174Ax Leg Summary: Sequences, Sea Level, Tectonics, and Aquifer Resources: Coastal Plain Drilling1

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Miller, K.G., Sugarman, P.J., Browning, J.V., et al. Proceedings of the Ocean Drilling Program, Initial Reports Volume 174AX (Suppl.)

174AX LEG SUMMARY: SEQUENCES, SEA LEVEL, TECTONICS, AND AQUIFER RESOURCES: COASTAL PLAIN DRILLING1

Kenneth G. Miller, James V. Browning, Peter J. Sugarman, Peter P. McLaughlin, Michelle A. Kominz, Richard K. Olsson, James D. Wright, Benjamin S. Cramer, Stephen J. Pekar, William Van Sickel2

SUMMARY

This chapter provides the background, objectives, and major scientific accomplishments of Ocean Drilling Program (ODP) Leg 174AX/ 174AXS, during which four boreholes were drilled onshore in the New Jersey (NJ) and Delaware (DE) Coastal Plains. These boreholes not only targeted the onshore equivalents of Miocene sequences drilled offshore during Leg 174AX with holes at Ocean View, NJ, and Bethany Beach, DE, but also provided an unprecedented sampling of marine Upper Cre- taceous–Paleogene onshore sequences with holes at Bass River and Ancora, NJ. Major scientific accomplishments of Leg 174AX include evaluating controls on sea level and sequences and global events in Earth history.

Sea Level

We established that eustasy is the dominant process that determines the template for potential sequences and their general architecture (stacking patterns and preservation of stratal surfaces) on the U.S. Mid- Atlantic margin. Leg 150X and 174AX onshore cores yielded a high- 1Examples of how to reference the resolution (1-m.y. resolution) chronology of ~30 Cenozoic and 11–14 whole or part of this volume. Late Cretaceous sequences by integrating Sr isotopic stratigraphy and 2 Shipboard Scientific Party biostratigraphy. Sequence boundaries (from 42 to 8 Ma) correlate with addresses. global 18O increases, linking them with glacioeustatic lowerings. One- Ms 174AXS-104 K.G. MILLER ET AL. LEG 174AX SUMMARY 2 and two-dimensional backstripping of mid-Cretaceous to Miocene sequences yields eustatic estimates for the interval from 100 to 8 Ma that are less than one-half of those published by Exxon Production Research (EPR). Oligocene sequences in NJ preserve a remarkably complete record of sea-level change derived from two-dimensional backstripping. Backstripping establishes that sea-level changes were large (>25 m) and rapid (<1 m.y.) even during the greenhouse world of the Late Creta- ceous to middle Eocene. The rapidity and amplitude of these changes requires a glacioeustatic control of sea-level variations during the Late Cretaceous, or our understanding of sea-level mechanisms is fundamentally flawed. Comparisons between Late Cretaceous sequence stratigraphy and 18O records are consistent with the presence of small ice sheets in this alleged greenhouse world. Comparisons between boreholes in NJ and DE allow evaluation of the effects of tectonics and sediment supply on sequence architecture. We discovered higher-order variability within lower Miocene sequences in NJ and DE embedded within the million-year-scale sequences previously defined onshore; these may be due to lobe switching or unusual preservation of high-frequency sea-level changes in areas with high sedimentation rates. Minor (~10-m scale) tectonic differences determine the preservation of sequences in different parts of the basin. Sediment supply determines paloeoenvironmental setting, regional and local facies, and the expression of stratal surfaces. Our studies show that Mio- cene facies in NJ are deltaic dominated, whereas those in DE are wave- dominated shorelines. Despite this difference, these areas share a similar Miocene sequence stratigraphic signature. Thin transgressive systems tracts (TSTs) are present at the base of most sequences. Highstand systems tracts (HSTs) can generally be divided into a lower fine-grained unit (silty clay in NJ and silts in DE) and an upper sandy unit. The general absence of lowstand systems tracts (LSTs) is due to bypassing. Un- derstanding of sequence stratigraphic architecture allowed development of an improved hydrostratigraphic framework to be used in evaluating local and regional water resource potential.

Earth History

The record obtained at these sites allowed us to evaluate the causes and effects of several major global events in Earth history, including:

1. Demonstrating that the latest Cenomanian–Turonian (C/T) ocean anoxic event was unrelated to sea-level change on million-year or 100-k.y. scales. 2. Suggesting that a major cooling spanning the Campanian/Maas- trichtian boundary was associated with a sea-level lowering and inferred ice volume increase. 3. Correlating a latest Maastrichtian global warming with Deccan trap volcanism. 4. Linking the marine mass extinctions at the end of the Creta- ceous with ballistic ejecta. In addition, we showed that collapse of the vertical isotopic gradient (“Strangelove Oceans”) extended to neritic environments and that there was minimal change in sea level associated with the Cretaceous/Tertiary (K/T) boundary. 5. Establishing that low 13C and 18O and high kaolinite values were associated with the Paleocene/Eocene thermal maximum (PETM) in NJ neritic sections and that isotopic values remained low and kaolinite remained high throughout a thick section K.G. MILLER ET AL. LEG 174AX SUMMARY 3

above the carbon isotope excursion (CIE). This reflects either that warmer and wetter climate persisted for >300–400 k.y. in NJ (unlike deep-sea records that show an exponential return to pre- PETM conditions after ~200 k.y.) or that the extremely rapid deposition of this section occurred in response to a cometary impact. 6. Showing that a large (~60 m), earliest Oligocene drop in sea level was associated with development of an ice sheet equivalent in size to the modern East Antarctic ice sheet, though sea level again rose by nearly 50 m ~1 m.y. later, suggesting near collapse of the ice sheet. The ice sheet subsequently grew and decayed numerous times in the Oligocene–middle Miocene.

Future studies will integrate onshore and offshore drilling with seismic profiles and provide a full sampling of sequences across the margin.

BACKGROUND

Passive continental margins such as those along the East and Gulf coasts of the U.S. contain thick sediment archives that record global sea level, depositional environments, regional/local tectonics, and global/ regional climate changes in unconformity-bounded packages termed sequences (Mitchum et al., 1977; Christie-Blick and Driscoll, 1995). De- ciphering these archives in a systematic manner has proven to be a challenge. Outcrops provided most of the information for early models of continental margin sedimentation, but these are often thin, weath- ered, poorly fossiliferous, and discontinuous on passive margins. Thicker sections are available in the subsurface downdip toward the submerged continental shelf, but subsurface sections have been mostly discontinuously sampled by oil or water wells. Continuous coring provides a direct means to sample the subsurface, although it is costly and complicated by unconsolidated nature of coastal plain strata. Advances in coring technology in the 1980’s, particularly with extended bits (e.g., the Christensen bit and ODP’s extended core barrel), has dramatically improved recovery rates and allowed recovery of undisturbed layers of strata to improve our information archives for passive margins. In order to understand continental margin processes, passive continental margin studies require sampling from outcrops onshore to regions far offshore. Sampling onshore to offshore in transects (i.e., along dip profiles) or in arrays (i.e., transects with along-strike components) has proven programmatically challenging because it requires the inter- action of organizations with distinctly different mandates (e.g., ODP and the International Continental Drilling Program [ICDP]). The Earth Science and Ocean Science Divisions of the National Science Founda- tion (NSF) recognized and met this challenge when they funded onshore drilling in the NJ Coastal Plain, which has been directly integrated with offshore efforts by ODP Legs 150 and 174A. F1. Location map for the NJ/MAT Coastal plain drilling by ODP began in 1993 with Leg 150X as part of Sea-Level Transect, p. 23. the NJ/Mid-Atlantic Sea-Level Transect (Fig. F1) (Miller and Mountain,

77°W 76° 75° 74° 73° 72° 41° N NJ/MAT Sea-Level Transect 1994). The primary goal of the transect was to document the response Seismic Profiles Ch0698 Ew9009 Oc270 Existing Drillsites I DSDP op + Exploration cr an pre-Cretaceousut ce o p of passive continental margin sedimentation to glacioeustatic changes AMCOR s ro 903 u tc eo u ntic O ODP Leg 150, 150X c o tla 1072 ta ic A ODP Leg 174A, 174AX re o 40° C oz en Future C New Jersey Island Beach ‘93 MAT1 during the Oligocene to Holocene “icehouse world,” a time when gla- Ancora ‘98 MAT2 Bass River ‘96 MAT3 1071 + 1072 1073 Atlantic City ‘93 ++ +++ + + ++ cioeustasy was clearly operating (Miller and Mountain, 1994). During + + + + + Ocean View ‘99 + + + 39° + Cape May ‘94 + 906 902 I 904 Leg 150 four sites were drilled on the NJ continental slope, providing a 903 Delmarva Peninsula 905 Bethany Beach, DE (‘00)

m 0 0 2 sequence chronology for the Oligocene–Miocene of the region (Moun- 1000 m m m

0 0 000 0 2 3 38° K.G. MILLER ET AL. LEG 174AX SUMMARY 4 tain, Miller, Blum, et al., 1994). Concurrent with and subsequent to Leg 150, a complementary drilling program designated Leg 150X was un- dertaken to core coeval strata onshore in NJ. This drilling was designed not only to provide additional constraints on Oligocene–Holocene sequences but also to address an important goal not resolvable by shelf and slope drilling: to document the ages and nature of middle Eocene and older “greenhouse” sequences, a time when mechanisms for sea- level change are poorly understood (Miller et al., 1991). Sites were drilled at Island Beach (March–April, 1993), Atlantic City (June–August, 1993), and Cape May (March–April, 1994) (Miller et al., 1994, 1996a; Miller and Snyder, 1997) (Fig. F1). Together, Legs 150 and 150X were extremely successful in dating Eocene–Miocene sequences, correlating them to the 18O proxy for glacioeustasy, and causally relating sequence boundaries to glacioeustatic fall (Miller et al., 1996b, 1998a; Browning et al., 1996). Little information was garnered on Paleocene and older sequences during these legs, with only one lower Eocene–Maastrichtian section sampled at Island Beach. ODP Leg 174A continued the Mid-Atlantic Transect by drilling between previous slope and onshore sites, targeting the NJ continental shelf (Austin, Christie-Blick, Malone, et al., 1998). The Joint Oceano- graphic Institutions for Deep Earth Sampling (JOIDES) planning committee endorsed a subsequent phase of onshore drilling as an ODP- related activity and designated the program ODP Leg 174AX. As part of this leg, sites were drilled at

1. Bass River, NJ (October–November, 1996; Miller et al., 1998b), targeting Upper Cretaceous to Paleocene strata (total depth [TD] = 1956.5 ft; recovery = 86%); 2. Ancora, NJ (July–August, 1998; Chap. 1, this volume), an updip, less deeply buried Cretaceous–Paleocene section complimentary to Bass River (TD = 1170 ft TD; recovery = 93%); 3. Ocean View, NJ (September–October, 1999; Chap. 2, this volume), targeting upper Miocene–middle Eocene sequences (TD = 1570 ft TD; recovery = 81%); and 4. Bethany Beach, DE (May–June 2000; Chap. 3, this volume) targeting Miocene sequences near where they reach their greatest thickness onshore (1470 ft TD; 80% recovery).

The U.S. Geological Survey (USGS) Eastern Earth Surface Processes Team drilled the Ancora, Ocean View, and Bethany Beach boreholes, whereas a commercial driller, Boart Longyear, drilled Bass River. Full suites of downhole geophysical logs were obtained at Ocean View and Bethany Beach by the DE Geological Survey (DGS) and gamma logs to TD were obtained at Bass River and Ancora by the NJ Geological Survey (NJGS). The excellent recovery overall (5409 ft recovered from 6172 ft drilled; recovery = 88%) is testimony to the skill of the drillers in coring the difficult to recover coastal plain strata. Onshore drilling during Leg 174AX has provided new insights into greenhouse sequences and added a third-dimensional, along-strike view of Oligocene–Miocene sequences, allowing the evaluation of the effects of tectonics and sediment supply on sequence stratigraphic architecture. This paper summarizes the objectives and accomplishments of onshore drilling during Leg 174AX and provides a brief prospectus for the future of drilling integrated arrays of boreholes on passive continental margins. K.G. MILLER ET AL. LEG 174AX SUMMARY 5

This chapter differs from a typical Initial Reports summary chapter in that it is not only a companion to the four site chapters reproduced on CD-ROM, it also summarizes publications and papers. The Bass River Site Report was published in paper form in 1998 and bound with the Leg 174A Initial Reports as Leg 174AX (Miller et al., 1998b). The Ancora (Chap. 1, this volume), Ocean View (Chap. 2, this volume) and Beth- any Beach (Chap. 3, this volume) Site Reports are published on the World Wide Web and in this volume on CD-ROM as Leg 174AXS. Be- cause drilling of Leg 174AX spanned 5 yr (1996–2000, inclusive), we summarize the scientific results of a significant body of published, in press, and submitted works. Ongoing studies will be published in 2004 in a Scientific Results volume.

OBJECTIVES

Coastal plain drilling conducted as part of Leg 174AX had several major objectives:

1. Evaluate the variability of Oligocene–Miocene sequences and the influences of tectonics and sediment supply on sequence distribution and architecture. This is a direct outgrowth of studies conducted during ODP Leg 150 slope and 150X coastal plain drilling, which dated Oligocene–Miocene sequences and correlated them with global 18O records. 2. Provide material suitable for one- and two-dimensional backstripping of mid-Cretaceous to Miocene sections, providing a eustatic estimate for the interval from 100 to 8 Ma that can be compared with backstripped records from other areas. Backstrip- ping is a proven method for extracting amplitudes of global sea level from passive margin records (e.g., Watts and Steckler, 1979). One-dimensional backstripping progressively removes the effects of sediment loading (including the effects of compaction), eustasy, and paleowater depth from basin subsidence to obtain tectonic subsidence. By modeling thermal subsidence on a passive margin, the tectonic portion of subsidence can be as- sessed and a eustatic estimate obtained (Kominz et al., 1998). Two-dimensional backstripping assumes projection of onshore Oligocene sections onto a single composite dip section of prograding clinoforms, integrating various data sets into a single, internally consistent interpretation of sea-level change (Kominz and Pekar, 2001). 3. Determine the ages and distribution of Cretaceous sequences not previously sampled during Legs 150X, 150, or 174A and provide additional samples of Paleocene–middle Eocene sequences that were only sparsely sampled previously. These sequences provide a window into understanding sea-level changes during the greenhouse world, a time considered to be ice free. 4. Evaluate major global events in Earth history in continental margin successions. Earth history has been punctuated by rapid events that have profoundly affected life. These events include the Cretaceous/Tertiary (C/T) extinction and ocean anoxic event (Arthur et al., 1985), the Campanian/Maastrichtian cooling (Bar- rera and Savin, 1999), the latest Maastrichtian warming (Barrera and Savin, 1999), the Cretaceous/Tertiary (K/T) impact event (Alvarez et al., 1980), the PETM and carbon isotopic excursion K.G. MILLER ET AL. LEG 174AX SUMMARY 6

(e.g., Kennett and Stott, 1990; Zachos et al., 1994), and the earliest Oligocene cooling and glaciation (Miller et al., 1987; Zachos et al., 2001). Whereas most reconstructions of global Late Creta- ceous–Holocene events have focused on the deep-sea record because of its more continuous nature, passive continental margins potentially provide thick, continuous records of many of these events. 5. Evaluate stratigraphic continuity and hydrogeological potential of aquifers and confining units. The NJGS and DGS provided funds for drilling to address hydrogeological objectives that directly affect groundwater resources in the rapidly growing areas of southern NJ and DE. Sequence stratigraphy has the potential to increase our understanding of the stratigraphic architecture of aquifers in the same way it has improved our understanding of reservoir architecture in the oil industry.

