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Netherlands Journal of Geosciences / Geologie en Mijnbouw 82 (3): 225-231 (2003)

Oligotrophic oceans and minimalist organisms: collapse of the marine ecosystem and recovery in the -Tertiary sequence of

W.B. Gallagher1

1 New Jersey State Museum,TRENTON, New Jersey 08625-0530, USA; and Department of Geological Sciences, Rutgers University, PISCATAWAY, New Jersey 08855, USA; "^ •"•" e-mail: [email protected] l^^ I

Manuscript received: June 2000; accepted in revised form: October 2001 | G

Abstract

The inner Atlantic Coastal Plain of New Jersey reveals exposures of fossiliferous Maastrichtian and deposits. Recent discoveries in this interval are here reported, and placed in the context of Cretaceous/Tertiary (K/T) faunal changes. The exposure at the Inversand Pit at Sewell (New Jersey) is the last active marl mine in the region, and stands as an important reference section for the many significant discoveries of vertebrate produced by the marl mining industry at its zenith. Changes in planktonic populations across the K7T boundary are related to Maastrichtian/Danian marine ecosystem commu­ nity reorganisation, by demonstrating changes in abundance of dominant marine invertebrates in successive fossil assem­ blages. Marine invertebrates with non-planktotrophic larval stages were briefly the commonest fossils preserved in the Danian sediments of this region. Late surviving examples of Cretaceous fauna now restricted to the Indo-Pacific region may imply biogeographic changes linked to the R7T mass extinction .

Keywords: Maastrichtian, Danian, K/T boundary, faunal assemblages, New Jersey

Introduction sils in . At Haddonfield (Camden County), the site of the discovery of Hadrosaurus New Jersey played a prominent role in the early de­ foulkii was an old marl pit that yielded the most com­ velopment of the science of palaeontology in North plete skeleton of a known at that (Lei- America, and although the fossiliferous deposits of dy, 1858). Since then, the marl deposits have yielded the New Jersey Coastal Plain have been studied for numerous specimens to private and professional col­ two centuries, new discoveries and interpretations are lectors. Fossils of Maastrichtian are found in the still emerging from these classic sections. The inner Monmouth Group, consisting of the Mount Laurel, Coastal Plain of New Jersey is underlain by deposits Navesink, Red Bank and Tinton formations, in as­ of and Early age (Fig. 1); cending order (Table 1). Typical Maastrichtian taxa these beds contain an abundant record of life at the include the bivalve genera Exogyra, Pycnodonte, and end of the . Some of the most fos­ Agerostrea, belemnite guards (Belemnitella americana), siliferous deposits are the beds of glauconite which the small brachiopod Choristothyris plicata, and were widely mined as fertiliser in the nineteenth cen­ teeth of several [Scapanorhynchus texanus, tury. pristodontus, Cretolamna appendiculata], The greensand marl pits produced many of the ear­ plus scrappy remains of various vertebrates. liest discoveries of and other vertebrate fos­ Recently, Miller et al. (1999) have interpreted the

Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 225 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813 Table. 1. Stratigraphy of Atlantic Coastal Plain in New Jersey.

PERIOD GROUP FORMATION

Quaternary Cape May

Tertiary Pensauken

Miocene Cohansey Kirkwood

Eocene Shark River Manasquan

Paleocene Rancocas Vincentown Hornerstown

. K/T boundary

Cretaceous Late Monmouth Tinton Red Bank Navesink Mount Laurel

Matawan Wenonah Marshalltown Englishtown Woodbury Merchantville

Magothy Raritan

Table 2. Formations, dominant fossils, and reproductive types in the inner Coastal Plain K/T section of New Jersey.

