trip 2, in Subitzky, S., ed., Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions: New Brunswick, N. J., Rutgers University Press, p. 235-278.

Owens, J. P., Sugarman, P. J., Sohl, N. F., Parker, R. A., Houghton, H. F., Volkert, R. A., Drake, A. A., Jr., and Orndorff, R. C., 1998, Bedrock geologic map of central and southern New Jersey: U. S. Geological Survey Miscellaneous Investigations Series Map I-2540-B, scale 1:100,000.

Parham, P. R., Riggs, S. R., Culver, S. J., Mallinson, D. J., Jack Rink, W., Burdette, K., 2013, Quaternary coastal lithofacies, sequence development, and stratigraphy in a passive margin setting, North Carolina and Virginia, USA: Sedimentology, v. 60, p. 503-547.

Petters, S. W., 1976, Upper Cretaceous subsurface stratigraphy of Atlantic coastal plain of New Jersey: AAPG Bulletin, v. 60, p. 87-107.

Potter, E.-K., and Lambeck, K., 2003, Reconciliation of sea-level observations in the western North Atlantic during the last glacial cycle: Earth and Planetary Science Letters, v. 217, p. 171-181.

Psuty, N. P., 2004, Morpho-sedimentological characterisitics of the Barnegat Bay-Little Egg Harbor estuary, in Davis, D. W., and Richardson, M., eds., The Coastal Zone: Papers in Honor of H. Jesse Walker: Lousiana State University, Geoscience and Man Series no. 38, Baton Rouge, Louisiana, p. 81-92.

Rachele, L. D., 1976, Palynology of the Legler lignite: a deposit in the Tertiary Cohansey Formation of New Jersey, USA: Review of Palaeobotany and Palynology, v. 22, p. 225-252.

Reimer, P. J., Bard, E., Bayliss, A., Beck, J. W., Blackwell, P. G., Bronk Ramsey, C., Buck, C. E., Cheng, H., Edwards, R. L., Friedrich, M., Grootes, P. M., Guilderson, T. P., Haflidason, H., Hajdas, I., Hatte, C., Heaton, T. J., Hoffmann, D. L., Hogg, A. G., Hughen, K. A., Kaiser, K. F., Kromer, B., Manning, S. W., Niu, M., Reimer, R. W., Richards, D. A., Scott, E. M., Southon, J. R., Staff, R. A., Turney, C. S. M., and van der Plicht, J., 2013, IntCal13 and Marine13 radiocarbon age calibration curves 0-50,000 years cal BP: Radiocarbon, v. 55, p. 1869-1887.

Ries, H., Kummel, H. B., and Knapp, G. N., 1904, The clays and clay industry of New Jersey: N. J. Geological Survey, Final Report of the State Geologist, v. 6, 548 p.

Scott, T. W., Swift, D. J. P., Whittecar, G. R., and Brook, G. A., 2010, Glacioisostatic influences on Virginia’s late Pleistocene coastal plain deposits: Geomorphology, v. 116, p. 175-188.

Stanford, S. D., 2000a, Surficial geology of the Asbury Park quadrangle, Monmouth and Ocean counties, New Jersey: N. J. Geological Survey Open File Map OFM 40, scale 1:24,000.

Stanford, S. D., 2000b, Surficial geology of the Farmingdale quadrangle, Monmouth and Ocean counties, New Jersey: N. J. Geological Survey Open File Map 35, scale 1:24,000.

Stanford, S. D., 2000c, Geomorphology of selected Pine Barrens savannas: report prepared for the N. J. Department of Environmental Protection, Division of Parks and Forestry, Office of Natural Lands Management, 10 p. and appendices.

Stanford, S. D., 2010, Onshore record of Hudson River drainage to the continental shelf from the late Miocene through the late Wisconsinan deglaciation, USA: synthesis and revision: Boreas, v. 39, p. 1-17.

Stanford, S. D., Ashley, G. M., Russell, E. W. B., and 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., 2017, Geology of the Toms River and Seaside Park quadrangles, Ocean County, New Jersey: N. J. Geological and Water Survey Open File Map OFM 116, scale 1:24,000.

Sugarman, P. J., Miller, K. G., Browning, J. V., Monteverde, D. H., Uptegrove, J., McLaughlin, P. P., Jr., Stanley, A. M., Wehmiller, J., Kulpecz, A., Harris, A., Pusz, A., Kahn, A., Friedman, A., Feigenson, M. D., Barron, J., and McCarthy, F. M. G., 2007, Cape May Zoo site, in Miller, K. G., Sugarman, P. J., Browning, J. V., and others, eds., Proceedings of the Ocean Drilling Program, Initial Reports, v. 174AX (Supplement 7), p. 1-66.

Sugarman, P. J., Miller, K. G., Owens, J. P., and Feigenson, M. D., 1993, Strontium-isotope and sequence stratigraphy of the Miocene Kirkwood formation, southern New Jersey: Geological Society of America Bulletin, v. 105, p. 423-436.

Sugarman, P. J., Monteverde, D. H., Boyle, J. T., and Domber, S. E., 2013, Aquifer correlation map of Monmouth and Ocean counties, New Jersey: N. J. Geological and Water Survey Geologic Map Series GMS 13-1.

Sugarman, P. J., Owens, J. P., and Bybell, L. M., 1991, Geologic map of the Adelphia and Farmingdale quadrangles, Monmouth and Ocean counties, New Jersey, New Jersey Geological Survey Geologic Map Series 91-1, scale 1:24,000.

Uptegrove, J., Waldner, J. S., Stanford, S. D., Monteverde, D. H., Sheridan, R. E., and Hall, D. W., 2012, Geology of the New Jersey offshore in the vicinity of Barnegat Inlet and Long Beach Island: N. J. Geological Survey Geologic Map Series GMS 12-3, scale 1:80,000.

Volkert, R. A., Drake, A. A., Jr., and Sugarman, P. J., 1996, Geology, geochemistry, and tectonostratigraphic relations of the crystalline basement beneath the coastal plain of New Jersey and contiguous areas: U. S. Geological Survey Professional Paper 1565-B, 48 p.

MAP SYMBOLS

Contact of surficial deposits—Solid where well-defined by landforms as visible on 1:12,000 stereo airphotos and LiDAR imagery; long-dashed where approximately located; short-dashed where gradational or featheredged; dotted where exposed in excavations.

Contact of bedrock formations—Approximately located. Dotted where concealed by surficial deposits.