ACCOMPLISHMENTS

Evaluated Sequence Variability

We confirmed the conclusions of Legs 150 and 150X (see summary in Miller et al., 1997) that eustasy is the dominant process that determines the template of potential sequences and their general architecture (stacking patterns and preservation of stratal surfaces). We attribute some of the differential preservation of sequences in boreholes from DE through NJ to minor (~10-m scale) tectonic differences caused by minor movement on basement blocks (e.g., the rolling basins concept of Owens et al., 1997). Sediment supply can also locally affect the preservation of sequences, with preferential preservation of sequences near depocenters resulting from excess accommodation by loading and preferential removal in regions of sediment starvation. Sediment supply also determines the paloeoenvironmental setting (e.g., wave vs. deltaic dominated) (Fig. F2), the facies expressed regionally and locally, and F2. Facies models, p. 24. the local expression of stratal surfaces. A Modern Niger Delta

Miocene sequence Sequence Correlation with Global Records Quartz sand delta front- nearshore (regressive) We identified, dated, and correlated sequences among sites in NJ and Clay-silt prodelta-inner Ocean View Ð 637 ft neritic 18 marsh DE with other global records (Fig. F3) (e.g., O), confirming the link (regressive)

Maximum Flooding Surface 18 Ocean View Ð 721 ft Quartz sand delta front sand between sequence boundaries and O determined by Miller et al. g g middle-outer neritic

Ocean View Ð 5873 ft Ocean View Ð 580 ft inner/middle neritic (1996b) based on Leg 150 and 150X studies. Sequence boundaries are Miocene deltaic-influenced facies successions, NJ prodelta clay unconformities that are recognized on the basis of physical stratigraphy, including irregular contacts, reworking, bioturbation, major facies F3. Comparison of Bethany changes, gamma ray peaks, and paraconformities inferred from age Beach borehole with NJ sequence breaks. Sr isotopic stratigraphy provided the primary age control on Oli- ages, p. 27. gocene–Miocene sections supplemented by calcareous nannofossil, Sr age regression of Timescale Atlantic δ18O stack Oslick et al. (1994)

m rity Bethany n NJ

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a (‰ VPDB) p g Composite Beach Delaware

P E A F planktonic foraminiferal, and dinocyst biostratigraphy. During Leg Chron N 2 1

C4 NN10

te N16 10 la 10 174AX, thick Miocene sequences at Ocean View and Bethany Beach NN9 Mi6 C5 NN8 Cibicidoides N15 spp. Mi5 NN7 N14 Kw-C 12 12 C5A N12 Mi4 were sampled, identified, and dated. It extended our record of se- NN6 C5AA Mi3a,b C5AB N10 Kw3 14 C5AC 14

le C5AD d NN5 id Kw2c quences dated onshore from ~10 Ma (Leg 150X) to 8 Ma, complement- m N9 Mi2a ) C5B ? a N8 Mi2 Kw2b 16 e 16

c g C5C NN4

io A N7 ing Leg 174A drilling. M Kw2a C5D Mi1b 18 N6 18 C5E NN3 Mi1ab Kw1c ? C6 Kw1b Cut out 20 N5 20 Mi1aa NN2 ? ly ?

r Kw1a

C6A a e Mi1a 22 C6AA 22 N4 C6B Kw0 Cut out NN1 Mi1 C6C

l. 24 te P22 NP25 24

la K.G. MILLER ET AL. LEG 174AX SUMMARY 7

Facies Models

We developed facies models for deltaic-dominated (NJ) (Fig. F2A) and wave-dominated (DE) (Fig. F2B) successions. The deltaically influenced Miocene sections in NJ fit a facies model similar to the Niger Delta (Fig. F2A) (Allen, 1970). Facies include marsh deposits, nearshore to delta front sands, prodelta silty clays, and shelfal sands (glauconitic in Paleogene and older sections and primarily quartz in the Miocene) (Fig. F2A) (Allen, 1970). The facies are arranged as basal transgressive sands, medial prodelta silty clays, and upper quartz sands. The DE Mio- cene and younger sequences sampled at Bethany Beach consist of silts and sands deposited in fluvial to upper estuarine, lower estuarine, upper shoreface/foreshore, distal upper shoreface, lower shoreface, and inner and middle neritic environments (Fig. F2B).

Intrasequence Architecture

We evaluated intrasequence architecture. Despite fundamentally different sedimentary regimes (wave-dominated shorelines in DE vs. deltaic systems in NJ), both regions share a similar sequence stratigraphic signature for the Miocene. LSTs are largely absent, and thus transgressive surfaces are usually merged with sequence boundaries; the exceptions include lowstand deposits identified for the first time in the Mio- cene Kirkwood Formation at Ocean View in the Kw2a and Kw1a sequences. TSTs are present at the bases of some sequences but are thin. In general, HSTs are divided into a lower fine-grained unit (silty clay in NJ and generally silts in DE) and an upper sandy unit. The upper HST sands comprise important aquifers in both regions that are generally confined by the overlying lower HST. Aside from these similarities, there are important sequence stratigraphic differences between regions. Maximum flooding surfaces (MFSs) identified in the Bethany Beach borehole show much greater evidence of erosion than MFSs in NJ, whereas sequence boundaries are often more subtle in DE because of the juxtaposition of similar facies.

Higher-Order Variability

We discovered higher-order (400?-k.y. scale) variability within lower Miocene sequences at Ocean View and Bethany Beach embedded within the million-year-scale sequences defined onshore during Leg 150X drilling. The Kw2a and Kw1a sequences are each provisionally subdivided into three higher-order sequences (Kw2a1, Kw2a2, and Kw2a3 and Kw1a1, Kw1a2, and Kw1a3, respectively). The preservation of higher-order lower–middle Miocene sequences may be the result of higher sediment supply and accommodation space because they are only recognizable in sections with high (~100 m/m.y.) sedimentation rates. Alternatively, the great thickness of the section is consistent with an autocyclical cause (lobe switching) for these apparent sequences. Analyses of nearshore seismic profiles recently collected near Ocean View (Fig. F1) should reveal if the higher-order cyclicity is due to base level lowering and, hence, if these are eustatically controlled sequences.

Comparison of NJ and DE Sequences

Comparison of NJ and DE (Bethany Beach) Miocene sequences high- lights regional differences in sedimentation and possible tectonic con- K.G. MILLER ET AL. LEG 174AX SUMMARY 8 trols. Equivalents of the Kw3, Kw2c, Kw2b, Kw1c, and Kw1a NJ sequences are represented at Bethany Beach (Fig. F3), although the sequences are generally thicker and sedimentation rates are higher in DE. Nevertheless, thickness does not equate to stratigraphic continuity: the NJ record is much more complete in the early part of the early Mio- cene (19–23.8 Ma), with the Kw1b and Kw0 sequence apparently miss- ing in DE. The DE section is more complete in the late part of the early Miocene (~19–16.2 Ma), with one sequence (18.0–18.4 Ma) not represented in NJ. The upper part of the Oligocene (~27–23.8 Ma; sequences O6 and O5 of Pekar et al., 2000) is also absent at Bethany Beach because of truncation. These minor differences in preservation may be due to (1) minor tectonic movements (tens of meters) of basement blocks (Owens et al., 1997) or (2) differential preservation resulting from local sediment loading.

Oligocene Strata Geometry Reconstruction

The geometry of Oligocene strata in NJ was reconstructed using two- dimensional flexural backstripping (Pekar et al., 2000; Kominz and Pekar, 2001), and water depths were estimated for the margin using two-dimensional paleoslope modeling of the benthic foraminiferal biofacies (Pekar and Kominz, 2001; Pekar et al., in press b). These results allowed quantitative evaluation of factors controlling sedimentation on passive margins and comparison with other stratigraphic models (Fig. F2C) (Pekar et al., in press b). NJ Oligocene sequences are highstand dominated, TSTs are thin, and LSTs are absent. Pekar et al. (in press b) suggested that the absence of LSTs was due to bypassing because of effi- cient transfer of sediment across the shallow shelf, combined with the absence of major river systems in the area of study. They concluded that well-developed offlap at each sequence boundary is due primarily to marine bypassing and degradation, rather than to “forced regression” (Pekar et al., in press b).

Stratigraphic Response to Eustatic Change

Stratigraphic architecture observed at the NJ continental margin was also compared with Oligocene eustatic records to evaluate the stratigraphic response to eustatic change (Pekar et al., 2001). Early to “mid”- Oligocene sequence boundaries (33.8–28.0 Ma) were associated with relatively long hiatuses (0.3–0.6 m.y.), in which sedimentation in many places terminated during eustatic falls and resumed early during eustatic rises. Late Oligocene sequence boundaries were associated with relatively short hiatuses (<0.3 m.y.); they provide the best constraints on phase relations between sea-level forcing and margin response. The interval represented by each late Oligocene sequence varies in dip pro- file. At updip locations landward of the clinoform rollover in the underlying sequence boundary, sedimentation commenced after the eustatic low and terminated before the eustatic high (with partial erosion of any younger record) (Fig. F2C). At downdip locations, sedimentation within each sequence was progressively delayed in a seaward direction, beginning during the eustatic rise and terminating near the eustatic low (Fig. F2C). Combining data from all available boreholes, Pekar et al. (2001) showed that the ages of sequence boundaries (correlative surfaces) cor- respond closely to the timing of eustatic lows, and ages of condensed sections (intervals of sediment starvation) to eustatic highs (Fig. F2C). K.G. MILLER ET AL. LEG 174AX SUMMARY 9

Core–Log Integration

Core log-downhole log integration provided a means of further evaluating sequences and variability within sequences. Lanci et al. (2002) integrated core-log magnetic susceptibility (MS) and natural gamma ray (NGR) measurements from Ancora with lithology and the downhole NGR log. They used a simple linear model to explain MS and NGR values by lithologic variation. Spectral NGR shows that high gamma values are due to the 40K radioisotope associated with glauconite and clay, sediment components that also tend to give high MS values. The major deviation from their model was at an anomalous level with high NGR but low MS values; this level was attributed to high uranium concentration in phosphorite. With only few exceptions, sequence boundaries identified at Ancora are expressed in the NGR and/or MS logs.

Backstripping and Eustatic Estimates

Leg 174AX provided material suitable for one- and two-dimensional backstripping of mid-Cretaceous to Miocene sections, providing a eustatic estimate for the interval from 100 to 8 Ma. Backstripping analysis of the Bass River and Ancora boreholes (Fig. F4) (Van Sickel et al., un- F4. Backstripped R2 eustatic esti- publ. data) provides complete Late Cretaceous sea-level estimates and mates, p. 28.

200 tests previously published Cenozoic sea-level estimates based on Leg Atlantic City Ancora Cape May 150 Bass River Island Beach 150X drilling (Fig. F4) (Kominz et al., 1998). Van Sickel et al. (unpubl. 100 50 Sea level (m) Sea level data) used electric logs to provide a new porosity-depth calibration for 0 -50 late earlylate early middle late early lateearly middle late Holo. Cretaceous Paleocene Eocene Oligocene Miocene Plio. decompacting sediments, showing considerably lower porosity than 100 90 80 70 60 50 40 3020 10 0 Time (Ma) those previously calculated at the offshore Cost B-2 well. Amplitudes and duration of sea-level changes were comparable when sequences were represented at multiple borehole sites, suggesting that the result- ant curves are an approximation of regional sea level (Fig. F4). Sea-level amplitudes as great as 50 m are associated with Cretaceous sequences, whereas most Late Cenozoic amplitudes were closer to 20 to 40 m (Fig. F4) (Van Sickel et al., unpubl. data). Two-dimensional backstripping of prograding Oligocene sequences reconstructed by Pekar et al. (2000) provided a detailed and precise eustatic estimate (Kominz and Pekar, 2001). Ten latest Eocene to earliest Miocene sequences provided the basis for estimates of ~20- to 60-m eustatic lowerings (Kominz and Pekar, 2001). The slightly higher eustatic estimates obtained by Kominz and Pekar (2001) vs. Van Sickel et al. (unpubl. data), particularly for earliest Oligocene rises and fall (see below) are attributed to the greater precision provided by two-dimensional backstripping that more nearly captured the full amplitude of eustatic change (Pekar and Kominz, 2001). Both one- and two-dimensional backstripping yielded Oligocene eustatic estimates that are lower than those published by the EPR group (e.g., Haq et al., 1987) by a factor of two or more (Kominz and Pekar, 2001; Van Sickel et al., unpubl. data). Oligocene eustatic lowerings were linked to global 18O increases (Pekar et al., 2001) and used to provide a sea level/18O calibration for the Oligocene (Pekar et al., in press a).

Greenhouse Sequences

The Bass River and Ancora Cretaceous sections provided the means to estimate global sea-level (eustatic) variations of the Late Cretaceous (99–65 Ma) greenhouse world (Miller et al., unpubl. data). These two sites recorded 11–14 Upper Cretaceous sequences that were dated by in- K.G. MILLER ET AL. LEG 174AX SUMMARY 10 tegrating Sr isotopic stratigraphy and biostratigraphy (Fig. F5). The ages F5. Age-depth plots for Bass River of sequence boundaries not only correlate regionally between sites (Fig. and Ancora, p. 29.