Horizon Fossils Reproductive type 75°00

Vincentown bryozoans non-planktotroph Fig. 1. Outcrop belt of Upper Cretaceous-Paleocene sediments in Oleneothyris brachiopod non-planktotroph the Atlantic Coastal Plain of New Jersey; the cross marks the loca­ Hornerstown sponges, brachiopods non-planktotroph tion of the Inversand Pit. MFL oysters, clams planktotroph Navesink oysters planktotroph Mount Laurel-Navesink contact as a sequence Mt Laurel (top) clams planktotroph boundary caused by glacio-eustatic sea level fall, with Marshalltown oysters planktotroph the novel conclusion that continental glaciation was a driving sea level change as far back as the Late Creta­ ceous. Certainly, our taphonomic studies support the Cretaceous multituberculate incisor (Grandstaff et idea of falling sea level in the upper Mount Laurel, al.,2000). and the contact between the two formations is quite The Red Bank and Tinton formations have limited abrupt. Just below the contact, a concentration of fos­ areal extent in Monmouth County before pinching sils comprises abundant fossil vertebrate remains, pri­ out to the southeast. In the southern part of the out­ marily chondrichthyan and material, as well crop belt, the Navesink Formation is directly overlain as an invertebrate assemblage dominated by inoce- by the , the bulk of which is ramids and ammonites. The superjacent Navesink Danian in age. Paleocene deposits are combined into Formation is a transgressive unit containing several the Rancocas Group, including the Hornerstown and oyster bed assemblages in its greensand marl. Recent­ Vincentown formations. The Red Bank Formation ly discovered, noteworthy finds in the Monmouth has yielded Maastrichtian fossils, primarily the bi­ Group marl beds of Late Cretaceous age include a valve Cucullaea and shark teeth. The boundary be­ hollow coelurosaurian long bone shaft, the first lung- tween the inner Coastal Plain underlain by Upper jaw plate known from the Upper Cretaceous of Cretaceous and Lower Cenozoic strata, and the outer North America (Parris et al., 2001), and a possible Coastal Plain composed of younger Cenozoic sedi-

226 Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813 Table 3. Faunal list for the Inversand Pit, Mantua Township, Gloucester County, New Jersey.

Navesink Formation (Maastrichtian) Basal Hornerstown Formation (MFL) Osteopygis emarginatus Cope Peretresius cf. emarginatus Leidy Porifera Brachiopoda Crocodylia Cliona cretacea Fenton & Fenton Terebratulina atlantica Morton rogersii Owen Brachiopoda Diplocynodon sp. Choristothyris plicata (Say) Nuculana stephensoni Richards cf. Procaimanoidea sp. Bryozoa Cucullaea vulgaris Morton Bottosaurus harlani Meyer indeterminate encrusting bryozoans Glycymeris mortoni (Conrad) Thoracosaurus neocesariensis (DeKay) Bivalvia Gervilliopsis ensiformis (Conrad) Squamata Cucullaea antrosa Morton Pycnodonte dissimilaris sp. Cucullaea neglecta Gabb Gryphaeostrea vomer Morton indeterminate mosasaurids Cucullaea