Concealed bedrock formation—Covered by surficial deposits.

Material penetrated by hand-auger hole, or observed in exposure or excavation. Number indicates thickness of surficial material, in feet, where penetrated. Symbols within surficial deposits without a thickness value indicate that surficial material is more than 5 feet thick. Where more than one unit was penetrated, the thickness (in feet) of the upper unit is indicated next to its symbol and the lower unit is indicated following the slash.

Photograph location

Well or test boring showing formations penetrated—Location accurate to within 200 feet. List of formations penetrated is provided in table 1.

Well or test boring showing formations penetrated—Location accurate to within 500 feet. List of formations penetrated is provided in table 1.

Dune ridge—Line on crest.

Shallow topographic basin—Line at rim; pattern in basin. Includes thermokarst basins formed from melting of permafrost and a few deflation basins, adjacent to eolian deposits, formed from wind erosion.

Excavation perimeter—Line encloses excavated area.

Sand and gravel pit—Inactive in 2018.

Dominant grain size of bay-bottom sediment in 6-foot vibracore—Data on file at N. J. Geological and Water Survey. sand sand and clay-silt clay-silt

Dominant grain size of bay-bottom sediment in shallow grab sample—Data from Andrews and others (2016). sand sand and clay-silt clay-silt

Dominant grain size of bay-bottom sediment in 6-foot vibracore—Data from Bernier and others (2016). sand sand and clay-silt clay-silt

GEOLOGY OF THE POINT PLEASANT QUADRANGLEMONMOUTH AND OCEAN COUNTIES, NEW JERSEY

byScott D. Stanford, Peter J. Sugarman, Michael V. Castelli, and Alexandra R. Carone

2018

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, 1999

TRU

E N

OR

TH

LOCATION IN NEW JERSEY

13O

CONTOUR INTERVAL 5 FEETBATHYMETRIC CONTOURS IN FEET

NATIONAL GEODETIC VERTICAL DATUM OF 1929

Base map from U. S. Geological Survey Point Pleasant quadrangle, 1995.Topography compiled 1986. Planimetry derived from imagery taken 1995.Survey control current as of 1984.North American Datum of 1983.

Bedrock geology mapped by P. J. Sugarman, M. V. Castelli, A. R. Carone, and S. D. Stanford, 2016-2018Surficial geology by S. D. Stanford, 2018

Drilling by B. ButtariDrilling assistance by M. Castelli, I. Snook, G. Steidl, N. Thistle

Geophysical logging by M. Gagliano and M. SpencerCartography by S. D. Stanford and A. R. Carone

Reviewed by J. W. Jengo and C. S. Swezey

Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program, under USGS award numbers G16AC00284 (bedrock) and G17AC00256 (surficial).The views and conclusions contained in this document are those of the authors

and should not be interpreted as necessarily representing the officialpolicies, either expressed or implied, of the U. S. Government.

DEPARTMENT OF ENVIRONMENTAL PROTECTIONWATER RESOURCES MANAGEMENTNEW JERSEY GEOLOGICAL AND WATER SURVEY

GEOLOGY OF THE POINT PLEASANT QUADRANGLE MONMOUTH AND OCEAN COUNTIES, NEW JERSEY

GEOLOGIC MAP SERIES GMS 18-5SHEET 1 OF 2

Pamphlet containing tables 1 and 2 accompanies map

Prepared in cooperation with theU. S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

Manas

quan

Rive

r

SawmillCreek

Metedeconk River

Beaverdam Ck

BarnegatBay

Kettle

Creek

-25

-50

-75

-25

-50

0

0

0-25

-250 0

-25

-25

Metedeconk Neck

Mantoloking

Bay Head

Point Pleasant

BrielleHerbertsville

RivieraBeach

Wardells Neck

figure 2

Atlantic Ocean

fine-grained

bay deposits

tidal-delta and

overwash sand

0 1 2

miles

Holocene features

salt marsh

ocean beach

beach dunes

overwash plain and urbanized barrier

Pleistocene and older features

inland limit of Cape May Formation, unit 2, dashed where erodedinland limit of Cape May Formation, unit 1, dashed where erodedlimit of Wisconsinan valleyincision (ticks point into valley)

inland limit of Cape May Formation,unit 2, fine-grained facies

well penetrating Cape May Formation,unit 2, fine-grained facies

stream drainage during deposition of upland gravel

possible routes of the Manasquan andMetedeconk rivers before depositionof Cape May Formation, unit 2

eolian deposits

paleodune ridge

elevation of base of Quaternarydeposits, contour interval 25 feet,shown only at and below sea level

-25

approximateboundary of overwash sand and fine baydeposits

Figure 1. Geomorphic and surficial geologic features of the Point Pleasant quadrangle.

dune ridges

thermokarstbasins

0 1000

feet

blow-outdunes

Figure 2. LiDAR hillshade image showing paleodune ridges and relict thermokarst basins on Metedeconk Neck. Dune orientation indicates winds blowing from the north and northwest. Easternmost thermokarst basin is partially covered by tidal-marsh deposits. Blow-out dunes rim basins that may have formed or been enlarged by wind erosion. Location shown on figure 1.

Tch

!

!

Qe5/Qcm2

4

!figure 5

!

47

.247

!

!

!

#

#

#

!

Qals

Qal

Qm

Qbs

Qbe

Qbo

Qbu

Qe

Qcl

Qtl

Qtu

Qcu

Qcm1

Qcm2

Qcm2f

TQg

Tg

Tch

Tkw

Tsr

Tmq

Tmb

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Krw

Krf

Kp3

Figure 3. Eolian sand (unit Qe) exposed in former sand pit in dune ridge on Metedeconk Neck. Location shown on map and inset.

MAP AREA

Figure 4. Cape May Formation, unit 2 (unit Qcm2), exposed in bank along Manasquan River. Thin horizontal bedding visible in upper part of bank is typical of tidally influenced deposition. Location shown on map and inset.

MAP AREA

Figure 5. Upland gravel, high phase (unit Tg), exposed in former gravel pit west of Brielle. Cross bedding indicates former stream flow to east (right on photo). Photo by Meredith Johnson, N. J. Geological Survey, April 1936. Location shown on map and inset.

MAP AREA

Figure 6. Interbedded clay (white beds) and sand (yellow and red beds) of the Cohansey Formation (unit Tch). Red color in sand above clay marks iron deposition where drainage is impeded. Location shown on map and inset.

