Abstract Volume 2Nd IGCP608 Waseda, Japan

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The second International Symposium of International Geoscience Programme (IGCP) Project 608 “Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and Western Pacific”

Abstract volume 2nd IGCP608 Waseda, Japan

“Land-Ocean Linkages and Biotic Evolution during the Cretaceous: Contribution from Asia and Western Pacific”

Edited by: Organizing Committee of the 2nd International Symposium of IGCP608 The Second International Symposium of International Geoscience Programme (IGCP) Project 608 “Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific”

Program and Abstracts

Land-Ocean Linkages and Biotic Evolution during the

Cretaceous: Contribution from Asia and Western Pacific

September 4-6, 2014 Tokyo, JAPAN

Edited by Organizing and Scientific Committee of the IGCP 608

1 EXECUTIVES AND ORGANIZING COMMITTEE

IGCP 608 Project Leaders: Prof. Hisao Ando (Leader) Department of Earth Sciences, Ibaraki University, Japan Prof. Xiaoqiao Wan (Co-Leader) School of Geosciences and Resources, China University of Geosciences, China, P.R. Prof. Daekyo, Cheong (Co-Leader) Department of Geology, College of Natural Sciences, Kangwon National University, Korea Prof. Sunil Bajpai (Co-Leader) Birbal Sahni Institute of Palaeobotany, Lucknow, India

Symposium Organizing Committee: Organizing Committee of the Second International Symposium of IGCP608 Prof. Hisao Ando, Ibaraki University (Chairman) Prof. Hiromichi Hirano, Waseda University (Vice-chairman) (deceased on 5 May, 2014) Prof. Takashi Hasegawa, Kanazawa University (Vice-chairman) Dr. Tohru Ohta, Waseda University (Secretary General) Prof. Hideo Takagi, Waseda University Prof. Ren Hirayama, Waseda University Dr. Mizuki Murakami, Waseda University (Secretary) Dr. Kazuma Seike, Waseda University (Secretary) Dr. Hitoshi Hasegawa, Nagoya University (Secretary) Dr. Kazuyoshi Moriya, Kanazawa University (Secretary) Dr. Seiichi Toshimitsu, Geological Survey of Japan Dr. Masanobu Yamamoto, Hokkaido University

Scientific Advisory Board: Prof. Yong Il Lee, Seoul National University, Korea Prof. Min Huh, Chonnam National University, Korea Prof. Hiroshi Nishi, Tohoku University, Japan Prof. Yasufumi Iryu, Tohoku University, Japan Dr. Junichiro Kuroda, JAMSTEC, Japan Dr. James W. Haggart, Canada

Co-Organizing Agency: School of Education, Waseda University Department of Earth Sciences, School of Education, Waseda University School of International Liberal Studies, Waseda University Ibaraki University Geological Survey of Japan, National Institute of Advanced Industrial Science and Technology The Geological Society of Japan Palaeontological Society of Japan Sedimentological Society of Japan Japanese Geoparks Network

Sponsors: UNESCO-IGCP Tokyo Geographical Society Inoue Foundation for Science J-DESC (Japan Drilling Earth Science Consortium)

INPEX Corporation, Japan Petroleum Exploration, JX Nippon Oil and Gas Exploration, Mitsubishi Corporation Exploration, Mitsui Oil Exploration Oyo Corporation, Meiji Consultants, DIA Consultants, Chuo Kaihatsu, Daito Consultants, Kiso Jiban Consultants, Daito Consultants, Sanbonsugi Geo-tec.

2 SYMPOSIUM PROGRAM

09:00 - 09:40 Registration

DAY 1: SEPTEMBER 4

09:40 - 11:00 Opening Session Chairperson: Dr. Tohru Ohta 09:40 - 09:50 Welcome speech Prof. Yasufumi Iryu (President of the Geological Society of Japan)

09:50 - 10:20 Opening address Prof. Hisao Ando (IGCP608 Project Leader)

10:20 - 11:00 Keynote Speech James W. Haggart: Biostratigraphy, paleoenvironments, and tectonic setting of the Cretaceous System of Pacific coast North America: towards a circum-North Pacific integrated correlation framework

11:00 - 11:25 Group Photo & Coffee Break

Session 1: OAE phenomena contributed from Asian and Western Pacific Records – I Chairpersons: Prof. Allan G.S. Fernando and Prof. Hiroshi Nishi

11:25 - 11:45 Kazuyoshi Moriya Prof. Hirano’s contribution to natural sciences of Oceanic Anoxic Events: Phyletic evolution of desmoceratine ammonoids through the Cenomanian–Turonian oceanic anoxic event

11:45 - 12:05 Junichiro Kuroda Radiogenic isotopic records of Early Cretaceous marine sediments: implications for large igneous provinces and the Aptian climatic crisis (Kuroda, J., Tanimizu, M., Tejada, M.L.G., Hori, R.S., Suzuki, K., Ogawa, N.O., Coffin, M.F. and Ohkouchi, N.)

12:05 - 12:45 David Selby Keynote Speech: High-resolution 187Os/188Os isotope stratigraphy and 206Pb/238U zircon geochronology reveal and verify the global occurrence of OAE 2: Yezo Group, Hokkaido, Japan (Du Vivier, A.D.C., Selby, D., Condon, D.J., Takashima, R. and Nishi, H.)

12:45 - 13:50 Lunch

Session 2: OAE phenomena contributed from Asian and Western Pacific Records - II Chairpersons: Dr. David Selby and Dr. Junichiro Kuroda

13:50 - 14:10 Hiroshi Nishi Integrated Stratigraphy and U-Pb ages of the Cretaceous Yezo Group, exposed in Hokkaido, Japan (Nishi, H., Takashima, R., Yamanaka, T., Orihashi, Y. and Hayashi, K.)

14:10 - 14:30 Naohiko Ohkouchi A fingerprint of primary producers during the OAEs (Ohkouchi, N., Ogawa, N.O., Kashiyama, Y. and Kuroda, J.) 3 14:30 - 14:50 Takuto Ando Primary producer community during the mid-Cretaceous oceanic anoxic events (OAEs) evaluated from algal biomarkers in sediments deposited in the Vocontian Basin, SE France (Ando, T., Sawada, K., Takashima, R. and Nishi, H.)

14:50 - 15:10 Hideko Takayanagi A newly identified positive excursion of 87Sr/86Sr ratio in the Lower Aptian platform carbonates offshore Abu Dhabi, UAE: Is it a local or global signature of Ocean Anoxic Event 1a? (Yamamoto, K., Ishibashi, M., Takayanagi, H., Asahara, Y., Sato, T., Nishi, H. and Iryu, Y.)

15:10 - 15:30 Clarence Magtoto Calcareous nannofossil biostratigraphy of the Cenomanian-Turonian Oceanic Anoxic Event 2 (OAE2) record in California, USA (Clarence Magtoto, Fernando, A.G.S., Takashima, R., Nishi, H. and Tomosugi, T.)

15:30 - 15:50 Takashi Hasegawa Another world of OAE2: development of oxic water around Pacific margin

15:50 - 16:10 Coffee Break

Session 3: Biotic evolution: Asian and Western Pacific fauna and flora I - Microfauna Chairpersons: Dr. Bandana Samant and Prof. Takashi Hasegawa

16:10 - 16:30 Allan G.S. Fernando Updates on Philippine Cretaceous system: Recent calcareous nannofossil biostratigraphic studies on selected Cretaceous localities in the Philippines (Fernando, A.G.S., Magtoto, C.Y., Guballa, J.D.S., Marquez-Ardiente, D.J., Nogot, J.R.C.P. and Uy, M.A.C.)

16:30 - 16:50 Kenji Kashiwagi Mesozoic and Paleozoic radiolarians from the Lower Cretaceous Choshi Group, Japan (Kashiwagi, K., Isaji, S. and Asai, H.)

16:50 - 17:10 Zaw Win Early Cretaceous foraminiferal fauna from the western margin of the Shan Plateau, Myanmar

18:00 - 20:00 Welcome Party (RIHGA Royal Hotel Tokyo)

4 DAY 2: SEPTEMBER 5

Session 4: Biotic evolution: Asian and Western Pacific fauna and flora II - Microflora Chairpersons: Dr. Kenji Kashiwagi

09:10 - 09:30 Jyotsana Rai Late Cretaceous calcareous nannofossils from Nimar Sandstone, Bagh area, central peninsular India (Rai, J., Garg R., Singh, A., Garg, S., Bajpai, S., Kapur, V.V., Agarwal, S. and Tripathi, S.C.)

09:30 - 09:50 Deepali Thakre Palynofloral changes across Cretaceous-Paleogene: A case study from Deccan Volcanic Sequence in Amarkantak Group of Central India (Thakre, D., Samant, B. and Mohabey, D.M.)

09:50 - 10:10 Bandana Samant Pattern of biodiversity changes in Late Cretaceous-Early Paleocene palynoflora of Deccan volcanic province (Samant, B. and Mohabey, D.M.)

10:10 - 10:30 Neeru Prakash First record of pollen organ genus Caytonanthus Thomas, from Early Cretaceous beds of South Rewa Gondwana Basin, India and its palaeogeographical significance (Prakash, N. and Das, N.)

10:30 - 10:50 Coffee Break

Chairpersons: Dr. Jyotsana Rai and Dr. Robert G. Jenkins

10:50 - 11:10 Kohei Yoshino Campanian-Maastrichtian palynomorph assemblages from East Asia (Yoshino, K., Matsuoka, A. and Wan, X.)

11:10 - 11:30 Valentina S. Markevich Evolution of morphotypes of triprojectate pollen during the Late Cretaceous-Paleocene of East Asia (Markevich, V.S. and Bugdaeva, E.)

11:30 - 11:50 Eugenia V. Bugdaeva The Cretaceous coal-forming plants of southern part of East Siberia and Russian Far East (Bugdaeva, E.V. and Markevich, V. S.)

11:50 - 13:00 Lunch

13:00 - 14:00 Poster Session I

5 Session 5: Geoparks highlighting Cretaceous Chairpersons: Dr. Masanobu Yamamoto and Dr. Kenichi Kurihara

14:00 - 14:20 Jim W. Haggart The Tumbler Ridge Aspiring Geopark, northeast British Columbia, Canada: the interrelation of significant geology, outstanding recreation potential, economic development, and strong community participation (Haggart, J.W., Helm, C.W., McCrea, R.T., Buckley, L.G., and Sharman, K.)

14:20 - 14:40 Min Huh Korean National Geoparks and tentative Global Geoparks in Korea: Mudeungsan Area and Korean Cretaceous Dinosaur Coast

14:40 - 15:00 Hideo Takagi Development of geopark activities of the past 10 years in Japan (Takagi, H. and Watanabe, M.)

Session 6: Land-ocean linkage: Correlation, sedimentology and paleoenvironments I Chairpersons: Prof. Sunil Bajpai and Prof. Atsushi Matsuoka

15:00 - 15:20 Galina Kirillova Cretaceous ecosystems of southeastern continental margin of Russia and their evolution

15:20 - 15:40 Boris Shurygin Isotopic evidence for earliest Cretaceous climate change: new data from Siberia (Shurygin, B.N., Dzyuba, O.S., Izokh, O.P. and Kosenko, I.N.)

15:40 - 16:00 Romain Amiot Early Cretaceous terrestrial climates in East Asia; long term and seasonal patterns inferred from the oxygen and carbon isotope co-positions of vertebrate apatite (Amiot, R., Kusuhashi, N., Buffetaut, E., Goedert, J., Hibino, T., Ikeda, T., Ikegami, N., Lécuyer, C., Philippe, M., Saegusa, H., Shibata, M., Shimojima, S. and Sonoda, T.)

16:00 - 16:20 Coffee Break

Chairpersons: Dr. Romain Amiot and and Dr. Hitoshi Hasegawa

16:20 - 16:40 Hitoshi Hasegawa Reconstruction of terrestrial paleo-hydrological change during the mid-Cretaceous “Supergreenhouse” period: Insights from the lacustrine records (Shinekhudag Fm.) of southeast Mongolia (Hasegawa, H., Ando, H., Ohta, T., Hasegawa, T., Yamamoto, M., Hasebe, N., Murata, T., Shinya, H., Li, G., Ichinnorov, N., Erdenetsogt, B. and Heimhofer, U.)

16:40 - 17:00 Robert G. Jenkins Evolution of photosynthetic ecosystem effects on chemosynthetic ecosystem in late Mesozoic

17:00 - 17:20 Kazuyoshi Moriya Deep/intermediate water formation along the Cretaceous Asian continental margin (Moriya, K., Moiroud, M., Pucéat, E., Donnadieu, Y., Bayon, G., Deconinck, J.-F. and Boyet, M.)

17:20 - 17:40 Atsushi Matsuoka Land–ocean linkage: pelagic materials in Mesozoic neritic–terrestrial sequences in East Asia (Matsuoka, A., Ito, T., Sakai, Y. and Nikaido, T.)

18:00 - 19:00 IGCP608 Business Meeting

DAY 3: SEPTEMBER 6

Session 7: Land-ocean linkage: Correlation, sedimentology and paleoenvironments II Chairpersons: Prof. Boris Shurygin and Dr. Shin-ichi Sano

09:10 - 09:30 Raghavendramurthy Nagendra Palaeotemperatures, palaeoclimate, plaeolatitude, palaeobathymetry and palaeocurrent appraisal of Cretaceous sediments of Cauvery Basin, South India (Nagendra, R., Zakharov, Y.D., Safronov, P.P., Smyshlyaeva, O.P., Popov, A.M., Shigeta, Y. and Venkateshwarlu, M.)

09:30 - 09:50 Syed A. Jafar Dynamics of terminal Cretaceous global biotic turnover

09:50 - 10:10 Sunil Bajpai Late Cretaceous ecosystems of peninsular India: An overview of current perspectives

10:10 - 10:30 Coffee Break

Session 8: Tectonic evolution and paleoenvironments of Asia and West Pacific Chairpersons: Prof. Yong Il Lee and Dr. Kazuyoshi Moriya

10:30 - 10:50 Hyojong Lee Tectonic and climatic controls on A/S ratio in a non-marine setting: an example from the Lower Cretaceous Sindong Group of the Gyeongsang Basin (southeastern Korea) (Lee, H. and Lee, Y.I.)

10:50 - 11:10 Carla Dimalanta Mesozoic fossil data from the “Eocene” Zambales Ophiolite (Dimalanta, C.B., Queaño, K.L., Salapare, R.C., Yumul, G.P.Jr., Marquez, E.J., Faustino-Eslava, D.V., Ramos, N.T. and Payot, B.D.)

11:10 - 11:30 Decibel V. Faustino-Eslava Implications to Central Philippine evolution from signatures of the Cretaceous Balud Ophiolitic Complex (Faustino-Eslava, D.V., Dimalanta, C.B., Queaño, K.L., Ramos, N.T., Payot, B.D., Manalo, P.C. and Yumul, G.P.Jr.)

11:30 - 11:50 Naing Maw Than Tectono-magmatic development of accreted West Burma Block from Gondwana Land

11:50 - 13:00 Lunch

13:00 - 14:00 Poster Session II

7 Session 9: Biotic evolution: Asian and Western Pacific fauna and flora – Macrofauna Chairpersons: Prof. G. V. R. Prasad and Prof. Ren Hirayama

14:00 - 14:20 Vipul Keerti Sharma Morphological details of a newly discovered Cretaceous echinoid species ‘Stereocidaris keertii’ (Smith, A. B., 2010)

14:20 - 14:40 Dhananjay M. Mohabey Eggs, nests and poops of Indian Late Cretaceous sauropods: behavior, habitat and diet (Mohabey, D.M. and Samant, B.)

14:40 - 15:00 M. Sadiq Malkani Titanosaurian sauropod dinosaurs from the Latest Cretaceous Vitakri Formation of Pakistan and their biogeographic link

15:00 - 15:20 Guntupalli V. R. Prasad New elasmobranch fauna from the Bagh Group, Narmada Valley, India - palaeobiogeographic context (Prasad G.V.R., Verma, V., Sahni, A., Priyadarshini, R.K. and Singh L.R.)

15:20 - 15:40 Coffee Break

Chairpersons: Dr. Dhananjay M. Mohabey and Dr. Tomoyuki Ohashi

15:40 - 16:00 Ai Takekawa Description of the Late Cretaceous Crocodylomorph, Shamosuchus from Mongolia (Takekawa, A., Hirayama, R. and Aoki, R.)

16:00 - 16:20 Masataka Yoshida Cranial morphology of a giant marine side-necked turtle (Pleurodira: Bothremididae) from the upper Cretaceous of Morocco (Yoshida, M. and Hirayama, R.)

16:20 - 16:40 Ren Hirayama Cranial morphology of Mesodermochelys (Testudines; Dermochelyidae) from the Upper Cretaceous Japan, with special reference to its feeding habitat

16:40 - 17:00 Masatoshi Sone Discovery of the first dinosaur fossils from Malaysia: spinosaurid theropod teeth from the non-marine Cretaceous of Pahang (Sone, M., Hirayama, R., Teng, Y.H., Yoshida, M. and Komatsu, T.)

Closing Session Chairperson: Dr. Tohru Ohta

17:00 - 17:20 Guobiao Li Introduction of the Third International Symposium of IGCP 608 in China

17:20 - 17:30 Hisao Ando Closing Address of the 2nd IGCP 608 Waseda, Tokyo, Japan

18:00 - 20:00 Farewell Party

8 POSTER SESSIONS

September 5 13:00 - 14:00 Core time September 6 13:00 - 14:00 Core time

Land-ocean linkage: Correlation, sedimentology and paleoenvironments

P1 Alyona V. Kurilenko and Yadrishchenskaya N.G. Lower Cretaceous deposits of southeastern Transbaikal

P2 Barsbold, R. and Yondon Khand Cretaceous of Mongolia

P3 Adiya Eviikhuu, Ichinnorov, N. and Gankhuyag, Ch. Geology and palynology of the Khetsuutsav area of south Mongolia

P4 Gombosuren Tsolmon, G., Uranbileg, L. and Ichinnorov, N. Paleobotanical and palynological characteristics of the Shivee-ovoo coal deposit, Central Mongolia

P5 Bat-Orshikh Erdenetsogt and Jargal, L. Fossil fuels hosted in Mesozoic sequences of Mongolia

P6 Takayuki Murata, Li, G., Ando, H., Hasegawa, H., Hasegawa, T., Ohta, T., Yamamoto, M., Hasebe, N. and Ichinnorov, N. Stratigraphic succession of Conchostracan fossils from the lacustrine deposits in the Shinekhudag area (Lower Cretaceous), Eastern Gobi basin, Southeast Mongolia

P7 Masanobu Yamamoto, Ando, H., Hasegawa, H., Hasegawa, T., Ohta, T., Hasebe, N., Murata, T., Li, G. and Ichinnorov, N. TEX86-based lake water temperatures in Jurassic and Cretaceous Mongolia

P8 Fujita Yusuke, Ohta, T. and Shinya, H. Base level and paleotemperature changes of Cretaceous lacustrine succession in southeast Mongolia

P9 Keita Arai, Ohta, T., Hirano, H., Harigaya, S., Sakai, T., Kozai, T. and Li, G. Paleoenviromental reconstruction of Cretaceous lacustrine succession in Xinjiang-Uygur Autonomous Region

P10 Gaku Sasaki and Ohta, T. Laboratory experiments for attesting the “weathering hypothesis” as a possible cause of the mid-Cretaceous Oceanic Anoxic Events

P11 Tohru Ohta, Kamigata, Y. and Takagi, H. Evidence of enhanced continental weathering during oceanic anoxic event 2 (OAE 2) in eastern continental margin of Asia

P12 Yosuke Kobiyama, Yonezawa, S., Suzuki, T. and Hasegawa, T. Bottom water paleothermometry: screening late Cretaceous calcareous nodules for application of oxygen isotope method

P13 Tsuyoshi Ito, Sakai, Y. Feng, Q.L. and Matsuoka, A. Denudation stages of mid-Mesozoic accretionary complexes in East Asia based on microfossil-bearing clasts within the Mesozoic strata

9 P14 Shin-ichi Sano New view of the Tetori Group in Central Japan: clues to the interregional correlation among the Early Cretaceous strata in East Asia?

P15 Lee, Y.I., Yi, J. and Choi Taejin Provenance analysis of Lower Cretaceous Sindong Group sandstones in the Gyeongsang Basin, Korea using integrated petrography, quartz SEM-cathodoluminescence, and zircon Zr/Hf analysis

P16 Ken Hirose and Ohta, T. Provenance analysis of clastic sediments of the Chichibu and Shimanto Belts in Okinawa Prefecture using modal and whole-rock chemical compositions

P17 Kentaro Oe and Ohta, T. Provenance analysis and paleoclimate reconstruction of the Khorat Group in northeastern Thailand using whole-rock chemical composition

Biotic evolution: Asian and Western Pacific fauna and flora

P18 Dhananjay M. Mohabey and Samant, B. Litho- and biofacies association of two Maastrichtian lakes across the earliest Deccan volcanic flow: environments and biota

P19 M. Sadiq Malkani Records of fauna and flora from the Latest Cretaceous of Pakistan: Evolution of Indo-Pakistan Peninsula (South Asia)

P20 M. Sadiq Malkani Theropd dinosaurs and mesoeucrocodiles from the Terminal Cretaceous of Pakistan: paleobiogeographic implications

P21 Chinzorig Tsogtbaatar and Tsogtbaatar, Kh. Preliminary study of the new juvenile dinosaur (Theropoda: Ornithomimosauria) from the Upper Cretaceous Baynshire Formation of Khongil Tsav, eastern Mongolia

P22 Momo Yamashita, Konishi, T. and Sato, T. Diving behavior of mosasaurs (Squamata: Mosasauridae) inferred from optics

P23 MasatakaYoshida and Hirayama, R. Functional morphology of unique feeding apparatus in the bothremydid turtles

P24 Teppei Sonoda, Azuma, Y., Hirayama, R. and Ando, H. Fossil turtles from the Lower Cretaceous Tetori Group in central Japan

P25 Shinya Miyata, Yabumoto, Y., Nakajima, Y., Ito, Y., Sasaki, T. and Hirano, H. The second specimen of the crossognathiform fish Apsopelix miyazakii from the Cretaceous Yezo Group of central Hokkaido, Japan

P26 Nao Kusuhashi, Suzuki, T., Terui, K., Sato, A. and Amiot, R. A mammal jaw from the Upper Cretaceous Ashizawa Formation (Futaba Group), Fukushima, northeastern Japan

P27 Tomoyuki Ohashi, Hasegawa, Y., and Suzuki, C. Dinosaur remains from the mid-Cretaceous shallow marine sediments of the Futaba Group, Japan.

P28 Singh, A. and Jyotsana Rai Seribiscutum primitivum, a high latitude, bipolar nannofossil taxon from Jaisalmer Basin: Implications on palaeogeographic distribution

P29 Aya Kubota, Iba, Y., Hikida, Y. and Yi, K Mid-Cretaceous micro-organisms captured in amber: first records in eastern margin of Eurasia

P30 Choi Byung-Do, Jugdernamjil, M. and Huh, M. The tentative new Cretaceous non-marine ostracods from the southern coast of Korean peninsula

P31 Chika Sakamoto, Dick, M. H., Komatsu, T. and Miyake, Y. Cheilostome bryozoans from the Upper Cretaceous Himenoura Group, Kyushu, Japan

P32 Yasuyuki Hirata, Minami, S., Adachi, N. and Ezaki, Y. Characteristics and modes of construction of rudist-bearing reefs unique to the Yura area, Wakayama Prefecture, southwest Japan

P33 Yuka Miyake and Komatsu, T. Bivalves from the Upper Cretaceous Himenoura Group on Shimokoshiki-jima Island, Kagoshima, Japan

Geoparks highlighting Cretaceous

P34 Ugai, H., Hirose, K., Hase, Y., Yuka Miyake and Komatsu, T. Working on ‘Amakusa Goshoura Geopark

P35 Dorota Anna Kapuscik Selecting potential geosites in the eastern Kii Peninsula, SW Japan

P36 Takashi Hasegawa and Hibino, T. Hakusan Tedorigawa Geopark: activity utilizing Early Cretaceous fossils and terrestrial sequences

P37 Kenichi Kurihara and Shimomura, K. Geopark activities utilized results and materials of Cretaceous researches in the Mikasa Geopark, Japan

11 0DSRI:DVHGD8QLYHUVLW\ :DVHGD&DPSXV

Venue

The Symposium and scientific sessions will be held at Okuma Auditorium of Waseda University, western central area of Tokyo, Japan.

Okuma Auditorium was opened in the year 1927, and has been designated as a national important cultural property of Japan in the year 2007. The bells, which ring six times a day, produce the same harmony as Westminster Abbey in London, for the whole city of Waseda. The history of Okuma Auditorium has been colorfully interspersed with many important invited lecturers. Lectures were made by Albert Einstein (physician), Robert Kennedy (President of USA), Bill Clinton (President of USA), George W. Bush (President of USA), Nelson Mandela (President of South Africa), Jiang Zemin (President of China), Gloria Macapagal-Arroyo (President of Philippines), Kim Young-Sam (President of Korea), Ban Ki-Moon (Secretary-General of United Nations), Bill Gates (Chief of Microsoft Corp.) and so on.

Waseda University was founded in the year 1882 and it is the first university in Japan that accepted women students in the year of 1939. The university has just celebrated the 125th anniversary of its founding in the year 2007. Now, Waseda is one of Japan’s top private and higher learning institutions. The university has over 50,000 students enrolled, which makes it as a second largest university in Japan.

Day One 4 September 2014

SESSIONS:

Keynote speech 1

OAE phenomena contributed from Asian and western Pacific records

Biotic evolution: Asian and western Pacific fauna and flora - Macrofauna

14 Keynote

Biostratigraphy, paleoenvironments, and tectonic setting of the Cretaceous System of Pacific coast North America: towards a circum-North Pacific integrated correlation framework

Haggart, J.W.

Natural Resources Canada, Geological Survey of Canada, 1500-605 Robson Street, Vancouver, British Columbia V6B 5J3 Canada ([email protected])

Cretaceous basins of the Pacific coast rich succession of invertebrate assemblages region of North America represent a variety of that could be used to effectively zone and tectono-sedimentary settings. The principal correlate strata at a broad scale, as well as basins arrayed along the outboard of the Pacific provide correlations at a global level. coast of North America include the Southern Molluscan fossils are not always available in Alaska basin, the Hecate and Nanaimo basins the clastic-dominated successions of the Pacific in British Columbia (BC), the Hornbrook and coast, however, and studies of microfossils, Great Valley basins in Oregon and California, principally foraminifers, radiolarians, and and the Peninsular Ranges basin in Baja calcareous nannofossils were initiated in the California, all of which represent fore-arc latter part of the 20th century to improve settings. Toward the active orogen, or biostratigraphic understanding of the integrated within it, the Bowser and Cretaceous rocks; however, the detailed Tyaughton-Methow basins represent back-arc stratigraphic work to fully integrate these settings in the more northerly BC region. existing biostratigraphies remains to be done. Stratigraphic successions in these basins are all Throughout most of the Cretaceous dominated, almost exclusively, by clastic Period, the basins of the Pacific coast of North deposition. The active tectonic setting of the America were in large part separated from the western North American margin resulted in Western Interior Seaway region of the significant topographic relief on the adjacent continent by an evolving orogenic belt, which mainland and minimal development of effectively precluded mixing of faunas between contemporary non-marine basins. the two regions. For this reason, faunas of the The initial study of the Cretaceous Western Interior are most closely related to basins of the Pacific coast was driven by a need those of the European standard succession, to understand the extent of coal resources in while those of the Pacific coast share more this largely uninhabited region of the continent similarities with those of the Indo-Pacific and early studies of the Cretaceous rocks were region. Indeed, the similarity of the Cretaceous undertaken by the Geological Survey of molluscan faunas of California and British Canada (GSC) in the north and the Geological Columbia and those of Japan and India was Survey of California in the south. Readily noted very early in the study of these faunas. available molluscan fossils in the strata allowed The higher levels of Cretaceous faunal the early geologists, working with their diversity in the western Pacific region are paleontological collaborators, to establish attributed to a more widespread tropical climate, regional and global correlations of the resultant from northerly-directed current Cretaceous successions. Principal fossil groups systems; these warm-water currents carried utilized included ammonites and bivalves, many Tethyan forms to higher latitudes than primarily inoceramids, and, to a lesser extent, seen in the eastern Pacific. In contrast, belemnoids and gastropods. By the mid-20th circulation patterns along western North century, it was recognized that the Cretaceous America were dominated by basins of the Pacific coast region contained a southward-flowing currents, which resulted in 15 the establishment of lower diversity, persist, however, resulting in continuing boreal-dominated cool-water faunal questions of regional correlation. One example assemblages along the margin. Importantly, the is the zonation for the Santonian and biogeographic affinities of Cretaceous faunas Campanian, where the ages of important of the North American Pacific coast suggest molluscan taxa are interpreted differently in that the accretion of outboard tectonic terranes East Asia and California/BC. It is anticipated, to the North American margin was essentially however, that detailed taxonomic and completed by the start of Cretaceous time. stratigraphic investigations will eventually The current Cretaceous ammonite resolve these apparent contradictions. biozonation for the Pacific coast of North Much progress has been made in America includes many forms also found in establishing formal biostratigraphic zonations important basins of East Asia, including those for the different faunal groups of Pacific coast of the Japanese Islands, Sakhalin Island, and North America, but much future work is the Kamchatka Peninsula. Virtually all required to amalgamate these multiple higher-level taxonomic groups (families) of independent zonations into a comprehensive ammonites present in the circum-North Pacific integrated framework, particularly one that is basin are found on both eastern and western applicable across the North Pacific. The goal is margins of the basin, as are most genera; worth striving for, however, and Cretaceous similar distributions apply for the inoceramid stratigraphers of the Pacific region will have to bivalves. As well, limited numbers of increasingly initiate integrated globally-distributed taxa allow confident multidisciplinary research programs to achieve correlations with European standard sections. it. To this end, use of other chronostratigraphic Given the overall strong similarities of these methods, such as magnetostratigraphy, molluscan faunas across the Cretaceous Pacific geochronology, sea-level trends, Sr-isotope Ocean basin, there is potential to develop a stratigraphy, and stable isotope stratigraphy can North Pacific-wide ammonite/inoceramid help elucidate the fine details of local basin biostratigraphic framework of significant detail histories, improve correlations around the and precision. Differing interpretations of the Pacific basin, and also provide the next stratigraphic distribution of some key taxa generation of global correlation tools.

16 OAE phenomena contributed from Asian and western Pacific records

Prof. Hirano’s contribution to natural sciences of Oceanic Anoxic Events: Phyletic evolution of desmoceratine ammonoids through the Cenomanian–Turonian oceanic anoxic event

Moriya K.

Div. Earth & Environ. Sci., Sch. Natural Sci. & Tech., Kanazawa Univ., Kakuma-machi, Kanazawa, Ishikawa 920-1192 ([email protected])

Prof. Hiromichi Hirano who was a environmental impact of OAE on speciation of Project Leader of IGCP 434 has passed away the Cretaceous ammonoids. Since Schlanger on 5th of May, 2014. He was 68 years old. and Jenkyns (1976) described worldwide During a series of IGCP projects on the distribution of organic rich sediments in Cretaceous environment in eastern Asia, his relatively restricted geological intervals, OAEs enthusiasm and dedicative effort to promote are well documented and vigorously discussed natural sciences in Japan and eastern Asian by many authors. Although most of those countries are highly reputed and respected. I do studies have been made in Atlantic and believe that he dearly enjoyed what he has done Western Interior Seaway in USA, Hirano et al. in the IGCP projects. (1991) first described the Cenomanian He stared his academic carrier with Turonian Boundary Interval (CTBI; OAE2) in ammonoid biostratigraphy of the Jurassic the Yezo Group distributed in the northwestern Toyora Group distributed in southwestern Pacific, in terms of OAE. They found that there Japan in 1970. He was supervised by Prof. is a barren interval in macrofossil of 20m thick Tokio Shikama in Yokohama National between the last occurrence of Cenomanian University. Although the word “Oceanic indices and the first occurrence of a Turonian Anoxic Events (OAEs)” had not been proposed index. This interval also includes a dark gray yet, the Toyora Group includes Toarcian OAE, shale bed characterized by a lack of indicating that his carrier just started with ichnofossils. Considering a sedimentation rate works on one of major OAEs. He realized the of ca. 30m/100kyr in this basin, this barren importance of organic rich sediments and zone spans approximately 70kyr. Hasegawa biological response, such as changes in and Saito (1993) found the carbon isotope biodiversity, through these works. excursion which is correlated to the CTBI After he graduated, he went to Kyushu within this barren zone. Hirano et al. (1990) University and was supervised by Prof. Tatsuro also documented that Desmoceras Matsumoto. In his Ph.D. project, Prof. Hirano (Pseudouhligella) japonicum phyletically studied the Cretaceous ammonites, speciated to Tragodesmoceroides subcostatus Gaudryceras, with intensive field works. He at the CTBI in the northwestern Pacific based analyzed the geographic distribution, ontogeny, on morphological analyses and stratigraphic and stratigraphic distribution of relative and geographic distribution. abundance of each morphotypes of three Hirano (1993) examined Sulphide and morphospecies of Gaudryceras, concluding total sulphur concentrations across the CTBI in that a dimorphic pair appeared in ancestral France, Japan, and Tunisia with X-ray populations can be identified as an example of fluorescence (XRF) to identify redox condition transient polymorphism. thorough the CTBI. Total sulphur After he received Ph.D. from Kyushu concentrations in the CTBI in all these three University, he merged and expanded his geographically isolated areas clearly show knowledge on OAE and phyletic evolution of distinctive positive excursions. In addition to ammonoid species to investigate an the lack of ichnofossils, these results indicate 17 hypoxic condition of the bottom water of these From these lines of evidence, Hirano basins. (1993) hypothesized that Turonian “D. (P.) They also analyzed stratigraphic japonicum lost its habitat and was then changes in shell morphology and geographic extinguished by the invasion or occurrence of distribution of desmoceratine ammonoids from anoxic water”. Hirano (1993) also speculated the Cenomanian through the Turonian in the that “small population of D. (P.) japonicum Yezo Group, Japan (Hirano et al., 1990; Hirano, escaped into shallow waters when anoxic water 1993). The morphometry clearly shows invaded, and T. subcostatus is thought to have punctuated changes in shell morphology from arisen from one of these populations”. Cenomanian ancestral species Desmoceras Although this hypothesis has not yet been (Pseudouhligella) japonicum to upper tested, this is astonishing idea on external Turoninan descendant Tragodesmoceroides forcing from Earth system perturbations onto matsumotoi through lower Turonian T. phyletic evolution of macro-organisms. subcostatus. Among them, extinction of As shown in this example, Prof. ancestral D. (P.) japonicum, and evolution of Hirano made grate contributions to advance our new genus Tragodesmoceroides occurred at the knowledge on the Carbon cycle and CTBI. Geographic distributions of D. (P.) bio-diversity change in the Cretaceous. His japonicum and T. subcostatus are very ideas and scientific understandings were interesting as well. While D. (P.) japonicum is exquisite. It would be a grate honor for all of us predominant in offshore silt and clay facies, T. if we could extend his legacy and develop new subcostatus occurred from shallower sandy silt science on the Asia-Pacific Cretaceous and silt facies. ecosystems. May his soul rest in peace.