vulgaris Morton Veniella conradi Morton Aves Glycymeris mortoni (Conrad) Cardium tenuistriatumWhitfield Telmatornis priscus Marsh Agerostrea nasuta (Morton) Etea delawarensis (Gabb) Paleotringa littoralis Marsh Pycnodonte convexa (Say) Crassatellites vadosus (Morton) Graculavis velox Marsh Gryphaeostrea vomer Morton Panopea decisa Conrad indeterminate Exogyra costata Say Lithophaga ripleyana Gabb Trigonia mortoni Whitfield Xylophagella irregularis (Gabb) Crassatellites vadosus (Morton) Gastropoda Middle Hornerstown Formation fossil Liopistha protexta (Conrad) Lunatia halli Gabb assemblage Spondylus (Dianchora) echinata (Morton) Gyrodes abyssinus Morton Pachycardium spillmani (Conrad) Turritella vertebroides Morton Porifera Solemya cf. lineolatus Conrad Anchura abrupta Conrad Peridonella dichotoma Gabb Lithophaga ripleyana Gabb Volutoderma ovata Whitfield Cnidaria Gastropoda Turbinella subconica Gabb Flabellum mortoni Vaughan Lunatia halli Gabb Turbinella parva Gabb Brachiopoda Gyrodes petrosus (Morton) Pyropsis trochiformis (Tuomey) Oleneothyris harlani forma manasquani Turritella cf. vertebroides Morton Acteon cretacea Gabb Stenzel Anchura cf. abrupta Conrad Nautilida Bivalvia Anchura pennata (Morton) dekayi (Morton) Cucullaea macrodonta Whitfield Pyrifusus macfarlandiWhitfield Ostrea glandiformisWhitfie\d Turbinopsis curta Whitfield Baculites sp. Crassatellites cf. littoralis Conrad Volutomorpha ponderosa Whitfield Pachydiscus {Neodesmoceras) sp. Caryatis veta Whitfield Nautilida Sphenodiscus lobatus (Tuomey) Gastropoda Eutrephoceras dekayi Morton Crustacea cf. Volutacorbis sp. Ammonoidea cf. Hoploparia sp. Nautilida Baculites ovatus Say cf. sp. Discoscaphites conradi (Morton) Edaphodon stenobyrus (Cope) Chondrichthyes Echinodermata Edaphodon mirificus Leidy Edaphodon agassizi (Buckland) Hemiaster sp. Ischyodus thurmanni Pictet & Campiche Odontaspis sp. Chondrichthyes Squatina sp. Otodus obliquus (Agassiz) Squalicorax pristodontus (Agassiz) Squalicorax pristodontus (Agassiz) Paleocarcharodon sp. Odontaspis sp. Cretolamna appendiculata (Agassiz) Chelonia Osteichthyes Odontaspis cuspidata (Agassiz) Dollochelys sp. ferox Leidy indeterminate elasmobranchs (teeth, Crocodylia Anomoeodus phaseolus (Hay) vertebrae) Hyposaurus rogersii Owen indeterminate large QXiphactinus) Rhombodus levis Cappetta & Case Chelonia Rhinoptera sp. Peretresius ornatus Leidy Myliobatis cf. leidyi Hay indeterminate cheloniids indeterminate batomorphs (vertebrae) Squamata Osteichthyes Bryozoa Halisaurus platyspondylus Marsh Acipenser cf. albertensis Lambe indeterminate encrusting bryozoans Mosasaurus maximus Cope (= M. hoffman- Enchodus ferox Leidy Bivalvia ni Mantell) cf. Bananogmus sp. Polorthus tibialis (Morton) Mosasaurus sp. indeterminate (vertebrae) Prognathodon rapax (Hay) Chelonia Dinosauria Taphrosphys sulcatus Leidy Hadrosaurus minor Marsh cf. Bothremys sp. indeterminate ?lambeosaurine Adocus beams Leidy Agomphus turgidus Cope Dollochelys atlantica (Zangerl)

Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 227 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813 Fig. 2. Exposures of the Maastricht- ian through section at the Inversand Pit, Sewell (New Jersey). The vehicle's tyres rest approximate­ ly on the K/T contact.

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ments is marked by a cuesta, a low discontinuous ridge often capped by Plio-Pleistocene gravels. Today, much of this section is exposed only in ero- Pensauken Fm sional stream cuts through the Maastrichtian-Danian XT—- beds, as well as in one surviving marl mining opera­ tion. The available sections have been studied and Kirkwood Fm collected in detail by New Jersey State Museum workers (Gallagher, 1991, 1993; Gallagher et al., O-O OOP Q-. 1986). This work has helped reveal some of the pa- laeoecological details of the faunal changes associated with the K/T boundary in this part of the world.

Vincentown Fm The Inversand Pit

The mining of greensand marl was a widespread in­ dustry in the nineteenth century, and numerous fos­ sils were obtained from the extensive excavations into the marl deposits surrounding the K/T boundary. At this time, glauconite was used as a long- soil con­ ditioner to enhance the yield of crops. Today, glau­ © W&&- S •

228 Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813 at the pit, ranging in age from the Maastrichtian oys­ The MFL at the base of the Hornerstown Forma­ ter bank assemblage in the Navesink Formation at the tion also contains a diverse molluscan fauna (26 bottom, through the basal Hornerstown layer to the species). The commonest amongst them is the thin- Danian layer in the middle part of the Hornerstown shelled, fragile oyster Pycnodonte dissimilaris, which Formation (Fig. 3). can be seen in abundance at outcrop, but which is The fossil faunas bridge the K/T boundary, and in very difficult to collect intact because of its delicacy. New Jersey the pit provides our best view in outcrop Often, if examined under the microscope, the oyster of this critical stratigraphic interval with its record of shells will show a patchy coating of bornite. This palaeoecological change. The precise relationship of mineralisation is probably why they yield an anom­ the Navesink and Hornerstown formations has been a alous stable strontium isotope age estimation. The minor controversy here, with United States Geologi­ next most abundant invertebrate is Cucullaea vulgaris. cal Survey (USGS) workers favouring an angular un­ Amongst gastropods, Turritella vertebroides and Pyrop- conformity between the two formations at their con­ sis trochiformis are the commonest. There are also tact (Owens et al., 1970), while others have proposed ammonite remains of several species, mostly in the differing interpretations (Gallagher et al., 1986; Gal­ form of broken and worn internal moulds. Overall, lagher, 1993). Currently, we think that the contact the molluscan fauna has decidedly Cretaceous affini­ between the Navesink and Hornerstown at this pit is ties. more accurately characterised as a disconformity or Vertebrates from the MFL are more diverse than in paraconformity; the precise boundary is smeared out the other two layers, and include a variety of chon- by bioturbation and the contact is usually more obvi­ drichthyans, bony fish, , crocodiles, , ous from a distance. The contact is certainly a se­ and birds, for a total of over 30 species. Certain ele­ quence boundary, with the overlying Hornerstown ments of this assemblage, i.e. Squalicorax pristodontus, representing the transgressive phase of the next cycle. Enchodus and mosasaurs, are characteristic Creta­ There may be missing section here, certainly in com­ ceous forms, while other taxa, e.g. turtles and croco­ parison to the downdip Bass River Core section diles, are less distinctively Mesozoic. which has a complete K/T sequence in the subsur­ Above this horizon an occasional floating shark face, including an impact ejecta layer (Olsson et al., or rare crocodile remains may be met with, but 1997). However, while lithostratigraphically there is a the section is essentially barren for two metres until break at the contact in the pit exposure, biostrati- another concentration of fossils occurs. This layer is graphically the basal fossiliferous layer, occasionally well exposed just now in the new excavation at the called the Main Fossiliferous Layer (MFL), in the pit, and it is significant for how it differs from the un­ lower Hornerstown Formation contains the last re­ derlying beds. Molluscs have been reduced in size, mains of Cretaceous organisms. The time gap is prob­ abundance, and diversity (6 species).The most abun­ ably an order of magnitude less than the amount of dant bioclasts are sponges, brachiopods, and solitary missing time implied by an angular unconformity; , each group represented by just one species. during this interval the MFL concentration accumu­ While the concentration of fossils is clumpy and the lated as a condensed section lag deposit. Thus, in the shape of the layer somewhat irregular, the continuity pit there is a typical Mesozoic marine community at of the concentration is apparent and the abundance the bottom in the Navesink Formation, a transitional of the fossils impressive. Vertebrates are rare, with assemblage in the MFL, and an unusual Danian fau­ small lamnid shark teeth the most frequently found na in the middle of the Hornerstown, giving us some specimens. insight into the nature of faunal changes across the At and above the level of the Hornerstown-Vincen- K/T boundary in New Jersey. town formational contact, there is in other sites a con­ The Navesink shell bed at the base of the pit is centration of the large terebratulid brachiopod Ole- characterised by a diversity of molluscs (26 species; neothyris harlani. This remarkable density of bra­ Gallagher et al., 1986) associated with the standard chiopods occurs sporadically where the same level is concentration of oysters, including Exogyra costata, exposed along strike as far to the south as southeast­ Pycnodonte convexa, Agerostrea falcata, and Gryphaeo- ern . In the upper part of the Vincen- strea vomer. The large arc shell, Cucullaea antrosa, is town Formation, glauconite content decreases and is found at in the upper part of the Navesink. replaced by quartz sands and patchy occurrences of Rarely, the small brachiopod Choristothyris plicata is bryozoan limestone. Diversity rebounds to pre-Dan- encountered. Vertebrates include infrequent shark ian levels, especially in the limestone beds at the top teeth, teeth and portions of jaw of Enchodus ferox, tur­ of the formation; these are interpreted here as a patch tles, mosasaurs, and dinosaurs. reef ecosystem (Gallagher, 1993).

Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 229 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813 Discussion eral have lower food requirements and lower metabo­ lism than other exoskeletonised benthos (Thayer, Mass extinctions in the marine realm are often 1981). The abundance of a single species such as Ole­ marked by reductions in the diversity and abundance neothyris harlani over a wide area after the K/T event of plankton. Diversity reduction among the plankton suggests it was an opportunistic species that could has been documented in the literature for the Fras- thrive in the oligotrophic ocean of the Danian. nian/Famennian event, the Permo- mass ex­ Hypothesized effects of large body impacts such as tinction, and the K/T boundary. The effects of this reduction in solar radiation reaching the earth's sur­ population crash at the base of the food chain should face, acid rain, and near-destruction of the ozone lay­ reverberate upwards to higher levels of the trophic er would all have negative effects on the plankton pyramid. What evidence can we see in the fossil population. As Olsson & Liu (1993) have shown, only record of mass extinctions for confirmation of this hy­ three species of planktonic foraminifera survived the pothesis?. K/T boundary. The resulting Danian marine commu­ Across the K/T boundary in eastern North Ameri­ nity would have to be adapted to severe reduction in ca, there is evidence for a resetting of the evolutionary food resources in an oligotrophic ocean, especially in in Danian marine ecosystems which are domi­ waters closer to the Chicxulub impact site, for exam­ nated by faunas of Palaeozoic aspect. Widespread di­ ple in eastern North America. Such a pattern is verse Cretaceous molluscan assemblages are replaced demonstrated in the minimalist assemblage of the temporarily in the Danian by a sponge-brachiopod- Danian of the Atlantic Coastal Plain. dominated assemblage. In particular, fossil con­ The plankton crash also probably affected those or­ centrations in the K/T section of the Atlantic Coastal ganisms that reproduced by means of planktotrophic Plain show a diverse oyster bank ecosystem replaced larvae. Normally, wide dispersal patterns and large by a brachiopod-dominated shell gravel where large numbers of planktotrophic larvae were favoured dur­ terebratulids of a single species (Oleneothyris harlani) ing times of high planktonic productivity. But, when may form up to 99%+ of the bioclasts. The Oleneo­ the planktonic populations crashed at the K/T thyris Zone can be traced from New Jersey in the boundary, those organisms that depended upon a de­ north down into southeastern North Carolina at the velopmental in the plankton were severely af­ same level in Paleocene outcrops. A sponge (Peri- fected. This explains why ammonites, which were donella dichotoma) and a solitary coral {Flabellum mor- planktotrophic reproducers, went extinct while nau- toni) often accompany the brachiopods (see Table 2). tiloids, which lay lecithotrophic eggs on the sea bot­ Dwarfed bivalves form an insignificant proportion of tom, survived. Brachiopods are larval brooders, while this fauna. sponges are able to reproduce asexually. During and immediately after the Frasnian-Famen- Dwarfing among Danian benthos may be explained nian mass extinction, hexactinellid sponges proliferat­ as a response to lower plankton levels in the post-K/T ed and diversified while numerous other groups were boundary ocean. Danian representatives of Maas- being decimated (McGhee, 1996). After the most se­ trichtian molluscan genera are generally smaller, if vere extinction event, the Permo-Triassic, demo- they survive at all (e.g. Pycnodonte, Cucullaea). In Rus­ sponges became important in the Triassic. Again, af­ sia, echinoids show dwarfing across the K/T bound­ ter the Triassic/ mass extinction, sponges are ary (Markov & Solovjev, 1997), and dwarfing has part of the reef community in the Jurassic. been established as a common feature of earliest Pale­ Sponges are minimalist organisms, able to filter up ocene marine faunas. to 10,000 to 20,000 times their own body volume of The niche of durophagous predator was an impor­ water per (Rigby, 1983). They specialise in ex­ tant trophic level in the Cretaceous marine food web. tracting smaller bits of nutrients from the water col­ There were a variety of shell-crushing tak­ umn. In mass extinction events such as the K/T ing advantage of the rich food resources of Creta­ event, the kinds of plankton (e.g. foraminifera) left ceous molluscs and crustaceans. Chimaerids, rays, over after the event are generally smaller than the certain , various bony fish species, some turtles larger and more ornate forms found prior to the ex­ and a few mosasaurs {Globidens, ) show tinction. Therefore sponges are likely to be favoured jaws or dentition adapted for shell crushing. By con­ as survivors since they are more effective at filtering trast, marine predators of the Paleocene tend to be out small particles, and at processing large amounts more generalised carnivores such as crocodiles or of water for these particles. lamnid sharks. Durophagy survived as a niche, but in Brachiopods are also minimalist organisms. They the Danian opportunistic predators with broader are able to survive at lower oxygen levels, and in gen­ tastes predominated. The scarce resources of the early