MAP AREA

Figure 7. Alluvial sand (unit Qal, above shovel head) over clay of the Cohansey Formation. Subvertical features highlighted by orange color (arrows) below yellow bed may be burrows. Location shown on map and inset.

MAP AREA

Page 2: GEOLOGY OF THE POINT PLEASANT QUADRANGLE …

186

185 18

4

19

Qcm1Qtl Qals Qals Qtl QtuQtl

Qcm1 TQg Qcm1

Qm Qtl

16

Qal

Qtu Qal Qcm1 Qcu

30 32

309 Tg

56excavatedexcavated

TgQal Qcu Qcm1

104

103

102

Qcm2

Qal

105

107

Qm

QbeQbs

ATLA

NTI

C O

CEA

N

STO

CK

TON

LA

KE

NJ

TRA

NSI

T R

R

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BER

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MP

BK

Qal

NJ

RO

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34

RA

MSH

OR

N D

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BEN

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SEC

TIO

N,

SEC

TIO

N C

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MA

NA

SQU

AN

RIV

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HER

BER

TSVI

LLE

RD

SAW

MIL

L C

REE

K

A200

-200

-400

-600

-800

-1000

-1200

-1400

-1600VERTICAL EXAGGERATION 10X

ELEV

ATIO

N (F

EET)

SEALEVEL

Tch TchTch

Tkw

Tsr

Tmq

Tmb

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Krw

Krf

Kp3

Tkw

Tsr

Tmq

Tmb

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Krw

Krf

Kp3

200

-200

-400

-600

-800

-1000

-1200

-1400

-1600

SEALEVEL

A’

310

B200

-200

-400

-600

-800

-1000

-1200

-1400VERTICAL EXAGGERATION 10X

ELEV

ATIO

N (F

EET)

SEALEVEL

200

-200

-400

-600

-800

-1000

-1200

SEALEVEL

B’

-1400

Qtl Qal Qtl Qals205

300

213

Qcm2Qm Qtl

Qcm2

164

162

163

161

147

157

SEC

TIO

N C

C’

Qcm2

Qm

149

153

152

Qbu Qbo QbeQbs

148

NJ

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UTE

70

BEA

VER

DA

M C

REE

K

NJ

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UTE

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DA

N R

D

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BR

AN

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BEA

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TT D

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D

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EASA

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NA

L

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35

ATLA

NTI

C O

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N

Tch

Tkw

Tsr

Tmq

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Tkw

Tsr

Tmq

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

DEPARTMENT OF ENVIRONMENTAL PROTECTIONWATER RESOURCES MANAGEMENTNEW JERSEY GEOLOGICAL AND WATER SURVEY

GEOLOGY OF THE POINT PLEASANT QUADRANGLE MONMOUTH AND OCEAN COUNTIES, NEW JERSEY

GEOLOGIC MAP SERIES GMS 18-5SHEET 2 OF 2

Pamphlet containing tables 1 and 2 accompanies map

Prepared in cooperation with theU. S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

Qal

C200

-200

-400

-600

-800

-1000

-1200

-1400

VERTICAL EXAGGERATION 10X

ELEV

ATIO

N (F

EET)

SEALEVEL

200

-200

-400

-600

-800

-1000

-1200

SEALEVEL

C’

-1400

-1600

-1800

-2000

-1600

-1800

-2000

43 44 309

SEC

TIO

N A

A’

55 54 66 65 67 75

TgTgexcavated excavated excavated

Qcm1

81 80 Qbs Qm QbsQtl Qcm2

Qm

Qtl QbsQcm2

305

140

141

TgQcm1

146

147

157

158

160,

159

231

232

234

SEC

TIO

N B

B’

Qm Qm Qtl

Qcm2

Qbs Qm Qtl Qm Qm

Qcm2Qcm2f

QmQcm2

Qbu Qbe

QboQbs26

726

8

QalTg

SEC

TIO

N D

D’

249

250

258

NJ

RO

UTE

34

NJ

RO

UTE

70

MA

NA

SQU

AN

RIV

ER

RIV

ER R

D

NJ

RO

UTE

88

BR

IDG

E AV

E

BEA

VER

DA

M C

REE

K

MET

EDEC

ON

K

RIV

ER

SWA

N P

OIN

T

BA

RN

EGAT

BAY

SWA

MP

CO

VE

NJ

RO

UTE

35

ATLA

NTI

CO

CEA

N

Tch

Tkw

Tsr

Tmq

Tmb

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Krw

Krf

Kp3

Tkw

Tsr

Tmq

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Krw

Krf

Kp3

Tch

259 Qals

241

242

240

243Qals

Qcm2

307

244

245

246

BEN

D IN

SE

CTI

ON

SEC

TIO

N C

C’

Qcm2Qcm2f

249

250

251

253

254

255,

256

Qm

Qcm2

QboQbs

QbeQbu

Tch

Tkw

Tsr

Tmq

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

Tkw

Tsr

Tmq

Tvt

Tht

Krb-ns

Kml

Kw-mt

Ketu

Ketl

Kwb-mv

Kmg

DR

UM

PO

INT

RD

REE

DY

CR

EEK

BA

RN

EGAT

BAY

NJ

RO

UTE

35

ATLA

NTI

CO

CEA

N

D200

-200

-400

-600

-800

-1000

-1200

-1400VERTICAL EXAGGERATION 10X

ELEV

ATIO

N (F

EET)

SEALEVEL

200

-200

-400

-600

-800

-1000

-1200

SEALEVEL

D’

-1400

7000 FEET1000 10000 2000 3000 4000 5000 6000

.5 1 KILOMETER1 0

HORIZONTAL SCALE 1:24 0001/21 0 1 MILE

EXPLANATION OF SYMBOLS

Well or boring—Number refers to listing in table 1.

Well with geophysical log—Gamma-ray log is shown by red line, with radiation intensity increasing to right. Resistivity log is shown by blue line, with resistivity increasing to right.

Tieline—Correlates lithologic units within forma- tions. Refer to unit descriptions on sheet 1.

4774

GEOLOGY OF THE POINT PLEASANT QUADRANGLEMONMOUTH AND OCEAN COUNTIES, NEW JERSEY

byScott D. Stanford, Peter J. Sugarman, Michael V. Castelli, and Alexandra R. Carone

2018

SHEET 2: CROSS SECTIONS

Page 3: GEOLOGY OF THE POINT PLEASANT QUADRANGLE …

1  

Geology of the Point Pleasant Quadrangle Monmouth and Ocean Counties, New Jersey

New Jersey Geological and Water Survey

Geologic Map Series GMS 18-5 2018

Pamphlet with tables 1 and 2 to accompany map

Table 1. Selected well and boring records. Footnotes at end of table (p. 7).