F5), they also correlate with the sea-level lowerings of EPR (Haq et al., Bass River, NJ base top P1a CC26 top CC26 Navesink II base A. mayo. zone eq. Navesink I 1300 400 top base CC23a CC25b Marshalltown 1987), northwest European (Hancock, 1993) and Russian sections (Fig. 1400 base CC21a top R. calcarata Englishtown 450 within CC19/20 F6) (Sahagian et al., 1996), indicating a global cause. Backstripping 1500 1600 Merchantville III base CC19 500 base CC18 Merchantville I & II base CC17 base Camp. foram. base CC16 Cheesequake base CC15 Bass River 1700 base CC14 yielded a Late Cretaceous eustatic estimate for these sequences, taking Magothy III pollen Zone IV Magothy I 550 1800

diagenetically BR III altered Sr 1900 Depth (ft) into account sediment loading, compaction, paleowater depth, and ba- Depth (m) base CC10

Navesink II Ancora, NJ Navesink I base CC26 200 base CC25a top CC22a Marshalltown base CC22a 700 sin subsidence (Fig. F6). Sea-level changes were large (>25 m) and rapid base CC21 Englishtown base CC20 800 250 Merchantville III

base Camp. foram. base CC19 HO M. furcatus 900 (<1 m.y.), strongly suggesting glacioeustatic control of sea-level varia- Merchantville II base CC18 Merchantville I LO B. parca Cheesequake base CC17, LO C. obscurus Magothy III pollen Zone V; 300 assumes same age as MIII at Bass River 1000 Magothy II pollen Zone V tions during the Late Cretaceous. Though the timing of EPR eustatic BR III top CC10 BR II 1100 BR I base CC10 350 lo. Ceno. pollen Zone III at base;

Nanno. Zone CC16 CC25a CC26 15 17 a b c CC10 CC24 CC12 CC14 CC19 CC18 CC9 CC13 CC21 CC11 CC23 CC20 CC22 lowerings may be more or less correct, the EPR curve cannot be used as Age/stage Cenomanian Turonian Con. Sant. Campanian Maastrichtian Danian Age, Ma 100 95 90 85 80 75 70 65 60

? ? ? ? Ancora ?? Sequence Age Bass ? a valid Late Cretaceous eustatic record. Eustatic estimates from NJ and River ? ? ? ? the Russian platform clearly show that the amplitudes of the major EPR eustatic lowerings were too high by a factor of at least two (Fig. F6). In F6. Estimate of eustatic changes, addition, the EPR record differs in shape from the backstripped eustatic p. 30. estimates. For example, the extremely large mid-Turonian and mid- EPR Sea level δ18 O NJ Composite European Estimate (m) R2 Sea level NJ Sea level Timescale (‰) Sequences Sea level Est. calibrated to Gradstein et al. (1995) Estimate (m) Estimate (m) 250 200 50 0 50 0 50 0 Paleocene benthic NW Europe lowerings not studied here Hancock (1996) 1 0 -1

Stage Relative units Nanno. Maastrichtian events reported by EPR are much lower in amplitude in Zone Tertiary 10 6 Navesink II 65 CC26 TA1.1 CC25c ? CC25b planktonic Navesink I -1 -2 CC25a UZA4.5 70 CC24 Maastrictian

CC23 Site 463 CC22 4.4 the backstripped records, whereas the major flooding events at 69, 76, Marshalltown CC22 Site 690 a 75 CC21 Site ? ? 1049 Englishtown CC20 4.3 Site 1050 ? 4.2 CC19 4.1 80 Campanian Merchantville III

CC18

Age (Ma) 3.5 and 84 Ma in the NJ record are less important in the EPR record (Fig. ? Merchantville II ? Merchantville I 3.4 CC16 ? Cheesequake

85 San. Site 511 3.3 CC14 ? 3.2 CC13 Magothy III Con. ? Magothy II? 3.1 CC12 90 ? Magothy I 2.7 F6). CC11 ? 2.6

Turonian BRIII Site 1050 2.5 CC10 BRII 95 BRI 2.4 CC9 Potomac Cenomian No data 2.3 100 E. K. Oxygen isotopic comparisons with Late Cretaceous sequence bound- 4 8 12 100 50 Bottom water Russian platform temperature Sahagian et al. (1996) aries have not attained the resolution needed to unequivocally link the (°C) two as has been done for the past 42 m.y. (Miller et al., 1998a). Never- theless, comparisons between Late Cretaceous sequence stratigraphy and 18O records are intriguing (Fig. F6) (Miller et al., unpubl. data), further suggesting small ice sheets in this alleged greenhouse world: (1) a major mid-Cenomanian sequence boundary (see also Gale et al., 2002) between the Potomac and Bass River I sequences (hiatus = ~96–97 Ma) correlates with a major (>1‰) 18O increase; (2) two minor 18O increases spanning the Cenomanian/Turonian boundary may correlate with sequence boundaries at the base of Bass River II and Bass River III; and (3) a mid-Turonian sea-level lowering associated with the Bass River III/Magothy contact (91.5–92 Ma) may correlate with a major increase in benthic foraminiferal18O values (~1.0‰), though additional data are needed to determine the precise timing of the increase (Fig. F6). Sev- eral other Coniacian–Campanian18O increases (dashed arrows in Fig. F6) may be related to sequence boundaries, but the data are too sparse to provide a firm correlation. Miller et al. (unpubl. data) note that 18O data are consistent with a glacioeustatic cause for Late Cretaceous sequence boundaries. The data shown on Fig. F6 require that either large, rapid sea-level variations occurred during the Late Cretaceous greenhouse world or our understanding of causal mechanisms for global sea- level change is fundamentally flawed.

Global Events in Earth History Cenomanian/Turonian Boundary Events

Uppermost Cenomanian to lower Turonian strata are characterized by worldwide organic carbon–rich deposits (Ocean Anoxic Event 2 [OAE2]) (Arthur et al., 1985, 1987) reflected in a pronounced positive excursion of 13C (e.g., Schlanger et al., 1987; Jenkyns et al., 1994). The Bass River borehole recovered a thick (61 m) record of the latest Cen- omanian to early Turonian that is continuous as measured by biostratigraphy (Sugarman et al., 1999) and cyclostratigraphy (Cramer in Wright et al., unpubl. data). Benthic foraminiferal 13C records show a K.G. MILLER ET AL. LEG 174AX SUMMARY 11 large (>2‰) increase immediately below the C/T boundary (Fig. F7) F7. Cenomanian–Turonian sec- (Sugarman et al., 1999). Above the sharp13C increase, elevated 13C tion at Bass River, NJ, p. 31.

and sedimentary organic carbon (>0.9%) values continue into the lower Cumulative Sequence/Environment δ13C δ18C (%) (‰) (‰) % TOC -4 -2 0 2 4 -2 -3 -4 -5 1800 13 550 0 1 2 >91.8 Ma

lta

Turonian, culminating in a sharp C decrease (Fig. F7) (Sugarman et d FS

p Gavelinella (calcite) Epistomina

13 560 ritic e (aragonite)

r n

? al., 1999). High C values in the uppermost Cenomanian–lower Turo- e s n e

in id 1850

s o FS d

. n

n Clay

) 570 e FS? nian at Bass River correlate with the OAE2, a global carbon burial event u

ft) q Glauconite

(

r S Fine quartz sand

n Gavelinella e

iv Foraminifers/

z (calcite) shell

lle

o Mica

a Epistomina

il Z recorded in Europe and the U.S. western interior (Sugarman et al., B 1900 s (aragonite) FS

580 s

lli

itic

iu r

im n

x w

o 1999); we estimate that the duration of this event at Bass River is 850 le FS

lo d . e ra B

id E o

590 m lip 93.5 Ma

ta s o

tiu R s x n ia

e 1950 . c a MFS

p k.y. based on cyclostratigraphy (Cramer in Wright et al., unpubl. data). M

n neritic 0 50 100 e mean Deeper Shallower C 0.87% TD = 596.34 m Water depth The OAE2 event occurred during long-term eustatic rise (10-m.y. Sequence boundary below total depth scale), yet it occurs within a 1- to 2-m.y.-long sequence at Bass River and is not associated with maximum flooding. Thus, there is no relationship between OAE2 and sea-level lowering on the million-year scale (Fig. F7) (Sugarman et al., 1999). Within the sequence spanning the carbon event, there are at least four shallowing-upward parasequences (du- rations = ~350–460 k.y.) indicated by changes in abundance and type of Epistomina species, 18O variations, and minor lithologic variations (Fig. F7). There is no clear association between parasequence boundaries (Fig. F7) and OAE2, indicating that there is no relationship of the event and sea-level change on the 100-k.y. scale (Fig. F7) (Sugarman et al., 1999). Thus, Sugarman et al. (1999) concluded that whereas the organic carbon burial event was associated with a general long-term (10-m.y. scale) eustatic rise, the initiation and termination of the peak organic burial event itself were unrelated to sea-level change (Fig. F7).

Campanian/Maastrichtian Boundary Events

A ~71-Ma sequence boundary separating the base of the Maastrich- tian Navesink Formation from the underlying Campanian Mount Lau- rel Formation (Fig. F5) is one of the most dramatic of the ~30 Cenozoic and 11–14 Late Cretaceous sequence boundaries identified in the NJ Coastal Plain (Miller et al., 1998a; Miller et al., 1999). This unconformity is found throughout the eastern U.S. (Owens and Gohn, 1985). The amount of eustatic lowering associated with this event is uncertain because of a hiatus, but ~30 m of eustatic rise is recorded at Ancora and Bass River, providing a minimum range of sea-level change (Fig. F6). The event has been linked to a 18O increase that occurred in both deep-sea benthic and low-latitude planktonic foraminifers (Fig. F6) (Miller et al., 1999). Based on this correspondence, Miller et al. (1999) argued that this event resulted from the growth of a transient ice cap (equivalent to ~40% the volume of the present-day east Antarctic ice cap) that caused a ~25- to 30-m glacioeustatic lowering at 71 Ma. The ~71-Ma Campanian/Maastrichtian boundary sea-level lowering was associated with a major reorganization in deepwater circulation as cool water from a high-latitude source influenced intermediate depths in the tropical Pacific (Barrera et al., 1997). A global 13C decrease is also correlated with the sea-level lowering, perhaps because of increased weathering of organic-rich sediments exposed on continental shelves (Barrera et al., 1997).

Latest Maastrichtian Events

Global 18O records show general cooling conditions in deep waters and high latitudes from the late Campanian to latest Maastrichtian (~73–66 Ma) (Fig. F6) (Barrera and Savin, 1999), punctuated by the ~71- Ma ice volume and sharp cooling event (Miller et al., 1999). During the K.G. MILLER ET AL. LEG 174AX SUMMARY 12 latest Maastrichtian, planktonic foraminiferal distributions (particularly the thermophilic taxon Pseudotextularia elegans) and global 18O records (Figs. F6, F8) (Barrera and Savin, 1999) show a warming of sea-surface F8. Maastrichtian events at Bass temperatures of ~5°C (Fig. F8) (Olsson et al., 2001). Planktonic foramin- River, NJ, p. 32.

t. 18 Bass River, New Jersey l /T ic ra

th tra n ife s s iferal O records from Bass River display this warming as a very large e re in ie δ18 δ13 87 86 B to C C Sr/ Sr m c fo

fa e ra n io

(‰) g (‰) fo b b

a Paleodepth a

M -1 -2 -3 0120.70786 0.707880 0.707900 0.707920 100 50 M Strangelove ocean P% = 30 decrease that began at ~500 k.y. and ended about 22 k.y. before the K/T 1260 2

spherule bed 0 m

1, 2, 3 n

m a w o e re lc

a r t b

v h a 9 e s p r a 2 in l a

C g ti r ? c boundary (Fig. F8) (Olsson et al., 2001). Neritic benthic foraminiferal T

3 c

D 18 C29r 1265

ft) 65.58 Ma ( C30n

O records from Bass River show only a 0.2‰–0.5‰ coeval decrease th

e (a 1°–2°C warming), indicating a strengthening in the thermocline at D global warming

1270 1 n

3 this time (Olsson et al., 2001). The latest Maastrichtian warming event C

P% = 80

Anomalinoides may have been caused by a greenhouse effect resulting from the main Rugoglobigerina 1 outpouring of the Deccan Traps in India beginning at ~65.6 Ma (Cour- tillot et al., 1986). Sr isotopic data from Bass River (Fig. F8) (Olsson et al., 2002) and other sections (Vonhof and Smit, 1997) that show a distinct decrease from ~65.5 to 65 Ma are consistent with increased basaltic weathering. This warming may have contributed to the decline in dinosaur diversity (Sloan et al., 1986), though it was the impact at the K/T boundary that is unequivocally linked to the mass extinction of marine and presumably terrestrial taxa.

K/T Boundary Impact and Tsunami

The Bass River borehole provides a continuous depositional record across the K/T event (Olsson et al., 1997), which has been attributed to a bolide impact (Alvarez et al., 1980) near Chicxulub, Mexico (Hilde- brand et al., 1991). K/T boundary sections in the Gulf Coast show thick ejecta, including glass spherules and tsunamites (Smit et al., 1992). Nonetheless, the relationship between ejecta and the marine mass extinction has been controversial (e.g., Keller et al., 1994), in part because the extensive mixing by a megatsunami in the Gulf Coast. In contrast, the U.S. East Coast was sheltered from the megatsunami’s direct effects. The Bass River borehole directly ties impact ejecta to the highest occur- rence of planktonic foraminifers and calcareous nannofossils (Fig. F9), F9. Cretaceous/Tertiary (K/T) providing the first unequivocal link between bolide impact and marine boundary at Bass River, NJ, p. 33.

Dino- Nanno- mass extinctions that mark the end of the Cretaceous (Olsson et al., LithologyIridium (ppb) δ18O (‰) Planktonic foraminifers flagellate fossils Cysts . P1a 0.511.52-1 -1.5 -2 , ta

y a

s n

la m r e

u o

c m F id m

ro in iu n u

ilty llo ra in ic w u e

s d

ilif n a b a r

to h

1997). Similar results were noted during ODP Leg 171B on the Blake t s α o

s P itic p s

s +10 e lifo d s rs a

a n u

in fo ia

e m y

a e Shocked n c a

m s o

rly

rn y D c n a

t D o minerals p

la e

o is is a S

s s o

G p

rtia a t e few many a s is n n s tin e e e o

in e ric n rm n o b u rg N id e e b T u w n je

g b w ta

y to llo b u to a u

u lo u y rs s e a

a b e Nose (Norris et al., 1999), with the ejecta present at the level of the ma- ric la a P0 o d ra u d Spherule c rn in a a r a m o

n e s e bed e P a in h u

u ig g a n ra

o b o rin P in rin c lo g e d o b g o in b o ig r 0 o g d lo

s b

o W G u ru lo o

K la g

ro W e u

e o ra v n e m

r o E a a

ilife rine mass extinction. A tsunami immediately followed the fallout of iu r Z th h

s P to ii p m in

s s

s o d

n lla o o

n lo rin

o fo c n ra is b

e ly g p

tio

s ra tia

fr g a n o

h la

a h

e e h P e la u

b c T u

o m th ic

c r u ta m

, ric

M o

y o

o re

a is s m e

s s

c a s n

n c

t F

c ia o a

w e Key

t M litr u

ro m ta

y tektites from the Chicxulub ejecta vapor cloud in the Gulf of Mexico itic

o r a e

e Clay clast lla e -10 y b o

a c

o e

r m

in e rg ta

r m

. C u e Glauc. silty clay

m A b

la G

a e d

p e x

N Spherules u H

t e

Burrows N

r (Smit et al., 1992); a clast unit present above the K/T ejecta at Bass River u Glauconitic clay

-0.5 0 0.5 1 1.5 δ13C (‰) (Fig. F9) (Olsson et al., 1997) and on the Blake Nose (Norris et al., 1999) 0.707880 0.707900 0.707920 87Sr/86Sr also appears to be related to a tsunami. Although direct effects of the impact can explain tsunamites in the Gulf of Mexico, it has been difficult to explain the cause of tsunamites outside this region because the Florida platform would have attenuated the waves. Massive slumping on the Atlantic slope, including NJ, may have triggered a tsunami on the Atlantic margin as exemplified by a clast layer found at Bass River (Fig. F9) (Olsson et al., 1997, 2002), Ancora, and outcrop sections in the NJ Coastal Plain. Though sea-level change has long been associated with the K/T boundary, the records from Bass River and Ancora clearly show that the impact event occurred within a sequence that spans the K/T boundary (the Navesink sequence; ~69–64.5 Ma) (Fig. F6) (Olsson et al., 2002). The sequence shallows upsection, particularly in the last 0.5 m.y. of the Cretaceous, culminating in a sharp shallowing in the last 100 k.y. of the Cretaceous (Fig. F8). However, there is no sequence boundary associ- K.G. MILLER ET AL. LEG 174AX SUMMARY 13 ated with the K/T boundary; a major sequence boundary is present in Biochron P1b, with a hiatus from ~64 to 63 Ma (Figs. F5, F6). Thus, Ols- son et al. (2002) concluded that there was a minimal change in sea level associated with the K/T boundary. Zachos and Arthur (1986) showed that the vertical carbon isotopic difference in the oceans (viz. between surface-dwelling planktonic and deep-sea [particularly Pacific] benthic foraminifers) disappeared at the K/T boundary. This “Strangelove” ocean was one with minimal export productivity (D’Hondt et al., 1998). Planktonic (Rugoglobigerina) and benthic (Anomalinoides) 13C records from Bass River (Fig. F8) (Olsson et al., 2002) demonstrate that the collapse of the vertical gradient also occurred in neritic sections. Sedimentation in the earliest Paleocene in the Mid-Atlantic shelf was dominated by slow glauconitic sedimentation, as both siliciclastic and pelagic input were low.