References: Hasegawa, T., Saito, T., 1993. Global synchroneity of a positive carbon isotope excursion at the Cenomanian/Turonian boundary: Validation by calcareous microfossil biostratigraphy of the Yezo Group, Hokkaido, Japan. Island Arc, 2, 181-191. Hirano, H., 1993. Phyletic evolution of desmoceratine ammonoids throuth the Cenomanian-Turonian oceanic anoxic event. In: House, M.R. (Ed.), The Ammonidea: Environment, Ecology, and Evolutionary Change. Systematics Association Spesial Volume. Clarendon Press, Oxford, pp. 267-284. Hirano, H., Nakayama, E., Hanano, S., 1991. Oceanic anoxic event at the boundary of Cenomanian/Turonian ages–First report on the Cretaceous Yezo Supergroup, Hokkaido Japan from the view of biostratigraphy of megafossils, sedimentary- and ichno-facies and geochemistry. Bull. Sci. Eng. Res. Lab., Waseda Univ., 131, 24-32. Hirano, H., Okamoto, T., Hattori, K., 1990. Evolution of some late Cretaceous desmoceratine ammonoids. Trans. Proc. Palaeont. Soc. Japan, N.S., 157, 382-411. Schlanger, S.O., Jenkyns, H.C., 1976. Cretaceous oceanic anoxic events: Causes and consequenses. Geol. Mijinb., 55, 179-184.

18 Radiogenic isotopic records of Early Cretaceous marine sediments: implications for large igneous provinces and the Aptian climatic crisis

Kuroda, J.1, Tanimizu, M.2, Tejada, M. L. G.1, Hori, R. S.3, Suzuki, K.1, Ogawa, N. O.1, Coffin, M. F.4 and Ohkouchi, N.1

1Japan Agency for Marine-Earth Sci. Tech., Yokosuka 237-0061 Japan ([email protected]) 2Kochi Inst. Core Sample Res., JAMSTEC, Nankoku 783-8502 Japan 3Grad. Schl. Sci. Engin., Dept. Earth Sci., Ehime Univ., Matsuyama 790-8577 Japan 4Inst. Marine Antarctic Stud., Univ. Tasmania, Hobart, Tasmania 7001, Australia

We present initial isotopic ratios of which severely limited dispersion of lead for Early Cretaceous (Barremian-Aptian) Pb-carrying particles out of the Pacific Ocean sections from Shatsky Rise (Pacific) and Gorgo (Kuroda et al., 2011). Published Os isotopic a Cerbara (Italy). The Pb isotopic data track an data from the Italian section (Tejada et al., interval representing Oceanic Anoxic Event 2009) indicate two episodes of massive (OAE)-1a, which is characterized by eruptions of OJP or the contemporaneous quasi-global deposition of organic carbon-rich Manihiki and Hikurangi plateaus starting from marine sediments (black shale). The Pb earliest Aptian time, slightly later than that isotopic compositions of sediments from indicated by the sedimentary Pb isotopic record Shatsky Rise decrease at the end of Barremian from Shatsky Rise. Differences in isotopic time, from radiogenic continental values to variations between Pb and Os likely reflect unradiogenic values, and subsequently differences in their chemical behaviors in the remained less radiogenic until the end of early oceans, i.e., Pb isotopic compositions would Aptian time. We explain the isotopic shift by a have varied in response to local or regional significant increase in supply rate of changes in sediment provenances, whereas unradiogenic Pb, most likely due to massive large-scale changes in Os inputs are required to volcanism. In contrast, the Pb isotopic explain variations in seawater Os isotopic compositions from the Italian section, which compositions. Our Pb isotopic data, together was situated at the western end of Tethys, are with the published Os isotopic record, provide mostly identical to those of upper continental new evidence for the eruptive history of OJP crust, showing no significant change in supply together with contemporaneous Pacific plateaus rate of unradiogenic Pb. We attribute the and the environmental consequences of the discrepancy between two sites to bathypelagic massive volcanism, starting at end-Barremian eruptions of Pacific large igneous provinces time and extending through early Aptian time. (LIPs) such as the Ontong Java Plateau (OJP),

References: M.L.G. Tejada, K. Suzuki, J. Kuroda, R. Coccioni, J.J. Mahoney, N. Ohkouchi, T. Sakamoto and Y. Tatsumi, 2009, Geology, 37, 855-858. J. Kuroda, M. Tanimizu, R.S. Hori, K. Suzuki, N.O. Ogawa, M.L.G. Tejada, M.F. Coffin, R. Coccioni, E. Erba and N. Ohkouchi, 2011, Earth Planet. Sci. Lett., 307, 126–134.

19 Keynote

High-resolution 187Os/188Os isotope stratigraphy and 206Pb/238U zircon geochronology reveal and verify the global occurrence of OAE 2: Yezo Group, Hokkaido, Japan

Du Vivier, A. D. C.1, Selby, D.1*, Condon D. J.2, Takashima, R.3 and Nishi, H.3

1* Dept. Earth Sci., Durham Univ., Durham, DH1 3LE, UK ([email protected]) 2NERC Isotope Geosci. Lab., British Geol. Sur., Keyworth, NG12 5GG, UK 3Cent. Acad. Res. Arch. Tohoku Univ. Mus., Tohoku Univ., Aramaki Aza Aoba 603, Aoba-ku, Sendai, 980-8578, Japan

Osmium isotope stratigraphy has OAE 2. In addition new CA-ID-TIMS proven to be a successfully applicable proxy to 206Pb/238U single zircon geochronology from 5 sections associated with the oceanic anoxic volcanic tuff horizons is obtained in the YG event (OAE) 2. Studies reveal a distinct and section; the Osi profile combined with new age 187 188 coeval initial Os/ Os (Osi) isotope profile constraints revises the stratigraphic position of from multiple sections in the proto-Atlantic, the onset of OAE 2 and the Western Interior Seaway (WIS) and European Cenomanian-Turonian boundary (CTB). pelagic shelf (Du Vivier et al., 2014). Every The original interpretation of the onset profile records radiogenic Osi before the onset of OAE 2 in the YG section was determined of OAE 2, a dramatic unradiogenic trend at the from characteristic excursions from a onset of OAE 2 proceeded by near chondritic high-resolution 5-point moving average 13 Osi values recorded for ~200 kyr of the δ Cwood record (Takashima et al., 2011). 13 syn-OAE 2 interval, after which the Osi values However, the inferred δ C excursion is not gradually return to radiogenic Osi. Prior to concurrent with the Osi profile. Further, facilitating Osi as a stratigraphic proxy, the evidence from additional litho- and onset of OAE 2 was identified by traditional biostratigraphy (Takashima, pers comm.) 13 13 matching of the δ Corg and δ Ccarb records; in combined with the Re-Os data for the YG 187 188 which a positive isotope excursion denotes the (unradiogenic Osi, low Re/ Os values and onset of the event (Schlanger et al., 1987). It is an increase in 192Os abundance) is consistent observed that studies to date unanimously show with the Re-Os data characteristics of the onset that the unradiogenic Osi trend is broadly of OAE 2 in sections previously analysed synchronous with the positive δ13C excursion. (Turgeon and Creaser, 2008; Du Vivier et al., The OAE 2 is referred to as a ‘global’ 2014). Therefore, despite the lack of additional event, however, study of late Cretaceous isotopic analyses (i.e., Nd, Pb, Sr, P, U) Pacific basins is limited compared to the compared to sites in the WIS and the European volume of data collection from the shelf, the onset of OAE 2 in the YG is revised proto-Atlantic, WIS and European shelf; from -39 m to -16.15 m. In addition, 206Pb/238U isotope proxy analysis and age constraints of zircon dates provide absolute evidence to Pacific sections are inadequate to verify the nominally revise the onset of OAE 2 and the truly global extent of the OAE 2. Therefore, CTB, which is derived from the integration of here a proto-Pacific section is evaluated: Yezo 206Pb/238U zircon geochronology of the Group (YG), Hokkaido, Japan, to determine the volcanic tuff horizons throughout the YG 40 39 global extent of OAE 2. A high-resolution Osi sequence relative to Ar/ Ar dates from the profile for the Pacific YG section demonstrates WIS (Meyers et al., 2012). We apply age-depth changes in global ocean chemistry across the models to calibrate dates from both sections

20 temporally and then assess if the Osi profiles cycle associated with high atmospheric and sea are coeval. Tuff unit HK017 in the YG section surface temperatures of the late Cretaceous occurs at -16.10 m, adjacent to the first least environment. The dramatic and seemingly radiogenic Osi value, which is 0.05 m above simultaneous unradiogenic trend has 13 the onset of the excursion in the δ Cwood record. implications on ocean circulation; evidence The HK017 206Pb/238U (zircon) systematics suggests that circulation was sufficient to yield a date of 94.44 ± 0.14 Ma, which provide transfer a change in seawater chemistry within a direct time constraint for the onset of OAE 2. the residence time of Os (≤10 kyr) to basins This age is identical, within uncertainty, to that within the proto-Atlantic and Pacific, WIS and established for the WIS (~94.38 ± 0.15 Ma). As European pelagic shelf. The synchronous trend a result, these dates verify the revision of the in the Osi profiles from high radiogenic Osi OAE 2 onset in the YG, and confirm the trend values to low unradiogenic Osi values infer that in the Osi profiles to unradiogenic Os values as global warming coupled with submarine globally penecontemporaneous (Turgeon and volcanism and a major sea level transgression Creaser, 2008; Du Vivier et al., 2014). initiated the OAE 2, which facilitates Furthermore, the age of HK018, 93.92 ± 0.11 widespread correlation of OAE 2. Ma, implies that the CTB (dated at 93.90 ± The Osi stratigraphy facilitates the 0.15 Ma from the WIS, Meyers et al., 2012) in traditional method of correlation and the YG is present in the horizon directly above integration of stratigraphic successions using or below the tuff since the date for HK018 is δ13C isotopes. In addition, 206Pb/238U zircon statistically indistinguishable from the date of geochronology has permitted the integration of the numerical age of the CTB (derived from the Osi profiles from WIS and Pacific basins WIS). As such the stratigraphic height of the through the application of age-depth models, CTB in the YG is amended to 25 m. which support the temporal interpretations Multiple isotope studies have shown a based on other isotope analyses and concurrence between the trend in isotope geochronology. Furthermore the duration of composition and the onset of the OAE 2. The volcanic activity associated with the Caribbean Re/Os systematics show a dramatic LIP is quantitatively estimated. The improved unradiogenic trend in Osi values synchronous integration of the proto-Pacific with the WIS with the onset of OAE 2. The transition of Osi across the CTB has created a nominal from radiogenic to unradiogenic is inferred to correlation to the GSSP in the WIS. Therefore, be associated with submarine volcanic activity with the addition of high-resolution Os isotope of the Caribbean LIP from which the stratigraphy from trans-world sections and new 206 238 unradiogenic Osi derived, and is thus associated Pb/ U geochronology from the YG section, with onset of OAE 2. The radiogenic Os it is concluded that the OAE 2 was an recorded before the OAE 2 is derived from isochronous event with worldwide basinal weathering of ancient continental crust, dispersion and penecontemporaneous with the consistent with an accelerated hydrological major pulse of volcanism of the Caribbean LIP.

References: Du Vivier, A.D.C., Selby, D., Sageman, B.B., Jarvis, I., Grocke, D.R., Voigt, S., 2014. Marine 187Os/188Os isotope stratigraphy reveals the interaction of volcanism and ocean circulation during Oceanic Anoxic Event 2. Earth Planet. Sci. Lett., 389, 23-33. Meyers, S.R., Siewert, S.E., Singer, B.S., Sageman, B.B., Condon, D.J., Obradovich, J.D., Jicha, B.R., Sawyer, D.A., 2012. Intercalibration of radioisotopic and astrochronologic time scales for the Cenomanian-Turonian boundary interval, Western Interior Basin, USA. Geology, 40, 7-10. Quidelleur, X., Paquette, J.L., Fiet, N., Takashima, R., Tiepolo, M., Desmares, D., Nishi, H., Grosheny, D., 2011. New U-Pb (ID-TIMS and LA-ICPMS) and 40Ar/39Ar geochronological constraints of the Cretaceous geologic time scale calibration from Hokkaido (Japan). Chem. Geol., 286, 72-83. Schlanger, S.O., Arthur, M.A., Jenkyns, H.C., Scholle, P.A. 1987. The Cenomanian/Turonian Oceanic Anoxic Event, I. Stratigraphy and distribution of organic carbon-rich beds and the marine δ13C excursion. In: Brooks, J. & Fleet, A.J. (eds) Marine Petroleum Source Rocks. Geol. Soc. London, Spec. Publ., 26, 371–399. Takashima, R., Nishi, H., Yamanaka, T., Tomosugi, T., Fernando, A.G., Tanabe, K., Moriya, K., Kawabe, F., Hayashi, K., 2011. Prevailing oxic environments in the Pacific Ocean during the mid-Cretaceous Oceanic Anoxic Event 2. Nature Comms., 2:234 DOI:10.1G38/ncomms1233. Turgeon, S.C., Creaser, R.A., 2008. Cretaceous Anoxic Event 2 triggered by a massive magmatic episode. Nature, 454, 323–326.

22 Integrated Stratigraphy and U-Pb ages of the Cretaceous Yezo Group, exposed in Hokkaido, Japan

Nishi, H.1, Takashima, R.1, Yamanaka, T.2, Orihashi, Y.3 and Hayashi, K.4

1The Center for Academic Resources and Archives, Tohoku University Museum, Tohoku University. Aramaki Aza Aoba 6-3, Aoba-ku, Sendai, 980-8578, Japan ([email protected]) 2Department of Earth Sciences, Okayama University. Tsushimanaka 3-1-1, Kita-ku, Okayama, 700-8530, Japan 3Earthquake Research Institute, the University of Tokyo. Yayoi 1-1-1, Bunkyo-ku, Tokyo, 113-0032, Japan 4Geological Survey of Hokkaido, Environmental and Geological Research Department, Hokkaido Research Organization, Nishi-12, Kita-19, Kita-ku,Sapporo, Hokkaido, 060-0819, Japan

The Cretaceous-Paleogene period is Hokkaido Japan because the resolution of known as the latest Greenhouse climate in the international stratigraphic correlation of these history of earth (e.g., Takashima et al., 2006). strata has not been enough to identify important In order to understand ocean–climate system climatic and/or extinction events such as the during past Greenhouse climate, numerous Oceanic Anoxic Events and others. attempt has long been made for the marine The strata researched in the present sequences in the Atlantic Ocean, Southern study is the Yezo Group (middle Aptian–late Ocean and Tethyas Sea. The Pacific Ocean was Campanian: 121–74 Ma) exposed in the the outstandingly largest ocean during Toammae, Oyubari and Urakawa areas. Cretaceous, and it may have played important Samples were collected at approximately 5- to roles in Earth’s ocean–climate system. Despite 15- m stratigraphic intervals from these groups. its importance, very little work has been done Dry mudstone and sandstone samples (400 g) to establish detailed paleo-oceanographic were crushed into approximately one cubic changes during Cretaceous-Paleogene. This is centimeter pieces and were disaggregated using largely because most of the tetraphenylborate and sodium chloride. Cretaceous–Paleogene Pacific oceanic crusts Planktic foraminifera and wood fragments were have subducted under continents, and poor removed from the washed residue. recoveries of Cretaceous–Paleogene sediments For the carbon isotope analyses, wood in the ODP and DSDP cores from the Pacific fragments were removed from the same residue sites have prevented studying as planktic foraminifera. The carbon isotope of paleoenvironmental changes of the Pacific the total organic carbon of the sample was then Ocean. measured using a mass spectrometer (IsoPrime, In order to understand Cretaceous GV Instruments, UK) in line with an elemental paleo-oceanographic changes in Northwest analyzer EuroEA3000 (EuroVector, Italy). For Pacific, the present study established the the U-Pb radio-isotopic age, we analyzed detailed integrated stratigraphy (planktic twenty tuffs intercalated in the Yezo Group. foraminiferal biostratirgraphy, carbon isotope Zircon crystals of tuffs were extracted, and the stratigraphy and U-Pb age of tuff beds) of the U-Pb ages of zircon crystals were determined Cretaceous marine sequences exposed in using ICP-MS (VG Plasma Quad 3) with a

23 frequency quintupled (λ = 213 nm) Nd-YAG in these horizons, evidences of oxygen laser ablation system (New Wave Research depletion were identified from the most of UP-213) at the Earthquake Research Institute, these horizon based on the analyses of benthic the University of Tokyo. The analytical foraminifera, degree of pyritilization and procedure of the LA ICP-MS is described in sedimentary structure such as degree of detail by Orihashi et al. (2008). bioturbation. Our integrated stratigraphy enables Furthermore, accurate Cretaceous identification of the exact horizons of following stage boundaries of the Albian/Cecnomanian climatic and extinction events in the Yezo (lower part of the Hikagenosawa Formation), Group. The Jacob, Kilian and Paquier levels of Cenomanian/Turonian (lower part of the Saku the OAE1b occur in the Refureppu Sandstone Formation), Turonian/Coniacian (lower part of Member of the Shuparogawa Formation, while the Haborogawa Formation), the Leenhadlt level of the OAE1b and the Coniacian/Santonian (middle part of the OAE1c level are placed in the Okusakainosawa Haborogawa Formation), Sandstone and Mudstone Member of the Santonian/Campanian (Upper part of the Shuparogawa Formation. The OAE1d and the Haborogawa Formation) are identified in the Mid-Cenomanian Event horizons are Yezo Group. The U-Pb age of the tuff recognized in the lower and middle parts of the intercalated near these boundaries are accord Hikagenosawa Formation, respectively. The well with the ages of the latest Cretaceous time OAE2 level occur in the Saku Formation. scale proposed by Ogg et al. (2012) and Although no so-called black shales were found Sageman et al. (2014).

References: Ogg, J. G., and Hinnov, L. A., 2012, Chapter 27, Cretaceous, in Gradstein, F., Ogg, J., Schmitz, M., and Ogg, G., eds., The Geologic Time Scale 2012: Oxford, Elsevier, p. 793-853. Orihashi, Y., Nakai, S. and Hirata, T., 2008, U-Pb age determination for seven standard zircons using Inductively Coupled Plasma-Mass Spectrometry coupled with Frequency Quintupled Nd-YAG (l=213nm) Laser Ablation System: Comparison with LA-ICP-MS zircon analyses with a NIST glass reference material. Resource Geology, v. 58, p. 101-123. Sageman, B. B., Singer, B. S., Meyers, S. R., Siewert, S. E., Walaszczyk, I., Condon, D. J., Jicha, B. R., Obradovich, J. D. and Daqyer, D. A., 2014, Integradting 40Ar/39Ar, U-Pb, and astronomical clocks in the Cretaceous Niobrara Formation, Western Interior Basin, USA. Geological Society of America Bulletin, doi: 10.1130/B30929.1. Takashima, R., Nishi, H., Huber, B. and Leckie, M., 2006. Greenhouse world and the Mesozoic ocean. Oceanography, vol. 19, p. 82-92.

24 A fingerprint of primary producers during the OAEs

Ohkouchi, N., Ogawa, N.O., Kashiyama, Y. and Kuroda, J.

Japan Agency for Marine-Earth Science and Technology, Yokosuka 237-0061, Japan

Black shale is dark-colored muddy nitrogen isotopic composition, we concluded sediment substantially enriched in organic N2-fixing cyanobacteria could be a major matter. Such a type of sediments has been primary producer during the formation of the distributed intermittently in many horizons of black shale. Earth’s history, from Archean to Holocene. In the black shales we also observed Among them, those from the mid-Cretaceous abundant 17-nor-DPEP (Fig. 1), a derivative of are characterized by episodic and chlorophylls c, whose nitrogen isotopic contemporaneous deposition in wide range of compositions are also suggestive of N2-fixation. oceanic settings. The black shales observed in The chlorophylls c are produced by various early Aptian around 120 Ma and algae (i.e., eukaryotes) including diatoms and Cenomanian-Turonian boundary around 94 Ma dinoflagellates, whereas the N2-fixation is have global distribution with extraordinarily exclusively prokaryotic metabolic process. To high content of organic carbon and often compromise these organic/isotope geochemical referred as Oceanic Anoxic Event (OAE)-1a evidences, we propose that the cyanobacteria and -2. The OAE-2 “Livello Bonarelli” black like Rechelia intracellularis as endosymbionts shales deposited at pelagic setting in the on diatom species in the genus Rhizosolenia or western Tethys are easily collected, since they Hemiaulus conducted N2-fixation during the are widely cropped out in the central Apennine, black shale formation and supplied fixed Italy. Fortunately, they are as “fresh” as those nitrogen to the host diatoms. recovered from the ocean floor, and thus they In the modern oligotrophic ocean, the are amenable to organic geochemical studies symbiosis between diatoms and cyanobacteria testing various methods for reconstructing the is widely observed and the association often oceanic environments at that time. forms extensive blooms. For example, In our study, we focus on alkyl Hemiaulus-Richelia association bloom was porphyrins (Fig. 1) that are originated from observed in Amazon River plume in the chlorophylls, photosynthetic pigments from the western tropical Atlantic Ocean. The source of autotrophs. The most abundant alkyl porphyrin new nitrogen entering the photosynthetic we found from Bonarelli black shales is DPEP system in such oceans is largely cyanobacterial (deoxophylloerythroetioporphyrin) that has N2-fixation, with a lesser contribution from five-ring structure in the lower half of the nitrate flux from the subsurface water. Such molecule (Fig. 1). The structure itself strongly N2-fixation process could have compensated suggested it originating from chlorophyll a. We the denitrification process in the anoxic water also observed porphyrins originating from column which releases nitrogen from the ocean chlorophylls c. After isolating and purifying to the atmosphere. In the late Quaternary these porphyrins, we determined both carbon Mediterranean sapropels, recent analogue of and nitrogen isotopic compositions of Oceanic Anoxic Events, micropaleontological individual alkyl porphyrins that are derived observation indicated that the major fossils from tetrapyrrole structures of chlorophylls and found in them were rhizosolenid diatoms. hemes. Except for ETIO porphyrins that are Therefore, it is consistent with our above potentially originated from hemes, the isotopic consideration. These fragmented evidences compositions range -22~-16‰ for carbon and suggested that the diatom-cyanobacteria -7~-3‰ for nitrogen. The isotopic range of endosymbioses played an important role in the nitrogen is in or close to that of N2-fixers. primary production during the black shale Based on the chlorophyll speciation and formation.

Fig. 1. Chemical structures of alkyl porphyrins abundantly observed in the Cretaceous black shales. DPEP (left) and 17-nor-DPEP (right) discussed in this study.

26 Primary producer community during the mid-Cretaceous oceanic anoxic events (OAEs) evaluated from algal biomarkers in sediments deposited in the Vocontian Basin, SE France

Ando, T.1, Sawada, K.1, Takashima, R.2 and Nishi, H.2

1Dept. Nat. Hist. Sci., Fac. Sci., Hokkaido Univ., N10W8, Kita-ku, Sapporo, 060-0810, Japan ([email protected]) 2Cent. Acad. Res. Arch., Tohoku Univ. Mus., Tohoku Univ.. Aramaki Aza Aoba 6-3, Aoba, Sendai, 980-8578, Japan.

Laminated black shales were found for cyanobacreria-dominant production under several formations deposited during the oligotrophic sea water. During the OAE1a, mid-Cretaceous, which suggests the oceanic cyanobacteria such as Synechococcus were anoxic events (OAEs) were repeatedly main primary producer in oligotrophic and occurred. Monteiro et al. (2012) simulated that stratified marine condition. The OAE2 was also the ocean anoxia could be expanded as a result thought to ‘Cyanobacterial Ocean’ (Kuypers et of elevated marine primary production al., 2004), although the 2-MHI values were associated to high nutrient, particularly lower during the Thomal levels. From these phosphorous. From this insight, it could be results in the OAE2 levels, higher 2-MHI important to understand high-producing marine sections were limited by more pelagic and organisms contributed for formation of black likely oligotrophic area at proto-Atlantic. These shales. In the present study, we focus on evidences also indicate 2-methy hopanoid variations in productivity of cyanobacteria, producing cyanobacteria favored oligotrophic dinoflagellate and coccolithophorid during the condition in the mid-Cretaceous. major OAEs (OAE1a, 1b, 1d, and 2) in the Triaromatic dinosteranes and C27 mid-Cretaceous by these biomarker analyses. triaromatic steranes (derived from C28 sterols) We analyzed black shales and adjacent can be used for dinoflagellate and sedimentary rocks collected from the outcrops coccolithophorid biomarkers, respectively, in of the Goguel (OAE1a), Jacob, Paquier the mid-Cretaceous pelagic sediments. Thus, (OAE1b), Breistroffer (OAE1d) and Thomel triaromatic steranes indices, C27 TAS (C27 (OAE2) levels, and sediment cores of the triaromatic steranes/ [C26+C27 and A-ring Kilian level (OAE1b) in SE France. Hopanes methyl triaromatic steranes]; Ando et al., and triaromatic steranes were detected in all submitted) and TADS (triaromatic samples. 2α-methyl hopanes, which are known dinosteranes/ [C26+C27 and A-ring methyl as cyanobacteria biomarkers, were significantly triaromatic steranes]; Ando et al., submitted), detected in only the Goguel level. The 2-methyl can evaluate contributions of coccolithophorid hopane index (2-MHI = 2α-C31 methyl hopane / and dinoflagellate among eukaryotic algae, [C30 hopane + 2α-C31 methyl hopane]), which respectively. General trends of TADS variation is used for evaluating contribution of during the mid-Cretaceous associated with cyanobacterial production, are 5-25% in the global sea-level change. However, TADS Goguel level, so that cyanobacteria production values increase but C27 TAS decrease in the might be higher during the OAE1a . However, Paquier and Thomel levels. At the present, the cyanobacteria presumably produced as dinoflagellate favor eutrophic and stratified minor component after the OAE1a (2-MHI < ocean. Therefore, higher TADS values in the 5%). The 2-methyl bacteriohopanepolyol Paquier and Thomel levels indicate that (BHP)-producing marine cyanobacteria (e.g., dinoflagellates predominated under eutrophic Synechococcus) is known to inhabit stratified and stratified marine condition during the and oligotrophic water at the present, and OAE1b and OAE2. On the other hands, in the therefore, the higher 2-MHI value suggests Goguel (OAE1a) level, both TADS and C27 27 TAS values are lower. These results from algal derived from environmental and tectonic biomarkers analyses indicate that sea surface changes during the mid-Cretaceous OAEs, condition in the Vocontian Basin might be which influenced for evolution and/or changed from oligotrophic to meso- or diversification of marine microalgae, such as eutrophic condition during and after the cyanobacteria, dinoflagellate and OAE1b (near the Aptian-Albian boundary). coccolithophorid. Moreover, these variations in marine condition

References: Ando, T., Sawada, K., Okano, K., Takashima, R., Nishi, H., Primary producer community during mid-Cretaceous oceanic anoxic events (OAEs) 1a, 1b and 1d in the Vocontian Basin (SE France) evaluated from triaromatic steranes in sediments. Submitted to Org. Geochem. Kuypers, M.M.M., van Breugel, Y., Schouten, S., Erba, E., Sinninghe Damsté, J.S., 2004. N2-ﬁxing cyanobacteria supplied nutrient N for Cretaceous oceanic anoxic events. Geology 32, 853-856. Monteiro, F.M., Pancost, R.D., Ridgwell, A., Donnadieu, Y., 2012. Nutrients as the dominant control on the spread of anoxia and euxinia across the Cenomanian-Turonian oceanic anoxic event (OAE2): Model-data comparison. Paleoceanography 27, doi:10.1029/2012PA002351.

28 A newly identified positive excursion of 87Sr/86Sr ratio in the Lower Aptian platform carbonates offshore Abu Dhabi, UAE: Is it a local or global signature of Ocean Anoxic Event 1a?

Yamamoto, K.1, Ishibashi, M.2, Takayanagi, H.1, Asahara, Y.3, Sato, T.4, Nishi, H.5 and Iryu Y.1

1Inst. Geol. Paleont., Grad. Schl. Sci., Tohoku Univ., 980-8578, Sendai, Japan ([email protected]) 2Abu Dhabi Oil Comp., Ltd (Japan), P.O. Box 630, Abu Dhabi, United Arab Emirates 3Dept. Earth Planet. Sci., Grad. Schl. Envir. Stud., Nagoya Univ., 464-8601, Nagoya, Japan 4Dept. Earth Res. Sci., Fac. Internat. Res. Sci., Akita Univ., 010-8502, Akita, Japan 5Center Acad. Res. Archiv., Tohoku Univ. Mus., Tohoku Univ., 980-8578, Sendai, Japan

The early Aptian represents a period latter area are ideal archives for obtaining of significant environmental changes under high-temporal resolution records of the early extreme greenhouse conditions. This period is Aptian paleoenvironmental changes. characterized by an episodic, widespread This study provides an fully-integrated accumulation of organic carbon-rich sediments data set consisting of lower Aptian high in a global anoxic marine setting. This resolution, bulk carbonate carbon (δ13C), depositional event, known as “Oceanic Anoxic oxygen (δ18O), and strontium (87Sr/86Sr) Event 1a” (OAE1a), was associated with isotope stratigraphies, together with results of environmental changes, such as major paleontological analyses on calcareous perturbations in global carbon cycling, global nannofossils and ammonites from a core (53 m) sea-level rise, increases in continental drilled at an oil field offshore Abu Dhabi, weathering and runoff, significant changes in United Arab Emirates (UAE). The studied core flora and fauna, and drowning of carbonate consists of shallow-water carbonates deposited platforms (e.g., Föllmi et al., 1994; Menegatti in the Bab Basin at the southern Neo-Tethys et al., 1998; Erba et al., 2010; Haq, 2014). margin. We conducted careful sampling of core The Arabian Plate was located in a materials and determined mineral abundances tropical low-latitude region and constituted part and trace element (strontium, manganese, and of the southern Neo-Tethys margin in a passive iron) concentrations to identify and exclude margin setting where shallow-water carbonates diagenetically altered samples. Following the extensively accumulated on the tectonically criteria proposed by Denison et al. (1994) and stable craton throughout the Early Cretaceous Jacobsen and Kaufman (1999), we confirmed (Murris, 1980). It has been reported that early that the analyzed samples retained initial Aptian carbonate platforms in the northern 87Sr/86Sr. Neo-Tethys margin were episodically drowned The established isotope stratigraphies due to environmental stresses to shallow-water constrained by biostratigraphic data confirms carbonate factories (e.g., Föllmi et al., 1994), that the examined core represents a continuous while the coeval carbonate platforms situated depositional record of the Lower Aptian with a along the central to southern Neo-Tethys high-temporal resolution. The stratigraphic margins record continuous carbonate interval of OAE1a (Livello Selli) is identified deposition marked by an abrupt faunal change by a stepwise positive δ13C excursion that from rudists to microencrusters begins in a lithostratigraphic unit characterized (Lithocodium–Bacinella) in the platform biota by a bloom of Lithocodium–Bacinella. (e.g., Huck et al., 2010). Therefore, The 87Sr/86Sr profile through the shallow-water platform carbonates from the studied core shows an overall decreasing trend 29 that is comparable to the global 87Sr/86Sr induced by intensified continental weathering evolution of seawater during the early Aptian due to the global warming suggested by the (McArthur et al., 2001). Intensified submarine increase in δ18O values observed in the studied hydrothermal activity related to the formation core. of Ontong Java Plateau is thought to be the (2) The radiogenic (higher 87Sr/86Sr) main cause of this decrease (Bralower et al., excursion reflects a global event that is missing 1997). Biostratigraphic data available only in other sections used for reconstructing the from the stratigraphic interval above the 87Sr/86Sr evolution of global seawater. This OAE1a do not conflict with the numerical ages may be supported by relatively higher isotope obtained by comparison of the 87Sr/86Sr profile values reported from the OAE1a interval of with the global 87Sr/86Sr record (McArthur et shallow-water platform carbonate section in the al., 2001). However, the obtained 87Sr/86Sr Resolution Guyot, mid-Pacific Mountains profile shows a gradual increase upsection in (Jenkyns and Wilson, 1999). In Italy, a similar the OAE1a interval, which clearly deviates pulse of positive 87Sr/86Sr excursion standing from the overall decreasing trend of the global out against the overall trend has been reported signature. from shallow-water carbonates deposited There are two possible candidates to during Ocean Anoxic Event 2 (OAE2) that explain the higher 87Sr/86Sr ratios compared occurred around Cenomanian–Turonian with those of global seawater; boundary (Frijia and Parente, 2008). It is highly (1) Isotopically heavier strontium derived from possible that enhanced continental weathering continental crust of the Arabian Shield and/or in a global scale during these anoxic events its associated sedimentary rocks locally flowed induced the minor, but clear positive 87Sr/86Sr into the proto-Bab Basin along with nutrients, excursions of global seawater. probably through rivers. Although the δ13C Further studies on high-resolution profile of the studied core correlates well with strontium isotope stratigraphy are needed in those from other regions around the world, the stratigraphically expanded sections to conclude locally-higher 87Sr/86Sr ratios may indicate whether the radiogenic excursion occurred slightly-limited connection between the locally or globally during the OAE1a. If it is a proto-Bab Basin and the outer ocean global event, the 87Sr/86Sr profile in this study (Neo-Tethys). The bloom of will be a key data to urge the revision of the Lithocodium–Bacinella were probably global curve of seawater 87Sr/86Sr evolution. triggered by the increased nutrient supply

References: Bralower, T. J., P. D. Fullager, C. K. Paull, G. S. Dwyer, and R. M. Leckie (1997) Mid-Cretaceous strontium-isotope stratigraphy of deep-sea sections, Geol. Soc. Amer. Bull., 109, 1421–1442. Denison, R. E., R. B. Koepnick, A. Fletcher, M. W. Howell, and W. S. Callaway (1994) Criteria for the retention of original seawater 87Sr/86Sr in ancient shelf limestones, Chem. Geol., 112, 131–143. Erba, E., C. Bottini, H. J. Weissert, and E. Keller (2010) Calcareous nannoplankton response to surface-water acidification around Ocean Anoxic Event 1a, Science, 329, 428–432. Föllmi, K. B., H. Weissert, M. Bisping, and H. Funk (1994) Phosphogenesis, carbon-isotope stratigraphy, and carbonate-platform evolution along the Lower Cretaceous northern Tethyan margin, Geol. Soc. Amer. Bull., 106, 729–746. Frijia, G., and M. Parente (2008) Strontium isotope stratigraphy in the upper Cenomanian shallow-water carbonates of the southern Apennines: Short-term perturbations of 87Sr/86Sr during the oceanic anoxic event 2, Palaeogeogr. Palaeoclimatol. Palaeoecol., 261, 15–29. Haq, B. U. (2014) Cretaceous eustasy revisited, Global Planet. Change, 113, 44–58. Huck, S., N. Rameil, T. Korbar, U. Heimhofer, T. D. Wieczorek, and A. Immenhauser (2010) Latitudinally different responses of Tethyan shoal-water carbonate systems to the Early Aptian oceanic anoxic event (OAE 1a), Sedimentology, 57.