Well Number

Identifier1 Formations Penetrated2

1 14004 22 Q 78 Tchs 81 Tkw2 18639 4 TQg 41 Tchs 49 Tchc 65 Tchs3 31445 20 Q 60 Tchs 4 31386 10 Q 40 Tchs+Tchc 75 Tchs5 20249 42 Q 6 24678 22 Q 40 Tchc 53 Tchs 55 Tkw7 21902 4 TQg 51 Tchs 75 Tkw8 2618 10 TQg 60 Tchs 70 Tkw9 21890 14 Q 73 Tchs 140 Tkw10 20533 35 Q 120 Tchs 135 Tkw11 14863 15 fill 49 Tg 70 Tchs12 23900 4 Tg 65 Tchs 13 15728 34 Q+Tchs 79 Tchs 90 Tkw14 4410 18 Q 88 Tkw 15 14981 25 Q 135 Tkw 16 17773 60 Q+Tchs 140 Tkw17 18910 35 Q+Tchs 140 Tkw18 16249 45 Q+Tchs 120 Tkw19 12002 72 Q+Tchs 125 Tkw20 N 29-33-542 34 Q 104 Tkw 21 31568 20 Q 80 Tkw 22 16681 20 Q 40 Q or Tkw 70 Tkw23 28 56 Q+Tchs 112 Tkw24 2599 30 Q+Tchs 50 Tchs 89 Tkw25 2365 25 Q+Tchs 101 Tkw26 15208 15 Q 75 Tkw 27 30872 20 Q 126 Tkw 28 16614 52 Q+Tkw 75 Tkw29 19741 30 Q 69 Tkw 30 20572 10 fill 24 Q 74 Tkw31 20353 18 Q 153 Tkw 155 Tsr32 20236 11 Q 136 Tkw 138 Tsr33 18817 44 Q+Tkw 140 Tkw34 2783 10 TQg+Tchs 39 Tchs+Tchc or Tkw 92 Tkw35 20121 11 Q 139 Tkw 140 Tsr36 23568 10 Tg 55 Tchs+Tkw 82 Tkw37 20294 8 Tg 45 Tchs 130 Tkw38 20351 30 Tg+Tchs 45 Tchs 125 Tkw

Page 4: GEOLOGY OF THE POINT PLEASANT QUADRANGLE …

2  

Well Number

Identifier1 Formations Penetrated2

39 20354 14 Q 26 Tchc 40 Tchs 100 Tkw40 6038 8 TQg 24 Tchs 45 Tchc+Tchs 55 Tchs 157 Tkw41 19569 16 TQg 23 Tchc 48 Tchs 154 Tkw42 21006 10 Tg 25 Tchs 35 Tchc+Tchs 80 Tchs 120 Tkw43 10603 4 Tg 9 Tchc 17 Tchs+Tchc 35 Tchs 39 Tchc 60 Tchs 128 Tkw44 16549 3 Tg 23 Tchc 55 Tchs 200 Tkw45 19264 13 Tg 20 Tchc 65 Tchs 140 Tkw46 15531 32 Q 135 Tkw 47 14994 35 Q 134 Tkw 48 20482 36 Q 75 Tkw 49 18922 27 Q 53 Tkw 50 22287 44 Q 132 Tkw 51 18649 41 Tg+Tchs 71 Tchs 130 Tkw52 20531 10 Q 29 Q or Tchs 138 Tkw53 20330 10 Q 45 Tchs 54 5491 10 Tg+Tchs 30 Tchs+Tchc 50 Tchs 205 Tkw55 2971 20 Tg+Tchs 40 Tchs+Tchc 148 Tkw56 13539 25 Tg 27 Tchc 38 Tchs 39 Tchc 59 Tchs57 16991 2 Q 150 Tkw 58 16533 5 Q 160 Tkw 59 22733 22 Q 152 Tkw 60 17528 4 fill 150 Tkw 61 18577 3 fill 22 Q 145 Tkw62 15090 5 fill 9 Qm 28 Qcm2 45 Tkw63 1336 25 Tg+Tchs 45 Tchs 192 Tkw64 20842 14 Tg 18 Tchc 85 Tchs 95 Tkw65 10208 20 Tg+Tchs 85 Tchs 98 Tkw or Tchs66 10487 23 Tg+Tchs 50 Tchs+Tchc 93 Tchs 98 Tkw67 12388 12 Tg 59 Tchs+Tchc 92 Tchs 94 Tkw68 15181 30 Tg+Tchs 100 Tchs 125 Tkw69 23455 4 Tg 17 Tchs 35 Tchs+Tchc 63 Tchs 176 Tkw 180 Tsr70 23642 4 Tg 17 Tchs 35 Tchs+Tchc 63 Tchs 176 Tkw 180 Tsr71 14415 20 Q+Tchs 25 Tchs 40 Tchs+Tchc 80 Tchs 116 Tkw72 17229 18 fill 22 Q 25 Tchc 40 Tchs 54 Tchs+Tchc 137 Tkw73 5292 8 Tg 119 Tchs 212? Tkw 848 TD74 24650 33 Tg+Tchs 90 Tchs 115 Tchs+Tchc 197 Tkw 200 Tsr75 12147 30 Tg+Tchs 50 Tchs 70 Tchs+Tchc 80 Tchs 140 Tkw76 11444 19 Q 160 Tkw 77 11445 45 Q 140 Tkw 78 12069 5 Q 50 Tchs 60 Tkw79 11246 19 Q 50 Tkw 80 22865 27 Q 52 Tkw 81 22492 5 Q 40 Tkw 82 22755 10 Q 40 Tchs 83 14302 30 Q 125 Tkw 84 15058 10 Q 40 Tchs+Tchc 140 Tkw85 3973 39 Q 72 Tkw 86 20531 29 Q 138 Tkw 87 16401 32 Q 132 Tkw 88 20691 30 Q 140 Tkw 89 22470 22 Q 60 Tkw 90 22471 26 Q 120 Tkw 91 12418 21 Q 114 Tkw 92 31688 29 Q 93 29528 30 Q 117 Tkw 94 14995 40 Q 119 Tkw 95 30148 26 Q 60 Tkw