P/E Boundary Event

First recognized by Kennett and Stott (1990), the PETM is associated with a large (2.5‰–4‰), rapid (<20 k.y.) transient global carbon isotopic excursion (the CIE of Zachos et al., 1993), a negative excursion (1‰–3‰) in oxygen isotopes (e.g., Kennett and Stott, 1991), a deep- sea benthic foraminiferal extinction event (e.g., Tjalsma and Lohmann, 1983), a terrestrial mammalian turnover (e.g., Gingerich, 1989), and a kaolinite spike (Robert and Kennett, 1994). The CIE has been attributed to methane release from gas hydrate reservoirs (e.g., Dickens et al., 1995; Katz et al., 1999). Gibson et al. (1993, 2000) and Cramer (2002) studied this event in a borehole from Clayton, NJ, providing clay mineralogic and isotopic data (Fig. F10). Drilling at Bass River and Ancora F10. Paleocene/Eocene boundary preserves an exceptional record of the PETM with a chronology pro- from Bass River, NJ, p. 34. vided by integrated nannofossil, planktonic foraminiferal, and magne- Clayton Ancora Bass River sand δ13C sand δ13C sand δ13C (wt%) (‰ PDB) (wt%) (‰ PDB) (wt%) (‰ PDB)

Depth (m) 0 20 40 -4 -2 0 Depth (ft) Depth (m) 0 20 40 -2 0 2 Depth (ft) Depth (m) 0 20 40 -2 0 2 Depth (ft) Chron NP Zone 85 1130 280 345 C24n NP11 tostratigraphy; these neritic sections rival the best deep-sea sections in 160 NP10 530 1140 290 90 350 540 165 1150 providing a complete record of these global climatic events (Cramer et 300 NP9b 550 1160 310 95 C24r 355 170 al., 1999, 2000; Cramer, 2002). Isotopic analyses at all three boreholes 560 1170 320 570 100 1180 330 13 18 360 spp. show a rapid (<10 k.y.) negative shift in C and O values (~4‰ in 175 580 1190 340 NP9a

Cibicidoides 105 C25n 365 590 180 1200 carbon and ~2‰ in oxygen), and clay mineralogical analyses for Bass 0 20 40 0 20 40 kaolinite (%) kaolinite (%) River and Clayton show a sharp increase in kaolinite coincident with the isotopic shift (Fig. F10) (Cramer et al., 1999; Cramer, 2002). Stable isotopic values remain low and kaolinite content remains high throughout a thick section above the CIE in these neritic sections. Cramer et al. (1999) interpreted these data as indicative of an abrupt shift at the time of the CIE to a warmer and wetter climate that persisted for >300–400 k.y. along the North American Mid-Atlantic coast, unlike deep-sea records that show an exponential return to pre-CIE conditions after ~200 k.y. (Katz et al., 1999, Rohl et al., 2000). The thick interval of low isotopic values at Bass River, Ancora, and Clayton coin- cides with an interval magnetically dominated by <100-nm-diameter magnetite grains. The magnetically anomalous material has been interpreted as derived from a compact impact plume condensate, leading to speculation that the P/E boundary event may have been triggered by a major impact event and reinterpretation of the thickness of this interval on the NJ coastal plain as due to rapid redeposition of impact ejecta over <20 k.y. rather than persistent warm conditions following the PETM (Kent et al., 2001; Cramer, 2002; Kent et al., unpubl. data). K.G. MILLER ET AL. LEG 174AX SUMMARY 14

Earliest Oligocene Event F11. Summary for Bass River, NJ, p. 35.

Kominz and Pekar (2001) provided a backstripped estimate of 54 ± 10 Bass River, ODP Leg 174AX

Environment Environment Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Systems tracts Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Systems Systems Sequence Recovery 50 100 50 tracts Sequence Recovery 50 100 50 Environment Sequence Recovery 50 100 50 tracts 0 700 1400 NP21 g m

g m g CC21/22 10 710 1410 g g m Cape May Fm. g m g

20 720 1420 lHST 19.7 g g m Wenonah Formation g g m g

E10 CC21/22 30 730 1430 gg ?MFS C3 g ggg Nearshore Back barrier/ g gg Fm. P15-17 TST

ggg Marshalltown 40 740 g 1440 CC21a mm 40.8 1440.5 g m

mm 50 750 g 1450 m of eustatic lowering that can be correlated (Pekar et al., 2001) with m g

g 60 760 1460 mm g m upper Englishtown Fm. mm ?MFS g gg 70 ?FS 770 ? 1470 ggg g 770.7 NP19-20

mm 1472.6 C2 g m 80 780 g 1480 mm Cohansey Formation

Absecon Inlet Formation m g

mm 90 790 g 1490 mm g m mm g 18 100 L L L 800 1500 P15 101.9 g uHST 110 810 g 1510

C1b g the well-known earliest Oligocene global O increase (e.g., Miller et 120 820 g ?MFS 1520 Nearshore Lagoonal Nearshore sands 124

C1a 130 830 1530 gg g 132.9 gg CC19/20 P. semiinvoluta

140 840 gg 1540 DN8 or 840.1 uHST gg ? older g gg 150 850 g NP18 1550

gg E9 sp. (reworked) g

gg P15 equivalent 160 860 g Acarinina 1560 DN8 or older Inner neritic gg upper

lHST HST 170 870 1570 Kw2b gg Shark River Fm. slurry ?NP16 E8 lHST

g Woodbury Formation ?MFS 180 880 gg 1580 TST P12

MFS gg 885.8 863.6 846.6 gg al., 1987). This implies development of an ice sheet that was as large, if 190 DN4 or 890 1590 older g TST Lagoon/ Nearshore gg 200 900 1600 LL L gg

205 g E7 210 910 1610 gg

mm g ?Neritic

FS? m 220 920 P11 1620

gg NP15-16 gg

g Outer neritic g 230 930 ggg 1630 ECDZ2 lower Shark River Formation g Rio Grande Aquifer gg ?Nearshore g 240 940 g 1640

E6 g gg

250 950 g 1650 DN4 or gg older ggg ffg lHST uHST gg not slightly larger, than the modern East Antarctica ice sheet, consistent NP14a E5 ggg g f g ?MFS 260 960 1660 g CC18 g g Kw2a g

Prodelta g g g TST 270 FS 970 1670 g g P9-10 g CC17 gg NP13 g g

g Merchantville Fm.

g g CC16 280 980 1680 E4 g g g ? ?981.3 959.9 954.4 932

g 1683.2 g g CC16 g 290 990 1690 g g MFS g g g g gg 300 Inner neritic 1000 1700 g g CC15 ?Cheesequake Fm. DN3-4; g TST prob. DN3 1704.1 ? LL gg 310 1010 1710 CC14? 1709.2 marine

g Marginal g LL 320 1020 g ?1016.5 1720 g

ECDZ2 L Delta front

with the results of Miller et al. (1987) and Zachos et al. (1994). Never- Lagoon/Bay P8 L lTST or ?LST

330 329 1030 1730 pollen Zone V

340 1040 1740 Terrestrial

L Tidal delta ?

350 Kirkwood Formation 1050 1750 Outer neritic HST Fluvial

LL Manasquan Formation 360 Marsh 1060 1760 L L NP12 Magothy Formation Kw1b? E3 L L 370 1070 1770 L L Delta front Tidal delta/lagoon

MFS L L L 380 TST 1080 P7 1780 Prodelta pollen Zone IV 383 L L theless, the large size of the earliest Oligocene (~33.8 Ma) ice sheet is 390 1090 1790 Prodelta

LL 400 1100 1800 L

L pollen Zone IV 1806.4

410 1110 1810 ?1108.5

CC11 1813.6 ?

420 1120 1820 1815.1 E2 P6b Prodelta NP11 430 1130 1830

ggg P6a NP10d 1134.6 E1

440 1140 1840 pollen Zone IV 1138.6 "800-ft sands" Inner neritic uHST 450 1150 1850

P5 surprising, especially considering its near disappearance about a million 460 1160 NP9 (upper) 1860

470 1170 1870 gg

?? Kw1a g 480 1180 1178 1880 g

g 490 1190 uHST 1890

g Bass River Formation pollen Zone IV NP9 (lower) 500 1200 1900 Vincentown Formation probable P5 lHST Outer neritic composite confining unit

Prodelta Delta-front sands Pa3 510 1210 1910

lHST

520 1220 1920 pollen Zone IV years later: Kominz and Pekar’s (2001) eustatic estimate shows a 46 ± P4c NP8 CC11

530 1230 MFS 1930 Middle neritic (lo. Mio.) ?FS

TST g g P4b 540 Neritic 1240 g 1940 21.1 G. zealandica

g g g 1240.8 CC10 20.8 g NP6 HST g Pa2 21.4 P4a barren 550 gg barren

MFS 1250 1950

g 20.9 gg MFS MFS? TST Hornerstown Fm. gg g P3b NP5 TST gg Outer neritic gg Pa1 555.3 g P1c TD = 1956.5 ft g g P1a-P 560 gg 32.0 1260 32.5 g 1258.7 g g

1260.25 1256.5 New Egypt/ gg 32.8 Red Bank Fm. gg

g Zone

570 gg 1270 g Micula prinsii NP23-25

A. mayaroensis g Zone equivalent

gg gg CC26 g 33.3/ 32.7 T. ampliapertura g 580 gg 1280 Zone g G. gansseri gg gg g g MFS Zone 590 gg CC25 1290 gg Navesink Fm. g G. aegyptiaca 15-m eustatic rise at 32.7 Ma, and records from Antarctica show the re- gg g Chiloguembelina 1294.5

g gg CC23a gg g 600 gg 1300 33.7 g g g gg g 610 gg 34.3/ 1310 g g unzoned g g 33.3 CC22b? Middle neritic g g

Atlantic City Formation g O1 620 gg 1320 g uHST gg

g P18-19 NP22 630 gg 1330 g g g g gg g g 640 gg 1340 g g gg g g g

650 gg Mount Laurel Formation 1350 g g g g gg

g g g ?CC21 660 gg 1360 g turn of alpine Nothofagus trees at about this time to the Ross Sea, Ant- g gg g g g g 670 1370 ?MFS g g

g CC21/22 gg Sewell Point Fm.

675.4 g g g 680 1380

g 684.9 g Hantkenina g 690 NP21 1390 g g

E10 g lHST

Absecon Inlet Fm. g g Wenonah Formation P15-17 g arctica (Cantrill, 2001). Transient ice sheets returned numerous times 700 1400 during the Oligocene–middle Miocene (e.g., Barrett, 1999), and eustatic estimates show numerous large rises and falls (Pekar et al., 2001; Miller F12. Summary for Ancora, NJ, et al., 1998a), testifying to a very dynamic ice sheet between ~33 and 14 p. 36.

Ma. By the middle Miocene, the East Antarctic ice sheet had become a Ancora ODP Leg 174AX

Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation

Recovery 050100 Sequence Recovery Sequence Recovery 050100 Sequence 0 400 800 50 100 g m

g m surficial 10 410 P11 810 m

g g E7 m uncertain m 20 420 g 820 g m

?Cohansey g g m 427.6 30 430 middle Eocene 830 g NP15b Shark River Formation

29.25 g permanent feature (e.g., Barrett, 1999) and ice volume changes were NP15a E6 CC19 40 440 840 g g m NP14a 443 g g g E5 m Zone 446.7 NP13/ E4 448.7 50 450 g NP14a 850

P7-P10 m m E3 m G. elevata g m

60 460 g g NP12 860 Woodbury Formation 461.2 m 77.4 Ma m m 70 470 870 m m m primarily controlled by small changes in Antarctica and the nascent 80 480 880 m

m m

lower Eocene m

90 490 890 Campanian E2 ?middle-?upper Miocene

Manasquan Fm. m NP11 g m g m g 100 500 900 m Foram. P6b g g MFS g g CC18 Zone 110 510 910 g g Cohansey Formation g g g g Nanno.

g NP10d 519.2 g g 120 520 920 D. asymetrica

g g g g NP10b E1 g NP10a g m g ? 522.2 growth of Northern Hemisphere ice sheets (Wright, 1998). m g g 130 530 930 g CC17 m g g g 79.1 Ma Merchantville Formation

m up. g Paleo g Santonian m g 140 540 m NP9b 940 g g CC16-17 ? ? B 945.3

150 550 P5 950 ? g g

953.2 MFS ?Santonian Cheesequake Fm. CIE fauna 957.4 160 560 960 g g ? g m 562.1 g 170 570 m upper Paleocene 970 g MFS

g m Vincentown Formation equivalent NP9a 167.9 180 580 980 g preserved

sparse, poorly Zone V, marsh/ g estuarine/bay

g 987? 190 590 990 g g L g NP8 g g g LL ?

LL 599 200 600 g P4a 1000 g NP6

g P3b

g P2 606.5 g NP4 210 610 g P1c 1010 g ?Kw1b g P1b NP3 612.5 P1a Formation Hornerstown g ? Magothy Formation g NP1 P g

220 620 618.3 g 1020 g A. g mayaroensis g CC26 equivalent m g undifferentiated lower Santonian-upper Turonian g m 230 630 1030 ??Zone V m g

lower Miocene g g Aquifer Resources Kirkwood Formation g b-c Maastrichtian l. Paleocene ? g 240 640 g 1040

G. gansseri Navesink Formation 227.2?? CC25 g g 67.3 Ma g MFS g a G. aegyptiaca 250 650 g 68.3 Ma 1050 CC25-23 651.3 20.2 Ma g 71.1 Ma G. havanensis Zone eq. Kw1a g 260 660 72.2 Ma 1060 LL g m 1062.5

263.7 g

266 72.3 Ma m

20.9 Ma CC22-23

270 670 ?lower 1070 Turonian g m Zone IV

m Zone 21.2 Ma 72.1 Ma upper Campanian NP18

g Subzone

M. chiastus

263.7 P. asper 280 680 1080 g g 72.6 Ma g 1082.5

u. Eocene m 286

Zone m

g Mount Laurel Formation 290 690 1090 CC10b (reworked) m g m 296 CC22a Acarinina g 300 700 1100 g m NP17

P15 equivalent Zone IV m g g g 306 m 310 710 g 1110 Toms River Member Zone 1110.9

m Bass River Formation Drilling as part of Leg 174AX (Figs. F11, F12, F13, F14) was very suc- ?E9 g Rugotruncana subcircumnodifer 73.3 Ma m middle upper CC10a 317

320 720 g 1120 m A. albianus m Cenomanian g

g m

330 730 Wenonah Fm. 1130 ?P13-P14 g m CC21 g g m

g g g m Zone IV 340 740 1140 CC9 m g g R. g g g MFS

g 746 g lower calcarata Zone eq. Shark River Formation g 73.4 Ma possibly 350 750 g 1150 1148.1 g Zone III/IV TS Marshalltown Fm. transition NP16 g 752.7 ? g 1154.5 CC20? g g

g 1158.2 middle Campanian cessful in addressing local water resource issues. The Bass River and 360 760 ? 757.2 1160 ? ?359.8 g middle Eocene Zone III/IV g Potomac Formation g transition 770