30 Jacobsen, S. B., and A. J. Kaufman (1999) The Sr, C and O isotopic evolution of Neoproterozoic seawater, Chem. Geol., 161, 37–57. Jenkyns, H. C., and P. A. Wilson (1999) Stratigraphy, paleoceanography, and evolution of Cretaceous Pacific guyots: Relics from a greenhouse Earth, Amer. J. Sci., 299, 341–392. McArthur, J. M., R. J. Howarth, and T. R. Bailey (2001) Strontium isotope stratigraphy: LOWESS version 3: Best fit to the marine Sr-isotope curve for 0–509 Ma and accompanying look-up table for deriving numerical age, J. Geol., 109, 155–170. Menegatti, A. P., H. Weissert, R. S. Brown, R. V. Tyson, P. Farrimond, A. Strasser, and M. Caron (1998) High-resolution δ13C stratigraphy through the early Aptian “Livello Selli” of the Alpine Tethys, Paleoceanography, 13, 530–545. Murris, R. J. (1980) Middle East: Stratigraphic evolution and oil habitat, Amer. Assoc. Petrol. Geol. Bull., 64, 597–618.

31 Calcareous Nannofossil Biostratigraphy of the Cenomanian-Turonian Oceanic Anoxic Event 2 (OAE2) Record in California, USA

Magtoto C.Y.1, Fernando, A. G. S.1, Takashima, R.2, Nishi, H.2 and Tomosugi, T.3

1Nannoworks Lab., Nat. Inst. Geol. Sci., Univ. Philippines, Diliman, Quezon City 1101 Philippines ([email protected]) 2Center Acad. Res. Arch., Tohoku Univ. Mus., Tohoku Univ., Aramaki Aza Aoba 6-3, Aoba-ku, Sendai 980-8578 Japan 3Hakata Koun Co., Ltd., Kashiihama Futo 4-2-2, Higashi-ku, Fukuoka 813-0016 Japan

The Cenomanian-Turonian Boundary of UC5c, latest Cenomanian) and the FO of (CTB) in the Great Valley Group (California, Eprolithus moratus (top of UC6a, earliest USA) was observed within the Gas Point Turonian). The CTB was observed near the end Member of the Budden Canyon Formation. The of the “plateau” phase of the carbon isotope boundary was delineated by Fernando et al. curve established by Takashima et al. (2011), (2011) using the FO of Eprolithus octopetalus, while Quadrum gartneri, the taxon widely used which is considered a supplementary bioevent as a CTB marker, was observed within the within the Nannofossil Zone UC5. Analysis of “recovery” phase (Figure 1). E. octopetalus, the samples collected at high resolution intervals taxon used as the CTB marker in the previous across the CTB confirms the delineation of the study by Fernando et al. (2011), was not boundary within the Gas Point Member. This is observed in the present study. An interval in addition to the recognition of other bioevents consisting of high values of total organic crucial to the establishment of nannofossil carbon (TOC) was noted between the zones and refinement of the biostratigraphy Nannofossil Zones UC3e to UC6a, which across the CTB in the Budden Canyon probably corresponds to the organic carbon Formation. excursion during the CTB Oceanic Anoxic In the present study, 6 zones were Event 2 (OAE2). This makes the Budden established (Figure 1). The CTB was delineated Canyon Formation one of the few sections in within the Nannofossil Zones UC5c to UC6a, the northeast Pacific Region where OAE2 can between the FO of Quadrum intermedium (base be observed and studied.

32 Another world of OAE2: development of oxic water around Pacific margin

Hasegawa T.

Dept. Earth Sci., Fac. Nat. Sys., Inst. Nat. Sci. Eng., Kanazawa Univ., Kakuma-machi, Kanazawa 920-1192, Japan. ([email protected])

What most intensively studied for stratigraphy associated with rigid support by Cretaceous paleoenvironment is Oceanic biostratigraphy. In the case of Tappu section Anoxic Events. Paleoenvironmental or from Hokkaido, Japan, it allows us to correlate paleoclimatological turnover associated with the section with Eastbourne section in England OAEs, especially OAE2 is often targeted by bed-to-bed. because of its brief but intensified nature and The signal of oxygenation is observed its introduction triggered by volcanisms. Black, with sedimentary structure in the Tappu section. organic-rich sediments showing oceanic anoxia Disturbance of lamination in the mudstone have been recognized in extensive areas become prominent just at the onset of the including Tethys, North and South Atlantic. carbon isotope excursion (CIE) associated with Volcanic eruption and associated OAE2 (Nemoto and Hasegawa, 2011). Across environmental changes are suggested as a the section in New Zealand, conspicuous red direct trigger of OAE2 onset (e.g. Tugeon and bed associated with very low content of Creaser, 2008). On the other hand, no terrestrial organic carbon develops at the OAE2-correlative sediments showing anoxia interval of OAE2. It indicates well-oxygenated with high organic carbon content has not been depositional condition and possible shift of found around Pacific except for material from transportation pathway of terrigenous material. equatorial region. Recent paleoenvironmental Considerable changes in faunal composition of studies exhibited it became oxic instead of micro- and/or macrofossils are observed in both anoxic or dysoxic at upper bathyal depth during sections prior to the CIE and oxygenation event. time interval of OAE2 relative to the interval Third example is a preliminary study from prior to OAE2 (Nemoto and Hasegawa, 2011; Northern East Pacific. The Hasegawa et al., 2013). Complicated mudstone-dominated outer shelf sequence from mechanism and extensive paleoceanographic Haida Guwaii (former Queen Charlotte Is.), BC, variation are suggested for introduction and Canada shows considerable fine stratification development of OAE2 over the globe. Better below the CIE but it weakens at the onset of the understanding of Pacific Ocean and its margin CIE (joint research worked with J. Haggart). is required to realize OAE2 comprehensively. Oxygenation instead of anoxia from The present talk for the IGCP608 will three isolated sites of Pacific margin suggests be based on the review of previous studies from anoxia is not a major paleoceanographic Hokkaido, Japan (Tappu and Oyubari areas), phenomenon in the Pacific during OAE2. Mangaotane and Sawpit Gully sections from Earlier shrinkage/disappearance of benthic New Zealand. Brief introduction of preliminary fauna in Japan and NZ relative to sites in the results from northern British Columbia, Canada Tethyan region and characteristic occurrences (joint research with Dr. Jim Haggart) will be of planktonic foraminifers in Japan suggest that presented. the scenario across the OAE2 interval in the Detailed inter-regional correlation is a Pacific is entirely different from that of the fundamental subject for OAE studies as they Tethyan region. In the presentation, discuss causal factors, onset, bioevents, time-stratigraphic series of OAE2-related interaction and feedback between intra-OAE subevents from sites in the Pacific and Tethyan subevents. The studies from Pacific margin regions will be summarized to discuss their achieved such correlation with carbon isotope causal relationship.

33 References: Hasegawa, T., Crampton, J. S., Shioler, P., Field, B., Fukushi, K. and Kakizaki, Y., 2013, Cret. Res., 40, 61-80. Nemoto, T. and Hasegawa, T., 2011, Palaeo-3, 309, 271-280. Tugeon, S. C. and Creaser, R. A., 2008, Nature, 454, doi:10.1038/nature07076.

34 Biotoic evolution: Asian and western Pacific fauna and flora – Microfauna I

Updates on Philippine Cretaceous System: Recent Calcareous Nannofossil Biostratigraphic Studies on Selected Cretaceous Localities in the Philippines

Fernando, A. G. S., Magtoto, C. Y., Guballa, J. D. S., Marquez-Ardiente, D. J., Nogot, J. R. C. P. and Uy, M. A. C.

Nannoworks Lab., Nat. Inst. Geol. Sci., Univ. Philippines, Diliman, Quezon City 1101 Philippines ([email protected])

Compared to other microfossil groups Catanduanes Island (eastern Philippines). like planktonic foraminifera, very few studies Recent fieldworks to these 2 localities were have been conducted regarding Cretaceous conducted to collect samples for a detailed calcareous nannofossils in the Philippines. This biostratigraphic study. The objectives include: is despite the fact that a number of Cretaceous (a) refinement of the age of the sedimentary localities/sedimentary formations have already formations using calcareous nannofossil been identified all over the archipelago. Based biostratigraphy; (b) more detailed description on available literature, nannofossil studies are of nannofossil taxa present in the 2 localities; limited to describing the species present in and (c) determination of the paleoceanographic several sedimentary formations in support of its and paleoclimatic significance of the Cretaceous age. nannofossil assemblage in relation to the The present study focuses on the overall western Pacific condition during the nannofossil biostratigraphy of Cretaceous Cretaceous. formations in Rizal Province (near Manila) and

35 Mesozoic and Paleozoic radiolarians from the Lower Cretaceous Choshi Group, Japan

Kashiwagi, K.1, Isaji, S.2 and Asai, H.3

1Grad. Schl Sci. Eng. Res., Univ. Toyama 930-8555, Japan ([email protected]) 2Nat. Hist. Mus. Inst., Chiba, Chiba 260-8682, Japan 3Chiba Pref. Inba Reg. Branch Office, Chiba 285-8503, Japan

Introduction and general geology of the The Ashikajima Formation includes Choshi Group conglomerate beds at its basal horizon, which is The Choshi Group, first stop of the conformably covered by stratified sandstone post excursion, extends ca. 4 km in a (Katsura et al., 1984). Chert pebbles and north–south direction along the eastern cobbles in the conglomerate beds frequently coastline of Kanto Region, Japan, and is contain radiolarians. Age assignable assigned to Barremian to late Aptian (maybe, radiolarians were obtained from two chert early Albian) due to ammonoids and samples out of processed 10 those. One sample foraminifers (Obata et al., 1975, 1982; Obata contains Eucyrtidiellum sp., Hsuum sp., and Matsukawa, 2007, 2009ab). The Choshi Striatojaponocapsa sp. (Striatojaponocapsa Group consists of terrigenous clastic rocks, and conexa or Striatojaponocapsa synconexa), is divided into five units; the Ashikajima, Syringocapsa sp. and Williriedellum sp. The Kimigahama, Inubozaki, Toriakeura, and age is Bajocian to early Callovian for the Nagasakihana formations in ascending order presence of Striatojaponocapsa conexa or (Obata et al., 1982). Its depositional Striatojaponocapsa synconexa (Baumgartner et environment has been interpreted as shoreface, al., 1995). Also the age of the other sample is offshore, and intra–shelf basin by means of the Permian. observation of the well–defined sedimentary The Kimigahama Formation is structures (Katsura et al., 1984; Ishigaki and Ito, composed of the alternation of medium– to 2000). Due to abundant occurrences of fine–grained sandstone and bioturbated macrofossils: ammonoids, bivalves, gastropods, mudstone, and its depositional environment has brachiopods, echinoids, shark teeth, plant been interpreted as offshore (Katsura et al., fossils (petrified woods and ambers) and so on 1984). Radiolarians were extracted from the (e.g., Shikama and Suzuki, 1972; Hayami and sandy shell bed intercalation within the Oji, 1980; Kase and Maeda, 1980; Obata et al., sandstone–mudstone alternations. Radiolarians 1982; Saiki et al., 1991; Sakagami, 1997; Obata are very rare and poorly ill–preserved. Most of and Matsukawa, 2007, 2009ab; Matsubara, them show spherical to subspherical test in 2009), the Choshi Group is one of the most outline, and 180-380 μm in length or diameter important strata to reconstruct shallow marine of test. Only 2 forms are identified; biofacies during Early Cretaceous along East Praeconosphaera sp. and Sethocapsa ? orca Asian continents. On the other hand, Foreman. Sethocapsa ? orca Foreman has a microfossils had been only foraminifers (Obata broad age range of early Hauterivian to early et al., 1982; Matsubara et al., 2005). Here we Aptian by Baumgartner et al. (1995). Also its preliminarily report some radiolarian last appearance datum is not restricted. So occurrences from the Choshi Group. radiolarian–bearing shell bed indicates early Materials for radiolarian analyses and Hauterivian to early Aptian or later based on radiolarian ages the presence of Sethocapsa ? orca. Radiolarians were obtained from the The Toriakeura Formation consists of the Ashikajima, Kimigahama and Toriakeura sandstone–mudstone alternations in the lower formations in the Lower Cretaceous Choshi horizon and muddy facies in the upper horizon, Group. and its depositional environment is interpreted as offshore (Katsura et al., 1984). The sample 36 for radiolarian analysis, provided by Asai, H. is to its lithology and age (e.g., Takahashi, 1990). calcareous nodule within muddy facies. Consequently chert gravels in the Ashikajima Identified radiolarians in generic and specific Formation have been derived from the Jurassic levels are Archaeodictyomitra mitra Dumitrica, accretionary complex. Dictyomitra pseudoscalaris (Tan) sensu Schaaf, Radiolarians from the sandy shell bed Holocryptocanium sp. as nassellarians, and in the Kimigahama Formation indicate a Angulobracchia sp., Cenosphaera sp., Hauterivian to early Aptian age or later, and its Orbiculiforma sp. and Praeconocaryomma sp. age is concordant with previously–reported as spumellarians. Archaeodictyomitra mitra ammonoid age as Barremian (Obata and ranges in age from Berriasian to Barremian as Matsukawa, 2007, 2009ab). The sandy shell far as known (Dumitrica et al., 1997). bed also yields diversified macro– and micro– Dictyomitra pseudoscalaris indicates a late fossil taxa: bivalves (Hayami and Oji, 1980), Valanginian to early Aptian (Baumgartner et al., gastropods (Isaji et al., 2014), otoliths (Miyata 1995), and its last occurrence datum is not et al., 2014), and so on. It should be noted that precisely restricted. Thus radiolarian–bearing radiolarian tests are restricted to similar forms sample indicates age interval of late in outline and size of test. Especially, sizes of Valanginian to early Aptian or later. tests show fine– to medium–grained sand. So Brief discussion these evidences suggest that the radiolarian The Middle Jurassic chert is one of the tests in the sandy shell bed had been strongly most common lithological components in the sorted in their size and form during its Jurassic to Early Cretaceous accretionary depositional process. complexes in Japan and East Asian continents. Radiolarians from the Toriakeura Formation In the Choshi area, Triassic chert, which has are also consistent with ammonoid age been tentatively named as “the Kurohae Chert”, previously–reported in Obata and Matsukawa is isolated by surrounding reclaimed land, and (2007, 2009ab). Also radiolarian assemblage crops out in small area adjacent to the shows well diversification, and support that Ashikajima Formation of the lowest Choshi radiolarians from the Kimigahama Formation Group (Kunihiro et al., 1984; Suzuki, 1986). was highly–sorted assemblage due to low “The Kurohae Chert” has been correlated with diversification. a part of the Jurassic accretionary complex due

References: Baumgartner, P. O., O'Dogherty, L., Goričan, Š., Dumitrica-Jud, R., Dumitrica, P., Pillevuit, A., Urquhart, E., Matsuoka, A., Danelian, T., Bartolini, A., Carter, E. S., De Wever, P., Kito, N., Marcucci, M. and Steiger, T., 1995, Radiolarian catalogue and systematics of Middle Jurassic to Early Cretaceous Tethyan genera and species. In Baumgartner, P. O., O'Dogherty, L., Goričan, Š., Urquhart, E., Pillevuit, A. and De Wever, P., eds., Middle Jurassic to Lower Cretaceous Radiolaria of Tethys: Occurrences, Systematics, Biochronology, Mém. Géol. (Lausanne) 23, 37–685. Dumitrica, P., Immenhauser, A. and Dumitrica-Jud, R., 1997, Mesozoic radiolarian biostratigraphy from Masirah Ophiolite, Sultanate of Oman Part 1: Middle Triassic, Uppermost Jurassic and Lower Cretaceous Spumelalrians and multisegmented nassellarians. Bull. Nat. Mus. Nat. Sci., 9, 1–106. Hayami, I. and Oji, T., 1980, Early Cretaceous bivalvia from the Choshi District, Chiba Prefecture, Japan. Trans. Proc. Palaeont. Soc. Japan, N. S., no. 120, 419–448. Isaji, S., Haga, T. and Kashiwagi, K., 2014, A planispiral 'lower heteronranch' gastropod from the Lower Cretaceous Choshi Group, Chiba Prefecture, Japan. Ann. Meet. Palaeont. Soc. Japan, Abstr., 46. (in Japanese) Ishigaki, A. and Itoh, M., 2000, Size population of hummocky bedforms: an example from the Lower Cretaceous Choshi Group, northeastern Boso Peninsula, Japan. Jour. Geol. Soc. Japan, 106, 472–481. (in Japanese with English abstract) Kase, T. and Maeda, H., 1980, Early Cretaceous gastropoda from the Choshi District, Chiba Prefecture, central Japan. Trans. Proc. Palaeont. Soc. Japan, N. S., no. 118, 291–324.

37 Katsura, Y., Masuda, F. and Obata, I., 1984, Storm-dominated shelf sea from the Lower Cretaceous Choshi Group, Japan. Ann. Rep., Inst. Geosci., Univ. Tsukuba, no. 10, 92–95. Kunihiro, S., Saito, H. and Sakagami, S., 1984, Discovery of Triassic conodonts from the “Kurohae chert” in the Choshi Peninsula. Jour. Tokyo Geogr. Soc., 93, 57–59. (in japanese) Matsubara, T., 2009, Summary of Amber and Inclusions from the Lower Cretaceous Choshi Group in Chiba Prefecture, Japan. Chigaku Kenkyu, 57, 199–206. (in Japanese with English abstract) Matsubara, Y., Hisada, K., Motoyama, I. and Nishi, H., 2005, Stratigraphy and geologic structure of the Cretaceous Choshi Group in the Inubosaki Point, Central Japan. Bull. Saitama Mus. Nat. Hist., no. 22, 1–14. (in Japanese with English abstract) Miyata, S., Isaji, S. and Kashiwagi, K., 2014, The first record of otloliths from the Kimigahama Formation (Lower Cretaceous) of the Choshi Group, Chiba Prefecture, Japan. Ann. Meet. Palaeont. Soc. Japan, Abstr., 45. (in Japanese) Obata, I., Hagiwara, S. and Kamiko, S., 1975, Geological age of the Cretaceous Choshi Group. Bull. Nat. Sci. Mus. Tokyo, Ser. C, 22, 17–36. (in Japanese with English summary) Obata, I. Maiya, S. Inoue, Y. and Matsukawa, M., 1982, Integrated mega- and micro-fossil biostratigraphy of the Lower Cretaceous Choshi Group, Japan. Bull. Nat. Sci. Mus. Tokyo, Ser. C, 8, 145–179. Obata, I. and Matsukawa, M., 2007, Barremian–Aptian (Early Cretaceous) ammonoids from the Choshi Group, Honshu (Japan). Cret. Res., 28, 363–391. Obata, I. and Matsukawa, M., 2009a, Supplementary description of the ammonoids from the Barremian to the Albian of the Choshi Peninsula, Japan. Cret. Res., 30, 253–269. Obata, I. and Matsukawa, M., 2009b, Some ammonoids from the Barremian and probable Albian of the Choshi Peninsula, Japan. Bull. Tokyo Gakugei Univ., Nat. Sci., 61, 97–103. Saiki, K., Kimura, T. and Horiuchi, J., 1991, Stenopteris cyclostoma Saiki, Kimura et Horiuchi sp. nov. (possible pteridosperm), from the Lower Cretaceous Choshi Group, in the Outer Zone of Japan. Trans. Proc. Palaeont. Soc. Japan, N. S., no. 164, 964–972. Sakagami, S., 1997, Geology of the Choshi area. Natural History of the Chiba Prefecture, Part 2, Series 41: Geology of the Chiba Prefecture, Chiba Prefecture, 83-100. * (in Japanese) Shikama, T. and Suzuki, S., 1972, Stratigraphy and Tectonic development mainly of Cretaceous formations of Choshi Peninsula, Chiba Prefecture. Sci. Rep. Yokohama Nat. Univ. Sec. Ⅱ, no. 19, 133–157. (in Japanese with English abstract) Suzuki, R., 1986, Radiolarians from “the Kurohae Formation” in the Choshi area, Chiba Prefecture, Japan. 93th Ann. Meet. Geol. Soc. Japan, Abstr., 208. * (in Japanese) Takahashi, N., 1990, Geology of the Pre–Cretaceous Atagoyama Group in the Choshi Peninsula, Chiba Prefecture, Japan–Description of the lithofacies and discussion of sedimentary and tectonic processes–. Jour. Natu. Hist. Mus. Insti. Chiba, no. 1, 1–13. (in Japanese with English abstract) * English translation from the original written in Japanese

38 Early Cretaceous Foraminiferal Fauna from the Western Margin of the Shan Plateau, Myanmar

Zaw Win

Mawlamyine Univ., Mawlamyine City, Mon State, Myanmar ([email protected])

The Shan Plateau constituting part of Simplorbitolina spp., Iraqia sp. and the Shan-Thai block in eastern Myanmar is Dictyoconus aff. walnutensis. Figure 1 shows fringed along its western margin with the location of the sampling areas and the Mogok Belt (Searle and Ba Than Haq, 1961, foraminiferal fauna recovered. Mitchell et al., 2007), a north-south trending Other smaller foraminifers are Feurtillia sp., narrow linear belt in which various Paleozoic Charentia kyaukkuensis sp. nov., and Mesozoic sedimentary rock units have Praechrysalidina sp. and a few textularids. been highly deformed and metamorphosed in Among these, the taxon, Charentia relation with younger igneous intrusions. A kyaukkuensis, is herein considered as a new sequence of shallow marine siliciclastic rocks species because of its smaller shell size, having with minor carbonate rock interbeds of broadly arched periphery and prominent Jurassic-Cretaceous age (known as the Pan triangular spiral projections. Laung Formation) has been recorded within The present fauna is associated by some algae this belt (e.g. Garson et al., 1976; UN Team, such as Cayeuxia sp., Cladocoropsis sp. and 1979; Myint Thein and Win Myint, 1988). Polygonella sp. Moreover, a few specimens of However, the stratigraphic entity of some nerinellid gastropods, conferrable to Nerinella limestones occurring as isolated hillocks in the cultrispira Roemer, occur in a limestone beds alluvial plain of this belt remained below this foraminiferal fauna-bearing controversial for a long time because of lacking limestone horizon at Kyaukku Hill. paleontological evidence. They were Among the foraminifers of the present sometimes lumped in the foraminiferal fauna, various members of the Carboniferous-Permian units, or regarded as of orbitolinids are proved to be the key to settle a Permian-Triassic unit, or thought likely to be the age problem of the limestone exposed in of Mesozoic Pan Laung Formation. these hillocks. From their relative simplicity of In order to settle this stratigraphic morphological features such as smaller size of uncertainty, some limestone samples were test and lack of reticulate inner parts, narrow collected from the isolated hillocks of two apical angle, the orbitolinid taxa of the present separate areas, namely, the Lungyaw area in fauna exhibit such Early Cretaceous aspects, Myittha Township in the north and the Lebyin most possibly Aptian to Albian. area in Thazi Township in the south. A total of Both sedimentary facies aspects of the sixteen samples (four from the Kyaukku Hill limestones and paleoecological aspects of and Pantingu Hill of Lungyaw area, and twelve orbitolinids and associated other fossils clearly from Peinyoin Hill of Lebyin area) were indicate the prevalence of shallow marine in collected randomly for micropaleontologic the present area during the Early Cretaceous examination. period. The present finding of orbitolinid fauna As a reward for the present attempt, is the first to record the southeastern most the limestone samples from both areas yielded occurrence of the orbitolinid-bearing belt in a foraminiferal fauna formed of orbitolinids Myanmar that has so far been recorded only on and other smaller foraminifers. The present the west of the second defile of the preliminary thin-section examination reveals Ayeyarwaddy (Irrawaddy) River, far north of that the orbitolinid fauna consists of the Mandalay City. This fauna, perhaps, witnesses following taxa: Paracoskinolina cf. most possibly the southeastern extension of the sunnilandensis, Paracoskinolina sp. ind., 39 Cretaceous equatorial Tethys marine incursion in this part of the Southeast Asian region.

Reference: Garson, M.S., Amos, B.J., Mitchell, A.H.G., 1976. The geology of the area around Neyaungga and Ye-ngan, southern Shan State, Burma. Overseas Mem. 2, Inst. Geol. Sci., London, pp. 1-70. Mitchell, A.H.G., 1979. Geology and Exploration Geochemistry of the Shan Scarp Area, East of Kyaukse, Thazi and Tatkon, Central Burma. Geological Survey and Exploration, Technical Report 3, UNDP, UN, New York. Mitchell, A.H.G., Htay, M.T., Htun, K.M., Win, Oo, T., Hlaing, T., 2007. Rock relationships in the Mogok Metamorphic Belt, Takon to Mandalay, central Myanmar. J. Asian Earth Sci., 29, 891-910. Myint Thein & Win Myint, 1988. Stratigraphy, Petrography and Paleoenvironment of the Jurassic-Cretaceous Sedimentary Rocks of the Lungyaw – Ma-u-bin Area, Myittha and Ye-ngan Townships. Research Paper (unpublished), Univ. Mandalay, 1-35, pl. 1-4. Searle, D.L. & Ba Than Haq, 1964. The Mogok Belt of Burma and its relationship to the Himalayan orogeny. 22nd Int. Geol. Cong., India, 11, 133-161, New Delhi.

Figure 1. Location of the sampling areas and the fauna recovered. 1: Paracoskinolina cf. sunnilandensis; 2: Iraqia sp.; 3: Simplorbitolina sp.; 4: Paracoskinolina sp.; 5: Charentia 2 kyaukkuensis sp. nov. 3 4 (not to definite scale).

2 3 4 5

Day Two 5 September 2014

SESSIONS:

Biotic evolution: Asian and western Pacific fauna and flora – Microflora

Geoparks highlighting Cretaceous

Land-ocean linkages: Correlation, sedimentology and paleoenvironments

41 Bitotic Ebolution: Asian and western Pacific fauna and flora II – Micro flora

Late Cretaceous calcareous nannofossils from Nimar Sandstone, Bagh area, central peninsular India

Rai, J.1, Garg, R.1, Singh, A.1, Garg, S.1, Bajpai, S.1, Kapur, V. V.1, Agarwal, S.1 and Tripathi, S. C.2

1Birbal Sahni Inst. Palaeobot., 53, University Road, Lucknow- 226007 ([email protected]) 2Sur. India, Aliganj, Lucknow-226020

The late Cretaceous infratrappean for the deposition of Cretaceous rocks in the sedimentary sequences of peninsular India Narmada valley and considered the Lameta occur along the ENE-WSW Narmada-Son Formation in Jabalpur area to be marine. lineament and are exposed in a belt extending However, the dinosaur remains including eggs, from the Saurashtra region of western India to fresh water mollusks and petrified fossil woods the central part of the Indian shield beyond favour a fresh water depositional environment Jabalpur. Resting unconformably over the for the Lameta Formation. Precambrian Basement or the Upper Gondwana A Cenomanian-Coniacian age was sediments, these infratrappean sequences are suggested (Chiplonkar,1980) for the Bagh characterized by both marine and continental Formation based on megafossils, and the facies with a wealth of fossils, ichnotaxa and microfossil data suggest a Coniacian age based sedimentary structures that point to repeated on ostracodes (Jain, 1975), late significant transgressive-regressive events. Cenomanian-early Turonian age based on Traditionally, these sequences are classified as planktonic foraminifers (Jain, 1961; Sharma, the Nimar Sandstone, Bagh and Lameta 1976) and a late Turonian-early Coniacian age formations, with a total thickness of only a few (Eiffellithus eximus Zone) based on calcareous dozens of meters. The oldest unit i.e. the Nimar nannofossil assemblage recovered from the Sandstone is an unfossiliferous sandy facies upper Nimar Sandstone (Jafar, 1982). It is to be consisting of conglomerates, coarse sandstone noted that, in the absence of Marthasterites and shales, gradually merging into a furcatus, Jafar (1982) suggested single, dominantly calcareous facies with subordinate short-lived (less than a million year) sandstone of the overlying Bagh Formation. transgressive event of late Turonian age Thalassinoides burrows are common in the responsible for the deposition of the entire Bagh Formation, along with rare echinoids and Narmada valley sequence. The nannofossil ammonoids, indicating low energy record of Jafar (1982) is useful to some extent environment of deposition below the wave base. for dating the Cretaceous sequence in central At places planar and trough cross bedding and India but the Cenomanian/ Turonian marker large rippled surfaces are seen. The youngest taxa Hayesites albiensis and unit i.e. the Lameta Formation (comprising Turonian/Coniacian marker taxa Lithastrinus dinosaur-bearing cherty limestones, sandstones grilli, Arkhangelskiella specillata and M. and shales) is well developed in the upper furcatus were not recorded. Jafar (1982) also Narmada valley. mentioned the absence of the Tethyan marker The age and depositional environment genus Nannoconus in the Bagh area. of the infratrappean sequence continue to be Systematic sampling was done during debatable (Raiverman,1975; Chiplonkar & the field excursion of the First Meeting of Borkar, 1975; Singh & Srivastava,1981). Singh IGCP 608 in central India in December 2013 to (1981) proposed an estuarine complex model find nannofossil productive levels for precise 42 dating. Samples collected from the Baria Nala There also appears hardground indicating section have revealed two nannofossil mixing of nannofossils of two- three subzones productive levels (Fig. A, B). Sample NS 6 of UC 9= CC 13b of Sissingh, 1977 and Perch- representing the top of the Nimar Sandstone is Nielsen, 1985 (UC 9a base = FO L. septenarius, overlain by a highly bioturbated horizon and a Turonian; UC9b base = FO Z. biperforatus, mega ripple horizon, and the sample NS 7 Turonian. H. turonicus indicates presence of represents the base of the overlying lower part of UC 9c zone of early Coniacian ammonite-yielding unit i.e. Nodular Limestone. age while the presence of M. adumbrata NS 6 has yielded 41 nannofossil species and indicates the middle of UC 9c also of early NS 7 has yielded 32 species. The rare Coniacian (N. Germany, Central Poland, SE occurrence of the genus Biscutum, combined England, NE England) whereas its FO is with elevated numbers of Watznaueria species recorded in Upper Turonian in Czech Republic and Polycyclolithaceae indicate reduced and Indian Ocean DSDP Site 258 (Burnett, surface water fertility possibly due to dilution 1998; Lees, 2008). caused by the mixing of marine water in the In the same area, samples from the riverine system. Polycyclolithaceae in general Chakrud section near Zeerabad area have and the genus Eprolithus in particular, which is yielded a moderately diversified nannofossil highly resistant to dissolution and considered a assemblage of late Campanian age. The cool water taxon, is present in abundance in the assemblage includes Marthasterites furcatus assemblage, similar to various European and (Rai et al., 2013a) whose FO may possibly Tethyan sections (Lamolda et al. 1994; Linnert demarcate the Turonian/ Coniacian global et al., 2011). A number of Nannoconus species boundary (Jafar, (1982) and LO in Campanian. represented by N. inornatus, N. steinmannii, N. The younger and the evolutionarily advanced truittii in the sample NS6 are recorded, whereas M. crassus is also present in the assemblage. in the sample NS 7 Nannoconus is lacking. Being diachronous M. furcatus is not Both E. eximus and E. turriseifelli are present considered a good marker (Lees, 2008). Thus it in NS6 whereas only E. eximus is present in NS could be surmised that there were multiple 7 along with E. gorkae and E. cf. E. parallelus. episodic and short lived transgressive events The record of Lithastrinus septenarius in NS 7 along the Narmada river valley in a tectonic is significant as the FO this taxon marks the graben during late Turonian – Coniacian - late Turonian with Micula adumbrata (Burnett, Campanian time leading to major facies 1998). The FO of the latter species is used in N. variation. The idea of a single short-lived Germany, Central Poland, SE and NE of transgression (Jafar, 1982) is not tenable. England to date the early Coniacian, although Further, the record of Nephrolithus frequens in Czech Republic and Indian Ocean Site 256 from the Chakrud section in a horizon bearing its FO is considered to mark Turonian. Also abundant petrified wood fossils (? Lameta recorded is the presence of Zeugorhabdotus Formation) provides evidence for a late biperforatus, the FO of which indicates UC9b Campanian age with marked cooling. The of Turonian in N. Germany (UC9b top), present data suggest the mixing of cold water Central Poland, Czech Republic, NE England taxa (Polycycolithaceae, Nephrolithus, and the Indian Ocean Site 256, but the Biscutum) and warm water Tethyan forms Coniacian in SE England (Lees 2008). Z. (Nannoconids) in the late Cretaceous of Central erectus present in NS 7 is a high fertility taxon. India as well as in Rajasthan region of western It appears that the India (Rai et al., 2013b) and the Cauvery Basin Turonian-Coniacian boundary in Baria Nala of southern India (Kale & Phansalkar, 1992; Section lies at or close to the Nimar Sandstone Jafar & Rai, 1989). and Nodular Limestone formational boundary.