Page 5: GEOLOGY OF THE POINT PLEASANT QUADRANGLE …

3  

Well Number

Identifier1 Formations Penetrated2

96 8184 44 Q 68 Q+Tchs 179? Tkw 577 TD97 69 +

N 29-33-648 56 Q 75 Tchs 150 Tkw 792 TD

98 14504 24 Q 99 5328 26 Q 115 Tkw 100 24936 35 Q 101 DOT 234W-5 21 Q 50 Tkw 102 2438 20 Q 124 Tkw 103 13124 17 Q 126 Tkw 104 1004 25 Q 117 Tkw 105 15371 25 Q 36 Tkw 106 3849 9 fill 13 Qm 27 Qcm2 110 Tkw107 49349, G

Sea Girt corehole (Miller and others, 2006)

3 fill 23 Q 140 Tkw 1600 TD

108 22123 12 fill 16 Qm 27 Qtl 140 Tkw 200 Tsr109 14583 12 fill 16 Qm 27 Qtl 160 Tkw110 22775 17 Q 80 Tkw 111 24872 24 Q 132 Tkw 617 TD112 10380 31 Q 80 Tkw 113 27975 28 Q 134 Tkw 157 Tsr114 28998 33 Q 52 Tkw 115 18723 30 Q 31 Tkw 116 19720 18 Q 40 Tkw 117 29201 20 Q 118 6299 30 Q 167 Tkw 168 Tsr119 24046 35 Q 37 Tkw 120 24049 32 Q 37 Tkw 121 5089 22 Q 165 Tkw 202 Tsr122 19415 28 Q 120 Tkw 123 23241 29 Q 177 Tkw 180 Tsr124 29323 22 Q 47 Tkw 125 26100 28 Q 126 18411 32 Q 80 Tkw 127 10235 35 Q 90 Tkw 128 32030 23 Q 100 Tkw 129 32001 32 Q 130 14834 30 Q 90 Tkw 131 DOT 478W-7 30 Q 56 Tkw 132 56684 35 Q 130? Tkw 800 TD133 15099 26 Q 134 2857 24 Q 148 Tkw 135 DOT 478W-6 25 Q 55 Tkw 136 25924 28 Q 137 12883 27 Q 50 Tkw 138 23214 17 Q 42 Tkw 139 36930 23 Q 41 Tchs+Tchc 78 Tchs 85 Tkw140 3345, G + 4530 43 Q 168 Tkw 1414 TD141 10234 39 Q 40 Tchc 55 Tchs 90 Tkw142 10233 35 Q 37 Tchc 57 Tchs+Tchc 72 Tchs 80 Tkw143 23730 35 Q 36 Tchc 144 23548 24 Q 145 26821 26 Q 146 13182 23 Q 65 Tkw 147 32526 20 Q 200 Tkw 341 Tsr

Page 6: GEOLOGY OF THE POINT PLEASANT QUADRANGLE …

4  

Well Number

Identifier1 Formations Penetrated2

148 21068 30 Q 149 16733 11 Q 112 Tkw 150 DOT 376W-2 5 fill 6 Qm 10 Qcm2151 DOT 376W-7 3 fill 7 Qm 10 Qcm2152 24652 6 Qbu 10 Qm 27 Qcm2 65 Tkw153 87 20 Q 180 Tkw 825 TD154 27365 6 fill 9 Qm 25 Qcm2 42 Tkw155 13158 4 fill 12 Qm 34 Qcm2 75 Tkw156 28135 4 fill 6 Qm 30 Qcm2 120 Tkw157 48193, G +

5445 + 49202 23 Q 210 Tkw 1457 TD

158 15003 25 Q 70 Tkw 159 13425 27 Q 72 Tkw 160 13275 25 Q 67 Tkw 161 24917 26 Q 162 11967 30 Q 163 15093 33 Q 35 Tchc 50 Tchs164 18803 25 Q 30 Tchs 165 30860 17 Q 50 Tkw 166 24782 27 Q 40 Tkw 167 29888 35 Q 36 Tkw 168 485 36 Q 169 4324 28 Q 137 Tkw 180 Tkw or Tsr170 6404 30 Q 130 Tkw 132 Tsr171 DOT B2 33 Q 143 Tkw 171 Tsr172 DOT B8 11 water 29 Qm 38 Qtl 129 Tkw 183 Tsr173 DOT S4 17 water 21 Qm 47 Qtl 126 Tkw 228 Tsr174 DOT B22 5 fill 11 Qm 31 Qcm2 145 Tkw 171 Tsr175 8953 32 Q+Tchs 56 Tchs176 17152 13 Q 35 Tchs 124 Tkw177 466 18 Q 63 Tkw 178 298 12 Q 33 Tkw 179 300 15 Q 63 Tkw 180 21387 50 Tchs 80 Tkw 181 308 15 Q 63 Tkw 182 5441 44 Q 97 Tkw 183 21148 16 Q 82 Tkw 184 12630 37 Q+Tchs 122 Tkw185 2956, G 8 Q 140? Tkw 1145 TD186 28845 10 Q 40 Tchs 142 Tkw187 413 30 Tchs 10 Tchc 66 Tchs188 258 46 Tchs+Tchc 189 257 47 Tchs+Tchc 190 369 24 Q+Tchs 34 Tchc 45 Tchs191 368 20 Tchs 32 Tchc 45 Tchs192 354 20 Tchs 30 Tchc 43 Tchs193 371 20 Q+Tchs 30 Tchc 44 Tchs194 271 36 Q+Tchs+Tchc 195 410 15 Q+Tchs 25 Tchc 37 Tchs196 543 10 Q+Tchs 21 Tchc 40 Tchs197 6022 + 5946 30 Q 40 Qcm2f or Tchc 68 Tchs 158 Tkw 586 TD198 21473 20 Q 70 Tchs 199 20711 51 Q+Tchs 200 24919 40 Q+Tchs 201 24634 36 Q+Tchs 202 10787 50 Q+Tchs 62 Tchs 63 Tchc or Tkw203 23286 14 Q 85 Tchs 90 Tkw