370 P12-mid P14 1170

up. Shark River Total depth 1170 ft 050 100 g ?E8 Total depth 759 ft

g CC19 ? g upper 380 780 g

g Englishtown Formation g g g

388.6 MFS 390 790 g 789.5

391 g g P11 g g 792.3 lower E7

lower g

uncertain m Shark River m Woodbury Fm. 400 800 Ancora boreholes targeted Cretaceous aquifers in the Mount Laurel, 010050 050100 Englishtown, and Potomac-Raritan-Magothy (PRM) Formations (see Zapecza, 1989, for discussion of these aquifers). Ocean View targeted F13. Summary for Ocean View, Miocene aquifers (e.g., the Atlantic City 800-ft sand aquifer of Zapecza, NJ, p. 37. 1989) and confining units between Cape May and Atlantic City. Beth- Ocean View, ODP Leg 174AX Systems Depth (ft)Lithology Gamma Log (API) Cumulative% Age Systems Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Systems Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation tracts tracts tracts Recovery 050100 Environment Sequence Recovery 0 50 100 150 50 Environment Sequence Recovery Sequence 0 500 1000 Soil 100 200 MFS Not cored TST g g 17.0 Ma g g g g P21/22 O5 g g TST 10 510 1010 g g g g Cape May Formation 16.7 Ma HST

unnamed gravel member, g g 17.3 Ma

2 g g Inner neritic 1015.8

20 520 Kw2a 1020 g g 17.2 Ma uHST ?O4

17.3 Ma

30 530 Prodelta 1030 g g 17.2 Ma TST Delta uHST 28.3 Ma O3 531.6

front g g ?1031.7 g g 533

g g lHST n

o i

NP24-25 t

40 540 1040 g g a

m r

g g o

g g t any Beach targeted the hydrogeology of the locally important g g i

TST C

i t

50 550 1050 g g n a

29.0 Ma l t

g g 1050.5 A Prodelta g g

Kw2a sequence g g g g 60 560 1060 g g g g 17.6 Ma g g uHST ?Nearshore g g

Cape May Formation g g 70 570 1070

g g unzoned O2b g g Hole A g g lHST g g 30.1 Ma lHST 80 580 1080 g g NP24

1 g g g g TST

Kw2a 30.4 Ma

90 590 1090 g g 1090 m g g g g m g g 31.0 Ma 17.4 Ma g g 100 600 1100 Pocomoke, Ocean City, and Manokin aquifers, especially in delineating m g g DN6-DN8 17.4/ g g DN8? m 15.8 Ma

107.5 g g TST m O2 110 610 1110 g g

m g g g g m g g P19 g g g g 120 620 m 1120 g g g g Nearshore 17.5 Ma (CH4) g g g g 17.9 Ma MFS g g 627 m 1126.3 130 630 g g 17.7 Ma TST 1130 17.8 Ma inner neritic Nearshore to g g 32.8 Ma 636.35

Estuarine Marsh LST 140 640 1140 g g 19.7 Ma 32.7 Ma HST 641.55 141.9 g g

DN6-DN8 ?Cohansey Formation

g g Sewell Point Formation DN8? O1

g g NP23 Nearshore 150 (CH3) 650 20.0 Ma 1150 g g 33.3 Ma g g

20.0 Ma g g 34.5 Ma the distribution of freshwater and saline-water zones deeper in the sub- Estuarine P18

160 ?159.8 660 1160

Shoreface g g 20.0 Ma Nearshore/ ? g g TST Estuarine Nearshore/

170 ?166.7 670 1170 19.9/ 1171.5

20.6 Ma (upper Atlantic City 800-ft sand aquifer)

Hantkenina 180 680 HST 1180 E. formosa HO HO 20.5 & 1180.3 Kw1b sequence 20.4 Ma

190 690 (CH2) 1190 NP21 Offshore bars Cohansey Formation

200 700 Delta front 1200 20.5 Ma Kirkwood Formation Barren for dinocysts 210 710 1210 D. saipanensis surface (see Andres, 1986, for discussion of these aquifers). Continuous ? HO g g g Shelf TST ? P16? 20.2 Ma 220 720 1220

220.55 Delta uHST front

D. barbadiensis 3 HO 230 730 1230 20.4/ Kw1a 20.3 Ma Prodelta lHST uHST ?Delta front 20.6 Ma 240 R. reticulata 740 740 718.7 1240 HO

250 750 1250 g g DN6-DN8 uHST DN6? lHST g g 2 Delta front

>8.6 Ma Nearshore/ Prodelta

260 760 Kw1a 1260 g lower Miocene Kw1a sequence 267 coring has shown that aquifer-confining unit couplets are sequences, 270 770 Prodelta lHST 1270 g (lower Atlantic City 800-ft sand aquifer) uHST 775.9/780 280 780 1280 E10

Inner neritic g Kirkwood-Cohansey sequence (= CH1) 290 13.5 Ma 790 Shelf uHST 1290 11.6

300 800 1300

g 12.4 Ma 10.0 Absecon Inlet Formation 310 lHST 810 1310 upper Eocene g 13.5/14.0 Ma

11.6/12.2 Prodelta/Inner neritic

320 820 1320 P15 Kirkwood Formation Kw1a sequence NP19/20 upper middle Miocene MFS 19.6 & g 13.1 Ma-11.0 324 20.5 Ma Inner TST bounded by unconformities (e.g., Sugarman and Miller, 1997). The up- neritic

13.7/13.9/13.4 Ma 327.1 20.7 Ma 11.8/12.1/11.4 330 . 830 1330 1 g Kw1a

13.1/13.2 Ma uHST Prodelta 340 10.9/11.1 840 1340 Delta front lHST

20.4 & 20.8 Ma 350 850 1350

DN6 12.7- 13.2 Ma 360 860 1360 20.9 Ma

370 870 MFS g g 20.6 Ma 1370 12.4/13.6 Ma g g g

10.1/11.7 Kw3 sequence g g g g 1375 ?lHST g 20.6/21.3/ Shelf 380 TST 1376.85 Prodelta 880 20.2 Ma 1380 per HST sands comprise important aquifers in both regions that are g m m g g

m m g 20.9 Ma g G. semiinvoluta 390 21.3 Ma 890 E10a LST 1390 g

22.5/ 891.65 14.1 Ma 23.8/ Kw0 seq. 22.5Ma NP18 12.3 g g g g 25.0 Ma Forams/ g Nannos 895.55 g g 25.4/ NP 400 900 24.9 Ma 1400 19/20 g g g g g 24.9 Ma 1402.9 ?NN1 g g g g

g g 410 910 1410 p p NP18

410.05 24.9 Ma g g g HST g g g DN4 E9 420 920 g g 1420 uHST g g g Acarinina O6 NP17? 15.9 Ma g g HO 15.8 Ma NP18 Deltaic-influenced shelf 430 930 g g 1430 15.1 Ma 25.1 Ma ?MFS g g g g g 433.25 g g 1434.4 generally confined by the overlying TST or lower HST. Thus, sequence (large burrows) NP17

440 940 n 1440

Kw2b sequence g g o

i g

15.9 Ma 25.3 Ma t a

g g TST m r

o g

P12 upper Shark River

TST F

g g y

t i

450 950 C 1450 g 950

Delta front

c i

g g t n

t A g g 26.6 Ma P21/P22 460 16.0 Ma 960 1460 g g uHST

462 (m5 equivalent?) Prodelta

465 g g 16.9 Ma

470 uHST 970 1470 g g Delta front (aquifer sands) 1474 16.4 Ma g g

477.1 26.4 Ma 480 3 980 g g 1480

17.0 Ma NP16 lHST O5

Kw2a g g lHST g 16.9 Ma g g 490 990 1490

Prodelta g g

m middle Eocene

m NP24-25 E7 stratigraphy provides a means to predict the continuity and regional m Shark River Formation 16.9 Ma g g 26.7 Ma MFS M. lehneri m 500 1000 1500

1510 1517 1520 NP15-16 undifferentiated lower Shark River

1530 NP15

M. formosa E6a 1540

g Hantkenina g distribution of aquifer-confining bed units (Sugarman and Miller, 1550 g g NP15b g g g 1559

1560 NP15a?

g E6 1570 g g g 1571 1997). Coring has helped resolve issues with the updip-downdip and Total Depth 1575 ft along-strike relationships of aquifer-confining bed units. For example, F14. Summary for Bethany the Atlantic City 800-ft sand near Atlantic City is comprised of two Beach, DE, p. 38. sand bodies that make up the HSTs of the Kw1a and Kw1b sequences Bethany Beach (Qj32-27), ODP Leg 174AX

Systems Systems Systems Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation tracts tracts tracts Recovery 50 100 Environment Sequence Recovery 50 100 Environment Sequence Recovery 50 100 Environment Sequence 0 500 1000 Not cored Tidal delta 10.8 Ma HST 19.2 Ma

10 510 1010

?MFS (FO=~8.3 Ma) offshore/middle neritic

Gt. pseudomiocenica 18.7 Ma Lagoon TST 20 520 1020 ggggg 10.8 Ma ggggg LSF uHST (Sugarman and Miller, 1997). However, at Cape May, there are two to 523.05 DN8 1 ± 0.4 Ma (8.6-11.2 Ma) 30 530 1030 Omar Formation 19.2 Ma 11.8 Ma HST 40 Marsh 540 1040 LLLL 48.0 ka (<12 Ma) L g Offshore lHST 47.1 ka g St. Marys Formation 50 550 g 1050 MFS Estuarine Gt. menardii 19.2 Ma 50.65

14.5 Ma offshore/middle neritic LSF 52.9 g g TST g g MFS

Uvigerina 557.5 60 560 1060 LSF uHST 1057.95 abundant 11.7 Ma TST NN3 70 ? 570 1070 13.8 Ma 70.6

Fluvial/ LSF Estuarine three sand bodies that could be mapped as the Atlantic City 800-ft Mid DN7 15.0 Ma

80 575.2/580 1080 580 18.4/ USF/Est. 19.4 Ma

86.85 dUSF NN3 90 590 13.1 Ma 1090

dUSF uHST Beaverdam Formation

100 Fluvial 600 1100 Offshore lHST 13.4 Ma LSF FS 16.4 Ma 110 610 1110 pUSF NN2 Estuarine

120 117.5 620 1120

16.5 Ma Fluvial/ dUSF 19.1/ sand, with the highest of these associated with the Kw1c sequence lHST 19.0 Ma L L Estuarine 130 630 1130 (ECDZ1)

13.7 Ma NN2 Lo. estuarine xA. heliopelta 140 640 LSF 1140 19.2 Ma Bay/Back barrier 13.2 Ma MFS L USF/Shelf 150 650 1150 MFS 150.6 648.3/649 g g TST 14.7 Ma USF/ Lower Estuarine 1153 shoreface HST L 160 660 1160 14.3 Ma ?mfs

dUSF Bethany formation USF uHST

170 670 HST 1170 TST (Miller et al., 1996a). Drilling at Ocean View shows that the Kw1c se- USF pUSF dUSF 180 680 1180 14.1 Ma ? 185.6 LSF 190 Lower 690 1190 shoreface Aquifer 13.4 Ma LSF Cheswold MFS? In. neritic ? pLSF 197.4

200 Lower 700 698.5 1200 shoreface g g 15.8 Ma LSF FS L

210 710 Choptank Formation 1210 g 14.3 Ma g g g FS/SB dLSF 220 720 1220 Calvert Formation 15.9 Ma L g quence pinches out between Cape May and Ocean View and thus the L HST LSF g 230 LLL 730 1230 g g

15.8 Ma 20.6 Ma 240 740 1240 g

g 16.2 Ma 250 750 1250 g

Manokin aquifer MFS Upper shoreface/

Foreshore/Lower estuarine g 20.7 Ma Offshore 260 760 1260 g 16.0 Ma Offshore g g 270 770 TST 1270 16.0 Ma LSF g upper sand at Cape May is not equivalent to the upper sands at Ocean L L g 280 780 1280 ?p dUSF g 787.1 290 790 pUSF 1290 lHST 16.5 Ma 20.3/ ?p 20.3 Ma 294.1

300 800 1300

uHST

17.3 Ma 310 810 1310 NN2 Milford Aquifer

dLSF p p 20.4 Ma LL L p FS/SB

320 820 1320 g g 1317.45 g View, Atlantic City, and points north. The drilling also makes clear the g 330 830 1330 16.5 Ma Offshore HST Manokin formation g Distal upper shoreface 340 840 1340 17.1 Ma g

g 350 850 1350 g Offshore lHST gg

g 16.7 Ma g 360 860 1360 g 20.5 Ma g dLSF g 370 MFS 870 1370 TST g 374 g control of depositional facies on aquifer architecture. In DE, aquifer 9.9 380 880 1380 g 9.8 20.7 Ma

MFS g 390 890 17.1 Ma 1390 Lower

shoreface dLSF TST g 10.3 g g 400 900 897.7 1400 g 17.1 Ma 20.9 Ma

9.9 HST g Offshore 410 910 1410 17.7 Ma dUSF uHST g

MFS 9.6 21.0 Ma TST

420 920 Calvert Formation 1420 1421.1 uHST g NN2? Offshore 18.1 Ma g MFS sand units developed in HST shoreface deposits are areally extensive Offshore/ TST LSF g g 430 Middle neritic 930 1430 g 11.7 g 21.0 Ma 1430.5 lHST

dUSF HST

440 940 FS 1440 Offshore 18.2 Ma pUSF MFS lHST g MFS LSF/Off TST 450 10.5 FS 1450 TST 950 ggg 18.3 Ma g pUSF g

452.45 g

HST Clayey Glauconite Sand g 1454.5 MFS dUSF lHST ggg Offshore 460 960 1460 Unnamed Glauconitic Clays and Offshore g g g TST 18.8 Ma MFS g g g 28.0 Ma Offshore 18.5 Ma LSF/Off 1465.7 Unnamed 470 970 1470 Foraminiferal TD 1470 TST Clay LSF gg 9.6 FS 18.4 Ma and can be correlated tens of kilometers from the Bethany Beach bore- HST 480 980 981.3 Offshore/Middle neritic St. Marys Formation

490 990 USF

18.6 Ma

500 1000 hole. These include the middle and lower Miocene aquifer units en- 1000 K.G. MILLER ET AL. LEG 174AX SUMMARY 15 countered at Bethany Beach: the Milford aquifer, which appears to rep- resent the upper HST of Kw2a based on current interpretation of the Sr age control; and the Cheswold aquifer, which is interpreted as the upper HST of the Kw1a. Both can be correlated on geophysical logs through most of southern and central DE. In contrast, aquifer units developed in estuarine-barrier facies, such as the upper? Miocene Pocomoke and Ocean City aquifers at Bethany Beach, are laterally discontinuous, reflecting the high degree of facies change in these environments. The amount of sand present in these estuarine-barrier intervals varies even on the kilometer scale, making detailed local correlation difficult. Pore water geochemical studies of onshore sites provide important constraints on the role of confining units (see Leg 150X studies by Szabo et al., 1997; Pucci et al., 1997). Pore waters of the lower Miocene confining units at Bass River were geochemically typed and compared with adjacent aquifers (Reilly, 2001). Pore water in the confining units are geochemically distinct from adjacent aquifers and correlative confining units at Atlantic City, 15 km to the south.