References: Burnett, J.A. (1998). Upper Cretaceous. In: Bown, P.R. (Ed.), Calcareous Nannofossil Biostratigraphy. Chapman & Hall, pp. 132-199. Jafar, S.A. (1982). Nannoplankton evidence of Turonian transgression along Narmada valley, India and Turonian-Coniacian boundary problem. J. Palaeont. Soc. India, 27: 17-30.

43 Jafar, S.A. & Rai, J. (1989). Discovery of Albian nannoflora from Type Dalmiapuram Formation, Cauvery Basin India, Palaeoceanographic remarks. Current Sci., 58: 358- 363. Kale, A.S. and Phansalkar, V.G. (1992). Nannofossil biostratigraphy of the Utatur group, Trichinopoly district, South India. Memorie di Scienze Geologiche, 63: 89-107. Lamolda, M.A., Gorostidi, A. & Paul, C.R.C. (1994). Quantitative estimates of calcareous nannofossil changes across the Plenus Marls (latest Cenomanian), Dover, England: implications for the generation of the Cenomanian-Turonian boundary event. Cret. Res., 15: 143-164. Lees, J.A. (2008). The calcareous nannofossil record across the Late Cretaceous Turonian/Coniacian boundary, including new data from Germany, Poland, the Czech Republic and England. 29: 40-64. Linnert, C., Mutterlose, J. & Herrle, J.O. (2011). Late Cretaceous (Cenomanian-Maastrichtian) calcareous nannofossils from Goban Spur (DSDP Sites 549, 551): Implications for the palaeoceanography of the proto North Atlantic. Palaeo-3., 15, 507-528. Perch- Nielsen, K. (1985). Albian to Pleistocene calcareous nannofossils from the western South Atlantic, DSDP Leg 39. Initial Reports Deep Sea Drilling Project, 39: 699-823. Rai, J., Garg, R. & Kumar, S. (2013a). Early Campanian nannofossils from Chakrud section of the Bagh area, central India. In: cretaceous ecosystems and their responses to palaeoenvironmental changes in Asia and the western Pacific (IGCP-608): pp. 55. (Abstract) Rai, J., Singh, A. & Pandey, D.K. (2013b). Early to Middle Albian age calcareous nannofossils from Pariwar Formation of Jaisalmer Basin, Rajasthan, western India and their significanc. Current Science, 105(11): 1604-1611.

44 Palynofloral Changes across Cretaceous-Paleogene: A Case study from Deccan Volcanic Sequence in Amarkantak Group of Central India

Thakre, D., Samant, B. and Mohabey, D. M.

1PG Department of Geology, RTM Nagpur University, Nagpur-440001, India ([email protected])

Introduction genera and 63 species were recorded from this The Deccan Continental Flood Basalt intertrappean, out of which Gabonisporis (DCFB) Province is one of the largest and best vigourouxii, Aquilapollenites bengalensis, studied continental flood basalt provinces in the Jiangsupollis straitus, Proxapertites world. It covers an area of about 500,000 km2 operculatus, P. cursus, Spinizonocolpites in the central and western India. The present echinatus, S. baculatus, Ephedripites spp., study focuses on the sedimentary beds Dipterocarpuspollenites sp., Normapollis (intertrappean) associated with the DCFB group pollen, Stritricolporites sp., Cranwellia sequences exposed in the volcanic subprovince striata, Scollardia trapaformis, Intrareticulites of Chhindwara district of Madhya Pradesh. The brevis, and Neocouperipollis spp., are the most Deccan Volcanic Sequence (DVS) in this area dominating taxa. In addition, taxa like Azolla are classified as the Amarkantak Group cretacea, Cyathidites australis, Triporoletes comprising Mandla, Dhuma, Pipardehi, Linga, reticulatus, Farabeipollis sp., Retitricolopites Multai, Amarwara, Khampa and Kuleru spp., and many tri- and tetra colpate pollen formations, in ascending stratigraphic order grains are also present in the assemblage. The (Geological Survey of India, 2000). Around 18 present study also recorded age marker taxa intertrappean sections were studied for such as Aquilapollenites bengalensis, Azolla palynological analysis. cretacea, Gabonisporis vigourouxii, which indicate Maastrichtian age for the intertrappean. Intertrappean flora The presence of Spinizonocolpites spp. (Nypa), In the lower part of the Amarkantak Proxapertites operculatus, P. cursus Group two intertrappean sections are present in (Arecaceae) and foraminiferal linings, suggest Mandla and Dhuma formations, the lower one marine influence in the area and possibly is Mohagaon Kalan Well Section (MKWS) and estuarine conditions. The successively the upper one is Mohagaon Kalan Fossil Forest overlying MKFF is rich in megafloral remains (MKFF). Both these intertrappean sections are including angiosperms, gymnosperms, separated by a flow. Magnetostratigraphy of pteridophytes, algae and fungi and on the basis these two sections indicate deposition in Chron of megaflora, Cretaceous to Paleocene age is 30N for MKWS and Chron 29R for MKFF. assigned to this intertrappean. Till date only Lithologically MKWS is composed of green record of palynomorphs from this intertrappean shales, finely laminated gray shales, is by Chitaley (1951) however, she gave only palynomorph bearing black lignitic shales and morphological description of palynomorphs carbonaceous clays in ascending startigraphic without any taxonomic nomenclature. In the order. Dinosaur eggshells and Maastrichtian present study, rich and diverse palynoasseblage palynomorphs (Srinivasan, 1996; Kar and has been recorded from MKWS intertrappean. Srinivasan, 1997; Kumaran et al., 1997) have The recovered palynoassemblage is grouped been recorded from this intertrappean. During into 10 genera and 32 species. Out of which, present study, detailed palynofloral analysis of Aquilapollenites bengalensis, Azolla cretacea nine well sections (WS) representing various and Gabonisporis vigourouxii are the most lithofacies of this intertrappean was carried out. dominating taxa. Due to the presence of The study recorded diverse palynoassemblages Maastrichtian marker palynotaxa such as and many new palynomorphs. Overall 28 Aquilapollenites bengalensis, Azolla cretacea 45 and Gabonisporis vigourouxii MKFF is firmly by 15 genera and 21 species. The dominance of assigned Maastrichtian age. MKFF has Sparganiaceaepollenites reticulates (Typha) in Spinizonocolpites (Nypa) pollen and Nypa fruit this intertrappean indicate open fresh water (Bonde, 2008) which suggest marine influence ponding condition. in this intertrappean. Overlying this The palynological and lithological intertrappean is Jhilmili intertrappean which analyses of intertrappean sediments in occurs in Dhuma formation. This Intertrappean Chhindwara indicate changing climatic did not yield any palynomorphs, however, it conditions in Amarkantak Group. The has been dated as Paleocene (Early Danian) on lowermost intertrappean bed of the MKWS is the basis of P1a zone foraminifera (Keller et al. associated with black carbonaceous lignitic to 2009). The successively overlying, Butera and sapropelic shales. These shales contain a Lohara intertrappean between Pipardehi and diverse and well-preserved palynoassemblage Linga formations did not yield any and high concentrations of fungal spores and palynomorph however it is rich in dicot fossil fruiting bodies, suggesting a humid woods. The overlying Umaria Isra (UI) and environment. The immediately overlying diatoms bearing Ghat Parasia (GP) MKFF section contains a diverse megafloral intertrappeans between Linga and Multai and palynofloral assemblages suggesting humid formations did not yield palynomorphs. Ghat climatic conditions (Kapgate, 2005). The Parasia intertrappean has good assemblage of subsequent climatic shift from humid to centric (Aulacoseira) and pinnate diatoms as semiarid-arid conditions is indicated in the well as sponge spicules. immediately overlying Paleocene sediments at The succesive Pindrai intertrappean Jhilmili intertrappean. Lithology, clay (between Multai and Amarwara formations) mineralogy, and oxygen isotopes of this 14 m and Surli intertrappen (between the Khampa thick intertrappean section suggest deposition and Kuleru formations) are rich in in mostly semiarid to arid climatic condition palynomorphs. The palynoassemblage of (Keller et al., 2009). Successively overlying Pindrai comprises of Spinizonocolpites spp., Butera-Lohara, Ghat Parasia and Umaria Isra Palmaepollenites nadhamunii, indicate fluctuating climate from arid to humid. Palmaepollenites elongatus, Aquilapollenites Palynoflora and lithology of Pindrai and Surli bengalensis, Proxapertites operculatus, intertrappean indicates slightly humid climatic Sparganiaceaepollenites reticulates. The conditions. Overall analysis of the presence of Spinizonocolpites spp. (Nypa) intertrappean deposits of Amarkantak Group in indicate marine influence whereas, Chhindwara area indicate long sedimentation Sparganiaceaepollenites reticulatus (Typha) history from Late-Cretaceous (Maastrichtian, pollen suggests fresh water ponding condition. Chron 30N) to Early Paleocene. It also The overall pollen data suggest deposition in indicates significant change in climatic open fresh water ponding condition with condition from humid-arid to semi-arid and marine influence (estuarine condition). The humid and depositional environment from overlying Surli intertrappean bed yielded a estuarine to fresh water ponding. good concentration of palynoflora represented

References: Bonde, S.D., (2008). Indian fossil monocotyledons: current status, recent developments and future direction. Palaeobotanist, 57, 141–164. Chitaley (1951). Fossil megaflora from the Mahagaon kalan beds of the Madhya Pradesh, India. Proc. Nat. Inst. Sci. India, v. XVII. Geological Survey of India (2000) District Resource Map, Chhindwara district, Madhya Pradesh. Kapgate, D. K., (2005). Megafloral analysis of intertrappean sediments with focus on diversity and abundance of flora of Mohagaon Kalan, Mandla and adjoining areas of Madhya Pradesh. Gondwana Geol. Mag., 20, 31-45. Kar, R. K., Srinivasan, S., (1997). Late Cretaceous palynofossils from the Deccan intertrappean beds of Mohagaon Kalan, Chhindwara District. Madhya Pradesh. Geophytology, 27, 17-22.

46 Keller, G., Adatte, T., Bajpai, S., Mohabey, D. M., Widdowson, M., Khosla, A., Sharma, R., Khosla, S. C., Getsch, B., Fleitmann, D., and Sahani, A., (2009). K-T Transition in Deccan Traps of Central India marks major marine seaway across India; Earth Planet. Sci. Lett., 282, 10-23. Kumaran, K. P. N., Bonde, and S. D., Kanitkar, M. D., (1997). An Aquilapollenites associated palynoflora from Mohagaon Kalan and its stratigraphic implications for age and stratigraphic correlation of Deccan intertrappean beds. Current Sci., 72, 590–592. Srinivasan, S.,(1996). Late Cretaceous egg shells from the Deccan volcano-sedimentary sequences of central India, in Sahni, A., ed., Cretaceous stratigraphy and environment. Rama Rao volume. Mem. Geol. Soc. India, 37, 321-336.

47 Pattern of biodiversity changes in Late Cretaceous-Early Paleocene Palynoflora of Deccan volcanic province

Samant, B. and Mohabey, D. M.

Postgrd. Dept. Geol., RTM Nagpur Univ., Amravati Road, Nagpur-440001, India. ([email protected])

Introduction et al, 1995, Mohabey 1996, Mohabey and Deccan Continental Flood Basalt Udhoji 1996,Mohabey et al, 1993) in Later (DCFB) province covers two third of landmass Cretaceous (Maastrichtian, Chron 30n-29r). in the central and western India. Impact of this Sediments are pedogenically modified having large volcanic event on biota and response of calcrete profile and comprises clays, siltstone, biota to volcanism induced climatic and sandstones, marlites and limestones. Of the five environmental changes is still under study. Lameta basins only three basins viz. Since last two decades a lot of data has been Balasinor-Jhabua, Nand-Dongargaon (N-D) generated on the biota of the Late and Jabalpur have been studied in detail for Cretaceous-Early Paleocene Deccan volcanic their lithofacies and faunal analysis associated sediments, however, the knowledge (summarised by Khosla and Sahni 2003, Prasad of their biodiversity and biotic response to 2012). Studies have indicated that Lameta volcanism has been inadequate owing to the sediments have diverse faunal assemblage lack of chronostratigraphic constraints on represented by both invertebrates- bivalves, Deccan volcanic sequences and inadequate gastropods and ostracods and stratigraphic control on sampling of the vertebrates-represented by titanosauriform and sediments from the multiple sedimentary beds abelisaurid dinosaurs, pelomedisoid turtles, (intertrappean) at different stratigraphic levels madtsoid snakes, crocodiles, frogs, fishes and within the Deccan volcanic sequences. Hence mammals. Megafossils of plants are rare and to understand the impact of 6-7 my long (Sheth are known mostly fom the N-D Basin only. The et al, 2001, Sheth and Pande 2014) volcanism reported megaflora include charophytes, on the biota, the sediments of infratrappean pteridophytes (Isoetes leaf impression), (Lameta Formation) and successive gymnosperms (Araucarites, Brachiophyllum, stratigraphically controlled intertrappean beds Pagiophyllum, Equisetites) and angiosperms within Deccan volcanic province were studied. (leaf impressions of palms and dicots), Lameta sediments are exposed as monocotyledonous and dicotyledonous fruits; detached outcrops in the five inland basins in Capper of the Capparidaceae, small pieces of central and western India and the intertrappean wood attributable to palm, Lecythidaceae sediments are mostly exposed in the fringes of (Barringtonioxylon) and Sapindaceae the DCFB province. Present study has helped (Euphorioxylon). in recording many new intertrappean localities The palynoflora from the Lameta including palynomorph productive localities in Formation is known only from two basins the Deccan volcanic province. For namely Jabalpur Basin and Nand-Dongargaon palynological study samples were collected Basin. Detailed palynological study of the from different lithofacies of the Lameta Jabalpur Basin shows presence of diverse Formation and successive intertrappean beds palynotaxa represented by pteridophytes (13 from different groups and formations. genera), gymnosperm (16 genera) and angiosperm (10 genera) pollen grains. Overall, Infratrappean (Lameta Formation) quantity of angiosperm taxa is more than the Sediments of the Lameta Formation gymnosperms and pteridophytes (Dogra et al, are deposited in a fluvio-lacustarine 1994). In the Nand-Dongargaon basin the environment in semiarid arid climate (Tandon angiosperms dominate (8 genera) over the 48 gymnosperms (4 genera). Pteridophytes (1 cherts while in the upper part at higher levels of genus) are scarcely represented. Significantly, the DVS the sediments are dominated by cherts Lameta sediments have also yielded oldest and porcellanitic clays/shales. The change in record of freshwater diatoms (Aulacoseira) the broad lithologic characters are suggested as (Mohabey, 2001, Ambwani et al, 2003), owing to the fluctuating climatic condtions phytoliths of grasses including rice tribe from humid to semiarid-arid and to humid. (Prasad et al, 2005, 2011), pollen grains of Based on geochemical study of the Poaceae and Asteraceae (Samant and Mohabey lava flows it has been suggested (Mohaney 2009). 1988, Yedekar et al, 1996) that lava flow sequence of eastern part of Deccan Volcanic Intertrappean Sedimentary beds within Sequence (DVS) is independent of Western DCFB province part of DVS and may have a separate site and Intertrappean beds deposited in Late source. Therefore, the chemical stratigraphy Cretaceous to Early Paleocene (Chron proposed by Chennet et al, (2008, 2009) for the 30n-29r-29n) in between the Deccan volcanic western DVS is not correlatable with eastern flows have records of environmental and DVS. Diverse Megaflora represented by climatic conditions that prevailed during the pteridophytes, gymnospermous and volcanism and response of the contemporary angiospermous plants as well as algal remains biota to the volcanism. Deccan volcanic flows is recorded mostly from the Late Cretaceous and associated sediments are classified into (Maastrichtian) deposits of Sahyadri and different groups and formations based on Amarkantak groups of central India suggesting petrography, flow chemistry and field mapping long pause in volcanic activity during which by Geological Survey of India. Flows of central the diverse magaflora developed. Fossil woods and southern India are grouped into Sahyadri of both dicots and monocots are most common Group which is further divided into Ajanta, followed by leafs, fruits and flowers of Chikali, Karanja and Ritpur formations having angiosperms (Kapgate 1995, Bonde 2005). 35 basaltic flows and thickness of over 600 m. Quantitative palynofloral analysis of the Deccan volcanic flows of palynoflora in successive intertrappean beds in Chhindwara–Mandla-Jabalpur sector are different volcanic province shows that in most grouped into Amarkantak Group having eight of the intertrappean sediments palynoflora has formations namely Mandla, Dhuma, Pipardehi, less diversity and mostly one or two taxa Linga, Multai, Amarwada, Khampa and Kuleru dominate the overall assemblage. The study formations and about 34 flows. To the north of also shows that intertrappean deposits of Narmada in Dhar and Indore districts the flows Maastrichtian part are characterized by Azolla are grouped into Malwa Group which are cretacea, Gabonisporis vigaurouxii, Triporites further divided into Mandleshwar, Kalisindh, reticulatus, Aquliapollenites bengalensis and Kankaria-Phulbaneri, Indore and Bargonda Normapollis group pollen. Pollen spore formations having 38 flows and total thickness recovery is very less or nil in the intertrappean of 610 m. South of Narmada and up to Salburdi deposits of still higher level, however, in some fault the flows are grouped into Satpura Group intertrappean sediments high concentration of having about 60 flows and compound thickness chlamydospores of mycorrhizal fungi is of 1200 m. The volcanic flows of north western recorded. The growth of this fungi is related to India are still unclassified. the fluctuating lake levels and decreasing soil The intertrappean beds which were moisture (Lodge 1989, Turner and Friese 1998). deposited in small ponds and lakes during Diverse and good palynoflora is recorded from pause in volcanic activity are generally 1-5 m intertrappean of Paleocene which shows close thick and rarely over 5 m thick intertrappean similarity with the Paleocene-Lower Eocene deposits are encountered in the Deccan flora of the western India (Federikson 1994, volcanic Sequence (DVS). The studies show Saxena 1980). that lithologically the intertrappean deposits in Overall study indicates that Deccan the lower part of the DVS are dominated by volcanic associated Lameta and intertrappean cherts, porcellanitic clays/shales and limestones, sediments were deposited in different in the middle part by the carbonate dominating depositional environment and fluctuating clays, shales and rarely porcellanitic clays and climatic conditions. These changes affected the 49 biota. The first floral change is observed with volcanic activity when aridity increased and the onset of volcanism when flora was affected overall vegetation growth declined. Later on both by direct and indirect effect of volcanism. during waning phase of volcanic activity flora The Lameta flora was terminated and in the established as indicated by qualitative and intertrappean under changed conditions new quantitative increase in palynofloral floral assemblage developed. The second major assemblage in the Early Paleocene change in flora occurred with the increasing intertrappean beds.

References: Ambwani, K.; Sahni, A.; Kar, R.K.; Dutta, D. 2003, Oldest known non-marine diatoms (Aulacoseira) from the uppermost Cretaceous Deccan Intertrappean beds and Lameta Formation of India. Revue Micropaleontologie, 46, 67-71. Bonde, S.D., 2008. Indian fossil monocotyledons: current status, recent developments and future direction. Palaeobotanist, 57, 141–164. Chenet, A, L., Fluteau, F., Coutrillot, V., Gerard, M., and Subbarao, K.V., 2008, Determination of rapid Deccan eruption across the KTB using paleomagnetic secular variation: (I) Results from 1200 m thick section in the Mahabaleshwar escarpment. J. Geophys. Res, 113, B, 04101. Chenet, A.-L., Courtillot, V., Fluteau, F., Gerard, M.,Quidelleur, X., Khadri, S.F.R., Subbarao, K.V. And Thordarson, T. ,2009, Determination of rapid Deccan eruptions across the Cretaceous-Tertiary boundary using paloemangnetic secular variation: 2. Constraints from analysis of eight new sections and synthesis for a 3500 mthick composite section. J. Geophys. Res., 114, B06103, doi:10.1029/2008JB005644. Dogra, N. N., Singh, R. Y., and Kulshreshta, S. K., 1994, Palynostratigraphy of infratrappean Jabalpur and Lameta Formations (Lower and Upper Cretaceous) in Madhya Pradesh, India: Cret. Res., 15, 205–215 Frederiksen, N. O., 1994, Middle and Late Paleocene angiosperm pollen from Pakistan: Palynology, 18, 91-137. Kapgate, D.K., 2005. Megafloral analysis of intertrappean sediments with focus on diversity and abundance of flora of Mohgaon Kalan, Mandla and adjoining areas of Madhya Pradesh. Gondwana Geol. Mag., 20, 31–45. Khosla, A., Sahni, A., 2003. Biodiversity during the Deccan volcanic eruptive episode. J. Asian Earth Sci., 21, 895- 908. Lodge, D. J., 1989, The influence of soil moisture and flooding on formation of VA-endo- and ectomycorrhizae in Pop. Salix: Plant and Soil, 117, 243– 253 Mohabey, D. M., 1996, Depositional environment of Lameta Formation (Late Cretaceous) of Nand-Dongargaon Basin, Maharashtra: the fossil and lithofacies evidence: Mem. Geol. Soc. India 37, 363–386. Mohabey, D. M., and Udhoji, S. G., 1996, Fauna and flora from Late Cretaceous (Maastrichtian) non marine Lameta sediments associated with Deccan volcanic episodes, Maharashtra: its relevance to the K/T boundary problem, palaeoenvironment and palaeoclimate: Gondwana Geol. Mag., Spec. Vol. 2, pp. 349–364. Mohabey, D. M., Udhoji, S. G., Verma, K. K., 1993, Palaeontological and sedimentological observations on non-marine Lameta Formation (Upper Cretaceous) of Maharashtra, India their palaeoecological and paleoenvironmental significance. Paleo-3. 105, 83-94. Mahoney, J.J. 1988, Deccan traps. In Macdougall, J.D. (ed) Continental Flood Basalt. Kluwar Acad. Publ., London. pp. 151-194. Prasad, G.V. R. 2012, Vertebrate biodiversity of the Deccan volcanic province of India: a review. Bull. Soc. Geol. Fanace, 183, 597-610. Prasad, V., Stromberg, C.A.E., Alimonammadian, H., Sahni, A., 2005. Dinosaurian coprolites and the early evolution of grasses and grazers. Science, 310, 1177-1180. Prasad, V., Stromberg, C.A.E., Leach, A.D., Samant, B., Patnaik, R., Tang, L., Mohabey, G,S., Sahni, A., 2011. Late Cretaceous origin of the rice tribe provides evidence for early diversification in Poaceae. Nature commun., 2, 480, 1-9. 50 Samant, B. and Mohabey, D.M., 2009, Palynoflora from Deccan volcano-sedimentary sequence (Cretaceous-Paleogene transition) of central India: implication for spatio-temporal correlation. J. Biosci., 34, 811-823 Saxena, R.K., 1980, Palynology of Matanomadh Formation in the type area, north western, Kutch, India (Part-2) Palaeobotanist, 26, 279-296.40 39 Sheth, H. C., Pande, K., and Bhutani, R., 2001. Ar/ Ar ages of Bombay trachytes: evidence for a Paleocene phase of Deccan volcanism: Geophysical Research Letters, v. 28(18), 3513-3516. Sheth, H. and Pande, K. 2014 Geological and 40Ar/39Ar age constraints on late-stage Deccan rhyolitic volcanism, inter-volcanic sedimentation, and the Panvel flexure from the Dongri area, Mumbai. Asian J. Earth Sci., 84, 167-175. Tandon, S. K., Sood, A., Andrews, J. E., and Davis, P. I., 1995, Paleoenvironments of dinosaur bearing Lameta beds (Maastrichtian) Narmada Valley, Central India: Palaeo-3,117, 153-184. Turner, S. D. and Friese, C. F., Plant mycorrhizal community dynamics associated with moisture gradient within a rehabilitated Prairie fern. Rest. Ecol., 1998, 6, 1-44. Yedekar, D.B., Aramiki, S., Fujii, T and Sano, T 1996, Chemical signature and stratigraphy of the chindwara-Jabalpur-Seoni and Mandal sector of the eastern Deccan volcanic province and problems of its correlation. Gondwana Geol. Mag. special vol. 2, pp. 49-68.

51 First Record of Pollen Organ Genus Caytonanthus Thomas, from Early Cretaceous Beds of

South Rewa Gondwana Basin, India and its Palaeogeographical Significance

Prakash, N. and Das, N.

Birbal Sahni Inst. Palaeobot., 53 University Road Lucknow, 226007, India ([email protected])

Pteridosperms (seed ferns) are extinct branchlet bear an anther like synangium group of large and diverse plant assemblage. composed of four pollen sacs’. They were dominant elements during The microsporophyll genus Palaeozoic and were also important component Caytonanthus has been obtained for the first in Mesozoic vegetation but declined globally in time from Early Cretaceous beds of South the Cretaceous time with radiation of Rewa Gondwana Basin of Indian peninsula. Its angiosperms. In Mesozoic rocks four groups morpho-characters, geographic distribution are delimited these are Corystospermales along with its plausible southern origin are (Upper Permian-Cretaceous), Peltaspermales documented here. ( Peninsylvanian-Triassic) and Caytoniales Plant-fossils (peridophytes, (Triassic-Cretaceous) are known from pteridoperms, bennettitales and conifers), are impression and compressions of specimens mostly obtained from buff coloured clay, shale while both structurally preserved and and lenticular bedded mudstone of 6 meter compressed fossils are assigned to Petriellales deep pit section of Taken area (80°47ˊ20˝ E; ( Triassic). 23°41ˊ35˝ N), situated in South Rewa Basin, Although, Caytoniales never attained comprising rocks ranging from Archean to dominant status but their rare occurrence in the Phanerozoic Eons. Gondwanic sediments Mesozoic vegetation is quite important and comprise coaliferous nature while Late fascinating. For that extinct group of plant Gondwanic sediments contain non- coaliferous remains, Thomas (1925) erected a new order sequences. About seven to eight specimens of Caytoniales which was first obtained from genus Caytonanthus has been collected from Gristhorpe and Cayton bay beds of Yorkshire. clay bed and studied under Olympus Stereo This group of plant consists of three organ microscope. Photographs are taken by using genera Caytonia (megasporophyll), Cell Sen software. Caytonanthus (microsporophyll) and leaves Globally, Caytonialean plant remains Sagenopteris. Caytonia stem has been reported are most commonly recorded from Northern by Harris (1971) from Yorkshire. The Hemisphere namely England (Thomas 1925, dispersed pollen grains Vitriesporites Leschik Harris 1964), Greenland (Harris 1932, 1937), and seed Amphorispermum Harris is also allied Poland (Reymanowna 1973), Sweden with this group. Caytonanthus was originally (Lundblad 1948), Sardinia (Edwards 1929), described under the genus Antholithus arberi Russia (Krassilov 1977), Japan (Kim & Kimura by Thomas (1925). But as, the genus 1987), Hungry (Barabaka &Boka 2000), North Antholithus was non committal designation for America (LaPasha and Miller 1985) and Iran reproductive organ then Harris (1937) erected (Schweitzer & Kirchner 1998) and are Caytonanthus as an organ-genus. He termed supposed to be northern in origin. Although it’s ‘Caytonanthus as microsporophyll consisting vegetative part i.e. Sagenopteris Presl leaves of pinnately branched rachis. Lateral branches are infrequently reported from Gondwana dividing into ultimate branchlets. Each sequence of Southern Hemisphere. In South 52 America Sagenopteris has been recorded from recorded from Indian continent. This is the first Early to Middle Jurassic (Frenguelli 1941, record of genus Caytonanthus from the Early Menéndez 1957, Bonetti 1963, Herbst 1965, Cretaceous beds of South Rewa Gondwana 1966) and from Australia Lower Jurassic of Basin of India. Clarence-Moreton Basin (Jones & DeJersy Recently Bhowmik and Parveen 1947, Gould 1917, Mc Longhlin & Drinan (2008) has documented an important 1996). While Sagenopteris leaves along with synangiate genus Nidianthus a Caytonanthus - seed cupule Caytonia had been recorded by like pollen organ, from Middle Triassic beds of Bose & Banerji (1984) from Early Cretaceous Nidpur of South Rewa Basin. Glossopteris beds of Bhuj Formation, Kachchh Basin and leaves have also been documented earlier by only Sagenopteris leaf is recorded from Early Srivastava (1974, 1988) and Banerji et al Cretaceous Beds of Athgarh Formation of (1976) from Nidpur beds. The present Mahanadi Basin, India (Patra 1979). Although, caytonialean find of microsporophyll genus till date, Caytonialean remains are unknown Caytonanthus is also been documented from its from NewZealand and South African flora. younger strata i.e. from Early Cretaceous beds The vegetative part i.e. Sagenopteris of the same basin. These finds are an array in Presl leaves is reported from Middle-Upper depicting its southern origin. The occurrence of Jurassic of Gondwana sequence of Southern oldest record of Nidianthus a Caytonanthus - Hemisphere with the only record of Genus like pollen organ, along with occurrence of Caytonanthus from Hope and Botany Bay of Glossopteris leaves from the same basin Antarctica (Rees 1993). From Indian continent indicate that the Caytoniales were originated vegetative as well as megasporophyll Caytonia from Glossopteridales from Indian continent of is recorded from Kachchh basin (Bose & Southern Hemisphere, as suggested by Banerji, 1984). But a definite microsporophyll Krassilov (1977) and Doyale (2006). genus Caytonanthus has so far not been

References: Barbacka M. & Bóka K. 2000.A new Early Liassic Caytoniales fructificationfrom Hungary. Acta Palaeobt. 4: 85-111. Bhowmik N, Parveen S. 2008. Nidianthus gen. nov. - A Caytonanthus– likepollen organ from the Triassic of Nidpur, M.P.,India. Palaeobotanist. 57, 389-398. Bonetti I. R. 1963. Flora mesojurásica de la zonaTaquetrén(CañadóndelZaino), Chubut. Revistadel Museo Argentino deCienciasNaturales Bernardino Rivadavia. Paleontologia.1:1-43. Bose M.N. & Banerji, J. 1984. Bose MN,Banerji J. 1984. The fossil floras of Kachchh.1-Mesozoicmegafossils.Palaeobotanist. 33:1-189. Banerji J. , Maheshwari, H.K. and Bos, M.N. 1976 Some plant fossils from the Gopad River section near nidpur, Sidhi istrict, Madhya Pradesh. Palaeobotanist 23: 59-71 Doyle JA. 2006. Seed ferns and the origin of angiosperms. J Torrey BotSoci.133:169-209. Edwards W.N. 1929. The Jurassic flora of Sardinia. Ann Mag Nat Hist. 10: 385-394. Frenguelli I. 1941.Sagenopterisy LinguifoliumdelLias de PiedraPintada en el Neuquén (Patagonia). NotasMiiseo de La Plafa.Paleontologia34:404-437. Gould, R.E. 1974. Report ofthe fossil plants from Durikai, southeastern Queensland. In:Exonn F, ReiserrF, Caseyd J, BrunkerRL editors. . The Post-Palaeozoic rocks of Warwick 1: 250,000sheetarea. Queensland and New South Wales. Australian Bureau ofMineral Resources, Geology and Geophysics Report, No. 140:63-64. Harris T.M. 1932. The fossil flora of Scoresby SoundEast Greenland, 3: Caytoniales and Bennettitales.Medd.omGrønland, 85(5): 1-130. Harris T.M. 1937. The fossil flora of Scoresby SoundEast Greenland, 5: Stratigraphic relations of theplant beds. Medd.omGrønland, 112(2): 1-112. Harris, T. M. 1964. The Yorkshire Jurassic flora II.Caytoniales,Cycadales, and pteridosperms. British Museum (Natural History),London, UK. Harris T.M. 1964. The Yorkshire Jurassic Flora, II:Caytoniales, Cycadales and Pteridosperms. TheBritish Museum (Natural History), London. Harris T.M. 1971. The stem of Caytonia.Geophytology, 1(1): 23-29. 53 Herbst R. 1965. La Flora Fósil de la Formación Roca Blanca, provinciade Santa Cruz, Patagonia. Con consideracionesGeológicasyEstratigráficas. Opera Lilloana.12:1-101. Herbst R. 1966. Revisión de la Flora Liásica de PiedraPintada,provincia de Nuequén, Argentina.Rev Mus La Plata (NS)Pal.5:27-53 Jones O. A, and De Jersey N.J. 1947. Fertile Equisetales and otherplants from the Brighton Beds. University of Queensland Papers.Deparfment of Geology.3(4):1-16. Kim J.H, Kimura T. 1987. Cuticle of Sagenopteris (Caytoniales), an extinct gymnospermous plant, first observed in Japan.ProcJpnAcadSer B PhysBiol Sci. 63:179-182. Krassilov V.A. 1977 Contributions to the knowledgeof the Caytoniales. Review ofPalaeobotany and Palynology,24: 155–178. LaPasha, C.A and Miller C.N. 1985. Flora of the Early Cretaceous Kootenai Formation in Montana; bryophytes andtracheophytes excluding conifers. PalaeontogrAbt B Palaeophytol.196:111-145. Lundblad B. 1948. On some Caytonia plant remains from the coal-mines of Bjuv in Scania (Rhaetic). Sven BotTidskr. 42:84-86. McLonghlin S and Drinan N. 1996.A Middle Jurassic flora from the Walloon Coal Measures, Mutdapilly, Queensland, Australia.MemQueensl Mus.38:257-272. Menéndez C.A. 1957. FlórulajurásicadelBajo de los Baguales enPlaza Huincul, Nuequén. ActaGeol.Lilloana.1:315-338. Patra, B.P. 1989 Sagenopteris sp., a rare plant remains from the EastCoast Upper Gondwana Athgarh Sandstone, Cuttack District, Orissa. J. geol. Soc. India 33:271-275. Pelzer G. 1984. Cross section through fluvial environment in the Wealden of Horthwest Germany. Third Symposium on Mesozoic Terrestrial Ecosystem, Tübingen, Short Papers: 181-186. Rees P.M. 1993. Caytoniales in Early Jurassicfloras from Antarctica.Geobios.26:33-42. Reymanówna M. 1973. The Jurassic flora fromGrojec near Kraków in Poland, part II: Caytonialesand anatomy of Caytonia. ActaPalaeobot. 14(2):45-87. Srivastava, Shyam C. 1974 Pteridospermic remains from the Triassic of Nidpur. M.P., India. Geophytology 4 :54-59 Srivastava, Shyam C 1988. Sstratigraphic position and age of plant bearing beds. Palaeobot. 36: 154-160. Thomas H.H. 1925. The Caytoniales, a new group ofangiospermous plants from the Jurassic Rocks ofYorkshire. Phil. Trans.Royal Soc. London, Ser. B,213: 299-363. Schweitzer HJ, Kirchner M. 1998 Dierhäto-jurassischenFloren des Iran und Afganistans.11. Pteridospermophyta und Cycadophyta I.Cycadales. Palaeontographica, B, 248(1-3): 1-85.