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Well Number

Identifier1 Formations Penetrated2

204 3076 14 Q 84 Tchs 178 Tkw 590 TD205 4283, G 20 Q 60 Tchs 180 Tkw 591 TD206 302 15 Q 20 Tchc 30 Tchs 32 Tchc 38 Tchs207 395 9 Q 11 Tchc 43 Tchs208 17024 12 Q 55 Q+Tchs 165 Tkw 172 Tsr209 25005 17 Q 21 Tchc 33 Tchs 35 Tchc 55 Tchs210 24822 17 Q 21 Tchc 38 Tchs+Tchc 55 Tchs211 26085 6 Q 65 Tchs 125 Tkw 162 Tkw or Tsr 175 Tsr212 17547 8 Q 54 Tchs 213 20878 32 Q 47 Tchs 214 13537 4 fill 10 Qm 24 Qcm2 35 Qcm2 or Tchs 42 Tchc+Tchs 56 Tchs215 32105 32 Q 45 Tchc+Tchs or Q 55 Tchs216 4420 67 Q+Tchs 67 Tchc or Tkw217 23886 6 Q 26 Tchc+Tchs 52 Tchs218 23898 5 fill 10 Q+Tchs 15 Tchc+Tchs 30 Tchc 52 Tchs219 23969 15 Q+Tchs 30 Tchs 46 Tchc 58 Tchs220 22822 15 Q+Tchs 45 Tchc 56 Tchs221 23887 12 Q+Tchs 26 Tchs 38 Tchc 53 Tchs222 20352 10 Q 20 Tchs 40 Tchs+Tchc 70 Tchs223 15059 20 Q 30 Tchs+Tchc 70 Tchs224 31316 10 Q 59 Tchs 225 32413 20 Q 45 Tchs+Tchc 77 Tchs226 23890 3 fill 11 Qm 20 Qcm2227 3637 8 fill 32 Qm over Qtl 72 Tchs 149 Tkw228 12825 43 Q 54 Tchc 70 Tchs229 5192 65 Q over Tchs 77 Tchs 164 Tkw230 22276 8 fill 13 Qm 31 Qcm2 52 Tchs 141 Tkw 150 Tsr or Tkw231 DOT B5 15 fill 35 Qm 42 Qtl+Qcm2 52 Tkw232 DOT B7 31 fill 32 Qm 41 Qtl+Qcm2 102 Tkw233 DOT B8 4 water 9 Qm 13 Qtl+Qcm2 102 Tkw234 DOT B9 4 water 20 Qm 32 Qtl+Qcm2 92 Tkw235 DOT B11 37 Qcm2 102 Tkw236 22100 17 Qbu 56 Qm 100 Tkw237 20032 20 Q 35 Tchc 53 Tchs 57 Tchc238 4444 4 fill 25 Qm 35 Qcm2239 2328 62 Q+Tchs 192? Tkw 528 TD240 5484 45 Q 68 Tchc 70 Tchs 100 Tkw241 6701 35 Q 69 Tchs 125 Tkw242 2875, R 45 Q 82? Tchs 202 Tkw 786 TD243 7753 42 Q 65 Tchc+Tchs 69 Tchs244 29727 25 Qcm2 50 Qcm2f 75 Tchs245 2279 28 Qcm2 58 Qcm2f 87 Tchs246 29941 30 Qcm2 31 Qcm2f247 13179 6 fill 11 Qm 35 Qcm2 62 Qcm2f 90 Tkw248 16334 3 fill 9 Qm 24 Qcm2 65 Qcm2f 100 Tkw249 19140 14 fill 22 Qm 30 Qcm2 60 Qcm2f 200 Tkw250 3494 28 Qm 48 Qcm2 70 Qcm2f 160 Tkw251 24254 9 water 21 Qbo 50 Qm 71 Qcm2f 109 Tkw252 24253 7 water 19 Qbo 44 Qm 77 Qcm2f253 24255 7 water 19 Qbo 44 Qm 77 Qcm2f254 24257 5 water 10 Qm 16 Qbo 26 Qm+Qbo 49 Qm 76 Qcm2f255 1325 + 3142, G 33 Qbu over Qbo 75 Qm+Qcm2 185 Tkw 1465 TD256 681 8 Qbu 17 Qm 29 Qbo 40 Qm 45 Qcm2 83 Qcm2f 215 Tkw 400 TD257 11951 + 11952 9 Qbu 20 Qbo+Qm 35 Qbo 72 Qm+Qcm2f 80 Tkw or Qcm2258 21587 3 fill 8 Qm 20 Qcm2 63 Qcm2f 67 Qcm2 123 Tkw259 15645 23 Q 49 Tchs 82 Tchs+Tchc 98 Tchs 207 Tkw 230 Tsr260 5331 3 fill 10 Qm 58 Qcm2 76 Tchs 79 Tchc 101 Tchs 113 Tchs 205 Tkw

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Well Number

Identifier1 Formations Penetrated2

261 5549 3 fill 12 Qm 55 Qcm2 87 Tchs 200 Tkw262 5521 5 fill 20 Qm 40 Qcm2 64 Tchs 80 Tchc 89 Tchs 108 Tchs+Tchc 185 Tkw 189 Tsr? 263 4463 50 Q 103 Tchs 187 Tkw 195 Tsr?264 2938 50 Q+Tchs 200 Tkw 210 Tsr265 9817 5 fill 10 Qm 20 Qcm2 35 Qcm2f 60 Qcm2 266 5885 45 Qm 65 Qcm2f 78 Qcm2267 24348 +