FUTURE PROSPECTS

Deep Sea Drilling Project (DSDP) and ODP coring has provided an unparalleled database from the oceans, recovering strata and hard rocks that were not accessible to geologists with hammer and Brunton. The sediments and rocks obtained by DSDP and ODP led to a revolution in how we view tectonics and the evolution of the planet. ODP has provided centralized core libraries and databases and coordinated publications and represents one of the finest examples of international cooper- ation in science. In comparison, continental drilling is still in its infancy. Outcrops and subsurface samples are more accessible to geologists onshore, and their study has not generally required large international programs like ODP. However, outcrop sections or discontinuously sampled oil or water wells are poor substitutes for continuous cores. Both national (NSF Continental Dynamics Program) and international (ICDP) efforts are now drilling the continents in an integrated fashion, providing the continuous cores and logs that scientists need to address major scientific themes. In this context, drilling during Legs 150X and 174AX has provided cutting-edge integration of ODP and onshore drilling efforts, coordinated on the themes of global sea-level change and sequence architecture (Miller and Mountain, 1994; Christie-Blick and Austin, 2002). In this contribution, we have shown that onshore drilling can rival the best of ODP drilling in the ocean for continuous records of major global events. For example, during Leg 171B the Blake Nose was drilled in search of continuous Cretaceous to Paleogene records and spectacular records of the C/T, K/T, and PETM events were obtained (Norris, Kroon, Klaus, et al., 1998). We show here that drilling at Bass River and Ancora has provided equally spectacular records of these events. It must be noted that drilling the oceans and continents are complementary: the deep-sea record is generally superior for long, continuous time series and contains a better record of global reservoirs of carbon, whereas the onshore records reflect the direct effects of sea-level change and continental climates. Future drilling efforts must continue to integrate the strengths of deep ocean drilling (such as planned for the Integrated Ocean Drilling K.G. MILLER ET AL. LEG 174AX SUMMARY 16

Program [IODP]) and coordinated onshore efforts. Several major onshore ICDP drilling projects have potential ties to IODP, including the Hawaii Drilling Project (Hawaii Scientific Drilling Project, 2001), the Gulf of Corinth (www.icdp-online.de/html/sites/corinth/news/ news.html), and Chicxulub (www.icdp-online.de/html/sites/chicxulub/news/20011203-Chicxulub_en.html). In addition, various ICDP lake drilling efforts (Titicaca, Malawi, Bosumptwi, and El’gygytgyn; www.icdp-online.de) have direct ties to global change studies of the global paleoceanographic array being constructed by ODP and future IODP drilling. Future drilling in NJ is also being planned as a joint ICDP/IODP effort on the inner continental shelf of NJ (Sites MAT1–MAT3 in Fig. F1) to evaluate the response of passive continental margin stratigraphic architecture to changes in global sea level, sediment supply, and regional tectonics. This drilling project will be the culmination of the NJ/Mid- Atlantic Sea-Level Transect strategy developed and endorsed by several advisory and review bodies over the last decade. Integration of borehole records (lithofacies, biofacies, and logs) with seismic profiles will provide the temporal and spatial control needed to evaluate the response and to perform two-dimensional backstripping, yielding eustatic estimates that can be compared with other eustatic proxies. Prior MAT drilling has focused on the NJ slope (ODP Legs 150 and 174A), outer shelf (ODP Leg 174A), and onshore (ODP Legs 150X and 174AX). Col- lectively, these efforts have provided ages of sequence boundaries and have tied each to the oxygen isotopic proxy of glacioeustasy, yet have fallen short of the ultimate objectives because facies that register the most sensitive record of sea-level change, the paleoinner shelf, have not been continuously sampled. Funds will be partially provided ICDP, and this project will be the first to unite ICDP and ODP in a cooperative international effort, forging new alliances for future drilling.

ACKNOWLEDGMENTS

We thank the Members of the Coastal Plain Drilling Project for help- ing to fulfill the promise of onshore drilling and G. Mountain, N. Christie-Blick, and J. Austin for collaboration in planning the NJ sea- level transect. We thank the numerous scientists involved in the Coastal Plain Drilling Project who are not listed here, especially those who supplied critical data sets for Sr isotopes (M. Feigenson, J. Hernan- dez, and D. Monteverde), nannofossils (M.-P. Aubry, D. Bukry, and L. de Romero), pollen (G. Brenner), and nearshore seismics (G. Mountain and D. Monteverde). The NJ Geological Survey (H. Kasabach, State Geologist [retired] and R. Dalton, Chief Geologist) supplied materials, personnel, and logging support, funded all drilling costs for Bass River, and provided partial support for drilling costs at Ancora and Ocean View. The Delaware Geological Survey (R. Jordan, State Geologist and J. Talley, Associate Director) provided logging for Ocean View and Beth- any Beach, materials, personnel, and partial support for drilling costs at Bethany Beach. The USGS Eastern Region Mapping Team (ERMT; J. Quick, Team Leader) provided partial support for Bethany Beach drilling. We thank the ERMT drillers for their exemplary efforts (G. Cobbs, G. Cobbs III, and D. Queen), their drilling coordinators (W. Newell and J. Self-Trail), and Boart Longyear and its drillers (T. McDonald, head driller). Rutgers University provided space for core storage and core analyses, field vehicles, and materials. The National Science Foundation K.G. MILLER ET AL. LEG 174AX SUMMARY 17

Continental Dynamics Program (L. Johnson, Program Director) funded the onshore boreholes (Leg 174AX) and, along with PCOM (JOIDES Planning Committee) and ODP, are to be commended for their flexibil- ity and vision in authorizing Leg 174AX as an ODP activity. The publications staff at ODP was supportive throughout production of this and other Leg 174AX volumes; Ann Klaus was particularly helpful in providing insights into publishing this unusual leg. Discussions with and re- views by M. Katz are greatly appreciated. This research is supported by NSF grants EAR94-17108, EAR97-08644, and EAR99-09179 (Miller) and EAR98-14025 (Kominz). K.G. MILLER ET AL. LEG 174AX SUMMARY 18 REFERENCES

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+ +

+ + 904 1072 m 3000 I + + + + + + + 1071 + Cape Hatteras Cape + ° + 73 + + + + + MAT3 + 903

MAT2

MAT1 m 2000

1000 m 1000

Atlantic Ocean Atlantic 200 m 200 Cruise (Oc270), and (Oc270), Cruise ° Island Beach ‘93 Island Beach 74

Oceanus Cenozoic outcrop Cenozoic Ocean View ‘99 Ocean View

Bass River ‘96 Bass River

Cretaceous outcrop Cretaceous ‘94 Cape May New Jersey New pre-Cretaceous Bethany Beach, DE (‘00) Bethany ° 75 Atlantic City ‘93 Atlantic City Ancora ‘98 Ancora Cruise 9009 (Ew9009), (Ew9009), 9009 Cruise Ewing Delmarva Peninsula ° 76 AMCOR ODP Leg 150, 150X Exploration DSDP ODP Leg 174A, 174AX Ch0698 Ew9009 Oc270 + I Future Seismic Profiles Existing Drillsites 903 1072 Location map showing existing Location boreholes map showing existing ODP analyzed as part a of the New Jersey/Mid (MAT) Sea-Level Transect. sh Atlantic Also NJ/MAT Sea-Level Transect Sea-Level NJ/MAT W ° ° ° ° ° N 77 38 41 39 40 are multichannel seismic data (MCS) from from (MCS) data seismic multichannel are Coring Project. Margin Geological Survey,Geological = U.S. AMCOR Atlantic Jersey USGS Survey, Figure F1. F1. Figure K.G. MILLER ET AL. LEG 174AX SUMMARY 24 e onshore sequence inner/middle neritic Ocean View Ð 5873 ft View Ocean prodelta clay Ocean View Ð 580 ft View Ocean Modern Niger Delta delta front sand Ocean View Ð 721 ft View Ocean marsh Ocean View Ð 637 ft View Ocean Facies model for deltaic-dominated facies showing core photographs from Miocene the section atOcean View. Modern environ- Clay-silt prodelta-inner neritic (regressive) Quartz sand middle-outer neritic Quartz sand delta front- nearshore (regressive) Maximum Flooding Surface Maximum g g Miocene sequence A Miocene deltaic-influenced facies successions, NJ successions, Miocene deltaic-influenced facies Figure F2. A. F2. Figure Miocen a within successions facies of summary a is left On the top. at illustrated are 1970) (Allen, Niger Delta the from ments pages.) two next on (Continued 1993). al., et Sugarman after (modified K.G. MILLER ET AL. LEG 174AX SUMMARY 25

Figure F2 (continued). B. Facies model for wave-dominated nearshore sedimentation, Miocene of Dela- ware. Trends in textural characteristics shown by bars of varying widths are generalized; see text for expla- nation. Photographs are examples of each facies in core from given levels in the Bethany Beach borehole.

B Backshore Foreshore Upper shoreface Offshore (intertidal)

10 fairweather wave base wave fairweather base storm wave 0 dune -10 beach face longshore bar

Shells Mostly fragments Mostly whole shells

Grain size Physical sedimentary structure preservation Biogenic sedimentary structure preservation

Upper shoreface Upper shoreface Upper shoreface (distal) Lower shoreface (LSF) Ð Offshore (>20 m) Ð (proximal) to foreshore (proximal) to (dUSF) Ð fine to medium, interbedded fine and very generally thinly (USF) Ð "beachy sands," foreshore (USF) Ð clean in places, others fine sands and silty, often laminated very fine clean sands of fine to shell hash with admixed silts and churned, to silty sand by sands, silts, and clays coarse admixtures, occasional clay layers, bioturbation, often very that generally fine ohm lams highlighting evidence of heavy shelly with whole shells further offshore, cross bedding bioturbation that tends to preserved (shell generally below storm obscure lamination meadows); below wave base fairweather wave base but within storm wave base

279.25 ft946 ft 332 ft 383 ft 538 ft K.G. MILLER ET AL. LEG 174AX SUMMARY 26

Figure F2 (continued). C. Conceptual architecture of an upper Oligocene sequence in New Jersey with borehole locations appropriate for sequences O5 and O6. Stratigraphic intervals preserved for each location are indicated in blue on the sea-level representations, striped intervals = nondeposition or erosion, gray = uncertainty. TST = transgressive systems tract, HST = highstand systems tract (after Pekar et al., in press b). C Great Bay Atlantic City Sequence O5 Island Beach Atlantic City Cape May Sequence O6

Rollover

Lower HST 1/ 1000 sequence Upper sequence boundary boundary TST CS 1/500

TST HST TST HST TST HST Quartz sand

Clay and silt

Clayey glauconite and glauconite sand K.G. MILLER ET AL. LEG 174AX SUMMARY 27

Figure F3. Comparison of the ages of the Miocene sequence from the Bethany Beach borehole with the ages of sequences identified in New Jersey. Cross hatched = uncertain ages. Also shown is the benthic for- aminifer oxygen isotopic record for Atlantic deep-sea sites (modified after Miller et al., 1997). Mi events are major isotopic increases that are inferred to correlate with ice growth events on Antarctica; arrows are placed at inflection points. Timescale is after Berggren et al. (1995). Sr age regression of Timescale Atlantic δ18O stack Oslick et al. (1994) NJ Bethany (‰ VPDB) Composite Beach Delaware

Polarity Epoch Age Foram. Nanno. Chron 2 1

C4 NN10 N16 10 late 10 NN9 Mi6 C5 NN8 Cibicidoides N15 spp. Mi5 NN7 N14 Kw-C 12 12 C5A N12 Mi4 NN6 C5AA Mi3a,b C5AB N10 Kw3 14 C5AC 14 NN5 C5AD Kw2c

middle N9 Mi2a C5B ? N8 Mi2 Kw2b 16 16 C5C NN4

Age (Ma) N7

Miocene Kw2a C5D Mi1b 18 N6 18 C5E NN3 Mi1ab Kw1c ? C6 Kw1b Cut out 20 N5 20 Mi1aa NN2 ? Kw1a ? C6A early Mi1a 22 C6AA 22 N4 C6B Kw0 Cut out NN1 Mi1 C6C 24 P22 NP25 24

Ol.

late K.G. MILLER ET AL. LEG 174AX SUMMARY 28

Figure F4. Backstripped R2 eustatic estimates (Van Sickle et al., unpubl. data) for five coastal plain boreholes. Backstripping studies of Ocean View and Bethany Beach are ongoing. Heavy lines = best estimates, light lines outlining color shared areas = error bars. R2 is the second reduction of Bond and Kominz (1984) that provides a eustatic estimate (see Kominz et al., 1998, for discussion).

200 Atlantic City Ancora Cape May 150 Bass River Island Beach

100

50 Sea level (m) Sea level 0

-50 late earlylate early middle late early lateearly middle late Holo. Cretaceous Paleocene Eocene Oligocene Miocene Plio. 100 90 80 70 60 50 40 3020 10 0 Time (Ma) K.G. MILLER ET AL. LEG 174AX SUMMARY 29

Figure F5. Late Cretaceous age-depth plots for sequences at Bass River (top) and Ancora (bottom). Solid black circles = Sr isotopic ages computed using the regressions (Age = 39104.339163 – 87Sr/86Sr P 55154.82511), applicable from 73.5 to 86.0 Ma and (Age = 31908.531372 – 87Sr/86Sr P 44984.801888), applicable from 65 to 73.5 Ma with ±1-m.y. error bars, blue circles = diagenetically altered samples, red = con- servative age models, green = alternate age models. Horizontal olive-green lines indicate sequence boundaries. Blue triangles = CC nannofossil zones, P planktonic foraminiferal age estimates. Blue blocks at bottom = time represented in each borehole (after Miller et al., unpubl. data).

Bass River, NJ base top P1a CC26 top CC26 Navesink II base A. mayo. zone eq. Navesink I 1300 400 top base CC23a CC25b Marshalltown 1400 base CC21a top R. calcarata Englishtown 450 within CC19/20 1500

1600 Merchantville III base CC19 500 base CC18 Merchantville I & II base CC17 base Camp. foram. base CC16 Cheesequake base CC15 Bass River 1700 base CC14 Magothy III

pollen Zone IV Magothy I 550 1800

diagenetically BR III altered Sr 1900 Depth (ft)

Depth (m) base CC10

Navesink II Ancora, NJ Navesink I base CC26 200 base CC25a top CC22a Marshalltown base CC22a 700

base CC21 Englishtown base CC20 800 250 Merchantville III

base Camp. foram. base CC19 HO M. furcatus 900 Merchantville II base CC18 Merchantville I LO B. parca Cheesequake base CC17, LO C. obscurus Magothy III pollen Zone V; 300 assumes same age as MIII at Bass River 1000 Magothy II pollen Zone V

BR III top CC10 BR II 1100 BR I base CC10 350 lo. Ceno. pollen Zone III at base;

Nanno. Zone CC16 CC25a CC26 15 17 a b c CC10 CC24 CC12 CC14 CC19 CC18 CC9 CC13 CC21 CC11 CC23 CC20 CC22 Age/stage Cenomanian Turonian Con. Sant. Campanian Maastrichtian Danian

Age, Ma 100 95 90 85 80 75 70 65 60

? ? ? ? Ancora ?? Sequence Age Bass ? River ? ? ? ? K.G. MILLER ET AL. LEG 174AX SUMMARY 30

Figure F6. Comparison of Late Cretaceous deep-sea oxygen benthic foraminiferal 18O records (Site 463, Barrera and Savin, 1999; Site 690, Barrera and Savin, 1999; Site 511, Fassel and Bralower, 1999; Sites 1049 and 1050, Huber et al., 2002), planktonic foraminiferal 18O records (Site 463, Barrera and Savin, 1999), New Jersey composite sequences (derived from Fig. F5, p. 29), the relative sea-level curve from northwest Europe (red continuous line; Hancock, 1993) and the backstripped record from the Russian platform (black continuous line; Sahagian et al., 1996), the EPR eustatic estimate (green line, Haq et al., 1987), backstripped R2 eustatic estimates for Bass River (pink discontinuous lines) and Ancora (red discontinuous lines), and our best estimate of eustatic changes derived from the R2 curves (dark blue indicates portions of the curve constrained by data, light blue indicate portions inferred). Pink arrows indicate positive 18O inflections (inferred cooling and/or ice volume increases). For the composite: blue boxes = time represented, white areas = hiatus, thin white lines = inferred hiatuses. Arrows are drawn through the inflection points of the Eu- ropean records. E.K. = Early Cretaceous (after Miller et al., unpubl. data).