54 Campanian-Maastrichtian palynomorph assemblages from East Asia

Yoshino, K.1, 2, Matsuoka, A.3 and Wan, X.2

1Grad. Schl. Sci. Tech., Niigata Univ., Niigata 950-2181, Japan ([email protected]) 2Stat. Key Lab. Biogeol. Env. Geol., China Univ. Geosci., Xueyuan Lu 29, Beijing 100083, China 3Dept. Geol., Fac. Sci., Niigata Univ., Niigata 950-2181, Japan

Introduction temperature zone, and humidity of their habitat. Knowledge of the Cretaceous climatic We applied our result to the conclusion of Gao changes has been derived principally from et al. (1999) for trying to examine oceanic scientific drilling, while the study of paleaoenvironmental change (Fig. 1). The terrestrial climate change of this period is still in assemblages found from meandering river its infancy. The Songliao Basin is the largest deposits were dominated by conifer pollen (e.g. Cretaceous oil-gas producing lacustrine basin in Abiespollenites spp., Cedripites spp., Northeast China. The Songliao paleo-lake was at Pinuspollenites spp., and Psophosphaera spp.). its greatest extent in the Late Cretaceous with Meanwhile, other plants of spore and pollen continuous sediment deposition (Wan et al., 2013). tended to increase in lake deposits. In recent years, the Continental Scientific Drilling Abiespollenites spp., Balmeisporites spp., Project was carried out to recover nearly complete Inaperturopollenites spp., and Ephedripites spp. Cretaceous terrestrial sedimentary records, which are considered to prefer temperate temperature named the Songke Core-1 (North) (SK1 (N)) and (Gao et al., 1999). These genera were obtained the Songke Core-1 (South) (SK1 (S)). These cores frequently from the Sifangtai to the lower will provide unique opportunities to advance the Mingshui Formations. Balmeisporites spp. that understanding of environmental change in the lived in a humid environment was obtained Cretaceous terrestrial realm. from the lower Sifangtai Formation and the Global cooling would have occurred lower Mingshui Formation. before and after the Campanian/Maastrichtian Stratigraphic position of (C/M) boundary (e.g. Miller et al., 2005). This Campanian/Maastrichtian boundary In the cooling event may have affected land plants Songliao Basin, stratigraphic position of the and other terrestrial organisms. The Songliao C/M boundary is controversial. We Basin is expected to provide hints of the re-examined the stratigraphic position of this influence of the cooling event in land. We stage boundary in the SK1 (N), based on examined spore and pollen obtained from the magnetostratigraphy, δ13C curve, and δ18O Songliao Basin (SK1 (N)) to discuss the curve derived from previous studies. Deng et al. influence of the global cooling in terrestrial (2013) revealed its magnetostratigraphy. In the region in East Asia. Geomagnetic polarity timescale (GPTS), the C/M boundary is in normal polarity of C32 (Gradstein Campanian-Maastrichtian palynomorph et al., 2012). Deng et al. (2013) suggested that N2 assemblages in the Songliao Basin could be readily correlated with C32n. In the SK1 (N), the C/M boundary is Chamberlain et al. (2013) provided δ13C curve considered to exist in the section of 400 m and δ18O curve in the Songliao Basin (Fig. 1). between the uppermost Nenjiang Formation and Thibault et al. (2012) reveals δ13C curve in the lower Mingshui Formation, based on GSSP of the C/M boundary, and identified the biostratigraphy and magnetostratigraphy (e.g. negative isotope shift above the C/M boundary. Wan et al., 2013). We found 70 genera and 136 In the Songliao Basin, the negative isotope shift species from 13 horizons. was identified in 822.5 m depth (Fig. 1). This Gao et al. (1999) carried out sift could correspond with the negative isotope palynorogical analysis in the Songliao Basin, shift above the C/M boundary in the GSSP. and explained parents of each genus, Moreover, δ18O values are unstable, and 55 Figure. 1. Integrated stratigraphy and changes of palynomorph assemblages from the uppermost Nenjiang Formation to the lowest Mingshui Formation. increased above and below 830 m depth. In the uppermost Sifangtai Formation (Fig. 1). We marine sediments, δ18O values revealed similar identified that some genera prefer temperate isotopic trend above and below the stage temperature increased from the upper Sifangtai boundary (e.g. Miller et al., 2005). Based on Formation, which is above and below the C/M

them, we suggest that the C/M boundary could boundary. This fact could be one of influences be above and below 830 m depth in the SK1 of the global cooling. If correct, parents of (N) (Fig. 1). Abiespollenites spp., Balmeisporites spp., Inaperturopollenites spp., and Ephedripites spp. Influences of global cooling in terrestrial could have increased in vegetation by the realm global cooling of the C/M boundary. Plants are sensitive to climate change, and flora would have been affected by the Future works global cooling before and after the C/M In this study, we proposed a new boundary. We expect that palynoflora had been stratigraphic position of the C/M boundary in affected by this cooling event. In this study, the the Songliao Basin. In the standard C/M boundary is considered to exist in the chronostratigraphy, however, the stratigraphic 56 position of the C/M boundary has been defined Campanian-Maastrichtian, which is available in marine sediments (e.g. Gradstein et al., 2012). for dating of non-marine deposits in the Lacustrine deposits of the Songliao Basin need Songliao Basin and other areas in East Asia. to correlate with marine deposits. The Izumi We found spore and pollen from 17 localities Group is one of the Upper Cretaceous marine above and below the C/M boundary in the deposits in southwest Japan. This group yields Izumi Group. We will attempt to correlate spore and pollen, and has a potential to produce palynomorph assemblages of the Songliao Basin a biostratigraphic framework for the with those of the Izumi Group.

References: China University of Geosciences (Beijing), Daqing Oilfield Limited Corporation, Jilin University, Resource of Land and Exploration Institute of Technology. 2009. Cretaceous Songliao Basin Continental Scientific Drilling Project: Songke Core-1 Research Report. 924 pp. (in Chinese). Chamberlain, C.P., Wan, X., Graham, S.A., Carroll, A. R., Doebbert, A. C., Sageman, B. B., Blisniuk, P., Kent-Corson, M. L., Wang, Z., Wang, C. 2013. Stable isotopic evidence for climate and basin evolution of the Late Cretaceous Songliao basin, China. Palaeo-3, 385: 106–124. Deng, C.L., He, H.Y., Pan, Y.X., Zhu, R.X. 2013. Chronology of the terrestrial Upper Cretaceous in the Songliao Basin, northeast Asia. Palaeogeography, Palaeoclimatology, Palaeoecology 385: 44–54. Gao, R., Zhao, C., Qiao, X., Zheng, Y., Yan, F., Wan, C. 1999. Cretaceous Oil Strata Palynology from Songliao Basin. Geological Publishing House, Beijing, 373 pp. Gradstein, F. M., Ogg, J. G., Schmitz, M., Ogg, G. 2012. The Geologic Time Scale 2012. Elsevier, Boston. 1176 pp. Li, J., Batten, D.J., Zhang, Y. 2011. Palynological record from a composite core through Late Cretaceous-early Paleocene deposits in the Songliao Basin, Northeast China and its biostratigraphic implications. Cret. Res. 32: 1-12. Miller, K.G., Wright, J.D., Browning, J.V. 2005. Visions of ice sheets in a greenhouse world. Marine Geol. 217: 215-231. Thibault, N., Harlou, R., Schovsbo, N., Schiøler, P., Minoletti, F., Galbrun, B., Lauridsen, B.W., Sheldon, E., Stemmerik, L., Surlyk F. 2012. Upper Campanian-Maastrichtian nannofossil biostratigraphy and high-resolution carbon-isotope stratigraphy of the Danish Basin: Towards a standard d13C curve for the Boreal Realm. Cret. Res. 33: 72-90. Wan, X., Zhao, J., Scott, R.W., Wang, P., Feng, Z., Huang, Q., Xi, D. 2013. Late Cretaceous stratigraphy, Songliao Basin, NE China: SK1 cores. Palaeo-3 385: 17-30.

57 Evolution of morphotypes of triprojectate pollen during the Late Cretaceous-Paleocene of East Asia

Markevich, V. and Bugdaeva, E.

Inst. Biol. Soil Sci. Far Eastern Bran. Russian Acad. Ssc., 159, Prospect 100-letiya, 690022, Vladivostok, Russia ([email protected])

The plants produced triprojectate as Aquilapollenites Rouse, Triprojectus pollen were widely distributed during the Late Mtchedlishvili, Mancicorpus Mtchedlishvili, Cretaceous throughout then-contiguous and Integricorpus Mtchedlishvili. In addition, Siberia-western North America landmass (an M. Farabee regards four other groups roughly area referred to as the Aquilapollenites corresponding to the previously described province). Triprojectates represent a group of pollen genera: Cranwellia Srivastava, parent angiospermous plants of unknown Pentapollenites Krutzsch, Morinoipollenites affinities. Their pollen had unusual bizarre Zhao et Wang, Jianghanpollis Zhao et Wang, morphology: three equatorial projections Loranthacites Mtchedlishvili. containing all or part of the purported germinal Based on our material including more apertures and as many as two polar projections. than 7000 palynological samples we retraced Triprojectate pollen appeared since the the geographical and taxonomical distribution Turonian, spread since the Santonian, reached of that pollen in the Santonian to the Eocene of its acme in the Maastrichtian, during the the Amur River region, North-East Russia, Palaeocene lost its role in the palynofloras, and Primorye region, Sakhalin Island and Kuril in the Eocene became extinct. These Islands. The rocks were retreated using the palynomorphs are abundant in the continental standard methods. The high taxonomical deposits. In the marine beds their significance diversity of the Late Cretaceous-Danian reduces. palynoflora of this vast region was revealed. Despite intensive study, precise This palynoflora mainly was dominated by morphological delimitation of fossil pollen in ferns and close to Pinaceae and Taxodiaceae. the Triprojectacites group has not been The angiosperms in the Late Cretaceous and achieved in the more than 50 years since their Danian palynofloras generally are a few; the first description. Using of light, scanning, and late Paleocene and Eocene are dominated by transmission electron microscopy facilitates to pollen of the flowering plants. The share of define internal and external group boundaries. triprojectate pollen in palynological Triprojectate pollen can be subdivided in assemblages usually not great, but these genera by body, sculpture, and aperture types. palynomorphs were their permanent M. Farabee (1993) informally recognized 15 constituents. This palynoflora included more morphological types of triprojectates: I. than 50 species of genera Aquilapollenites, Heteropolar morphotypes - 1. punctate Pseudoaquilapollenites, Parviprojectus, spinulate, 2. angled reduced-spinulate; II. Triprojectus, Mancicorpus, Integricorpus, Isopolar morphotypes - 3. psilate angled-body, Pseudointegricorpus, Pentapollenites, 4. eureticulate punctate spinulate, 5. Cranwellia, and Fibulapollis, attributed to 13 angled-body parallel-striate; 6. radiating-striate, morphotypes. 7. punctate spinulate, 8. punctate spinulate In intracontinental basins smooth-poled, 9. clavate isopolar, 10. psilate, (Zeya-Bureya Basin of Amur River region, 11. strioreticulate long-colpate, 12. Songliao Basin) triprojectate pollen appeared in strioreticulate long-colpate lateral-furrowed, 13. the Santonian (13 species). Its diversity rose strioreticulate short-colpate, 14. retipilate type, culminating in the late Maastrichtian (43 15. parallel-striate. In some cases these groups species) and sharply reducing in the Danian. correspond to previously described genera such During this age only one species existed. The 58 following morphotypes first appeared in the spinulate smooth-poled, strioreticulate Santonian: heteropolar punctate spinulate, long-colpate, strioreticulate short-colpate, angled reduced-spinulate; isopolar punctate retipilate, parallel-striate. spinulate, punctate spinulate smooth-poled, In the Maastrichtian-Danian psilate, strioreticulate long-colpate, retipilate palynofloras of the North-East Russia formed types. Since the Campanian the isopolar under conditions of paralic coal formation the radiating-striate and short-colpate morphotypes triprojectates are not numerous (8 species). The arose. Since the Maastrichtian - isopolar latest triprojectate pollen (Aquilapollenites strioreticulate long-colpate lateral-furrowed insignis N. Mtch., A. procerus Samoil., A. and parallel-striate morphotypes. At the K-T spinulosus Funkh., Pentapollenites normalis boundary majority of triprojectates Takah.) was revealed from the Eocene disappeared; only three morphotypes remained palynoflora of the Alkatvaam and Amaam - isopolar punctate spinulate, punctate spinulate basins (Chukotka). These species refer to two smooth-poled, retipilate, and strioreticulate morphotypes: isopolar punctate spinulate and long-colpate. punctate spinulate smooth-poled. The vegetation with high content of Aquilapollenites spinulosus in eastern triprojectates inhabited wet marshy biotopes Russia appeared in the end of the Maastrichtian, with ferns and taxodialeans. The plant and this species is characteristic for the Danian. communities with low diversity and This taxon is widely distributed in the insignificant share of triprojectates - fluvial Palaeocene of North America and the biotopes and one with periodic insiccations. Palaeocene and Eocene of North-East, East and The conditions of habitats (temperature, Central China (Song, Huang, 1997). This humidity) were rather important factors for species demonstrates an undoubted existence of triprojectates. However, there has post-Cretaceous record of the triprojectate been no unequivocal determination of their group. parent plants' ecological requirements. Paleoecological analysis revealed that In the regions of active volcanism plants produced triprojectate pollen constituted (Primorye region, Sakhalin Island) this pollen slope plant communities. appeared in the Santonian (6 species), Triprojectates thus constitute a group flourishing in the middle Maastrichtian (35 of evolutionary and biostratigraphic species). In the terminal Maastrichtian amount significance. Because of their distinctive of its species is 26, the early Danian - 8, the morphology, often short stratigraphic ranges, late Danian - 3. It should be noted that along facies independence, and relatively widespread with lesser taxonomical diversity the quantity distribution, triprojectates serve as excellent of triprojectate pollen in palynospectra is index fossils for Cretaceous and higher; its percentage can be more 80%. The post-Cretaceous sediments. They are frequently morphotypes are represented by: heteropolar included in palynological zonations (Markevich, punctate spinulate and angled 1994, 1995; Nichols et al., 1982; Pocknall, reduced-spinulate morphotypes; isopolar 1987; Srivastava, 1970) and can be used in radiating-striate, punctate spinulate, punctate geological age assignments. spinulate smooth-poled, strioreticulate Triprojectacites are first reported from short-colpate, parallel-striate. the Turonian of Siberia and possible Turonian In marine and shoreline sediments of North America. Their subsequent (Sakhalin Island, Kuril Islands, Hokkaido diversification climaxed during Campanian and Island) the number of triprojectate pollen Maastrichtian ages before declining at the end decreased, and its diversity was low: the of the Cretaceous. Some taxa apparently Coniacian - 1 species, the Santonian - 5, the persisted into the Paleogene in Arctic and East Campanian and lower Maastrichtian - 15, Asian refugia. Although the group was middle and late Maastrichtian -12, and Danian obviously much reduced, the terminal -10. The following morphotypes were revealed: Cretaceous extinction of all heteropolar punctate spinulate and angled triprojectate-producing plants may thus be reduced-spinulate; isopolar eureticulate merely illusory. punctate spinulate, angled-body parallel-striate; radiating-striate, punctate spinulate, punctate 59

The Cretaceous coal-forming plants of southern part of East Siberia and Russian Far East

Bugdaeva, E. V. and Markevich, V. S.

Inst. Biol. Soil Sci., Far Eastern Bran. Russian Acad. Sci., 159, Prospect 100-letiya, 690022, Vladivostok, Russia ([email protected])

The coal formation was linked with the The coal-bearing deposits of development of plant communities produced a Transbaikalia (Chita-Ingoda, Khilok, large biomass at the same time possessed Bukachacha, Turga-Kharanor basins), Amur relatively simple structure. A considerable part of River region (Bureya Basin) and Primorye region phytomass removed from swamp ecosystems as (Razdolnaya and Partizansk basins) were studied. mortmass. The great importance had The coals from thick productive and thin seams paleoecological and taphonomical factors, were sampled. encouraged rapid burial of plant remains. On this territory the The coal seams are particular subject of Tithonian-Valanginian, and Barremian-Albian paleobotanical research. The study of initial plant stages of coal formation can be distinguished. material has great importance for knowledge of During this time favorable conditions for genesis of coal, its composition, and quality of existence of mire vegetation occurred. The coal. abundant plant material was feedstock for peat Many elements of the coal-forming accumulation and coal origin. Coal-forming plant community can still be identified in the coal. plants buried in close proximity to their habitats. At the time of the mire formation and growth, The very thin cuticles of ferns do not remain after climatic conditions were such that very little chemical maceration of coal, but their spores, sediment was being transported into the basin having exine resistant to acids and alkali, can allowing biogenic sedimentation, with almost evidence about existence of ferns in mire complete absence of clastic sediments. Therefore, vegetation. Both palaeobotanical and it is possible to assume that plants that gave rise palynological data revealed plants contributed in to the coal deposits were autochthonous and coal formation. provided the first elements of peat accumulation. The Bureya Basin located in upper part Since the clastic deposits represent the material of the Bureya River has been the best subject of transported from the source area, phytofossil study of the Upper Jurassic to Lower Cretaceous assemblages from the terrigenous deposits coal-bearing deposits, because the sequence of between the coal layers are often mixed, this tectonic structure includes productive coals consisting of elements from both the slope and of the Tithonian, Berriasian, Barremian, and lowland communities. Aptian ages. The coals of other ages are thin and To obtain cuticles of the coal-forming do not have commercial significance. plants, the coals were oxidized by concentrated The Upper Jurassic strata were nitric acid, washed with distilled water, then, deposited in brackish coastal environments. treated with 10% alkali (KOH) and rinsed. The Characteristic of the Late Jurassic epoch are cuticular membranes were mounted on homogeneous composition, not clearly defined permanent slides for observation under a light differentiation, low diversity and smoothed microscope (LM) or were placed on standard zonation of vegetation. The main coal-forming stubs, splutter coater with gold and imaged using plants were cyatheaceous ferns, ginkgoaleans, a scanning electron microscope (SEM). and conifers. This stage is most conspicuous in Photographs were produced using a Zeiss Bureya Basin. The coal-bearing Upper Jurassic Axioscop 40 with camera Axiocam HRc light (Talyndzhan Formation) to Lower Cretaceous microscope and a Zeiss EVO-40 scanning (Dublikan, Soloni, Chegdomyn, and Chemchukin electron microscope (IBSS FEB RAS). 60 formations) deposits have thickness about Ginkgocycadophytus and conifers prevail among 200-3000 m. gymnosperms. The diversity and amounts of Palynological assemblage of the ferns are high in palynological assemblage of Talyndzhan Formation is characterized by Chemchukin Formation (the Aptian); they are predominance of fern spores, mainly have been represented by cyatheaceous, gleicheniaceous assigned to osmundaceous and cyatheaceous and osmundaceous ferns. The Pinaceae and ferns (up to 90%). The participation of diverse Taxodiaceae predominate among gymnosperms. mosses is considerable. Gymnosperms are The involvement of Ginkgocycadophytus remains dominated by pollen close to Pinaceae and rather high. Ginkgocycadophytus. The plant megafossils of The cyatheaceous ferns, conifers this stratigraphic unit are represented by Bilsdalea, ginkgoaleans (Pseudotorellia horsetails, bryophytes, ferns, cycadophytes, angustifolia Dolud., P. longifolia Dolud., ginkgoaleans, czekanowskialeans, and conifers Sphenobaiera urgalica Krassil., S. ikorfatensis (Vachrameev, Doludenko, 1961; Krassilov, 1972, (Sew.) Florin), and provided a basis for the Early 1973, 1978). The burials are dominated by Cretaceous mire plant communities. The ginkgoaleans and czekanowskialeans, the role of osmundaceous ferns lost their significance and ferns and cycadophytes is high. The gleicheniaceous and schizaeaceous replaced them. representative of ginkgoaleans (Pseudotorellia Essential features of these plant communities are angustifolia Dolud.) sometimes forms inherited from the Jurassic vegetation. monospecific burials; their cuticle remains are Based on a number of criteria, such as common in coals. Perhaps, this arboreal plant the abundance of bryophytes, cycadophytes index prevailed in mire vegetation, osmundaceous and and replacement of ecological dominance, V.A. cyatheaceous ferns were in understory. Krassilov has suggested a warming trend during Cycadophytes are often abundant in the clastic the Talyndzhan and Dublikan time. Follow by a beds, but coals entirely lack remains of these cooling trend in Soloni and Chegdomyn time. plants. Consequently, cycadophytes were not The czekanowskialeans are reduced whereas constituent of mire vegetation. cheirolepidiaceous plants increase during the The Lower Cretaceous (the Chemchukin climatic warming (Krassilov, 1973). Berriasian-Valanginian) strata accumulated in The Barremian-Albian stage was in a vast swampy lowlands. The peculiarity of great part. Coal accumulation was manifested on palynological assemblage from Dublikan vast areas of Siberia and Far East. During the Formation (the Berriasian) is considerable Barremian-Aptian main coal-forming plants amount of fern spores (up to 84%). Among varied in composition depending on gymnosperms as well as Classopollis prevails in environments. parallel with conifers. The floristic changes at the In Transbaikalia the study of coals in Jurassic-Cretaceous boundary have consisted in Chita-Ingoda, Khilok, Bukachacha, and the increase of ferns and cheirolepidiaceous Turga-Kharanor basins revealed that they are gymnosperms, which might be related to the formed by remains of ginkgoaleans marginal uplift and drier climate (Markevich, (Pseudotorellia, Sphenobaiera and Baierella), 1981, 1995; Markevich, Bugdaeva, 2008). conifers of pinaceous (Farndalea Bose, 1955) The coal-forming plants are represented by and araucariaceous affinity, cheirolepidiaceous Bilsdalea Harris, 1952, Eretmophyllum H. Tomas, plants (Pagiophyllum sp.) as well by 1913. cyatheaceous and gleicheniaceous ferns. Palynological assemblage of Soloni In Primorye region there are two Formation (the Valanginian) is dominated by coal-bearing Razdolnaya and Partizansk basins. conifers (up to 60%) and Ginkgocycadophytus. In the latter Starosuchan Formation of the Aptian Ferns reduce up to 50%. The gleicheniaceous and age was studied. The coals of this stratigraphic schizaeaceous ferns have assumed great unit are mostly composed of remains of importance. taxodialean Elatides asiatica (Yok.) Krassil., In the middle Cretaceous the sea retreats subordinate Miroviaceae, rare ginkgoalean from this area and the coal are accumulated in the Pseudotorellia sp., and bennettite Nilssoniopteris interior depressions. The palynoflora of rithidorachis (Krysht.) Krassil. The spores Chegdomyn Formation (the Barremian) is Gleicheniidites and pollen Taxodiaceaepollenites represented by mainly spores of Cyathidites. are dominant in the palynospectra. 61 In Razdolnaya Basin the unique resinous ginkgoaleans (Pseudotorellia, Sphenobaiera coals (rhabdopissites) occur in upper part of and Baierella), bennettites, and conifers having Lipovtsy Formation. The plants that produced pinaceous, taxodiaceous, araucariaceous, them are revealed. They belong mainly to the cheirolepidiaceous, and miroviaceous affinity. group Miroviaceae (Mirovia orientalis (Nosova) The conservatism of taxonomic Nosova), ginkgoalean Pseudotorellia krassilovii composition of mire plant communities is related Bugd., in a less degree these coals are composed to similar environments. It is well known that of other groups of conifers and bennettites N. coal accumulation was controlled by tectonics, rithidorachis, N. prynadae, Anomozamites climatic conditions, and the structures of arcticus Vassil. An important role in the coal ecosystems that provided the organic material for formation based on the palynological data played the coal formation. also cyatheaceous and gleicheniaceous ferns. Our research was supported by grants So, the Early Cretaceous coal-forming of Presidium RUS (12-I-P28-01), FEBRAS plants comprise cyatheaceous, gleicheniaceous, (12-III-А-06-070, 14-III-D-06-005, osmundaceous, and schizaeaceous ferns, 14-III-D-06-009).

62 Geoparks highlighting Cretaceous

The Tumbler Ridge Aspiring Geopark*, northeast British Columbia, Canada: the interrelation of significant geology, outstanding recreation potential, economic development, and strong community participation

Haggart, J. W.1, Helm, C. W.2, McCrea, R. T.2, Buckley, L. G.2 and Sharman, K.2

1Nat. Res. Canada, Geol. Surv. Canada, 1500-605 Robson Street, Vancouver, British Columbia V6B 5J3 Canada ([email protected]) 2Peace Reg. Palaeontol. Res. Cent., P.O. Box 1540, Tumbler Ridge, British Columbia V0C 2W0 Canada

The Tumbler Ridge region of blastoids, bryozoans, and bivalves. In addition northeastern British Columbia, Canada, is to their common invertebrate faunas of bivalves, endowed with significant geological features, ammonoids, and belemnoids, Mesozoic strata important paleontological heritage, and of the region contain abundant vertebrates and stunning natural beauty. The human history of include the internationally-renown Wapiti Lake this area is likewise diverse, with an locality, with over 20 known genera of fishes, appreciable First Nations presence and a among them sharks and ray-finned and subsequent history of habitation and lobe-finned fishes, including coelacanths. development based on natural resources. More Marine reptiles include ichthyosaurs, recently, tourism has become an important myxosaurs, and thalattosaurs. Cretaceous strata economic driver for the region. For all of these include both marine and non-marine deposits, reasons, the Tumbler Ridge region is a natural with common ammonites, bivalves, gastropods, candidate to join the Global Geoparks reptiles in marine facies, and vertebrates in Network. non-marine facies. Some of the first dinosaur The Tumbler Ridge region sits at the tracks in western Canada were found in the junction of the Interior Plains of Canada and Peace River canyon region, just north of the the eastern Rocky Mountains. As such, it proposed Geopark boundary. Subsequent includes a diversity of geological domains, discoveries over the past two decades have just each with its own important aspects and begun to highlight one of the world’s great geomorphological characters. The region dinosaur trackway regions, with numerous taxa exhibits abundant evidence of the great of dinosaur and other vertebrate tracks having orogenic event that created the Rocky been identified in the proposed Geopark area, Mountains, and great thrust faults related to this including the world’s first tyrannosaurid tectonism exhibit strong control on erosion and trackways. Although tracks are plentiful, actual geomorphologic evolution. Sedimentary rocks fossil remains of dinosaurs and other predominate and include late Precambrian vertebrates are only now being recovered, through Late Cretaceous strata, with an thanks to the persistent work of researchers at overlying covering of Pleistocene glacial the regional Peace Region Palaeontology deposits. Carbonate and clastic deposits are Research Centre (PRPRC), based in Tumbler both known in abundance, and the former is Ridge. Finally, overlying all older geology is host to extensive karst and cavern development. extensive evidence of the great thicknesses of Paleozoic strata contain abundant trilobites, ice that covered the region during the nautiloids and ammonoids, corals, Wisconsin glacial period; such evidence stromatoporoids, brachiopods, crinoids, includes moraines, tills, and glacial lake 63 terraces. Pleistocene vertebrate fossils are also and eco-tourism in support of the above-noted to be found in these relatively young geologic recreational opportunities now provides deposits. invaluable local economic support. The underlying geology and northern The Tumbler Ridge Aspiring Geopark climate of the Tumbler Ridge region are initiative has grown out of the recognition that responsible for the rich natural history that the region harbours a vast assemblage of characterizes the region, including extensive significant geological features, to which the boreal forests and delicate alpine regions. The human and natural history are inextricably forested lowlands and high-elevation bound. Such diversity of geological and mountaintops provide a diverse array of ecological phenomena has resulted in a recreational opportunities, including landscape rich in natural landscapes and superb rock-climbing and alpine mountaineering, recreational opportunities. The community of glacier travel and ice-climbing, cross-country Tumbler Ridge recognized the unique aspects skiing and snowmobile travel, spelunking, of this region and its scientific, economic, and mountain biking, canoeing and kayaking, recreational significance to the global jet-boat experience on river rapids, hiking to community, and has thus moved to promote the the many dozens of spectacular waterfalls that positive tourism values associated with the region is home to, and stargazing and Geoparks. The community developed a viewing the aurora borealis. Business Plan to assess the potential economic The harvesting of forest products benefits that would accrue from achieving provides a significant resource contribution in Geopark status, and then has worked diligently the region but the big economic drivers have to garner support for the proposal from been mineral resource extraction and communities, local First Nations, industry, and development. Coal in Cretaceous strata has multiple levels of government. Whether or not been an economic resource staple for decades; the proposal for Geopark status is successful, indeed, the community of Tumbler Ridge was the Tumbler Ridge region has grown founded in support of local coal mining. More immeasurably through its efforts to generate recently, natural gas in Triassic and younger international interest in the wonderful natural strata is opening up a new era of energy-related beauty inherent in the region and its export and development, so crucial for communities. supporting Canadian social programs. The cyclical nature of resource extraction, however, * This Geopark proposal is not formally has necessitated that local communities endorsed by the Geological Survey of Canada embrace a wider range of employment options, or Natural Resources Canada

65 Korean National Geoparks and tentative Global Geoparks in Korea: Mudeungsan Area and Korean Cretaceous Dinosaur Coast

Min Huh

Faculty of Earth Systems and Environmental Sciences & Korea Dinosaur Research Center, Chonnam National University, Gwangju 500-757, Republic of Korea

In Korea, we have five Korean Dinosaur fossil sites are one of the best known National Geoparks, 1 nominated Korean regions in the world for Cretaceous fossil National Geopark (Mudeungsan Area Geopark) footprints, which are also world-renowned. The and 1 Global Geopark (Jeju Island Geopark). sites have produced more scientifically named Korean National Geoparks Network consist of bird tracks (ichnotaxa), and have also produced Busan Geopark, Cheongsong Geopark, the world’s largest pterosaur tracks. Dinosaur Gangwon Peace Geopark, Jeju Geopark and tracksites also have the highest frequency of Ulleungdo-dokdo Geopark. Among them, vertebrate track-bearing levels currently known unique and tentative global geopark areas with in any stratigraphic sequence. Dinosaur fossil universal scientific values are located in the sites rank very highly. Objective analysis of southwestern and southern part of Korean important individual tracksites and tracksite peninsula: Mudeungsan Area and Korean regions must be based on multiple criteria Cretaceous Dinosaur Coast. including size of site, number of tracks, Jeju Island Geopark listed as Global trackways and track bearing levels, number of Geoparks Network in 2010 is the emergent valid named ichnotaxa including types, number portion of an intraplate basaltic volcanic field of scientific publications, and the quality of developed during the last 1.8 Ma. The island is preservation. There is an outdoor dinosaur made up of a broad and gently sloping lava education park including museum, protected shield and also dotted by at least 360 volcanic hall at the all KCDC sites as well as a pathway cones and craters. The geopark includes 12 with interpretive signs. A striking feature of the universal geosites. dinosaur sites is the intense interest in utilizing Mudeungsan Area Geopark compose the sites for school and community education. of a wide range (> 11 km2) of columnar joints in These sites span the whole Cretaceous to the high altitude (> 750 m). The columnar joints are end of the 'Age of Dinosaurs' and provide made up of Mudeungsan Tuff, which is thought considerable insight into the ecology and to be a result of a large-scale volcanic activity behavior of dinosaurs in contrast to the more during the Late Cretaceous. The size of column abundant, but less-securely date, nearby joint is much larger in scale than any other Mongolian and Chinese body-fossil deposits. columnar joints reported around the world. Also KCDC area consists of various, differentiated there is a variety of geo-heritage sites located Korean traditional cultural asserts such as near the area, including the Hwasun Dinosaur Buddhist and confucianism remains, traditional Track Site, Hwasun Dolmen Park, Rock Cliffs, foods, ancient and mordern arts, folk cultures Hot Springs, Coalfield, Caves, Talus Slopes etc. and festivals. Many sites are protected as Korean Cretaceous Dinosaur Coast National Monuments and have been developed (KCDC) are well known by its universal and for public education and geotourism associated scientific significance, and are listed as a with its adjacent cultural and historical tentative site for the UNESCO World Heritage. heritages, geographical and scenic sites.