25859, G 20 Qbu+Qm 28 Qbo 58 Qm 100 Qcm2+Tchs+Tchc 205 Tkw 2250 TD

268 29267 30 Qbu+Qm 62 Qm 103 Qcm2+Tchs+Tchc 206 Tkw 275 Tsr269 17606 24 Qcm2 30 Qcm2f 57 Tchs 112 Tkw270 16212 68 Qcm2 75 Qcm2f271 19257 24 Qcm2 68 Qcm2+Qcm2f 79 Tchs 100 Tkw272 759 15 fill 21 Qm 60 Qcm2 80 Qcm2f 112 Tchs 160 Tkw273 2732 10 fill 20 Qm 93 Qcm2+Qcm2f 215 Tkw274 5391 2 fill 6 Qm 39 Qcm2 45 Qcm2f 55 Qcm2 57 Qcm2f 81 Tchs 175 Tkw 275 76 61 Qcm2 66 Qcm2f 93 Tchs 210 Tkw276 1327 48 Qcm2 60 Tchs 212 Tkw277 724 2 fill 6 Qm 18 Qcm2 39 Qcm2f 72 Qcm2+Qcm2f 164 Tkw278 53 3 fill 8 Qm 30 Qcm2 93 Qcm2 or Tchs 112 Tchs 165 Tkw279 4896 50 Qcm2 60 Tchs+Tchc 218 Tkw280 5396 79 Qcm2 118 Tchs 170 Tkw281 30623 65 Qcm2 90 Tchs 103 Tchs+Tchc 233 Tkw 290 Tsr282 385 30 Qcm2 50 Qcm2f 70 Tchs 85 Tchc 109 Tchs 120 Tchc or Tkw 214 Tkw 283 1648 50 Qcm2 60 Qcm2f+Qcm2 130 Tchs+Tkw 170 Tkw284 516 3 fill 7 Qm 59 Qcm2 78 Qcm2f 131 Tchs+Tkw 167 Tkw285 1191 40 Qcm2 60 Qcm2f 70 Qcm2 140 Tchs+Tkw 169 Tkw286 714 3 fill 7 Qm 20 Qcm2 35 Qcm2f 69 Qcm2+Tchs 167 Tkw287 1137 4 fill 15 Qm 56 Qcm2+Qcm2f 71 Tchc 86 Tchs 171 Tkw288 1116 15 Qm 50 Qcm2 56 Qcm2+Qcm2f 96 Tchs+Tchc 173 Tkw289 172 25 Qcm2 40 Qcm2f 50 Tchs 67 Tchc 88 Tchs 164 Tkw290 47 40 Qm 50 Qcm2 63 Tchs 166 Tkw291 1329 4 Qcm2 20 Qcm2+Qcm2f 38 Qcm2f 50 Qcm2 65 Qcm2+Qcm2f 90 Tchs 168 Tkw 292 57 10 Qm 50 Qcm2 83 Qcm2f 130 Tchs 250 Tkw 321 Tsr293 34306 5 fill+Qm 25 Qcm2 30 Qcm2f 50 Tchs294 42972 26 Qcm2 40 Qcm2f295 42973 30 Qcm2 45 Qcm2f 60 Tchs296 15080 5 fill 7 Qm 20 Qcm2 22 Qcm2f297 559 19 Q+Tchs 27 Tchc 36 Tchs298 344 30 Tchs 38 Tchc 47 Tchs299 305 35 Tchs 45 Tchc 50 Tchs300 540 15 Q+Tchs 23 Tchc 34 Tchs301 6103 20 Q 45 Tchc+Tchs 56 Tchs302 2770 36 Tchs 303 16713 21 Qcm2 62 Qcm2f 100 Tkw304 26086 20 Qcm2 64 Qcm2f 82 Tkw305 USGS Point

Pleasant 3 28 Q 71 Tkw

306 USGS Point Pleasant 2

8 Q 24 Q+Tchs 26 Tkw

307 USGS Point Pleasant 1

32 Qcm2 41 Qcm2f

308 26099 24 Q 27 Tchs 34 Tchs+Tchc 46 Tchc 52 Tchs+Tchc 56 Tchs309 40257, G 80 Tchs 197 Tkw 310 E201704340,

G 9 Q 20 Tchs 100 Tkw

311 E201704341, G

10 Q 55 Tchs 83 Tkw

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1Numbers of the form xxxxx are N. J. Department of Environmental Protection well-permit numbers. All are preceded by the prefix “29-.” A “+” indicates that two or more wells were drilled at same location. Numbers of the form E20170xxxx are also N. J. Department of Environmental Protection well-permit numbers. Numbers of the form N xx-xx-xxx are Atlas Sheet Coordinate locations for entries in the N. J. Geological and Water Survey permanent note collection. Identifiers prefixed by “DOT” are bridge borings from the N. J. Department of Transportation, accessed at http://www.state.nj.us/transportation/refdata/geologic/. Identifiers prefixed by “USGS” are auger borings drilled in cooperation with the U. S. Geological Survey during a statewide geologic mapping program in the 1990s. The Sea Girt corehole (well 107) is a stratigraphic research corehole with detailed information available in the cited reference. A “G” following the identifier indicates that a gamma-ray log is available for the well; an “R” indicates that a resistivity log is available for the well. 2Number is depth (in feet below land surface) of base of unit indicated by abbreviation following the number. Final number is total depth of well rather than base of unit. For example, “12 Q 34 Tchc 62 Tchs” indicates Q from 0 to 12 feet below land surface, Tchc from 12 to 34 feet, and Tchs from 34 to bottom of hole at 62 feet. Units are inferred from drillers’ or geologists’ lithologic descriptions on well records filed with the N. J. Department of Environmental Protection, or provided in the cited publications, and from geophysical well logs. Formation abbreviations and the corresponding drillers’ descriptive terms used to infer the formation are: Q = Quaternary surficial deposits, undifferentiated (units Qtu, Qtl, Qals, Qal, Qcu, Qcl, Qcm1, Qcm2) = yellow, white, tan, brown, gray sand and gravel, minor silty and clayey sand. TQg, Tg = upland surficial deposits = yellow, brown, white, gray sand, silty sand, and gravel. Quaternary surficial units along the bayshore and oceanfront are differentiated as follows: Qcm2, Qbo, Qbe, Qbs, Qbu = yellow, brown, gray, white sand and gravel, Qm = peat, meadow mat, meadow mud, sod, organic mud, and gray to brown mud, Qcm2f = gray to brown clay, silt, fine sand, marl, soft clay, minor peat and vegetation. Bedrock formations are: Tchs = white, yellow, gray, brown (minor red, orange) fine, medium, and coarse sand (and minor fine gravel) of the Cohansey Formation; Tchc = yellow, white, gray (minor red, orange) clay, silty clay, and sandy clay of the Cohansey Formation; Tkw = gray and brown clay, hard clay, silt, fine sand, medium sand, clayey sand, “marl”, minor white, yellow, and red coarse sand, of the Kirkwood Formation; Tsr = green clay and sand, glauconite clay and sand. A “+” sign indicates that units are mixed, interbedded, or cannot be separately identified from the information provided in the log for that depth interval. “TD” indicates total depth of deep wells for which units below the Kirkwood Formation are not listed. Typically, drilling methods and lithologic descriptions are not sufficiently detailed to identify formations below the Kirkwood from the lithologic descriptions alone. Refer to cross sections for deeper formations in these wells, as identified from geophysical well logs. Units shown for wells may not match the map and sections due to variability in drillers’ descriptions and the similar lithology of the surficial deposits, Cohansey Formation, and Kirkwood Formation.

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Table 2. Lithologic logs of test borings. Gamma-ray logs after table (p. 10).