EPR Sea level δ18 O NJ Composite European Estimate (m) R2 Sea level NJ Sea level Timescale (‰) Sequences Sea level Est. calibrated to Gradstein et al. (1995) Estimate (m) Estimate (m) 250 200 50 0 50 0 50 0 Paleocene benthic NW Europe lowerings not studied here Hancock (1996) 1 0 -1

Stage Relative units Nanno. Zone Tertiary 10 6 Navesink II 65 CC26 TA1.1 CC25c ? CC25b planktonic Navesink I -1 -2 CC25a UZA4.5 70 CC24 Maastrictian

CC23 Site 463 CC22 4.4 CC22 Site 690 Marshalltown a 75 CC21 Site ? ? 1049 Englishtown CC20 4.3 Site 1050 ? 4.2 CC19 4.1 80 Campanian Merchantville III

CC18

Age (Ma) 3.5 ? Merchantville II ? Merchantville I 3.4 CC16 ? Cheesequake

85 San. Site 511 3.3 CC14 ? 3.2 CC13 Magothy III Con. ? Magothy II? 3.1 CC12 90 ? Magothy I 2.7 CC11 ? 2.6

Turonian BRIII Site 1050 2.5 CC10 BRII 95 BRI 2.4 CC9 Potomac Cenomian No data 2.3 100 E. K. 4 8 12 100 50 Bottom water Russian platform temperature Sahagian et al. (1996) (°C) K.G. MILLER ET AL. LEG 174AX SUMMARY 31

o- Depth (ft) Depth 1800 1850 1900 1950 FS FS FS FS FS? MFS total depth (mod- depth total isotopic data,and Shallower neritic -5 Water depth Water Deeper -4 ) C

Gavelinella Gavelinella (calcite) ‰ 18 ( δ -3 -2 2

Epistomina (aragonite) 1 mean 0.87% % TOC 0

Epistomina (aragonite) Sequence boundary total depth below ) equivalent C

‰ 13 ( Bonarelli δ

Gavelinella Gavelinella (calcite) >91.8 Ma 93.5 Ma

Glauconite Mica Clay Foraminifers/ shell Fine quartz sand

Cenomanian

lower Turonian lower upper (%)

-4 -2 0 2 4 pollen zone IV zone pollen

Rotalipora

? M. nodosoides M.

nannofossil Zone nannofossil M. chiastius chiastius M. E. eximius eximius E.

prodelta inner neritic inner middle neritic middle Bass River Sequence River Bass Cumulative Sequence/Environment Cumulative 100 50 Cenomanian–Turonian section at Bass River, New Jersey, showing lithology, environment of deposition, nannofossil and pollen bi pollen and nannofossil of deposition, environment lithology, showing New Jersey, at River, Bass section Cenomanian–Turonian 0 TD = 596.34 m

550 560 570 580 590 Depth (m) Depth Figure F7. Figure oxygen foraminiferal benthic sediments, in the carbon organic percent data, isotopic carbon foraminiferal benthic stratigraphy, water depth changes inferred from benthic foraminiferal FS biofacies. = flooding surface, MFS = maximum surface,flooding TD = data). unpubl. al., Wright et from data using 1999, al., et Sugarman after ified K.G. MILLER ET AL. LEG 174AX SUMMARY 32 on ) and Anom-

Anomalinoides Deccan Trap volcanism Trap Deccan 65.58 Ma

Ma before K/T before Ma C30n C29r

; 3 = inner–middle neritic neritic = inner–middle ; 3

C29r C30n Magnetostrat. C30n 1 50 Paleodepth P% = 80

P% = 30 100 biofacies

2 3 1

Benthic foraminiferal 1, 2, 3 A. midwayensis–Anomalinoides acuta A. midwayensis–Anomalinoides more basaltic

Sr weathering? 86 Sr/ 87 spherule bed ; 2 = middle ; 2 neritic = middle 0.70786 0.707880 0.707900 0.707920 Strangelove ocean Strangelove ) C ‰ 13 ( δ ) foraminifers, Sr isotopic data generated on foraminiferal tests, benthic foraminiferal biofacies (1 = mid- = (1 biofacies foraminiferal benthic tests, on foraminiferal generated isotopic data Sr foraminifers, ) 012 Bass River, New Jersey New Bass River,

Anomalinoides Rugoglobigerina -3 Rugoglobigerina global warming ) C P% = percent planktonic foraminifers (solid circles). Interpreted paleodepth curve (light line), magnetic polarity interpretati Interpreted= percentforaminiferspaleodepthline), magnetic polarity (solid circles). planktonic P% curve (light ‰ 18 ( δ -2 welleri), welleri), Anomalinoides midwayensis–Gyrodinoides imitata midwayensis–Gyrodinoides Anomalinoides Maastrichtian events at Bass River, New Bass oxygen at River, Jersey,(solid data circles, events carbon for benthic and isotopic showing Maastrichtian cf. -1

1260 1265 1270 Depth (ft) Depth Figure F8. Figure alinoides 2002). al., et Olsson after (modified Traps Deccan the of correlation the indicating line a and River, Bass for planktonic (closed circles, dle neritic K.G. MILLER ET AL.

LEG 174AX SUMMARY 33

Cretaceous Tertiary

lowermost Danian lowermost

ocked Maastrichtian uppermost

Not examined Not Zone Micula prinsii prinsii Micula

fossils

. Nanno- Not examined Not

grallator californicum

Palynodinium

reted as being em- Damassadinium

bloom

Senoniasphaera inornata Senoniasphaera Thoracosphaera Dino- Cysts

flagellate Parasubbotina pseudobulloides pseudobulloides Parasubbotina

Globoconusa daubjergensis Globoconusa

Woodringina hornerstownensis Woodringina Woodringina claytonensis Woodringina

Key

Praemurica taurica Praemurica

Glauconitic clay Burrows Glauc. silty clay Glauc. Spherules Clay clast Clay

Eoglobigerina eobulloides eobulloides Eoglobigerina

Parvularugoglobigerina eugubina Parvularugoglobigerina

Cretaceous assemblage Cretaceous

Hedbergella monmouthensis Hedbergella

Guembelitria cretacea Guembelitria

Zone α mayaroensis A. P0 P P1a -2 ) ) Sr ‰ ‰ 86 C ( O ( -1.5 Sr/ 13 18 87 δ δ -1 -0.5 0 0.5 1 1.5 0.707880 0.707900 0.707920 minerals Shocked few many

0.5 1 1.5 2 Iridium (ppb)

Hornerstown Fm. Hornerstown New Egypt Formation Egypt New

poorly fossiliferous poorly

Burrowed glauconitic clay, richly fossiliferous richly clay, glauconitic Burrowed Glauconitic silty clay, clay, silty Glauconitic

bed

Burrows Clay clast Clay Spherule Lithology Planktonic foraminifers Cretaceous/Tertiary (K/T) boundary at Bass River, New Jersey, showing core photograph and lithology of spherule bed, Ir and sh 0

-10 +10 cm from the K/T boundary K/T the from cm mineral concentration, and biostratigraphic data (planktonic foraminifers, dinocysts, and nannofossils). Clay clasts are interp are clasts Clay and nannofossils). dinocysts, foraminifers, (planktonic data biostratigraphic and concentration, mineral 2002). 1997, al., et Olsson after (modified a tsunami by placed Figure F9. Figure K.G. MILLER ET AL. LEG 174AX SUMMARY 34

Figure F10. Paleocene/Eocene boundary from Bass River, New Jersey, showing magnetostratigraphic interpretation of nannofossil biostratigraphy, percent kaolinite of total clay fraction, stable isotopic data, and grain-size data. Grain-size data and nannofossil biostratigraphy are shown for Ancora, New Jersey (modified after Cramer et al., 1999, 2000).

Clayton Ancora Bass River sand δ13C sand δ13C sand δ13C (wt%) (‰ PDB) (wt%) (‰ PDB) (wt%) (‰ PDB)

Depth (m) 0 20 40 -4 -2 0 Depth (ft) Depth (m) 0 20 40 -2 0 2 Depth (ft) Depth (m) 0 20 40 -2 0 2 Depth (ft) Chron NP Zone 85 1130 280 345 C24n NP11 160 NP10 530 1140 290 90 350 540 165 1150 300 NP9b 550 1160 310 95 C24r 355 170 560 1170 320 570 100 1180 330 360 spp. 175 580 1190 340 NP9a

Cibicidoides 105 C25n 365 590 180 1200 0 20 40 0 20 40 kaolinite (%) kaolinite (%) K.G. MILLER ET AL. LEG 174AX SUMMARY 35

Figure F11. Summary for Bass River, New Jersey. (This figure is available in an oversized format.)

Bass River, ODP Leg 174AX

g m g CC21/22 10 710 1410 g g m Cape May Fm. g m g

20 720 1420 lHST 19.7 g g m Wenonah Formation g g m g

E10 CC21/22 30 730 1430 gg ?MFS C3 g ggg Nearshore Back barrier/ g gg Fm. P15-17 TST

ggg Marshalltown 40 740 g 1440 CC21a mm 40.8 1440.5 g m

mm 50 750 g 1450 m g

g 60 760 1460 mm g m upper Englishtown Fm. mm ?MFS g gg 70 ?FS 770 ? 1470 ggg g 770.7 NP19-20

mm 1472.6 C2 g m 80 780 g 1480 mm Cohansey Formation

Absecon Inlet Formation m g

mm 90 790 g 1490 mm g m mm g 100 L L L 800 1500 P15 101.9 g uHST 110 810 g 1510

C1b g

120 820 g ?MFS 1520 Nearshore Lagoonal Nearshore sands 124

C1a 130 830 1530 gg g 132.9 gg CC19/20 P. semiinvoluta

140 840 gg 1540 DN8 or 840.1 uHST gg ? older g gg 150 850 g NP18 1550

gg E9 sp. (reworked) g

gg P15 equivalent

160 Acarinina 860 g 1560 DN8 or older Inner neritic gg upper

lHST HST 170 870 1570 Kw2b gg Shark River Fm. slurry ?NP16 E8 lHST

g Woodbury Formation ?MFS 180 880 gg 1580 TST P12

MFS gg 885.8 863.6 846.6 gg 190 DN4 or 890 1590 older g TST Lagoon/ Nearshore gg 200 900 1600 LL L gg

205 g E7 210 910 1610 gg

mm g ?Neritic

FS? m 220 920 P11 1620

gg NP15-16 gg

g Outer neritic g 230 930 ggg 1630 ECDZ2 lower Shark River Formation g Rio Grande Aquifer gg ?Nearshore g 240 940 g 1640

E6 g gg

250 950 g 1650 DN4 or gg older ggg ffg lHST uHST gg NP14a E5 ggg g f g ?MFS 260 960 1660 g CC18 g g Kw2a g

Prodelta g g g TST 270 FS 970 1670 g g P9-10 g CC17 gg NP13 g g

g Merchantville Fm.

g g CC16 280 980 1680 E4 g g g ? ?981.3 959.9 954.4 932

g 1683.2 g g CC16 g 290 990 1690 g g MFS g g g g gg 300 Inner neritic 1000 1700 g g CC15 ?Cheesequake Fm. DN3-4; g TST prob. DN3 1704.1 ? LL gg 310 1010 1710 CC14? 1709.2 marine

g Marginal g LL 320 1020 g ?1016.5 1720 g

ECDZ2 L Delta front Lagoon/Bay P8 L lTST or ?LST

330 329 1030 1730 pollen Zone V

340 1040 1740 Terrestrial

L Tidal delta ?

350 Kirkwood Formation 1050 1750 Outer neritic HST Fluvial

LL Manasquan Formation 360 Marsh 1060 1760 L L NP12 Magothy Formation Kw1b? E3 L L 370 1070 1770 L L Delta front Tidal delta/lagoon

MFS L L L 380 TST 1080 P7 1780 Prodelta pollen Zone IV 383 L L 390 1090 1790 Prodelta

LL 400 1100 1800 L

L pollen Zone IV 1806.4

410 1110 1810 ?1108.5

CC11 1813.6 ?

420 1120 1820 1815.1 E2 P6b Prodelta NP11 430 1130 1830

ggg P6a NP10d 1134.6 E1

440 1140 1840 pollen Zone IV 1138.6 "800-ft sands" Inner neritic uHST 450 1150 1850

P5 460 1160 NP9 (upper) 1860

470 1170 1870 gg

?? Kw1a g 480 1180 1178 1880 g

g 490 1190 uHST 1890

g Bass River Formation pollen Zone IV NP9 (lower) 500 1200 1900 Vincentown Formation probable P5 lHST Outer neritic composite confining unit

Prodelta Delta-front sands Pa3 510 1210 1910

lHST

520 1220 1920 pollen Zone IV

P4c NP8 CC11 530 1230 MFS 1930 Middle neritic (lo. Mio.) ?FS

TST g g P4b 540 Neritic 1240 g 1940 21.1 G. zealandica

g g g 1240.8 CC10 20.8 g NP6 HST g Pa2 21.4 P4a barren 550 gg barren

MFS 1250 1950

g 20.9 gg MFS MFS? TST Hornerstown Fm. gg g P3b NP5 TST gg Outer neritic gg Pa1 555.3 g P1c TD = 1956.5 ft g g P1a-P 560 gg 32.0 1260 32.5 g 1258.7 g g

1260.25 1256.5 New Egypt/ gg 32.8 Red Bank Fm. gg

g Zone

570 gg 1270 g Micula prinsii NP23-25

A. mayaroensis g Zone equivalent

gg gg CC26 g 33.3/ 32.7 T. ampliapertura g 580 gg 1280 Zone g G. gansseri gg gg g g MFS Zone 590 gg CC25 1290 gg Navesink Fm. g G. aegyptiaca gg g Chiloguembelina 1294.5

g gg CC23a gg g 600 gg 1300 33.7 g g g gg g 610 gg 34.3/ 1310 g g unzoned g g 33.3 CC22b? Middle neritic g g

Atlantic City Formation g O1 620 gg 1320 g uHST gg

g P18-19 NP22 630 gg 1330 g g g g gg g g 640 gg 1340 g g gg g g g

650 gg Mount Laurel Formation 1350 g g g g gg

g g g ?CC21 660 gg 1360 g g gg g g g g 670 1370 ?MFS g g

g CC21/22 gg Sewell Point Fm.

675.4 g g g 680 1380

g 684.9 g Hantkenina g 690 NP21 1390 g g

E10 g lHST

Absecon Inlet Fm. g g Wenonah Formation P15-17 g 700 1400 K.G. MILLER ET AL. LEG 174AX SUMMARY 36

Figure F12. Summary for Ancora, New Jersey. (This figure is available in an oversized format.)