66 Development of geopark activities of the past 10 years in Japan

Takagi, H.1 and Watanabe, M.2

1Depart. Earth Sci., Waseda Univ., 169-8050, Shinjuku-ku Tokyo, Japan. [email protected] 2Geol. Mus., AIST, 305-8567, Tsukuba, Ibaraki, Japan

The activities related to geoparks were Geoparks Committee (JGC, chaired by K. Oike, initially promoted in 2003 by Prof. S. Hada Professor Emeritus, Kyoto University) was regarding San-in Coast National Park in Japan. established as the official accreditation agency Subsequently, Prof. Hada would become of geoparks in Japan. The committee is chairman of Japan National Committee for composed of geoscience professionals IGCP by 2011. Dr. A. Iwamatsu (Geological nominated by Japanese geoscience societies Information Utilization and Promotion such as the Geological Society of Japan, the Initiative: GUPI) started to promote geopark Association of Japanese Geographers, Japan activities in 2004 when the Global Network of Association for Quaternary Research, the National Geoparks (GGN) was established. The Volcanological Society of Japan, the Geological Society of Japan organized the Seismological Society of Japan, Natural Parks Geoparks Establishment Promotion Committee Foundation, Japan Geotechnical Consultation in 2005 in cooperation with the National Association and AIST. In this year, JGN has Institute of Advanced Industrial Science and established and started Japanese geopark Technology (AIST)．In 2006, Dr. W. Eder, activities. Six GGN geoparks are included in UNESCO senior advisor, was invited by AIST the 33 JGN geoparks that have been established to assist the establishment of geoparks. Starting since 2008, indicating that the number of in 2006, Japanese organizations outside of the Japanese geoparks has increased very rapidly Earth science community became more active (Table 1). The reason for such a rapid increase in promotion of geoparks. Activities of IYPE is probably because sustainable development is (UNESCO-IUGS program) were held in an urgent issue for rural regions due to 2007-2009. In 2007, mayors of nine decreasing birthrate and aging population. The municipalities in Japan established the Japan number of geoparks in Japan most likely will Geoparks Promotion Council (later Japan continue to increase over the next ten years, Geoparks Network: JGN), and started to plan because there are already 17 candidate areas for Japanese geoparks. In 2008, the Japanese Japanese geoparks now.

Table 1. Histry of geopark establishment number of GGN and Japanese geoparks (JGN).

More than 60% of the 33 JGN ten years, however, to develop GGN activities, geoparks are related to active volcanism, and guidelines of the UNESCO Global Geopark about 10 are related to the Cretaceous period within the plan of IGGP (International including stratigraphy, fossils and Geoscience and Geoparks Programme) paleo-environment. combined with IGCP and GGN have been The activities of the GGN have been recently discussed in the working group of supported by the initiative of UNESCO in last UNESCO.

68 Land-oceon linkage: correlation, sedimentology and paleoenvironments I

Cretaceous ecosystems of southeastern continental margin of Russia and their evolution

Kirillova, G. L.

Russian Acad. Sci., Far Eastern Branch ([email protected]) Yu.A. Kosygin Inst. Tectonics and Geophy.

Cretaceous ecosystems of continental were rare in occurrence. Tethyan bivalves and margin of Russia were rather diversified and ammonites also occur indicating a shelf they were repeatedly affected by global and environment, but Boreal fauna of buchia was regional factors. predominant. Olistostromes composed of Spatially there are distinguished two olistoliths are widely distributed too. These are large regions where the Cretaceous sediments represented by Carboniferous, Permian accumulated, namely, Sikhote-Alin–Lower formations with the prevalence of Amur (Anoikin et al., 2007; Kirillova, 2011) Middle-Upper Triassic cherts. Clay shales, and the eastern margin of the Central Asian mudstones, tuffaceous siltstones and Late orogenic belt (Fig.1). They differ greatly. The Jurassic acid tuff form the matrix. Laterally (to first region is characterized by the deposition of the east), shelf facies are rapidly replaced by mostly marine sediments, whereas the second turbidites (trench slope environment) which one by continental (terrigenous coal-bearing contain no fauna. However, fucoids are and volcanogenic) sediments. universal in occurrence. During the Early Cretaceous, the Westward, intermountain basins of southeastern margin of Russia was located at submeridional extension (Bureya, the junction of three zoogeographical Zeya-Bureya) were filled up with continental provinces: Boreal, Tethyan, and Pacific, and sediments of a thick river system with abundant two paleofloristic realms: Siberian-Canadian lakes and bogs in which peat accumulated. with moderately warm climate and Euro-Sinian There a rich assemblage of fossil flora is subtropic (Vakhrameev, 1988; Kirillova et al., known, among which are Coniopteris 2000). hymenophylloides, Cladophlebis nebbensis, C. The Early Cretaceous environment haiburnensis, Podazamines lanceolatus, closely follows that of the Upper Jurassic. An Sphenopteris nantogensis, and others. extended marginal marine basin with island In the Hauterivian to Barremian a arcs existed in the east (Kiselevka-Manoma depositional hiatus was fixed for the most part zone) in the Late Jurassic (Tithonian) of the studied territory. But in the east of –Valanginian. Recent investigations suggested Sikhote-Alin a marine sedimentation continued. that cherts, volcanites, argillaceous Nevertheless, Buchia were replaced by siliceous-clayey shales containing radiolarians inocerams represented by heteropteria, accumulated at a low rate of sedimentation. colonicerams (Markevitch, et al., 2000). In the They indicated the basin plain environment Barremian ammonites Crioceratites cf. with volcanic structures crowned with emericii and Barremites sp. inhabited at the limestone “caps” (Anoikin et al., 2007; depths of 300-400 m have come into existence Kirillova and Anoikin, 2001). Further west, in (Baraboshkin, Enson, 2003). The continental the Komsomolsk series of the Gorin zone, the ecosystems of the western area were dominated buchians such as Buchia aff. inflata (Toula) by fluvial, lacustrine, and bog environments Lah., B. cf. wollosovitchi (Sok.), and B. cf. where terrigenous coal-bearing sediments about keyserlingi Lah. along with radiolarians were 1000 m thick accumulated. In the conditions of found in the argillaceous facies. Ammonites temperate warm humid climate two floristic 69 assemblages formed, Soloni and Chemchuki. sandstone, siltstone and clay shales They are most fully represented in the sections accumulated. Boreal seas were dominated by the marine boreal biocoenoses. Additionally, aucellines became widely distributed (Sha et al., 2009). Ammonite distribution provide evidence on a relatively equilibrium between the Boreal and Tethyan seas. As a result of the Albian tectonic movements and intrusion a Cretaceous tectono-stratigraphic complex acquired a nappe-plicated structure. By the end of the Albian an essential rejuvenation in biota took place. In intracontinental basins in the Aptian through Albian continental coal-bearing sediments up to 2 km thick continued to form under the influence of riftogenic processes. They were marked by rich floral assemblages: Ruffordia goeppertii (Dunk) Nath., Asplenium dicksonianum Heer, Coniopteris compressa Vassil., Birisia onichiodes (Vassil. et K.-M.) Samyl., Onichiopsis psilotoides (Stock. et Webb) Ward., Gingo ex gr. adiantoides (Ung.) Heer., Cephalotaxopsis heterophylla Holl., Araliaephyllum sp., Cisites sp., Cinamomoides elongate Koshm., and cones of Sequoia cf. condita Lesg. Due to activation of differential tectonic movements, there were formed structures of ridges and basins (Cao et al., 2013) the most distinctly manifested in the Zeya-Bureya Basin (Fig. 2). In the valleys, affected by river currents, conglomerate beds about 600 km thick were deposited (Kirillova et al., 2012). The Late Albian to Paleogene Okhotsk-Chukotka and East Sikhote-Alin of the Bureya Basin (Kirillova et al., 2012). volcanic belts are referred to post-accretionary The first assemblage of the Berriasian to formations. On the basis of the studies carried Valanginian age is marked by ferns, out by many researchers (Volcanogenic …, Bennettitales, Cycadaceae, and Ginkgoales and 1989) six phytostratigraphic horizons have the appearance of Schizaea, typical Cretaceous been determined for the Late Cretaceous. The flora. In the Chemchuki assemblage of the first three of them belong to the Hauterivian to early Aptian age the dominants Okhotsk-Chukotka province. They are were replaced by Lobifolia novopokrovskii, Petrozuevsky (Late Albian-Early Turonian) Sphenopteris lepiskensis, Athrotaxopsis with a rich floral assemblage, spores and pollen expansa, and Elatocladus manchurica. In the dominated by gymnosperms; Arzamazovsky Barremian the first flower plants appeared. A (Middle Turonian to Middle Coniacian) with sharp reduction in cycadophytes indicates the predominance of flowering plants among cooling. palynoflora, and the Kisinsky horizon (Late In the Aptian through middle Upper Coniacian to Early Santonian) with the Albian, two marine troughs became isolated prevalence of Sequoia. It should be noted that being separated by the central uplift, in which the boundary of the provinces shifted due to the thick (about 6 km) cyclically intercalated climatic changes. The upper three assemblages 70 are of a younger age and they are assigned to Cretaceous/Paleogene boundary in Priamurye the Japan province which is characterized by a in the course of the Russian-Chinese projects. warm climate with an optimum in the Geochemical and paleontological Campanian. In the Santonian to Campanian the investigations were made aiming to determine vegetation is represented by diverse and the causes responsible for a sharp change in abundant tropical and subtropical species. biota and dinosaur extinction at the There three horizons are identified: Cretaceous-Paleogene boundary. Monastyrsky (Late Santonian to Early It should be also taken into Campanian), Samarga (Late Campanian to consideration constant attention to Early Maastrichtian), and Bogopolsky (Late enhancement of the Cretaceous stratigraphic Maastrichtian). scale for Russsia and, in partilucar, its Boreal According to Krassilov (1989), an standard at the annual stratigraphic meetings abrupt change in vegetation occurred in East concerning Cretaceous stratigraphy and Sikhote-Alin belt at the Cretaceous-Paleogene paleography of Russia (Baraboshkin et al., boundary. Spore and pollen assemblages show 2013). an increase in pollen, close to that of the This work was financially supported by the Far present (Markevich, 1995). East Branch of the Russian Academy of In the recent years much attention has Sciences (project nos. 12-1-P27-06 and been paid to examination of the 12-11-SU-080009.

References: Anoikin V.I., Kirillova G.L., Eichwald L.P. New concepts of the composition, structure and age of the lower Amur fragment of the Late Jurassic-Early Cretaceous accretionary prism, Russian Far East. Russian J. Pacific Geol. 2007. N. 6. P. 556-571. Baraboshkin E.Yu., Enson K.V. Paleobathymetry of K1v-ap basin, Mountain Crimea, from indices of ammonite cone strength. Bull. Moscow State Univ. Geol ser. 2003. No. 4. P. 8-17 [in Russian]. Baraboshkin E.Yu. et al. The Cretaceous stratigraphic scale of Russia: state of affairs, major problems, and the ways of its improvement In General stratigraphic scale of Russia: state of affairs and a problem of its improvement. Moscow: Geol.Inst. RAS, 2013. P. 289-297. Сао С.R., G.L. Kirillova, A.P. Sorokin et al. Structure and evolution of the Sunwu-Jiayin Basin in NE China and its relation to the Zeya-Bureya Basin in the Far East of Russia // Russian Journal of Pacific Geology. 2013. Vol. 7, N 6. P. 420-429. Kirillova G.L. The Cretaceous of the East Asian continental margin: stratigraphy, paleogeography, and paleoclimate // Island Arc. 2011. V. 20. Pp. 57-77. Kirillova G.L., Krapiventseva V.V., Zabrodin V.Yu. et al. The Bureya sedimentary basin: Geological and geophysical characteristics. Geodynamics, and Fuel and Energy Resources / Vladivostok: Dalnauka, 2012. 360 p. [in Russian]. Kirillova G.L., V.S. Markevich and V.F. Belyi V.F. Cretaceous environmental changes of East Russia In Cretaceous Environments of Asia / H. Okada and N.J. Mateer (eds.). Elsevier Science, 2000. P. 1-48. Krassilov V.A. The Cretaceous time. Evolution of the Earth’s crust and biosphere. M.: Nauka, 1985. 239 p. [in Russian]. Markevitch P.V. et al. Lower Cretaceous deposits of Sikhote-Alin. Vladivostok: Dalnauka, 2000. 283 p.[in Russian]. Markevitch V.S. Cretaceous palinoflora of the northern East Asia. Vladivostok: Dalnauka, 1995. 200 p. [in Russian]. Sha J.G., Wang J.P., Kirillova G.L. et al. Upper Jurassic and Lower Cretaceous of Sanjiang-Middle Amur Basin: Non-marine and marine correlation // Sci China Ser. D-Earth Sci, 2009, 52(12):1873-1889. Vakhrameev V.A. Jurassic and Cretaceous floras and climates of the Earth. M.: Nauka, 1988. 210 p. [in Russian]. Volcanogenic Cretaceous of the Far East. Vladivostok: FEB USSR Acad., 1989. 148 p. [in Russian]. 71 Isotopic evidence for earliest Cretaceous climate change: new data from Siberia

Shurygin B. N.1,2, Dzyuba O. S.1, Izokh O. P.3 and Kosenko I. N.1,2

1Trofimuk Inst. Petrol. Geol. Geophy. SB RAS, 630090 Novosibirsk, Russia 2Novosibirsk State Univ., 630090 Novosibirsk, Russia ([email protected]) 3Sobolev Inst. Geol. Mineral. SB RAS, 630090 Novosibirsk, Russia

Early Cretaceous deposits are widely of north-western West Siberia and Berriasian of distributed on the huge territories of Siberia, northern East Siberia (Price & Mutterlose where they are represented by continental and 2004; Žák et al. 2011; Dzyuba et al. 2013). marine terrigenous rocks. Potential levels for New oxygen isotope data from belemnite rostra the Berriasian GSSP are discussed so far, and and oyster shells are received by us for the J–K the position of the Jurassic–Cretaceous (J–K) boundary interval. boundary in Siberian sections is still unresolved Detailed O-isotope curve is question. However, the J–K boundary intervals constructed for the Maurynya section (eastern of the Siberia and Tethys have been firmly slope of the Northern Urals) and is updated for correlated using integrated bio-, chemo- and the Nordvik section (northern East Siberia) (Fig. magnetostratigraphy (Bragin et al. 2013; 1). Different methods were applied to identify Dzyuba et al. 2013; Shurygin & Dzyuba 2014). samples with altered isotope values: (1) the It is clear that the basal Berriasian interval is investigation of polished belemnite chips using located within Upper Volgian of Boreal regions. cathodoluminescence; (2) geochemical analysis The Volgian and lowermost Ryazanian in to distinguish altered from non-altered samples Siberia is assigned to relatively homogeneous, via the Fe, Mn and Sr contents of carbonates; mainly argillaceous rock mass, the so-called (3) an analysis of relationship between trace Bazhenovo Horizon. This horizon formed element contents and the C- and O-isotopic under conditions of extremely low composition. The majority of investigated sedimentation rate. In the Ryazanian samples satisfy criteria of well-preserved Hectoroceras kochi Zone, sedimentation rate carbonate material. slightly increased to reach maximal values in Oysters tolerate a wide range of the terminal Ryazanian–Valanginian. The onset salinity and therefore they are rarely used for of avalanche sedimentation corresponds to temperature reconstruction. However, there is regression of Siberian seas. In the terminal no evidence of salinity fluctuations in the Valanginian–initial Hauterivian, influx of studied sites that allows us to use O-isotope siliciclastic material slightly decreased, though data derived from oysters too. remained several times higher than in the Late Temperatures are calculated using the Jurassic. In our opinion, there is connection equations of Anderson & Arthur (1983): between sedimentation rates in Siberian marine T(°C)=16,0–4,14*(δc–δw)+0,13*(δc–δw)2, palaeobasins and climate changes. where δc is the δ18O value of calcite relative to Palaeotemperature studies using PDB and δw is the δ18O value of water relative oxygen isotope ratios from Early Cretaceous to SMOW; with an adjustment made to δw of molluscan carbonate were carried out in Siberia, −1‰ as used by other authors, based on the until recently, in a sporadic manner. It was only essentially ice-free world during the Mesozoic. recently the oxygen isotope analysis was Research indicates that oysters provide carried out in some areas of Siberia, which warmer oxygen isotope temperatures than provided the first palaeoclimatic data for the belemnites (temperature difference of 2.6°C in Berriasian, Valanginian and Early Hauterivian average). This difference in temperature values

72 may be caused by different mode of life of Chetaites sibiricus–Hectoroceras kochi these molluscs. Many belemnite taxa are ammonite zonal boundary. This trend coincides nekton and can migrate to cooler waters at a with the initiation of a climate cooling significant distance from the site of collection. supposed for the earliest Cretaceous (e.g., However, the trend of δ18O variations for Podlaha et al. 1998; Mutterlose & Kessels oysters is similar to that for belemnites (Fig. 1). 2000; Weissert & Erba 2004). According to A comparison of the O-isotope curves Abbink et al. (2001), the climatic shift in the obtained for the Maurynya and Nordvik North Sea region represented by a change from sections showed an agreement between the warm and arid to slightly cooler and humid general trends in the oxygen isotopic conditions occurred in the H. kochi Zone. In composition; the only difference is that the Dorset (southern U.K.), sections provide average O-isotope values in the Maurynya evidence of a climatic shift from semi-arid section are lower than those in the Nordvik phase to more humid phase in the middle and section. This difference is most likely due to late Berriasian (Schnyder et al. 2009). The shift the difference of water temperature in the in climate from warm in the late Volgian to marine basins, which is corroborated by the cooler in the middle–late Ryazanian was northern palaeogeographic position of the previously recognised in the Yatriya River Nordvik section in comparison with the successions, in Western Siberia (Price & Maurynya section. Mutterlose 2004). These earliest Cretaceous The O-isotope values in the Maurynya palaeoclimatic changes coincided with the and Nordvik sections are characterised by a decrease of atmospheric CO2 levels established generally decreasing upward trend to the base by Huang et al. (2012) from the early–middle of the Ryazanian. This negative trend is Berriasian to the early Valanginian. associated with a gradual warming of the In Western and Eastern Siberia, the climate during the Late Jurassic and the early increase of sedimentation rate in the earliest Berriasian (from the middle Oxfordian to the Cretaceous (at the Bazhenovo and Kulomzino earliest Ryazanian) (Abbink et al. 2001; Price horizon boundary) coincides with change from & Rogov 2009; Žák et al. 2011). warm and arid to slightly cooler and humid The belemnite data from Siberian conditions. sections show a positive trend in the O-isotope This is a contribution to the RAS Programs 23 curve (trend towards heavier values of δ18O) and 28, the RFBR120500453 and IGCP608. only at the top of studied section across the

References: Abbink, O., Targarona, J., Brinkhuis, H. & Visscher, H., 2001. Late Jurassic to earliest Cretaceous palaeoclimatic evolution of the Northern Sea. Global and Planet. Change. 30, 231-256. Anderson, T.F. & Arthur, M.A., 1983. Stable isotopes of oxygen and carbon and their application to sedimentologic and paleoenvironmental problems. In: Stable Isotopes in Sedimentary Geology, Arthur, M.A., T.F. Anderson, I.R. Kaplan, J. Veizer and L. Land (Eds.). SEPM, Georgia, pp: 1-151. Bragin, V.Yu., Dzyuba, O.S., Kazansky, A.Yu. & Shurygin, B.N., 2013. New data on the magnetostratigraphy of the Jurassic–Cretaceous boundary interval, Nordvik Peninsula (northern East Siberia). Russian Geol. Geophy. 54, 329-342. Dzyuba, O.S., Izokh, O.P. & Shurygin, B.N., 2013. Carbon isotope excursions in Boreal Jurassic–Cretaceous boundary sections and their correlation potential. Palaeo-3 381-382, 33-46. Huang, C.M., Retallack, G.J. & Wang, C.S., 2012. Early Cretaceous atmospheric pCO2 levels recorded from pedogenic carbonates in China. Cretaceous Res. 33, 42-49. Mutterlose, J. & Kessels, K., 2000. Early Cretaceous calcareous nannofossils from high latitudes: implications for palaeobiogeography and palaeoclimate. Palaeo-3 160, 347-372. Podlaha, O.G., Mutterlose, J. & Veizer, J., 1998. Preservation of δ18O and δ13C in belemnite rostra from the Jurassic/Early Cretaceous successions. Amer. J. Sci. 298, 324-347.

73 Price, G.D. & Mutterlose, J., 2004. Isotopic signals from the late Jurassic–early Cretaceous (Volgian–Valanginian) sub-Arctic belemnites, Yatria River, Western Siberia. J. Geol. Soc. 161, 959-968.

74 Early Cretaceous terrestrial climates in East Asia; long term and seasonal patterns inferred from the oxygen and carbon isotope compositions of vertebrate apatites

Amiot, R.1, Kusuhashi, N.2, Buffetaut, E.3, Goedert, J.1, Hibino, T.4, Ikeda, T.5, Ikegami, N.6, Lécuyer, C.1, Philippe, M.1, Saegusa, H.5,7, Shibata, M.8, Shimojima, S.9 and Sonoda, T.8

1CNRS UMR 5276 LGL-TPE, Université Claude Bernard Lyon1 and École Normale Supérieure de Lyon, 2 rue Raphaël Dubois, 69622 Villeurbanne Cedex, France ([email protected]; [email protected]; [email protected]) 2Department of Earth's Evolution and Environment, Graduate School of Science and Engineering, Ehime University, 2-5 Bunkyo-cho, Matsuyama, Ehime 790-8577, Japan ([email protected]) 3CNRS UMR 8538, Laboratoire de Géologie de l’Ecole Normale Supérieure, 24 rue Lhomond, 75231 Paris Cedex 05, France ([email protected]) 4Shiramine Institute of Paleontology, Kuwajima, Hakusan, Ishikawa 920-2502, Japan ([email protected]) 5Museum of Nature and Human Activities, Hyogo 669-1546, Japan ( [email protected]) 6Mifune Dinosaur Museum, Kumamoto 861-3207, Japan ([email protected]) 7Division of Natural Environment, Institute of Natural and Environmental Sciences, University of Hyogo, Sanda, Hyogo 669-1546, Japan ([email protected]) 8Fukui Prefectural Dinosaur Museum, Katsuyama, Fukui 911-8601, Japan ([email protected]; [email protected]) 9Shokawa, Takayama, Gifu 501-5416, Japan ([email protected])

During the past decades, continental the occurrence of physical barriers such as biodiversity in East Asia during the Early mountain ranges or oceanic inlets resulting Cretaceous has been the center of intensive from the Late Paleozoic and Early Mesozoic research, but the causes of its peculiar spatial tectonic history (see Metcalfe, 2013 for a and temporal distribution remains poorly review), and climate that played notably a understood and heavily debated. One puzzling major role in the dynamics of continental aspect is that strong provincialism biodiversity in northeastern China during the characterized continental faunas (e.g. Buffetaut Barremian-Albian interval. Indeed, various et al., 2006; Fernandez et al., 2009; Zhou et al., proxies for air temperature and water 2003) distributed in vasts and apparently availability have been used such as the stable continuous terrestrial areas composed by oxygen isotope compositions of vertebrate various tectonic blocks (e.g. Enkin et al., 1992). apatite (Amiot et al., 2009; 2011), The main causes invoked for this distribution is hydrothermal zircon (Yang et al., 2013), 75 weathering index (Ohta et al., 2011) and the differences in precipitation regime are observed distribution of taxa known to be sensitive to between China, Thailand and Japan. These climate (Amiot et al., 2011; Philippe et al., differences are at least partly attributed to the 2009; 2014). occurrence of mountain ranges extending along The spatial and temporal distributions the East margin of the Chinese block that likely of climates in East Asia during the Early prevented humid air masses from the Pacific to Cretaceous have are investigated using stable penetrate some parts of East Asia, thus creating oxygen and carbon isotope composition of various micro-environmental conditions. In reptile apatites. Published results as well as turn, these isolated mosaic environments may ongoing studies involving a joint have acted as cradles for the origination of French-Japanese collaboration initiated in 2012 advanced vertebrate taxa that subsequently are presented. Whereas the reconstructed mean radiated over Eurasia and North America air temperatures show a steep latitudinal during the Late Cretaceous. gradient similar to the present day one,

References: Amiot, R., Buffetaut, E., Lécuyer, C., Fernandez, V., Fourel, F., Martineau, F., Suteethorn, V., 2009. Oxygen isotope composition of continental vertebrate apatites from Mesozoic formations of Thailand; environmental and ecological significance, in: Buffetaut, E., Cuny, G., Le Loeuff, J., Suteethorn, V. (Eds.), Late Paleozoic and Mesozoic Continental Ecosystems in SE Asia, Geol. Soc. London Spec. Publ.. The Geological Society, London, pp. 271–283. Amiot, R., Wang, X., Zhou, Z., Wang, X., Buffetaut, E., Lécuyer, C., Ding, Z., Fluteau, F., Hibino, T., Kusuhashi, N., Mo, J., Suteethorn, V., Wang, Y., Xu, X., Zhang, F., 2011. Oxygen isotopes of East Asian dinosaurs reveal exceptionally cold Early Cretaceous Climates. Proceedings of the National Academy of Sciences 108, 5179–5183. Buffetaut, E., Suteethorn, V., Tong, H., 2006. Dinosaur assemblages from Thailand: a comparison with Chinese faunas, in: Lu, J.C., Kobayashi, Y., Huang, D.Y., Lee, Y.N. (Eds.), Papers from the 2005 Heyuan International Dinosaur Symposium. Geol. Publ. House, Beijing, 19–37. Enkin, R.J., Yang, Z., Chen, Y., Courtillot, V., 1992. Paleomagnetic constraints on the geodynamic history of the major blocks of China from the Permian to the present. Journal of Geophysical Research 97, 13953–13989. Fernandez, V., Claude, J., Escarguel, G., Buffetaut, E., Suteethorn, V., 2009. Biogeographical affinities of Jurassic and Cretaceous continental vertebrate assemblages from SE Asia. Geological Society, London, Special Publications 315, 285–300. Metcalfe, I., 2013. Gondwana dispersion and Asian accretion: Tectonic and palaeogeographic evolution of eastern Tethys. J. Asian Earth Sci. 66, 1–33. doi:10.1016/j.jseaes.2012.12.020 Ohta, T., Li, G., Hirano, H., Sakai, T., Kozai, T., Yoshikawa, T., Kaneko, A., 2011. Early Cretaceous Terrestrial Weathering in Northern China: Relationship between Paleoclimate Change and the Phased Evolution of the Jehol Biota. J. Geol. 119, 81–96. doi:10.1086/657341 Philippe, M., Boura, A., Oh, C., Pons, D., 2014. Shimakuroxylon a new homoxylous Mesozoic wood genus from Asia, with palaeogeographical and palaeoecological implications. Review of Palaeobotany and Palynology 204, 18–26. Philippe, M., Jiang, H.E., Kim, K., Oh, C., Gromyko, D., Harland, M., Paik, I.N.., Thevenard, F., 2009. Structure and diversity of the Mesozoic wood genus Xenoxylon in Far East Asia: implications for terrestrial palaeoclimates. Lethaia 42, 393–406. Yang, W.-B., Niu, H.-C., Sun, W.-D., Shan, Q., Zheng, Y.-F., Li, N.-B., Li, C.-Y., Arndt, N.T., Xu, X., Jiang, Y.-H., 2013. Isotopic evidence for continental ice sheet in mid-latitude region in the supergreenhouse Early Cretaceous. Scientific reports 3. doi:10.1038/srep02732 Zhou, Z., Barrett, P.M., Hilton, J., 2003. An exceptionally preserved Lower Cretaceous ecosystem. Nature 421, 807–814.

76 Reconstruction of terrestrial paleo-hydrological change during the mid-Cretaceous “Supergreenhouse” period: Insights from the lacustrine records (Shinekhudag Fm.) of southeast Mongolia

Hasegawa, H.1 Ando, H.2 Ohta, T.3 Hasegawa, T.4 Yamamoto, M.5 Hasebe, N.6 Murata, T.2 Shinya, H.3 Li, G.7 Ichinnorov, N.8 Erdenetsogt, B.9,10 and Heimhofer, U.11

1Nagoya Univ. Mus., Nagoya Univ., Nagoya 464-8601, Japan ([email protected]) 2Dept. Earth Sci., Fac. Sci., Ibaraki Univ., Mito 310-0056, Japan 3Fac. Edu., Int. Arts, Sci., Waseda Univ., Tokyo 169-8050, Japan 4Dept. Earth Sci., Fac. Sci., Kanazawa Univ., Ishikawa 920-1192, Japan 5Fac. Env. Earth Sci., Hokkaido Univ., Sapporo 060-0810, Japan 6Division Ear. Env. Techn., Kanazawa Univ., Ishikawa 920-1192, Japan 7Nanjing Inst. Geol. Palaeont., Chinese Acad. Sci., Nanjing 210008, China 8Paleont. Center, Mongolian Acad. Sci., Ulaanbaatar 210351, Mongolia 9Dept. Geol. Geophy., Nat. Univ. Mongolia, Ulaanbaatar 13320, Mongolia 10Genie Oil Shale Mongolia LLC, Ulaanbaatar 14210, Mongolia 11Inst. Geol., Leibniz Univ. Hannover, D-30167 Hannover, Germany

The mid-Cretaceous is characterized light-grey calcareous shale, and whitish to by an extremely warm “greenhouse” climate, yellowish dolomite. Strata are continuously elevated atmospheric CO2 levels, and repeated exposed up to 400 m in thickness. At the Shine occurrences of Ocean Anoxic Events (OAEs). Khudag locality, the shale and dolomite However, the detailed processes and causal successions are rhythmically bedded mechanisms of these marked events, (decimeter-, meter-, tens of meter-scale), particularly the response of the terrestrial probably controlled by orbital cycles. The climate system, are only poorly understood. paper shales contain micrometer-scale Possible causal mechanisms of OAEs in the laminations, which are most likely varve origin mid-Cretaceous greenhouse climatic conditions reflecting seasonal cyclicity. Using include the following: (1) Increased continental varve-counting methods on thin sections, an humidity and terrigenous input into the oceans, estimated sedimentation rate of ca. 6-7 cm/k.y. (2) enhanced ocean surface productivity, and is preserved. The age of the Shinekhudag (3) enhanced organic carbon burial in the Formation is assigned as Aptian or oceans. Increased continental humidity and Barremian-Aptian based on ostracode, chemical weathering may have increased conchostracans, floral and molluscan evidence terrigenous input into the oceans (so called (Krassilov, 1982; Jerzykiewicz and Russell, “Weathering Hypothesis”; e.g., Emeis and 1991; Yuan and Chen, 2005), and Ar40/Ar39 Weissert, 2009). In order to evaluate the dating of basaltic rocks in the uppermost part of interaction between land and ocean during the the underlying Tsagantsav Formation (ca. mid-Cretaceous OAE interval, we investigate 121-125 Ma; Graham et al., 2001). terrestrial paleoenvironmental changes using In order to identify the depositional intra-continental lacustrine deposits in the conditions and controlling factors for the eastern Gobi basin, southeast Mongolia (Ando rhythmically alternating lithofacies, we et al., 2011). conducted X-ray diffraction (XRD) analysis to Mid-Cretaceous lacustrine deposits decipher changes in the mineral composition. (Shinekhudag Formation) are widely We also performed elemental analysis (C, N, S), distributed in southeastern Mongolia Rock-Eval pyrolysis, and a quantitative study (Jerzykiewicz, and Russell, 1991; Hasegawa et of the palynofacies to evaluate the distribution al., 2012). The Shinekhudag Formation, well and composition of the organic matter (OM) in exposed in the Shine Khudag locality in the the shale and dolomite couplets. The mineral Shaazangiin Gobi area, is composed of an composition results reveal that the cyclic alternation of dark-grey paper shale (oil shale), alternations (ca. 1.5 m cycle) of the 77 dolomite-rich layer and detrital minerals and 1990; Dupraz et al., 2009). Botryococcus calcite rich layer. C/N ratios are significantly colonies were abundant under such small in the dolomite samples, compared to oligotrophic and alkaline lake conditions. On relatively high ratios in the shale samples. the other hand, the shale layers were deposited Rock-Eval analysis shows high hydrogen index during high lake levels, which were values (> 650 mg/g) with relatively high T-max characterized by higher algal productivity and values (430–440˚C). All analyzed samples are increased inputs of detrital minerals. Spectral composed of Type I–II kerogen. Palynofacies analysis of the lithofacies change in the analysis further indicates a strong dominance of Shinekhudag Formation shows the cyclicities Botryococcus colonies in the dolomite layers, involving ca. 1.5 m, 7 m, and 26 m cycles, whereas the shale layers are essentially corresponding to periodicities of ca. 22 kyr, composed of amorphous OM, algal cysts, and 108 kyr, and 394 kyr, respectively, based on a terrestrial palynomorphs. varve-tuned average sedimentation rate of 6.5 The different lines of evidence cm/kyr. These values are in accordance with indicate that the rhythmically alternating orbital precession (18–23 kyr cycle) and lithofacies changes in the Shinekhudag eccentricity cycles (100 and 400 kyr cycles). lacustrine deposits were mainly controlled by Therefore, the Aptian lacustrine deposits in changes in lake-level and lake productivity. southeastern Mongolia are interpreted to record Namely, the dolomite layers were formed the orbital-scale paleo-hydrological changes during low lake level by microbially mediated during the OAE1a–1b interval. precipitation in alkaline lake waters (e.g., Last,

References: Ando H., Hasegawa, H., Hasegawa, T., Ohta, T., Yamamoto, M., Hasebe, N., Li, G., Ichinnorov, N. (2011) J. Geol. Soc. Japan, 111, XI–XII. Dupraz, C., Reid, R.P., Braissant, O., Decho, A.W., Norman, R.S., Visscher, P.T. (2009) Earth-Sci. Rev., 96, 141–162. Emeis, K.C., Weissert, H. (2009) Sedimentology 56, 247–266. Hasegawa, H., Tada, R., Jiang, X., Suganuma, Y., Imsamut, S., Charusiri, S., Ichinnorov, N., Khand, Y. (2012) Climate of the Past, 8, 1323–1337. Jerzykiewicz, T. and Russell, D.A. (1991) Cretaceous Res. 12, 345–377. Johnson, C.L. and Graham, S.A. (2004) J. Sediment. Res., 74, 786–804. Last, W.M. (1990) Earth-Sci. Rev., 27, 221–263.