N. J. permit number and

identifier

Lithologic log

Depth (feet

below land

surface)

Description (map unit assignment in parentheses) Color names from Munsell Color Company (1975)

E201704340 well 310

(Brick Fire Academy)

0-5 5-10 10-15 15-20 20-25 25-30 30-35 35-40 40-45 45-50 50-55 55-60 60-65 65-70 70-75 75-80 80-85 85-90 90-95 95-100

medium to very coarse quartz sand, trace fine sand and granules; grayish orange (10 YR 7/4) to dark yellowish orange (10 YR 6/6) (Qtu) fine to medium quartz sand, tr. coarse sand and granules, poorly sorted; dark yellowish orange (10 YR 6/6) (Qtu to 9 based on gamma log) medium to coarse quartz sand, occasional granules, trace fine sand, moderately sorted; grayish orange (10 YR 7/4) (Tch) medium to coarse quartz sand, trace very coarse sand, 1-2% opaque heavy minerals; moderate yellowish brown (10 YR 5/4) (Tch) fine to medium sand, some coarse, trace granules, 1% opaque heavy minerals; grayish orange (10 YR 7/4) (Tch) medium to very coarse coarse quartz sand, some quartz granules, rare mica, 1% heavy minerals, wet; moderate yellowish brown (10 YR 5/4) (Tch) fine sand, some very fine and medium, slightly silty, 2-3% heavy minerals; dark yellowish orange (10 YR 6/6) (Tkw, gamma log shows contact with Tch at 20) very fine to fine sand, well sorted, 3-4% opaque heavy minerals; dark yellowish orange (10 YR 6/6) to moderate yellowish brown (10 YR 5/4) (Tkw) silty fine sand, occasional granule, slightly micaceous, 3% opaque heavy minerals, well sorted; dark yellowish orange (10 YR 6/6) to moderate yellowish brown (10 YR 5/4) (Tkw) silty fine sand, occasional granule, slightly micaceous, 3% opaque heavy minerals, well sorted; dark yellowish orange (10 YR 6/6) to moderate yellowish brown (10 YR 5/4); on auger when pulled up: silty very fine to fine sand, slightly micaceous; pale yellowish brown (10 YR 6/2) (Tkw) silty fine sand, occasional granule, slightly micaceous, 3% opaque heavy minerals, well sorted; dark yellowish orange (10 YR 6/6) to moderate yellowish brown (10 YR 5/4) (Tkw) silty fine sand, occasional granule, slightly micaceous, 3% opaque heavy minerals, well sorted; dark yellowish orange (10 YR 6/6) to moderate yellowish brown (10 YR 5/4) (Tkw) clayey very fine to fine sand, micaceous, with finely disseminated organic material; dark yellowish brown (10 YR 7/2) (Tkw) silty very fine to fine sand, micaceous, 2-3% heavy minerals, moderately sorted; moderate yellowish brown (10 YR 5/4) (Tkw) silty fine sand, slightly micaceous (muscovite), 2-3% opaque heavy minerals; moderate yellowish brown (10 YR 5/4) (Tkw) silty very fine to fine sand, slightly micaceous (muscovite), 2-3% opaque heavy minerals; moderate yellowish brown (10 YR 5/4) (Tkw) on auger when pulled up: clayey very fine sand, micaceous, with finely disseminated organic material; dark yellowish brown (10 YR 7/2) (Tkw) clay-silt, micaceous, with finely disseminated organic material; dark yellowish brown (10 YR 7/2) (Tkw) fine sand, micaceous, 1-2% heavy minerals; well sorted; moderate yellowish brown (10 YR 5/4) (Tkw) fine sand, micaceous, 1-2% heavy minerals; well sorted; moderate yellowish brown (10 YR 5/4) (Tkw)

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E201704341 well 311 (Sawmill Bicycle Trail)

0-5 5-10 10-15 15-20 20-25 25-30 30-35 35-40 40-45 45-50 50-55 55-60 60-65 65-70 70-75 75-80 80-85 85-90

peaty very fine to fine quartz sand, some roots; dark yellowish brown (10 YR 2/2) (Qcm1) silty somewhat organic fine to medium quartz sand, tr. coarse sand, 2% very fine opaque heavy minerals?, pale yellowish brown (10 YR 6/2) to dark yellowish brown (10 YR 2/2) (Qcm1) silty very fine to fine sand, some ironstone laminae and thin beds; dark yellowish brown (10 YR 4/2) (Tch but Tkw-like composition to 45) silty very fine to fine sand, 1-2% opaque heavy minerals; pale yellowish brown (10 YR 6/2) (Tch) peaty clay-silt, trace granules, micaceous; dusky yellowish brown (10 YR 2/2) weathering to dark yellowish brown (10 YR 4/2) (Tch) silty very fine to fine quartz sand, some medium, trace mica, 1% heavy minerals; pale yellowish orange (10 YR 8/6) to dark yellowish orange (10 YR 6/6) (Tch) silty fine sand, some very fine and medium, slightly micaceous, 2% heavy minerals; grayish orange (10 YR 7/4) (Tch) silty fine sand, some very fine and medium, slightly micaceous, 2% heavy minerals; grayish orange (10 YR 7/4) (Tch) fine sand, some very fine, slightly micaceous, 2% heavy minerals; very pale orange (10YR 8/2) to grayish orange (10 YR 7/4) (Tch) fine sand, some very fine and medium, slightly micaceous, 1% opaque heavy minerals; pale yellowish brown (10 YR 6/2) (Tch) medium to very coarse quartz sand, poorly sorted; moderate yellowish brown (10 YR 5/4) (Tch) medium to very coarse quartz sand, poorly sorted, slightly micaceous, 2% opaque heavy minerals, grayish orange (10 YR 7/4) to moderate yellowish brown (10 YR 5/4) (Tch from 50-55 interval, gamma log indicates Tkw at 55) medium to very coarse quartz sand, poorly sorted, some granules; pale yellowish brown (10 YR 6/2) (Tch from 50-55 interval, gamma log indicates Tkw below 55) very fine to fine sand, some medium, trace granules, 2% heavy minerals, moderately sorted; grayish orange (10 YR 7/4) (Tkw) silty very fine to fine sand, trace mica; dark yellowish brown (10 YR 4/2) silty fine sand, some finely disseminated organic matter, trace mica; dark yellowish brown (10 YR 4/2) (Tkw) silty very fine sand, some finely disseminated organic matter, trace mica; dusky yellowish brown (10 YR 2/2) (Tkw) clay-silt, micaceous, with finely disseminated organic material; dusky yellowish brown (10 YR 2/2) (Tkw)

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