Ancora ODP Leg 174AX

Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation

Recovery 0 50 100 Sequence Recovery Sequence Recovery 050100 Sequence 0 400 800 50 100 g m

g m surficial 10 410 P11 810 m

g g E7 m uncertain m 20 420 g 820 g m

?Cohansey g g m 427.6 30 430 middle Eocene 830 g NP15b Shark River Formation

29.25 g NP15a E6 CC19 40 440 840 g g m NP14a 443 g g g E5 m Zone 446.7 NP13/ E4 448.7 50 450 g NP14a 850

P7-P10 m m E3 m G. elevata g m

60 460 g g NP12 860 Woodbury Formation 461.2 m 77.4 Ma m m 70 470 870 m m m 80 480 880 m

m m

lower Eocene m

90 490 890 Campanian E2 ?middle-?upper Miocene

Manasquan Fm. m NP11 g m g m g 100 500 900 m P6b g Foram. g MFS g g CC18 Zone 110 510 910 g g Cohansey Formation g g g g Nanno.

g NP10d 519.2 g g 120 520 920 D. asymetrica

g g g g NP10b E1 g NP10a g m g ? 522.2 m g g 130 530 930 g CC17 m g g g 79.1 Ma Merchantville Formation

m up. g Paleo g Santonian m g 140 540 m NP9b 940 g g CC16-17 ? ? B 945.3

150 550 P5 950 ? g g

953.2 MFS ?Santonian Cheesequake Fm. CIE fauna 957.4 160 560 960 g g ? g m 562.1 g 170 570 m upper Paleocene 970 g MFS

g m Vincentown Formation equivalent NP9a 167.9 180 580 980 g preserved

sparse, poorly Zone V, marsh/ g estuarine/bay

g 987? 190 590 990 g g L g NP8 g g g LL ?

LL 599 200 600 g P4a 1000 g NP6

g P3b

g P2 606.5 g NP4 210 610 g P1c 1010 g ?Kw1b g P1b NP3 612.5 P1a Formation Hornerstown g ? Magothy Formation g NP1 P g

220 620 618.3 g 1020 g A. g mayaroensis g CC26 equivalent m g undifferentiated lower Santonian-upper Turonian g m 230 630 1030 ??Zone V m g

lower Miocene g g Kirkwood Formation g b-c Maastrichtian l. Paleocene ? g 240 640 g 1040

G. gansseri Navesink Formation 227.2?? CC25 g g 67.3 Ma g MFS g a G. aegyptiaca 250 650 g 68.3 Ma 1050 CC25-23 651.3 20.2 Ma g 71.1 Ma G. havanensis Zone eq. Kw1a g 260 660 72.2 Ma 1060 LL g m 1062.5

263.7 g

266 72.3 Ma m

20.9 Ma CC22-23

270 670 ?lower 1070 Turonian g m Zone IV

m Zone 21.2 Ma 72.1 Ma upper Campanian NP18

g Subzone

M. chiastus

263.7 P. asper 280 680 1080 g g 72.6 Ma g 1082.5

u. Eocene m 286

Zone m

g Mount Laurel Formation 290 690 1090 CC10b (reworked) m g

296 m CC22a Acarinina g 300 700 1100 g m NP17

P15 equivalent Zone IV m g g g 306 m 310 710 g 1110 Toms River Member Zone 1110.9

m Bass River Formation ?E9 g Rugotruncana subcircumnodifer 73.3 Ma m middle upper CC10a 317

320 720 g 1120 m A. albianus m Cenomanian g

g m

330 730 Wenonah Fm. 1130 ?P13-P14 g m CC21 g g m

g g g m Zone IV 340 740 1140 CC9 m g g R. g g g MFS

g 746 g lower calcarata Zone eq. Shark River Formation g 73.4 Ma possibly 350 750 g 1150 1148.1 g Zone III/IV TS Marshalltown Fm. transition NP16 g 752.7 ? g 1154.5 CC20? g g

g 1158.2 middle Campanian ? 757.2 360 760 1160 ? ?359.8 g middle Eocene Zone III/IV g Potomac Formation g transition 770

370 P12-mid P14 1170

up. Shark River Total depth 1170 ft 050 100 g ?E8 Total depth 759 ft

g CC19 ? g upper 380 780 g

g Englishtown Formation g g g

388.6 MFS 390 790 g 789.5

391 g g P11 g g 792.3 lower E7

lower g

uncertain m Shark River m Woodbury Fm. 400 800 050 100 0 50 100 K.G. MILLER ET AL. LEG 174AX SUMMARY 37

Figure F13. Summary for Ocean View, New Jersey. (This figure is available in an oversized format.)

Ocean View, ODP Leg 174AX Systems Depth (ft)Lithology Gamma Log (API) Cumulative% Age Systems Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Systems Formation Depth (ft)Lithology Gamma Log (API) Cumulative% Age Formation tracts tracts tracts Recovery 0 50 100 Environment Sequence Recovery 0 50 100 150 50 Environment Sequence Recovery Sequence 0 500 1000 Soil 100 200 MFS Not cored TST g g 17.0 Ma g g g g P21/22 O5 g g TST 10 510 1010 g g g g Cape May Formation 16.7 Ma HST

unnamed gravel member, g g 17.3 Ma

2 g g Inner neritic 1015.8

20 520 Kw2a 1020 g g 17.2 Ma uHST ?O4

17.3 Ma

30 530 Prodelta 1030 g g 17.2 Ma TST Delta uHST 28.3 Ma O3 531.6

front g g ?1031.7 g g 533

g g lHST n

o i

NP24-25 t

40 540 1040 g g a

m r

g g o

g g y g g it

TST C

ic t

50 550 1050 g g n a

29.0 Ma l t

g g 1050.5 A Prodelta g g

Kw2a sequence g g g g 60 560 1060 g g g g 17.6 Ma g g uHST ?Nearshore g g

Cape May Formation g g 70 570 1070

g g unzoned O2b g g Hole A g g lHST g g 30.1 Ma lHST 80 580 1080 g g NP24

1 g g g g TST

Kw2a 30.4 Ma

90 590 1090 g g 1090 m g g g g m g g 31.0 Ma 17.4 Ma g g 100 600 1100 m g g DN6-DN8 17.4/ g g DN8? m 15.8 Ma

107.5 g g TST m O2 110 610 1110 g g

m g g g g m g g P19 g g g g 120 620 m 1120 g g g g Nearshore 17.5 Ma (CH4) g g g g 17.9 Ma MFS g g 627 m 1126.3 130 630 g g 17.7 Ma TST 1130 17.8 Ma inner neritic Nearshore to g g 32.8 Ma 636.35

Estuarine Marsh LST 140 640 1140 g g 19.7 Ma 32.7 Ma HST 641.55 141.9 g g

DN6-DN8 ?Cohansey Formation

g g Sewell Point Formation DN8? O1

g g NP23 Nearshore 150 (CH3) 650 20.0 Ma 1150 g g 33.3 Ma g g

20.0 Ma g g 34.5 Ma Estuarine P18

160 ?159.8 660 1160

Shoreface g g 20.0 Ma Nearshore/ ? g g TST Estuarine Nearshore/

170 ?166.7 670 1170 19.9/ 1171.5

20.6 Ma (upper Atlantic City 800-ft sand aquifer)

Hantkenina 180 680 HST 1180 E. formosa HO HO 20.5 & 1180.3 Kw1b sequence 20.4 Ma

190 (CH2) 690 1190 NP21 Offshore bars Cohansey Formation

200 700 Delta front 1200 20.5 Ma Kirkwood Formation Barren for dinocysts 210 710 1210 D. saipanensis

? HO g g g Shelf TST ? P16? 20.2 Ma 220 720 1220

220.55 Delta uHST front

D. barbadiensis 3 HO 230 730 1230 20.4/ Kw1a 20.3 Ma Prodelta lHST uHST ?Delta front 20.6 Ma 240 R. reticulata 740 740 718.7 1240 HO

250 750 1250 g g DN6-DN8 uHST DN6? lHST g g 2 Delta front

>8.6 Ma Nearshore/ Prodelta

260 760 Kw1a 1260 g Kw1a sequence lower Miocene 267 270 770 Prodelta lHST 1270 g (lower Atlantic City 800-ft sand aquifer) uHST 775.9/780 280 780 1280 E10

Inner neritic g Kirkwood-Cohansey sequence (= CH1) 290 13.5 Ma 790 Shelf uHST 1290 11.6

300 800 1300

g 12.4 Ma 10.0 Absecon Inlet Formation 310 lHST 810 1310 upper Eocene g 13.5/14.0 Ma

11.6/12.2 Prodelta/Inner neritic

320 820 1320 P15 Kirkwood Formation Kw1a sequence NP19/20 upper middle Miocene MFS 19.6 & g 13.1 Ma-11.0 324 20.5 Ma Inner TST neritic

13.7/13.9/13.4 Ma 327.1 20.7 Ma 11.8/12.1/11.4 330 . 830 1330 1 g Kw1a

13.1/13.2 Ma uHST Prodelta 340 10.9/11.1 840 1340 Delta front lHST

20.4 & 20.8 Ma 350 850 1350

DN6 12.7- 13.2 Ma 360 860 1360 20.9 Ma

370 870 MFS g g 20.6 Ma 1370 12.4/13.6 Ma g g g

10.1/11.7 Kw3 sequence g g g g 1375 ?lHST g 20.6/21.3/ Shelf 380 TST 1376.85 Prodelta 880 20.2 Ma 1380 g m m g g

m m g 20.9 Ma g G. semiinvoluta 390 21.3 Ma 890 E10a LST 1390 g

22.5/ 891.65 14.1 Ma 23.8/ Kw0 seq. 22.5Ma NP18 12.3 g g g g 25.0 Ma Forams/ g Nannos 895.55 g g 25.4/ NP 400 900 24.9 Ma 1400 19/20 g g g g g 24.9 Ma 1402.9 ?NN1 g g g g

g g 410 910 1410 p p NP18

440 940 n 1440

Kw2b sequence g g o

i g

15.9 Ma 25.3 Ma t a

g g TST m r

o g P12 upper Shark River

TST F

g g y it

450 950 C 1450 g 950

Delta front

c i

g g t n

t A g g 26.6 Ma P21/P22 460 16.0 Ma 960 1460 g g uHST

462 (m5 equivalent?) Prodelta

465 g g 16.9 Ma

470 uHST 970 1470 g g Delta front (aquifer sands) 1474 16.4 Ma g g

477.1 26.4 Ma 480 3 980 g g 1480

17.0 Ma NP16 lHST O5

Kw2a g g lHST g 16.9 Ma g g 490 990 1490

Prodelta g g

m middle Eocene

m NP24-25 E7 m Shark River Formation 16.9 Ma g g 26.7 Ma MFS M. lehneri m 500 1000 1500

1510 1517 1520 NP15-16 undifferentiated lower Shark River

1530 NP15

M. formosa E6a 1540

g Hantkenina g 1550 g g NP15b g g g 1559

1560 NP15a?

g E6 1570 g g g 1571 Total Depth 1575 ft K.G. MILLER ET AL. LEG 174AX SUMMARY 38

Figure F14. Summary for Bethany Beach, Delaware. (This figure is available in an oversized format.)

Bethany Beach (Qj32-27), ODP Leg 174AX

10 510 1010

?MFS (FO=~8.3 Ma) offshore/middle neritic

Gt. pseudomiocenica 18.7 Ma Lagoon TST 20 520 1020 ggggg 10.8 Ma ggggg LSF uHST DN8 523.05 1 ± 0.4 Ma (8.6-11.2 Ma) 30 530 1030 Omar Formation 19.2 Ma 11.8 Ma HST 40 Marsh 540 1040 LLLL 48.0 ka (<12 Ma) L g Offshore lHST 47.1 ka g St. Marys Formation 50 550 g 1050 MFS Estuarine Gt. menardii 19.2 Ma 50.65

14.5 Ma offshore/middle neritic LSF 52.9 g g TST g g MFS

Uvigerina 557.5 60 560 1060 LSF uHST 1057.95 abundant 11.7 Ma TST NN3 70 ? 570 1070 13.8 Ma 70.6

Fluvial/ LSF Estuarine

15.0 Ma Mid DN7

80 575.2/580 1080 580 18.4/ USF/Est. 19.4 Ma

86.85 dUSF NN3 90 590 13.1 Ma 1090

dUSF uHST Beaverdam Formation

100 Fluvial 600 1100 Offshore lHST 13.4 Ma LSF FS 16.4 Ma 110 610 1110 pUSF NN2 Estuarine

120 117.5 620 1120

16.5 Ma Fluvial/ dUSF 19.1/ lHST 19.0 Ma L L Estuarine 130 630 1130 (ECDZ1)

dUSF Bethany formation USF uHST

170 670 HST 1170

TST USF

pUSF dUSF 180 680 1180 14.1 Ma ? 185.6 LSF 190 Lower 690 1190 shoreface Aquifer 13.4 Ma LSF Cheswold MFS? In. neritic ? pLSF 197.4

200 Lower 700 698.5 1200 shoreface g g 15.8 Ma LSF FS L

210 710 Choptank Formation 1210 g 14.3 Ma g g g FS/SB dLSF 220 720 1220 Calvert Formation 15.9 Ma L g

L HST LSF g 230 LLL 730 1230 g g

15.8 Ma 20.6 Ma 240 740 1240 g

g 16.2 Ma 250 750 1250 g

Manokin aquifer MFS Upper shoreface/

Foreshore/Lower estuarine g 20.7 Ma Offshore 260 760 1260 g 16.0 Ma Offshore g g 270 770 TST 1270 16.0 Ma LSF g L L g 280 780 1280 ?p dUSF g 787.1 290 790 pUSF 1290 lHST 16.5 Ma 20.3/ ?p 20.3 Ma 294.1

300 800 1300

uHST

17.3 Ma 310 810 1310 NN2 Milford Aquifer

dLSF p p 20.4 Ma LL L p FS/SB

320 820 1320 g g 1317.45 g

g 330 830 1330 16.5 Ma Offshore HST Manokin formation g Distal upper shoreface 340 840 1340 17.1 Ma g

g 350 850 1350 g Offshore lHST gg

g 16.7 Ma g 360 860 1360 g 20.5 Ma g dLSF g 370 MFS 870 1370 TST g 374 g 9.9 380 880 1380 g 9.8 20.7 Ma

MFS g 390 890 17.1 Ma 1390 Lower

shoreface dLSF TST g 10.3 g g 400 900 897.7 1400 g 17.1 Ma 20.9 Ma

9.9 HST g Offshore 410 910 1410 17.7 Ma dUSF uHST g

MFS 9.6 21.0 Ma TST

420 920 Calvert Formation 1420 1421.1 uHST g NN2? Offshore 18.1 Ma g MFS

Offshore/ TST LSF g g 430 Middle neritic 930 1430 g 11.7 g 21.0 Ma 1430.5 lHST

dUSF HST

440 940 FS 1440 Offshore 18.2 Ma pUSF MFS lHST g MFS LSF/Off TST 450 10.5 950 FS 1450 ggg TST 18.3 Ma g pUSF g

452.45 g

HST Clayey Glauconite Sand g 1454.5 MFS dUSF lHST ggg Offshore 460 960 1460 Unnamed Glauconitic Clays and Offshore g g g TST 18.8 Ma MFS g g g 28.0 Ma Offshore 18.5 Ma LSF/Off 1465.7 Unnamed 470 970 1470 Foraminiferal TD 1470 TST Clay LSF gg 9.6 FS 18.4 Ma 480 HST 980 981.3 Offshore/Middle neritic St. Marys Formation

490 990 USF

18.6 Ma

500 1000 1000