78 Evolution of photosynthetic ecosystem effects on chemosynthetic ecosystem in late Mesozoic

Jenkins, R. G.

Kanazawa Univ., Kanazawa City, 920-1192, Japan. [email protected]

This presentation will provide a Paleogene is the crucial age for gaining an review of the history of chemosynthetic understanding of the evolutionary history of ecosystem based on their fossil record with chemosynthetic ecosystems. Many molluscs special focuses on relationship with living at hydrothermal vents and hydrocarbons photosynthetic ecosystem. seeps today first appeared during this period. It The unexpected discovery of deep-sea is noteworthy that number of records of ancient hydrothermal-vents and their unique hydrocarbon seeps has been increased in late surrounding ecosystems (Lonsdale, 1977; Mesozoic. It is probably due to an increasing Corliss et al., 1979) changed our view of life. organic flux into sediment resulting from The ecosystems are based on chemosynthetic increasing planktonic productivity and diversity bacteria which obtain energy from reduced in late Mesozoic. The organic compounds in molecules (e.g. oxidizing hydrogen sulfides) so the sediments have leaded to increasing as to make organic compounds. Such an generation of methane in the sediments. environment is thought to be a place suited to In addition, much direct effects on to the origin of life. Although such reduced chemosynthetic ecosystem from photosynthetic chemical compounds are often toxic for ecosystem has been started since the ‘normal’ animals, some animals have adapted Cretaceous. The chemosynthesis-based to the environment by harboring ecosystems sustained by vertebrate- and chemosynthetic bacteria in their body. In the wood-falls first appeared in the Cretaceous, nearly 40 years since the discoveries, similar when plesiosaurid carcasses carried out the chemosynthetic communities have been found same role as do whale bones nowadays. at various other sites in the world’s oceans Recently, my colleagues and I found where bottom water is enriched with reduced chemosynthetic fauna around a Cretaceous sea compounds, e.g. hydrocarbon-seeps, sunken turtle, Mesodermochelys sp. collected from whale carcasses and sunken driftwood. The Nakagawa Town, Hokkaido. This finding fossil record of chemosynthetic ecosystem has indicates that the chemosynthetic communities been increased for past few decades, and now were supported not only by plesiosaurid we could partially follow the history of carcasses but also by decomposing sea turtles. chemosynthetic ecosystem. It turned out that The sea turtles are a rare example of chemosynthetic ecosystem is not independent Cretaceous marine reptiles surviving the from photosynthetic ecosystem, although many Cretaceous/Paleocene extinction event. Thus, it people thought independency of is reasonable to assume that sea turtle carcasses chemosynthetic ecosystem from photosynthetic provided continuous support for ecosystem. chemosynthetic ecosystems throughout the ‘Chemosynthetic animals’ can be K/Pg boundary. On the basis of the evidence traced back to the Silurian and many animal outlined above, it can be considered that taxa flourished in the chemosynthetic chemosynthetic fauna have been received great ecosystems until the Recent. The period influences from the photosynthetic ecosystem. ranging from the Late Mesozoic to the

79 Deep/intermediate water formation along the Cretaceous Asian continental margin

Moriya, K.1, Moiroud, M.2, Pucéat, E.2, Donnadieu, Y.3, Bayon, G.4, Deconinck, J.-F.2 and Boyet, M.5

1Div. Earth & Environ. Sci., Sch. Natural Sci. & Tech., Kanazawa Univ., Kakuma-machi, Kanazawa, Ishikawa 920-1192; ([email protected]) 2UMR CNRS Lab. Biogeosciences, Univ. Bourgogne ; 3UMR CEA/CNRS Lab. Sci. Climat Environ., CE Saclay ; 4IFREMER,Unite Recherche Geosciences Marines ; 5UMR CNRS Labo. Magmas Volcans, Univ. Blaise Pascal

The Cretaceous is known to be one of Cretaceous (late Turonian through early the archetypal greenhouse periods, and Campanian) northwestern Pacific. intensively studied for evaluating the climate Neodymium isotopic signatures in fish sensitively in the high pCO2 region. The remains obtained from clayey sediments in the meridional sea surface temperature distribution, Yezo Group show highly radiogenic values of secular changes in sea surface and deep water –1 to –2 ε-unit. These values are significantly temperatures have also been discussed globally. higher than those in the Atlantic and the In addition to the thermal structure, analyses of equatorial Pacific. This result indicates the ocean circulations on the basis of neodymium presence of highly radiogenic isotope signatures become more popular intermediate/deep water formation in the especially in the Atlantic Ocean. On the other northwestern Pacific, because it is expected hand, the ocean circulation in the Pacific Ocean that the radiogenic neodymium has been is still uncertain, because of fundamental lack delivered from volcanic arcs in the of deep sea sediments in the Pacific. In this northwestern Pacific. This results is also study, instead of deep sea sediments, fore arc supported by climate models showing the basin sediments have been utilized for potential deep water formation in the late discussing the ocean circulation in the late Cretaceous northwestern Pacific.

Reference: Moiroud, M. et al., 2013. Evolution of the neodymium isotopic signature of neritic seawater on a northwestern Pacific margin: new constrains on possible end-members for the composition of deep-water masses in the Late Cretaceous ocean. Chem. Geol., 356: 160-170.

80 Land–ocean linkage: pelagic materials in Mesozoic neritic–terrestrial sequences in East Asia

Matsuoka, A.1, Ito, T.2, Sakai, Y.1 and Nikaido, T.1

1Niigata Univ., Niigata, 950-2181, Japan ([email protected]) 2China Univ. Geosci., Wuhan, 430074, China

Introduction from north to south. The Torinosu Group Mesozoic sedimentary sequences in occupies the Southern Chichibu and East Asia are categorized into two types; Kurosegawa terranes. In the type locality of the marine accretionary complexes and Torinosu Group (Sakawa area in central epi-continental neritic–terrestrial sequences. Shikoku), this group unconformably covers the The accretionary complexes are distributed in Togano Group (Matsuoka, 1984, 1992) of the eastern margin of Asia including Russian Jurassic accretionary complex or the Naradani Far East, the Japanese Islands, and the Formation of trench slope sediments. The basal Philippines (Kojima and Kametaka, 2000; part of the Torinosu Group is the Tsukadani Wakita and Metcalfe, 2005). The Formation composed mainly of chert clasts. epi-continental neritic–terrestrial sequences are They are regarded to have been derived from distributed mainly in Russian Far East, China, the Togano Group because the group is the the Korean Peninsula, and the Japanese Islands. basement of the Torinosu Group and contains a Oceanic rocks such as pelagic chert are typical large amount of chert sequences. No components of accretionary complexes. They microfossils, however, have been obtained are also included in neritic–terrestrial from the chert clasts due to recrystallization. sequences as recycled clasts. They are important not only in recognizing the Tetori Group provenance of sedimentary basins but also in The Tetori Group ranging in age from tracing the denudation history of accretionary the Middle Jurassic to Cretaceous is distributed complexes. The pelagic materials are tools for over the Hokuriku District in central Japan. linking lands and oceans. We introduce three Most parts of the Tetori Group overly examples of chert-bearing conglomerate in unconformably constituent geologic units of neritic–terrestrial sequences in Japan: the the Hida and Hida-Gaien terranes. These units Torinosu Group in the Southern Chichibu do not include mid-Mesozoic accretionary Terrane, Outer Zone of southwest Japan, the complexes. This group is divided into the Tetori Group in the Hida and Hida-Gaien Kuzuryu, Itoshiro, and Akaiwa subgroups in terranes, Inner Zone of southwest Japan, and ascending order and interbeds conglomerate the Miyako Group in the North Kitakami layers. Permian, Triassic, and Jurassic Terrane, northeast Japan (Fig. 1). Significance microfossils were obtained from siliceous and of the pelagic materials within muddy rock clasts in the conglomerates. Based neritic–terrestrial sequences is discussed. on fossil dating and lithological characteristics, most of these clasts were presumably derived Torinosu Group from the mid-Mesozoic accretionary complexes The Torinosu Group and its in East Asia (Ito et al., 2012). equivalents are late Jurassic to early Cretaceous neritic sequences distributed disconnectedly in Miyako Group the Chichibu Belt in southwest Japan. Three The Miyako Group is distributed terranes are recognized in the Chichibu Belt along the eastern coast of the North Kitakami based on characteristic features of their Massif. The group covers unconformably the components and geologic structures: the Magisawa Formation, a Jurassic accretionary Northern Chichibu, Kurosegawa (Middle complex, and other geologic units in the North Chichibu), and Southern Chichibu terranes Kitakami Terrane. The Miyako Group is 81 divided into the Raga, Tanohata, and Hiraiga Radiolarian fossils of Middle Jurassic age were formations in ascending order and is dated as obtained from siliceous mudstone and late Aptian to early Albian (Hanai et al., 1968). mudstone clasts in conglomerate. The fossil The Raga Formation is composed mainly of evidence and lithological similarities indicate conglomerate of non-marine origin and that these rocks were derived from the contains sandstone, mudstone, siliceous Magisawa Formation. mudstone, chert, and volcanic rocks.

References: Kojima, S., Kametaka, M., 2000. Jurassic accretionary complexes in East Asia. Mem. Geol. Soc. Japan, no. 55, 61–72 (in Japanese with English abstract). Hanai, T., Obata, I., Hayami, I., 1968. Notes on the Cretaceous Miyako Group. Mem. National Mus., Nat. Sci., 1, 20–18 (in Japanese with English abstract). Ito, T., Sakai, Y., Ibaraki, Y., Yoshino, K., Ishida, N., Umetsu, T., Nakada, K., Matsumoto, A., Hinohara, T., Matsumoto, K., Matsuoka, A., 2012. Radiolarian fossils from siliceous rock pebbles within conglomerates in the Mizukamidani Formation of the Tetori Group in the Itoigawa area, Niigata Prefecture, central Japan. Bull. Itoigawa City Mus., no. 3, 13–25 (in Japanese with English abstract). Matsuoka, A. 1984. Togano Group of the Southern Chichibu Terrane in the western part of Kochi Prefecture, southwest Japan. Jour. Geol. Soc. Japan, 90, 455–477 (in Japanese with English abstract). Matsuoka, A. 1992. Jurassic-Early Cretaceous tectonic evolution of the Southern Chichibu Terrane, Southwest Japan. Palaeogeogr., Palaeoclimatol., Palaeoecol., 96, 71–88. Wakita, K., Metcalfe, I., 2005. Ocean Plate Stratigraphy in East and Southeast Asia. Jour. Asian Earth Sci., 24, 679–702.

Fig. 1. Distribution of mid-Mesozoic accretionary complexes in Japan, Russian Far East, and northeast China with the localities of the Torinosu, Tetori and Miyako groups.

Day Three 6 September 2014

SESSIONS:

Land-ocean linkages: Correlation, sedimentology and paleoenvironments

Tectonic evolution and paleoenvironments of Asia and west Pacific

Biotic evolution: Asian and western Pacific fauna and flora - Macrofauna

83 Land-ocean linkage: correlation, sedimentology and paleoenvironments II

Palaeotemperatures, Palaeoclimate, Palaeolatitude, Palaeobathymetry and Palaeocurrent appraisal of Cretaceous sediments of Cauvery Basin, South India

Nagendra, R.1, Zakharov, Y. D.2, Safronov, P. P.2, Smyshlyaeva, O. P.2, Popov, A. M.2, Shigeta, Y.3and Venkateshwarlu, M.4

1Dept. Geol., Anna Univ., Chennai 600025, India 2Far Eastern Geol. Inst. Russian Acad. Sci. (Far Eastern Branch), Stoletiya Prospect 159, Vladivostok 690022, Russia 3Nat. Mus. Nature Sci., 4-1-1 Amakubo, ToTsukuba, Ibaraki 305-0005,Japan 4Geochronol. Palaeomagnetic Stud., CSIR-Nat. Geophy. Res. Inst., Uppal Road, Hyderabad, India

Introduction The Cauvery Basin is a pericratonic basin located along the south east coast of India. It was developed as a consequence of the breakup of Gondwana during the Late Jurassic (Rangaraju et al., 1993) (Fig. 1). The Cauvery Basin has undergone at least two major tectonic phases during its evolution. The early sheared rift extensional faulting initiated during Late Jurassic/Early Cretaceous (Shyam Chand and Subrahmanyam, 2001), and was followed by a progressive rift that seems to have continued until the end of the Turonian (Watkinson et al., 2007). The subsequent reverse movement caused by basinal uplift and contraction during the Campanian- Maastrichtian ended in the Figure.1. Geological map of Cretaceous outcrops, early Tertiary. This major tectonic activity may Ariyalur area, Cauvery Basin, Southern India have profoundly influenced relative sea level changes in all east coast basins. southern India and Mahajang Basin, Madagascar. Well-preserved material from Methodology southern India used for isotopic analysis Field data has been obtained by direct consisted of: (1) exceptionally well-preserved observation of lithofacies, stratal patterns, their belemnite rostra from the middle part (Albian) physical relationship and macrofossil content of the Karai Shale Formation, and (2) from quarries, river channels, and mine cuttings. well-preserved bivalve Lopha sp. shells from In the laboratory, two hundred sedimentary the upper part of the Kallankurichchi rock samples from sixty outcrop locations were Formation (Maastrichtian). Investigated early studied for microfacies, biostratigraphy for Albian cephalopods from Madagascar consist palaeobthymetry and palaeoenvironment study. of one nautiloid species (Cymatoceras? sp.) and The paleotemperature and palaeoclimate and four ammonoid species Cleoniceras besairei palaeolatitude studies were studied by isotope Collignon, Eotetragonites umbilicostriatus analyses of macrofossils from Cauvery Basin, Collignon, Desmoceras sp., and Douvilleiceras 84 sp. The palaeocurrent results obtained from significantly higher than those calculated from forty six oriented sediment block samples from isotopic composition of Albian belemnites seven sites covering the total thickness (∼40 from southern Argentina and the Antarctic and m) of the exposed rocks of Ariyalur Group. All middle Albian belemnites of Australia located the samples were drilled and cut into standard within the warm-temperate climatic zone. specimens (2.2 cm length and 2.5 cm diameter) The isotope results of early Albian and measured in the palaeomagnetism cephalopods from Madagascar infers the higher Laboratory of National Geophysical Research palaeotemperatures for summer near-bottom Institute, Hyderabad, India, following the shelf waters in this area (20.2°C to 21.6°C) in standard procedures described by Jelinek comparison with late Albian (1978). The samples were subjected to AMS palaeotemperatures calculated from southern measurements in 15 different directions using India fossils, but similar winter values Kappa Bridge MFK1-FA (Brno, Czech (13.3-16.4° C); however, the latter values are Republic) susceptibility meter following the higher than those calculated from early Albian standard method as per Agico user’s guide fossils (brachiopods and ammonoids) of the ver-4 2009. tropical-subtropical climatic zone of the high latitude area of southern Alaska and the Koryak Results and Discussions Upland. The new isotopic palaeotemperature Palaeotemperatures, palaeoclimate, data suggest that southern India and palaeolatitude, palaeobathymetry and Madagascar were located apparently in middle palaeocurrent interpretations were outlined for latitudes (within the tropical-subtropical Cretaceous sediments of Ariyalur District climatic zone) during Albian time. (Trichinopoly) of the Cauvery Basin, South In contrast to the Albian fossils, India. The oxygen isotope studies of Albian isotope results of well-preserved early belemniterostra are accounted along with Maastrichtian bivalve shells from the Ariyalur isotopic composition of middle Albian Group, Trichinopoly district, are characterized 18 ° belemnites of the middle latitude area of by lower δ O values (up to -5.8 /°°) but normal Pas-de-Calais in Northern hemisphere, δ13C values, which might be a result local southern Argentina, Antarctic and middle freshwater input into the marine environment. Albian belemnites of Australia and Albian This results suggest that the early Maastrichtian cephalopods from Madagascar, and Albian palaeotemperatures of the southern Indian fossilsof the tropical-subtropical climatic zone near-bottom shelf waters was probably about of the high latitude area of southern Alaska and 21.2°C, and that this middle latitude region the Koryak Upland. The Albian continued to be a part of tropical-subtropical palaeotemperatures for Ariyalur outcrop climatic zone, but with tendency of increasing sections of the Cauvery Basin are inferred to of humidity at the end of Cretaceous time. range from 14.9°C to 18.5°C for the epipelagic The palaeobathymetry trends of the zone, and from 14.3°C to 15.9°C for the Albian to Maastrichtian outcrop of Cauvery mesopelagic zone, based on analyses of 65 Basin reveal two major sea level falls during samples; isotopic palaeotemperatures Late Turonian and Late Maastrichtian, which interpreted as summer and winter values for correlate well with global sea level curves of near-bottom shelf waters in this area fluctuate Vail et al. (1977), Haq et al. (1987) andMiller from 16.3°C to 18.5°C and from 14.9°C to et al. (2005). These sea level drops are linked 16.1°C, respectively. Besides, the to the rise of Marion mantle plume during the paleobathymetry, magnetic fabrics and Late Turonian and reunion mantle plume palaeocurrent directions were studied with during Late Maastrichtian (Raju et al., 1993; oriented samples of the Cauvery Basin for low Courtillot et al., 1988; Nagendra et al., 2002a). field anisotropy of magnetic susceptibility The low field anisotropy of magnetic measurements. susceptibility (AMS) measurements of Cauvery The palaeotemperatures of the Basin sediments unravels the magnetic fabrics Cauvery Basin are similar to those calculated and palaeocurrent directions. The results of from isotopic composition of middle Albian AMS parameters of the sediments indicate belemnites of the middle latitude area of primary depositional fabrics for Campanian Pas-de-Calais in Northern hemisphere but (Sillakkudi), and Maastrichtian (Ottakovil and 85 Kallamedu) sandstone and secondary fabric for secondary fabrics in Maastrichtian limestone as Maastrichtian (Kallankurichchi) limestone. The a result of post-depositional processes. The obtained low degree of anisotropy (Pj), oblate petrography is established that K1 AMS axis of shape AMS ellipsoid and distribution of biotite mineral could represent the flow maximum (K1) and minimum (K3) direction. The established palaeocurrent susceptibility axes on equal area projection direction for Campanian sediments (Sillakkudi confirm the primary sedimentary fabric for Fm.) is NW–SE direction while Maastrichtian Campanian and Maastrichtian formations. The (Ottakovil and Kallamedu) sediments recorded observed AMS parameters like shape factor (T) NE–SW direction. Overall the palaeoflow (prolate to oblate), q value and random directions observed for Ariyalur Group distribution of minimum (K3) and maximum sediments of the Cauvery Basin is NE–SW to (K1) susceptibility axes are supported for NW–SE.

References: Courtillot, V., Feraud, G., Maluski, H., Vandamme, D., Moreau, M.G., Besse, J., 1988. Deccan flood basalts and the Cretaceous/Tertiary boundary. Nature 333, 843-846. Haq, B.U., Hardenbol, J., Vail, P.R., 1987. Chronology of fluctuating sea levels since the Triassic. Science 235, 1156-1167. Jelinek V 1978 Statistical processing of anisotropy of magnetic susceptibility measured on groups of specimens; Studia Geo-physica et Geodetica 22, 50–62. Nagendra, R., Raja, R., Nalappa Reddy, A., Jaiprakash, B.C., Bhavani, R., 2002a. Outcrop sequence stratigraphy of the Maastrichtian Kallankurichchi formation, Ariyalur Group, Tamil Nadu. J. Geol. Soc. India 59, 243-248. Raju, D.S.N., Ravindran, C.N., Kalyansundar, R., 1993. Cretaceous cycles of sea level changes in the Cauvery Basin, India e a first revision. Bull. Oil and Nat. Gas Comm. 30, 101-113 Rangaraju, M.K., Agarwal, A., Prabhakar, K.N., 1993. Tectno-stratigraphy, Structural Style, Evolutionary Model and Hydrocarbon Prospects of the Cauvery Palar Basins of India, vol. 1. Indian Petroleum Publishers, Dehradun, 371-398 pp. Shyam Chand, Subrahmanyam, C., 2001. Subsidence and isostacy along a Sheared margin- Cauvery Basin, Eastern continental margin of India. Geophy. Res. Lett. 28, 2273-2276. Vail, P.R., Mitchum, R.M., Thompson, 1977. Seismic stratigraphy and global changes of sea level, part 3: relative changes of sea level from coastal onlap. In: Clayton, C.E. (Ed.), Seismic Stratigraphy -Applications to Hydrocarbon Exploration. Amer. Ass. Petrol. Geol. Mem. 26, 63-81. Tulsa,Oklahoma. Watkinson, Matthew P., Hart, Malcolm B., Joshi, Archana, 2007. Cretaceous tectonostratigraphy and the development of the Cauvery Basin, Southern India. In: Geol. Soc. London, Spec. Publ., vol. 13, 181-191 pp.

86 Dynamics of Terminal Cretaceous global biotic turnover

Jafar, S. A.

Flat Number 5-B, Whispering Meadows, Haralur Road, off Sarjapur Road, Bangalore-560 102, India: ([email protected])

Recently discovered Peter Higg’s Catastrophic hypothesis and during the last Boson or “God Particle” is the fundamental three and a half decades, the geoscience particle which coalesce to form Atoms and community was absolutely robbed of their Molecules in the Universe. A wonderful Life conscience and reasoning. Catastrophic Molecule was created on planet Earth some 4 episodes, whether natural or manmade can billion years ago for unknown reasons, which cause only Local extinctions or biotic turnover initially replicated and evolved by multitasking of life and none of the Catastrophic events in RNA to be followed by DNA. Life originated geologic history ever caused global biotic as Small magnitude entities invisible to turnover cutting across all ecological niche. unaided human eye which gradually attained Over 3500 publications in reputed journals Large dimensions both in Ontogeny and came out and the hypothesis was hotly debated Phylogeny. Small Magnitude of both Animals in public and widely covered by media (Schulte, and Plants have lesser Volume in comparison 2010). The surgical precision analysis of to their Area, are more in numerical strength, Cretaceous-Palaeogene sections world over, have shorter life span, have more rapid including popular Chicxulub Crater revealed turnover rate and are lighter. Small Magnitude serious contradictions, and certain group of forms whether in Nature or Manmade scientists out of desperation suggested Structures are invariably stronger than their “Multiple Causes” (Archibald, 2010). The Larger counterpart under the influence of Deccan degassing model of McLean met the Gravity. It will be demonstrated here that same fate, despite very tempting coincidence of Relative Magnitude is a powerful trait which Mass Extinctions matching Permian-Triassic dictates the Innovation/Extinction pattern of with Siberian and Triassic-Jurassic with Life as it evolved and helped us to identify Central Atlantic Flood Basalt episodes. Other Giant forms among Virus, Bacteria and Protist Hypotheses like Marine Regression, Multiple etc. Global Mass extinctions as identified in the Impact and Supernova Explosion did not find Phanerozoic (The Big Five) including Terminal any scientific backing. In order to get to the Cretaceous, are interpreted as normal root of the problem, we need to relook at the gradualistic Background extinctions, when only Gradualistic model of Evolution proposed by Five times in 600Ma record of Phanerozoic Charles Robert Darwin (1809-1882) and (Ordovician-Silurian 443Ma, supported by Charles Lyell (1797-1875), as any Frasnian-Famennian 372Ma, Permian-Triassic Catastrophic model would prove fatal for 254Ma, Triassic-Jurassic 201Ma and Darwin’s Gradualistic model of Evolution. Cretaceous-Palaeogene 66Ma) several groups In order to understand the basic essence of of Life forms were accidently clustered and modern “Neodarwinian Paradigm”, it is perished, giving false impression of Mass instructive to be aware of three mutually Extinction. interacting components A. Natural Selection Georges Cuvier (1769-1832) an (Adaptability to Environmental change and eminent Vertebrate Palaeontologist strongly Ecosystem), B. Molecular Genetics argued for the Catastrophic Floods causing (Inheritance of characters) and C. Migration Mass Extinctions, but his belief in Biblical (Competition for Resource exploitation). Let us Floods dampened his claim. More recently, briefly examine the quality of paleoclimatic much dramatised Extraterrestrial Impact data available for Terminal Cretaceous, which hypothesis of Alvarez et al. (1980) revived the has a direct bearing on the nature of witnessed 87 biotic turnover dictated by Natural Selection. Cretaceous completely changed the chemistry Mid-Cretaceous represents “Greenhouse” of global oceanic realm. Diatom Bloom driven climatic conditions and the global average Silica depletion affected other Silica dependent temperatures were exceeding 10○C than present plankton and benthos in present day Antarctic day; periods of dysoxic-anoxic conditions waters. Mahajanga Basin Flood Basalt activity matched but did not cause extinction and around 90Ma, when Seychelles separated from evolution of marine nekton and plankton. Madagascar probably caused 1000Km deep Cretaceous was marked by exceptionally high westerly incursion of sea along Narmada rate of creation of oceanic crust at spreading Valley in India during Turonian. Extrusion of centers and eruption of Large Igneous Deccan Flood Basalt in India when Seychelles Provinces viz. Ontong Java and Kerguelen separated from the Indian subcontinent, caused Plateau, leading to the release of huge amount over 800Km deep easterly incursion of Subathu of greenhouse gases and water vapour which in Sea along Subathu-Dogadda rift zone of Lesser turn affect atmospheric and oceanic chemistry. Himalaya during Late Maastrichtian. Data from high and middle latitude sites In order to critically evaluate biotic suggest warming peak followed by cooling at turnover at Terminal Cretaceous, let us cast a Terminal Cretaceous. The levels of glance at what perished and what survived. In atmospheric pCO2 were higher by a factor of Marine Realm, Marine Reptiles – Plesiosaurus about 12 than present day level. The precise and Mosasaurus perished but Crocodiles and manner in which a variety of environmental Turtles survived. Giant Sharks, Ray-finned factor drive evolution in plant and animals is a Fish, Rudists, Inoceramids, Belemnites and subject matter of discussion and in certain Ammonoids perished. Foraminifera, both cases the reverse is true, like the 90% demise of planktic and benthic were eliminated in large Calcareous Nannoplankton at Terminal numbers. Among Phytoplankton 90% of

Fig. 1 Relative Magnitude Model (after Jafar, S. A. 2000).

88 Calcareous Nannoplankton perished causing continued throughout Phanerozoic upto present severe crisis in Ocean chemistry and time as it was discovered that by applying atmospheric CO2. Siliceous and organic walled Relative Magnitude concept, surprisingly, Phytoplankton and Zooplankton were severely forms invisible to unaided human can have affected. Picoplankton which are smaller than Giants. Darwin also believed that “It is not the Calcareous Nannoplankton lack mineralized strongest of the species that survives, nor the plates and therefore do not leave any fossil most intelligent that survives. It is one that is record, but the modern analogues probably the most adaptable to change.” Charles Darwin suggest that on account of extremely fast (1859): On The origin of Species by means of turnover rate they significantly contributed to Natural Selection or The preservation of biomass production and Ocean fertility. In Favoured Races in the Struggle for Life, Terrestrial Realm, Animals greater than 5Kg. Chapter 2, Variation Under Nature para 18, were eliminated. Larger Dinosaurs eliminated says “....in as much as geology plainly tells us globally, whereas smaller counterparts survived that the small genera have in the lapse of to produce several kind of birds. Pterosaurs, the time often increased greatly in size; and that flying Reptiles perished. Mesozoic Mammals large genera have often come to their largely survived. One major group of Plants maxima, declined and disappeared.” perished while Gymosperm dominated Samples from uninterrupted Cretaceous Flora was replaced by Angiosperm Cretaceous-Palaeogene sections were examined dominated one. It is difficult to scientifically in Germany, Austria, Spain and Denmark for accept that any single Catastrophe could cause Calcareous Nannofossils, Planktic/Benthic such an Extinction-Innovation on a global scale. Foraminifera. Goniatites from Moreover, no Catastrophic model can explain Frasnian-Famennian Boundary representing simultaneous Extinction-Innovation pattern Mass Extinction, were also examined.The seen in the geological record. We might safely results are summarized in Fig1(reproduced conclude that such a pattern of from Jafar, 2000). Thick horizontal Dotted line Extinction-Innovation can best be explained represents a Filter corridor which would allow under the Hypothesis of Neodarwinian certain forms to go through and certain forms Paradigm elaborated to be known as Relative to retain. There is no absolute size in Universe, Magnitude Model (Jafar, 2000, Fig. 1)). It must it is boundless towards both small and large; be borne in mind that this model does not seek nothing is big or small except by comparison, to address causative issue, instead highlights a hence this relative Magnitude model. A critical certain PATTERN to be observed throughout glance at Fig.1, reveals three spheres geological column including at Big Five Mass representing relatively Small, Medium and Extinction Boundaries. Is this hypothesis Large or Giant forms. Large Form has thickest testable? Yes, it is testable with any group of wall, lest it would collapse under its own fossils one is working with. Is this hypothesis weight under the influence of Gravity. Medium predictable? Yes, it can make fairly accurate Form has medium thickness and Small one has predictions, except timing, for ensuing Sixth thin wall for the same reason. Salient features Mass Extinction. of this Relative Magnitude model are A. All Over 3000Ma of history of Life three Spheres are dynamic in nature; if Small preserved in Precambrian rocks represents entity grows faster, then Medium entity would “Darwin’s Dilemma” as absence of magnifying become relatively Small. B. All three entities technology during his time did not allow one to become extinct at or near Mass Extinction see Small Magnitude fossils. “Darwin’s Boundary, but a few Small and Medium Dilemma” was once considered as the most entities manage to cross over, the medium ones powerful refutation of his hypothesis, as cross over practically unchanged producing ancestral forms of Cambrian-Ordovician fossils Living Fossils (Crossing Over). A few Small remained obscured. However, as we know now entities cross over and dramatically display that Darwin (1859) was right when he declared most rapid rate of innovation to restore “Consequently if the theory be true, it is dwindling biodiversity (Appearing). Large or indisputable that before the lowest Silurian or Giant forms represent evolutionary dead ends Cambrian was deposited, long period and invariably fail to produce offspring and in elapsed.....” Darwin’s Dilemma, even certain groups prior to extinction may or may 89 not produce dwarf or neotenic forms surviving Planet Earth without invoking any Catastrophic for extremely short period before extinction model. Empirical data on various fossil groups (Disappearing). We might conclude that the needs to be critically collected at Mass Pattern of Relative Magnitude Model is an Extinction Boundaries and predictions made in essential extension of Neodarwinian Paradigm the backdrop of the proposed Relative explaining the Gradualistic evolution of Life on Magnitude model.