230 Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813 ceedings of the Academy of Natural Sciences of Philadelphia 10: Paleocene oligotrophic ocean affected specialised 215-218. predators. While mosasaurs are the dominant large Markov, A.V. & Solovjev, A.N., 1997. Echinoids at the Creta- predators in the Maastrichtian marine realm, the ear­ ceous/ Boundary. In: Rozanov, A.Yu., Vickers-Rich, P. ly Danian beds in New Jersey show an increase in & Tassell, C. (Eds): Evolution of the biosphere. Records of the crocodilian fossils. In the aftermath of the extinction, Queen Victoria Museum 104: 35-37. crocodilians became the large dominant marine McGhee, G.R., 1996. The Late Mass Extinction: the Frasnian/Famennian crisis. Columbia University Press (New predators. This 'crocodile spike' reflects an ecological York): 303 pp. replacement at the level of apical marine predator. Miller, K.G., Barrera, E., Olsson, R.K., Sugarman, PJ. & Savin, This general pattern of extinction and survival S.M., 1999. Does ice drive early Maastrichtian eustacy?. Geolo­ across the K/T boundary provides a model for the gy 27: 783-786. collapse of marine ecosystems under stresses generat­ Olsson, R.K. & Liu, C, 1993. Controversies on the placement of Cretaceous-Paleogene boundary and the K/P mass extinction of ed by large-scale environmental disturbance, such as planktonic foraminifera. Palaios 8: 127-139. an asteroid impact. Such a pattern should be zonally Olsson, R.K., Miller, K.G., Browning, J.V, Habib, D. & Sugarman, distributed, reflecting decreasing intensity of impact P.J., 1997. Ejecta layer at the Cretaceous-Tertiary boundary, effects further away from the crater. Preliminary Bass River, New Jersey (Ocean Drilling Program Leg 174AX). proof for this comes from new Late Cretaceous fossil Geology 25: 759-762. Owens, J.P., Minard, J.P., Sohl, N.F. & Mello, J.F., 1970. Stratigra­ discoveries in eastern North America; coelacanths phy of the outcropping post-Magothy Upper Cretaceous forma­ and lungfish of Late Cretaceous age were wiped out tions in southern New Jersey and northern Delmarva Peninsula, in this part of the world but survived at the antipodes Delaware and Maryland. United States Geological Survey, Pro­ of the impact in the Indo-Australian region. This idea fessional Paper 674: 1-60. is also supported by the distribution of other well- Parris, D.C, Grandstaff, B.S. & Gallagher, W.B., 2001. A lungfish (dipnoan) from the Upper Cretaceous of New Jersey. Journal of known living fossils such as the bivalve Neotrigonia, vertebrate 21 (Supplement to 3): 87A. various plant families, and marsupials. Rigby, J.K., 1983. Introduction to the Porifera. In: Rigby, J.K. & Stearn, C.W. (Eds): Sponges and spongiomorphs. University of Acknowledgments , Department of Geological Sciences (Knoxville), Studies in Geology 7: 1-11. Thayer, C.W., 1981. Ecology of living brachiopods. In: Dutro, J.T. I wish to thank David C. Parris (New Jersey State & Boardman, R.S. (Eds): Lophophorates. University of Ten­ Museum) and the Inversand Company of Clayton nessee, Department of Geological Sciences (Knoxville), Studies (NJ) for their encouragement of this work. Thanks al­ in Geology 5: 110-126. so to the numerous people who have helped in this ef­ fort over the , through assistance in the field, useful discussions, and donation of specimens, in­ cluding James Barnett, Joseph and Sandra Camburn, Gudni Fabian, Ned Gilmore, Barbara Grandstaff, Paul Hanczaryk, Margaret Martinson, Richard Ols­ son, Earle Spamer, and Chris Storck. This project is supported through the Horace G. Richards Fund of the Friends of the New Jersey State Museum.

References

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Netherlands Journal of Geosciences / Geologie en Mijnbouw 82(3) 2003 231 Downloaded from https://www.cambridge.org/core. IP address: 170.106.202.8, on 01 Oct 2021 at 20:30:31, subject to the Cambridge Core terms of use, available at https://www.cambridge.org/core/terms. https://doi.org/10.1017/S0016774600020813