References: Alvarez, L.W. et al. (1980). Science, 208 (4448), 1095-1108. Archibald, J. D. et al. (2010). Science, 328 (5981), 973. Jafar, S. A. (2000). N. Jb. Paleont. Abh., 217 (2), 161-197. Schulte, P. et al. (2010). Science, 327 (5970), 1214-1218. Darwin, C. (1859) John Murray, London, 1st. Edition

90 Late Cretaceous ecosystems of peninsular India: An overview of current perspectives

Bajpai, S.

Birbal Sahni Inst. Palaeobotany, Lucknow 226007, India ([email protected])

Recent data from peninsular India occurred earlier, during the have led to major advances in our Turonian-Coniacian (Nimar and Bagh Beds). understanding of the late Cretaceous Compelling evidence for the latter marine ecosystems around the time of Deccan flood incursions in central India has recently come basaltic eruptions. Until recently, sediments from the discovery of calcareous intercalated within the Deccan volcanics nannoplankton. (intertrappeans) in the main part of the volcanic Furthermore, recent geochemical data province were generally considered to be on the freshwater intertrappean ostracods has terrestrial deposits of late Maastrichtian age. provided new insights into the late Cretaceous However, the recent discovery of planktic environments of peninsular India. These data foraminifers, together with brackish water point to evaporative conditions prevailing in ostracods, in an intertrappean locality in central the intertrappean ecosystems, with evidence of India about 800 km from the nearest wide variability in the aquatic environment on present-day ocean, points to a more complex short timescales. This conclusion is consistent scenario for paleocommunities, with other palaeoclimatic data for northwestern palaeoenvironment, palaeoecology and peninsular India during the late Cretaceous and palaeogeography of the late Cretaceous-early suggests that the intertrappean lacustrine Paleocene ecosystems. The discovery of marine systems had a relatively long residence time elements in the main Deccan volcanic province that allowed diverse faunal and floral has challenged the traditional views, and communities to thrive, and that they were strongly suggests that a major marine seaway behaving as hydrologically-closed systems. existed across India during the Biogeographically, the late Cretaceous biota of Maastrichtian-early Paleocene. This seaway peninsular India shows evidence of an has major implications for the paleogeography, admixture of Gondwanan, Eurasian, and the evolution and biotic diversity during the K-Pg recently recorded endemic elements, transition in India. Current data suggests that suggesting long-distance trans-oceanic the seaway may possibly have followed the dispersal in a geographically isolated Indian Narmada and Tapti rift zones where marine plate. transgressions are already known to have

91 Tectonic evolution and paleoenvironments of Asia and west Pacific

Tectonic and climatic controls on A/S ratio in a non-marine setting: an example from the Lower Cretaceous Sindong Group of the Gyeongsang Basin (southeastern Korea)

Lee, H. and Lee, Y.I.

Sch.l Earth Envir. Sci., Seoul Nat. Univ., Seoul 151-747, Republic of Korea ([email protected])

Previous studies on non-marine occur. The unit 3 is an exception of this general successions have demonstrated that fluvial trend, comprising dominantly dark gray styles, thickness and width of channel sand floodplain mudstones and dark gray calcareous bodies, and channel/floodplain ratio are lacustrine mudstones. The thickness of channel determined by relative changes in the ratio of sand bodies is variable in each fluvial unit, but accommodation generation and sediment it generally increases upward from the bottom supply (A/S ratio). According to these studies, of the unit, reaching its maximum in the middle thin, isolated, high-sinuous channels are easily with the occurrence of multi-story, developed in high-accommodation settings high-sinuous, sandy channel deposits or (high A/S ratio), whereas thick, amalgamated, multi-story, low-sinuous, sandy channel low-sinuous channels tend to be developed in deposits, and decreases again toward the top low-accommodation settings (low A/S ratio). with a single to double-story, high sinuous, Although tectonics and climate are regarded to sandy channel deposits. Although single to be two main controlling factors for the A/S double-story, high-sinuous, pebbly channel ratio in non-marine basins where the influence deposits are also recognized, they do not show of eustasy is mostly excluded, the relative any systematic occurrence in a unit. The pebbly importance of tectonics and climate is difficult channel deposits most frequently occur near the to discriminate, and tectonic events such as bottom of the unit 3. basin subsidence (increase of A) or source-area The sand-depleted, reddish floodplain uplift (increase of S) have been commonly deposits at the tops of each unit was probably assumed as a primary control on the A/S ratio. deposited during dry periods when To investigate the relative importance transportation capacity critically decreased due of tectonics and climate on the A/S ratio and to low precipitation. The repeated occurrence resulting the distribution of depositional of them indicates that the studied succession systems and its staking pattern in a non-marine had influenced by cyclic climate changes from basin, facies analysis was carried out for the dry to wet to dry conditions. In this context, the fluvial succession of the Sindong Group increase of sandbody thickness in the middle of (Aptian to Albian) in the southern part of the each unit might be related with the wettest Gyeongsang Basin. The facies analysis reveals condition for the deposition of each unit. that the studied succession can be subdivided Sudden occurrences of pebbly channel deposits into five units, each having 300 to 400 m can be interpreted to be related to episodic thickness. Most of the units comprise various source area uplifting events, resulting in the colors of floodplain mudstone from dark gray increase of sediment supply (decrease of A/S to greenish gray to reddish. The boundaries of ratio). If so, remarkable increase of the the units are characterized by decimeter-thick sandbody thickness should be accompanied by reddish to greenish mudstones. Near the the occurrence of pebbly channel deposits. In boundaries, the reddish floodplain mudstone the studied succession, however, the pebbly are common, whereas in the middle of the units, channel sandbodies are single to double-story, they are generally absent, and greenish gray to and their thickness generally does not exceed 2 dark gray floodplain mudstones dominantly m. As described above, moreover, the 92 deposition of dark gray mudstones and 3. Therefore, the tectonic event causing the lacustrine mudstones in the unit 3 (probably episodic source area uplift (increase in representing significant increase of the A/S sediment supply) might also cause basin ratio) coincides with the stratigraphic interval subsidence (increase in accommodation with the most frequent occurrence of the generation), causing the deposition of single to pebbly channel deposits near the bottom of unit double-story channels.

93 Mesozoic fossil data from the “Eocene” Zambales Ophiolite

Dimalanta, C. B.1, Queaño, K. L.2, Salapare, R. C.1, Yumul, G. P.Jr.2,3, Marquez, E. J.4, Faustino-Eslava, D. V.5, Ramos, N. T. 1 and Payot, B. D.1

1Rushurgent Working Group, Tectonics and Geodyn. Acad. Gr., Nat. Inst. Geol. Sci., Coll. Sci., Univ. Philippines, Diliman, Quezon City, Philippines 1101 ([email protected]) 2Monte Oro Res. Energy Inc., Makati City, Philippines ([email protected]) 3Apex Mining Comp., Inc., Pasig City, Philippines ([email protected]) 4Dept. Phys. Sci. and Math., Univ. Philippines, Manila, Manila, Philippines ([email protected]) 5Schl. Envi. Sci. Manag., Univ. Philippines, Los Baños, Laguna, Philippines ([email protected])

Numerous studies have been Formation, an Early to Middle Miocene clastic conducted on the Zambales Ophiolite Complex formation that consists of ophiolitic detritus (ZOC), one of the best-exposed crust-mantle including blocks of cherts, peridotites and sequences in the region. The ophiolite, which gabbros. Radiolarians extracted from the chert occupies the north-south trending Zambales samples include Eucyrtidiellum sp., Range, is divided into three massifs – Masinloc, Wrangellium sp. and Triactoma sp., Cabangan and San Antonio (Figure 1). An Holocryptocanium barbui, Pseudodictyomitra Eocene age had previously been assigned to the carpatica, Archaeospongoprunum sp., ophiolite on the basis of the overlying Crytamphorella sp., Wrangellium (?) sp. cf. sedimentary units in the southeastern part of W(?) columnum (Figure 1). This assemblage the Zambales Range. Geochronologic dating of suggests a Middle Jurassic to Early Cretaceous diabase, granodiorite and other late-stage age (Bathonian to Aptian). magmatic products similarly yielded the same The recognition of an age older than Eocene age. previously reported for the ZOC warrants a The northernmost massif which re-examination of its tectonic evolution. comprises the ZOC, Masinloc Massif, is Correlating with other similarly-aged ophiolites, overlain by Cenozoic clastic sedimentary units we suggest the possible existence of a (Figure 1). Field campaigns in the area revealed Mesozoic ophiolite belt along the western that the Acoje Block which forms part of the Philippine archipelago. Masinloc Massif is overlain by the Cabaluan

Figure 1. (left top) Index map of the Philippines showing the location of the Zambales Range. (left bottom) Map of Luzon island showing the Zambales Ophiolite Complex which is divided into the Masinloc, Cabangan and San Antonio massifs. Boxed region shows the area occupied by the overlying sedimentary units investigated in this study. (middle) The chert samples which yielded radiolarians were collected near the Cabaluan River (marked by black star). The chert blocks are incorporated within the Early to Middle Miocene Cabaluan Formation in the Acoje Block of the Masinloc Massif. (right top) Photo of the radiolarian blocks which were observed in the Acoje Block. (right bottom) Radiolarians extracted from the chert samples suggest a Middle Jurassic to Early Cretaceous age.

95 Implications to Central Philippine evolution from signatures of the Cretaceous Balud Ophiolitic Complex

Faustino-Eslava, D. V.1, Dimalanta, C. B.2, Queaño, K. L.3, Ramos, N. T.2, Payot, B. D.2, Manalo, P. C.2 and Yumul, G. P. Jr.3,4

1Schl. Envi. Sci. Manag., Univ. Philippines, Los Baños, Laguna, Philippines ([email protected]) 2Rushurgent Working Gr. – Tectonics and Geodyn. Acad. Gr., Nat. Inst. Geol. Sci., Coll. Sci., Univ. Philippines, Diliman, Quezon City, Philippines 1101 ([email protected]) 3Monte Oro Res. Energy Inc., Makati City, Philippines ([email protected]) 4Apex Mining Company, Inc., Pasig City, Philippines ([email protected])

The island of Masbate in Central of the Cretaceous Southeast Bohol Ophiolite Philippines lies east of the previously Complex (SEBOC). These characteristics are established arc-continent collision boundary fairly similar to most Mesozoic Central between the Palawan microcontinental block Philippine ophiolites that exhibit transitional (PCB) and the Philippine mobile belt (PMB). island arc – mid-ocean ridge geochemical Recent mapping of the western section of the signatures that strongly contrasts with younger island revealed fragments of upper crustal (Eocene) e-MORB-influenced crust-mantle rocks that make up the recently recognized suites such as the Amnay ophiolite in Mindoro Balud Ophiolitic Complex (BOC). A relatively Island. thick unit of siliceous sedimentary deposits was Gravity signatures over the BOC are also found directly overlying the BOC. This characterized by low anomaly values, Panguiranan Chert formation is believed to consistent with the signatures of other represent the sedimentary carapace of the BOC dismembered ophiolites. Gravity data of and initial processing for radiolarian remains Masbate have significantly higher Bouger yielded an upper Cretaceous form, anomalies than those of Mindoro, Romblon Holocryptocanium barbui. Island Group and northwestern Panay. This In order to characterize this newly contrast is attributed to the continental delineated ophiolitic body, its geochemical and character of PCB-affiliated islands that geophysical features attributes are compared generally register lower anomalies. Incidentally, with similarly-aged crust-mantle sequences in these results support an arc-collision model that neighboring islands within the Central places the boundary of the PMB and the PCB Philippines. Geochemically, the BOC basalts between the islands of Sibuyan and Masbate. are characterized by depletion in HFSEs (e.g. Most models for Mesozoic central Nb, Ti, Zr) consistent with generation in a Philippine ophiolites suggest proto-Philippine subduction environment. Their strong light Sea plate origins for these oceanic fragments. REE depletion and flat mid REE to heavy REE Similarities between the BOC and many of patterns are also most similar to volcanic rocks these ophiolitic bodies suggest parallel origins.

Figure 1. A. Index map of the Philippines showing the Central Philippines and the extent of the Palawan Microcontinental Block (PCB). B. The Central Philippine Islands. Mindoro, Romblon Island Group and western Panay are considered to belong to the PCB. To the east of the boundary is Masbate Island, where the Balud Ophiolitic Complex (BOC) is being mapped. C. Geology of the BOC. There are mapped exposures of basalts, dikes and gabbros. D. Holocryptocanium barbui extracted from the Panguiranan chert, which is the sedimentary carapace of the BOC. E. Comparison of the trace element chemistry of the BOC with Amnay Ophiolite in Mindoro and Sibuyan Ophiolite in Romblon Island Group (RIG).

97 Tectono-magmatic Development of Accreted West Burma Block from Gondwana Land

Naing Maw Than

Myanmar Geol. Soc., Singapore (MGSS), Blk 238#05-59, Serangoon Ave.2, Singapore550238 ([email protected])

Western Myanmar, between the of the West Burma Block and late Jurassic strike-slip Sagiang Fault in the east and the radiolarian cherts in ophiolites at Myitkyina frontal thrusts of the Indo-Burman Ranges in area (Maung Maung et al., 2008). the west, was identified by Mitchell (1989) as Metcalfe (1996, 2005) suggested that an allochthonous continental block, now the Sikuleh microcontinental terranes, largely overlain by Cenozoic sediments and an incorporated in the Woyla terranes and the active magmatic arc. Mitchell (1989) named West Burma block, separated in the Late this continental block ‘Mount Victoria Land’ Jurassic to Early Cretaceous and were accreted from an occurrence of metamorphic rocks, in the mid Cretaceous. The Woyla nappe is taken to represent the outcrop of the continental interpreted as an intraoceanic arc thrust over basement. This block has been termed the the West Sumatra block and the Woyla Arc ‘West Burma Block’ by Hutchison (1989). was certainly accreted to Southeast Asia as part Southeast Asia is made up of a series of of the Woyla nappe in the mid Cretaceous continental blocks which separated from (Barber 2000; Barber & Crow 2008). northern Gondwana during the Late Paleozoic Michell et al. (2012) speculated that, and Mesozoic and were subsequently accreted in the Cretaceous the Wuntho–Popa arc (United to the southern margin of Asia with the Nations 1978c) was much further south, within subduction of the intervening oceanic crust. the western part of the present Andaman Sea From east to west the Malay peninsula and and possibly Sumatra are composed of three continental Sumatra–Wuntho–Popa–Mokpalin arc blocks: East Malaya, Sibumasu and West continued northwards through diorite and Sumatra (Barber and Crow (2009). granodiorite intrusions within the Tagaung Hutchison (1994) and Barber et Myitkyina Belt (TMB) of Burma. al.(2003) proposed a hypothesis, during the During northward indentation of India Triassic an elongated slice, including West into Asia the region east and southeast of Tibet Sumatra and West Burma, became detached underwent large scale right-lateral shear and from Cathaysia (Indochina) along a major clockwise rotation, the right-lateral Sagaing transcurrent fault and was translated along the fault in Burma which marks the eastern margin western margin of Southeast Asia to its present of the NNE moving Indian plate during the position outboard of the Sibumasu terrane. Neogene. The contact between the Sibumasu Igneous rocks ranging in age from block and the West Sumatra block is marked by Lower Jurassic to Pleistocene or early Recent the Medial Sumatra Tectonic Zone (MSTZ), a occur sporadically in a1500 km long ‘volcanic distance of 1760 km and interpreted as a major arc’ throughout the Central Lowlands transcurrent fault. Barber and Crow (2005) (Chhibber 1934). The arc coincides with an correlated the MSTZ with the Mogok Belt of axis within the Central Lowlands sedimentary Myanmar and the West Burma block is the basin (Central Burma Basin), dividing it into extension of the West Sumatra block, from Western and Eastern Troughs that represents which it was separated by the formation of the arc volcanism above an east-dipping Andaman Sea in the Miocene (Curray, 2005). subduction zone . The Central Volcanic Line By paleontological findings, Oo et al. (2002) (CVL) arc is terminated by South at Andaman have described Permian fusulinids of sea spreading center which has been active Cathaysian type in Karmine in the northern part since Mid-Miocene (Curray, 1979). 98 Mitchell (1981), Stephenson and dehydrating oceanic crust of the subduction Marshall (1984) stated that prior to the zone. The generation of potassic magma initiation of the Andaman Sea spreading centre involved the partial melting of the volcanic arc was continuous southwards phlogopite-bearing garnet peridotite at with the Sumatra and Sunda arcs of Indonesia relatively deep levels in the upper mantle (120 (Hutchison 1982), in which many high-K Km+), below the amphibole stability (Gupta calc-alkaline volcanic centers have and Yagi, 1980) and the more siliceous lavas geochemical and mineralogical similarities to may have been derived by fractional the Burma volcanics (Whitford 1975; Whitford crystallization of such magmas at crustal levels & Nicholls 1976; Leo et al. 1980; See in (Stephenson and Marshall, 1984). Stephenson and Marshall, 1984) (Maury et al. The present-day active subduction 2004). This is particularly true in northern zone is the Burma seismic zone, a narrow zone Sumatra where fault controlled Miocene to of deep earthquakes extending down generally Recent volcanoes, with remarkable similarity to to ~150 km, but with a few earthquakes down those of comparable age in Burma, are to 250 km depth (Ni et al., 1989). It is notable developed on the southwestern continental that if extrapolate the trend surface slightly so margin of the Sundaland Craton (Rock & Syah as to produce 160 Km contour would pass 1983) (See in Stephenson and Marshall, 1984). through the volcanic arc in map view. Petrochemical analysis of Mt. Popa According to petrochemical and seismicity data, area (Upper Miocene to early Recent) and its it can be mentioned that the magma generation northern continuation shown high -K of the Popa area indicate a depth range of calc-alkaline suite (Ye Min, 1992, Khin Maung (120-160) Km at relatively deeper part of the Tun,1993, Naing Maw Than,1993) that is upper mantle. attributed to the waning stage of orogeny as the Morrison (1980) suggested that obliquely eastward subduction of the Indian steepening of subduction plate can occur Plate beneath the Eurasian Plate that gave way beneath a thickening crust towards the end of to strike-slip movement associated with the an orogenic phase and prior to a flip Andaman Sea spreading-centre (Stephenson (overturning) of the zone or a change to and Marshall 1984). strike-slip movement such as has recently Although such high-K Calc alkaline occurred in Myanmar. suite are known from island arcs, they are more These results provide a most useful prevalent on continental margin where they are local tectono-magmatic analogy and supportive often associated with extremely K rich for consideration of the West Burma block is shoshonitic rocks.Magmas were probably the extension of the West Sumatra block. generated by hydrous mantle melting above

References: Barber A. J. 2000. The origin of the Woyla Terranes in Sumatra and the Late Mesozoic evolution of the Sundaland margin. J. Asian Earth Sci. 18, 713–38. Barber A. J. & CROW M. J. 2003. Evaluation of plate tectonic models for the development of Sumatra. Gondwana Res. 20, 1–28. Barber A. J., CROW M. J. & MILSOM J. S. (eds) 2005. Sumatra: Geology, Resources and Tectonics. Mem. 31. Geol. Soc. London, London. Barber A. J. & CROW M. J. 2009. Structure of Sumatra and its implications for the tectonic assembly of Southeast Asia and the destruction of Paleotethys Island Arc 18, 3–20 Chibber, H.L., 1934, The Geology of Burma : New Jersy, Prentice-Hall, Inc. Curay J.R., Moore D.G., Lawver L.A., Emmel F.J., Raitt R.W., Henry M. & Kieckhfer R. (1979). – Tectonics of the Andaman Sea and Burma. In: T.S. Watkins, L. Martadet & P.W. Dickerson, Eds, Geological and geophysical investigations of continental margins. AAPG Mem., 29, 189-198. Curray, J.R. 2005. Tectonics and history of the Andaman Sea region. J. Asian Earth Sci., 25, 187-232.

99 Gerven. M.van. and Pichler.H., 1995, Some aspects of volcanology and geochemistry of the Tengger Caldera, Java, Indonesia : Eruption of a K-rick tholeitic series, J. SE Asian Earth Sci. 1, 125-133 Gupta, A.K and Yagi, K., 1980, Minerals and rocks . V.14; Petrology and genesis of lucite – bearing rocks. Sprimger- Verlag, Newyork Hutchison, C.S., 1989. Geological Evolution of Southeast Asia. Oxford University Press. Khin Maung Tun, 1993, Petrology of the Shin Ma Taung Area, Pakkoku Tsp., Univ. of Mandalay, unpub. Master’s thesis Maung Maung, Aung Naing Thu, Suzuki, H., 2008. Latest Jurassic radiolarian fauna from the Chyinghkran area, Myitkyina Township, Kachin State (Region), Maury. R.C., et. al., 2004, Quaternary calc-alkaline and alkaline volcanism in an hyper-oblique convergence setting, central Myanmar and western Yunnan (Bull. Soc. géol. Fr., 2004, t. 175, no 5, pp. 461-472) Metacalfe I. 1996. Pre-Cretaceous evolution of SE Asian terranes. In Hall R. & Blundell D. J. (eds).Tectonic Evolution of Southeast Asia. Geol. Soc., London, Spec. Publ. 106, 97–122. Metacalfe I. 2005. Asia: South-East. In Selley R. C., Cocks L. R. M. & Plimer I. R. (eds). Encyclopedia of Geology, pp. 169–96. Elsevier, Amsterdam. Mitchell, A.H.G., 1981. Phanerozoic plate boundaries in mainland SE Asia, the Himalayas and Tibet. J. Geol. Soc., 138, 109–122. Mitchell, A.G.H. 1989. The Shan Plateau and Western Burma: Mesozoic-Cenozoic plate boundaries and correlation with Tibet. In: Sengör, A.m.C. (ed.)Tectonic Evolution of the Tethyan Region. KluwerAcademic Publishers, 567-583. Morrison, G.W. 1980, Charcteristics and tectonic setting of the shoshonite rock association : Lithos, 13, 101-112. Naing Maw Than, 1993, Petrology of the Taungni-Pingadaw Area, Kyaukpadaung Tsp., Univ. of Mandalay, unpub. Master’s thesis Naing Maw Than, 2012, Nature of the Central Volcanic Line in Taung Ni area, Central Myanmar. AOGS 2012 abstract volume. Ni, James F. Marco, Gunzman Speziale et al.,1989, Accreationary tectonics of Burma and the three dimensional geometry of the Burma subduction zone: Geology, 17, P.68-71. Marshall.T.R, Amos.B.J. & Stephenson.D, 1983, Base Metals Concentrations in Silicified and Argilized lavas of the The central Burma Volcanics. Geol. Soc., Spec. Publ., 11, 59-68. Oo,Tin H. & Nyuny H. 2002. Permian of Myanmar. J. Asian Earth Sci. 20, 683–699. Stephenson, D. and Marshall.T.R. , 1984, The petrology and mineralogy of Mt. Popa volcano and the nature of the late Cenozoic Burma volcanic arc; J. Geol. Soc. London, 141, 747-762. United Nations, 1978c. Geology and Exploration Geochemistry of the Salingyi-Shinmataung area, Central Burma. Technical Report No. 5, DP/UN/BUR-72-002/14, Geol. Sur. and Expl. Project, United Nations Development Programme. United Nations, New York, p. 29. Ye Min, 1992, Petrology of the Banmauk-Pinlebu Area, Kawlin-Wuntho Tsp., Univ. of Mandalay, unpub. Master’s thesis

100 Biotic evolution: Asian and western Pacific fauna and flora - Macrofauna

Morphological details of a newly discovered Cretaceous echinoid species ‘Stereocidaris keertii ’ (Smith A. B., 2010)

Sharma, V. K.

Dept. Zoology, Govterment, Holkar Sci. Coll., PIN- 452001. Indore, (M.P.) India. ([email protected])

Introduction: The Bagh formation in central India Results: (Madhya Pradesh) represents good examples of The two species of Stereocidaris a diverse Turonian shallow-marine rich reported from the Bagh region are superficially echinoid fauna, but dating of this sequence has very similar to each other but they are different so far been controversial. The marine echinoid to each other in many respects. The newly faunas come from a condensed shallow water discovered species S. keertii differs with S. succession of carbonates interrupted by several namadica in ambulacral tuberculations, broader well-marked hard grounds and depositional perradial zone, size of gonopore and the thick hiatuses. margins of the inner side of the genital plates. High magnesium calcite skeleton of echinoderms makes them very durable during Conclusions: the process of fossilization, and offers Late Cretaceous (Turonian) well-understood and beautiful fossils. Out of echinoids of Bagh formation (Chiplonkar et eleven regular and irregular echinoid species al.,1973) Madhya Pradesh of central India reported from this region one regular echinoid represents a large collection of epibenthic Stereocidaris keertii is new to science, regular echinoids. The Mesozoic to recent discovered by the author during a field work in crown group echinoids all have tests February 2007 in the Man –Sukkar Nala river constructed of 20 columns of plates, but show region to the south of Zeerabad, Madhya great variation in shape. Cidaroid are among Pradesh. Although it resembles Stereocidaris the most highly conserved echinoids in terms namadica but differs in its finer morphological of their skeletal morphology. Tests of both the details. The detail study also confirm some regular echinoids are especially well adapted to more identification features in the apical plate. the mechanical activity of the ambulacral tube feet. The shape of the test is flattening towards Summary of methods: the substrate. The differential distribution of Samples were collected from five material within the test make it outward bulge of localities around Zeerabad District Dhar. The the ambulacra. Both the fossil Stereocidaris specimens were collected both by hand picking were compared to each other and also with the and bulk sampling. Bulk samples were present day sea urchins to see the sexual processed using repeated tooth brush cleaning. dimorphisms on the basis of shape and the size In total, 21complete specimens and many of the genital pores, position of the genital fragmentary plates were collected along with pores in the genital plates, the height of the test spines. Among these 5 specimens were (height diameter ratio) and the type of the identified as S. keertii and remaining 16 were spines. All these morphological details were identified as S. namadica. After the laboratory found to be useful in the species and sexual cleaning all echinoids have been subjected to a differentiation. detailed taxonomic study as per Echinoid directory, a web resource.

101

Figure 1: Newly discovered species of a regular sea urchin Stereocidaris keertii showing interambulacral and ambulacral zones.

Referances: Smith A.B. (2010) The Cretaceous Bagh Formation, India: a Gondwana window onto Turonian shallow-water echinoid faunas. Cretaceous Res.31:368-386. Chiplonkar, G.W., Ghare, M.A., Badve, R.M. (1973). Bagh Beds e their fauna, age and affinities. Biovigyanam.3: 33-60.

102 Eggs, nests and poops of Indian Late Cretaceous sauropods: behavior, habitat and diet

*Mohabey, D. M. and Samant, B.

Postgrad. Dept. Geology, RTM Nagpur Univ., Amravati Road, Nagpur-440001, India. ([email protected]; [email protected])

*Ex. Geological Survey of India

The Late Cretaceous (Maastrichtian) and Chanda (=Chandrapur districts), which are dinosaur fossils are recorded mostly in the now part of Maharashtra and Madhya Pradesh sediments associated with Deccan volcanic states. The first named Indian dinosaur, the flood basalts sequences. The sediments are sauropod “Titanosaurus indicus” was based on designated as Lameta Formation two caudal vertebrae originally discovered by (=infratrappean, below the volcanic flows) and W. H. Sleeman in 1828 from and designated as intertrappean (positioned between the flows) of Titanosaurs indicus by Lydekker (1877). which the former is rich in dinosaur fossils. Charles Matley made intensive excavations at The sediments of central and western India Jabalpur during the two expeditions in records a diverse suite of terrestrial 1917-1919 collecting many dinosaur bones environments, including low-gradient from the Bara Simla and in 1932-33 from fluvio-laustrine flood plains, braided river Chhota Simla,that were described by Von systems, and upland soil-forming settings in Huene and Matley (1933). They named nine semiarid climates having strong seasonality new theropod genera and species including six (Mohabey et al. 1993). Were it not for the medium-to-large-sized theropods, a small emplacement of the overlying flood basalts of bodied theropod and four titanosauriform the Deccan Traps which deeply buried the sauropods- Titanosaurus indicus, T. blandfordi, palaeotopography, it is very unlikely that any Antarctosaurus septentrionalis and of the environments represented by the Lameta Laplatasaurus madagascariensis. Jain and would have been preserved in the geological Bandyopadhyay (1997) described a new record. It is probably for this reason that the species T. colberti from Dongargaon Hill. Lameta has afforded numerous unique insights However, revision currently considers only into Late Cretaceous terrestrial life (Mohabey, titanosauriform genera, Isisaurus and 1996). The major Lameta localities which have Jainosaurus as valid from the Late Cretaceous been yielding dinosaur fossils are (i) of India (Wilson et al. 2009). Two new genera Nand-Dongargaon in Maharashtra in central and species of abelisaurid theropod- India, (ii) Kheda and Panchmahal areas of Rajasaurus narmadensis (Wilson et al. 2003) Gujarat in western India and (iii) Jabalpur and and Rahiolisaurus gujaratensis (Novas et al. Bagh areas of Madhya Pradesh in central India. 2010) have been described from the Lameta Recently, titnosauriform bones have also been Formation of Rahioli in Kheda District, Gujarat. reported from the Lameta of Maru river section From the Lameta of Rahioli dinosaur teeth in Salburdi area in the adjoining districts of have also been described (Mathur and Amravati in Maharashtra and Betul in Madhya Srivastava, 1987). Pradesh (Srivastava and Mankar, 2013). The Since the discovery of first dinosaur Lameta sediments are time transgressive and eggs in India in 1983, a large number of deposited during the Maastrichtian nest-sites, nests and eggs have been recorded magnetochron C30n to C29r. from the Lameta in western and central India. Indian dinosaurs were first reported A large diversity is noticeable in the Indian from the Lameta of “Jubbulpore” (=Jabalpur) dinosaur eggs. Based on the morphology and

103 eggshell microstructure and histostructure, the hatchling (Wilson et al. 2010). Multiple dinosaur eggshells have been assigned to the snake-egg associations at the site strongly oofamily Megaloolithidae, Elongatoolithidae suggest that S. indicus frequented nesting and a possible Spheroolithidae (Mohabey, grounds and preyed on hatchling sauropods. 1998). At least eight new oospecies of the The stable carbon and oxygen isotope studies oogenus Megaloolithus attributed to sauropods of has indicated that these egg-laying reptiles have been established. drank waterfrom water-bodies having an Intensive field research has resulted in excessive evaporation, and consumed plants interpreting the nesting behaviour and that utilised C3 photosynthetic pathways palaeoecology of the nest-sites of (Sarkar et al. 1993). It is suggested that the titnosauriform dinosaurs based on the vegetation was scanty and mostly confined taphonomical and sedimentological studies of around the water bodies. the egg-bearing sediments. The studies reveal A large concentration of dinosaur that most of the eggs, nest and nest-sites occur poops (coprolites) has been recorded in the exclusively in the channel-related sandstone or Lameta sediments at Pisdura in the emergent palustrine flat deposits that are Nand-Dongargaon area. Hislop (1860) was the mostly pedogenically modified. At a single first to report coprolites from the Lameta nesting site all the nests are found at the same Formation of Pisdura. Subsequently, Matley stratigraphic level. The individual nests (1939) made a large collection of coprolites constitute a cluster of eggs in a saucer shaped from this section and classified them into four depression generally having a depth up to 50 types viz. Type-A, Type-B, Type-Ba and cm and diameter up to 100 cm. In a majority of Type-C. He referred the Type-A coprolites to the nests, the eggs are found to be laid in a titanosaur sauropods based on their large size single layer having no well-defined pattern. (cylindrical, straight to curved segment up to The eggs in the nests are preserved either as 12 cm long, 7 cm wide and smooth) and their lower halves of eggs surrounded by eggshell indirect association with the bones of debris or as complete to near-complete titanosaurid sauropods that represented the (generally intact) eggs. In the former category, largest-sized animals amongst the generally, the lower halves of eggs are found. contemporary vertebrates. The other Eggshells fragments may occur inside the eggs vertebrates found are pelomedusoid turtles, or in the surrounded matrix. Such eggs possibly snakes (madtsoid), crocodiles, pelobatid frogs represent the hatched category of eggs. The and fishes (Mohabey 1996, Mohabey et al. Megaloolithus eggs mostly occur in a single 2011). Matley (1939) described Type-A layer with no well-defined pattern. The nest droppings as free of any plant or animal tissues. and nest-sites associated with the Mohabey (2001), reported coprolites with Megaloolithus eggs are strong evidences for exclusive well preserved plant tissues that communal nesting by titanosauriform provided evidence for revealing the intake of sauropods. The evidences suggest that these solid and liquid diet of their producers. dinosaurs always preferred to nest and bury Globally, before this find, the coprolites with their eggs in the soft sands along the plant tissues remained unknown and the river-banks. No evidence of any plant material understanding of the dietary habit of sauropods which could have possibly produced heat for remained mostly based on the study of the teeth the incubation of the eggs is found inside the and the jaw mechanism of the herbivore nests. In India no bones are found associated sauropods and their indirect association with with the eggs and nests excepting at the Dhori contemporary plants fossils in the sediments. Dungri in Gujarat where bones of sauropod The Type A coprolites from the Pisdura contain hatchlings have been found associated with the plant tissues of pteridophytes, gymnosperms eggs (Mohabey, 1987). At this locality a partial and angiosperm including grasses in various skeleton of a new 3.5-m-long snake, Sanajeh proportions suggesting a mixed diet for the indicus gen. et sp. nov., has been recovered animals and availability of multiple of sources from Lameta sediments. S. indicus was of plants. Presence of insect burrows, bacteria, fossilized in association with a sauropod epiphyllus fungi, sponge and freshwater dinosaur egg clutch, coiled around an egg and diatoms (Aulcoseira) is not uncommon adjacent to the remains of a ca. 0.5-m-long (Mohabey and Samant, 2003, Ghosh et 104 al.2004). Palynomorphs are scarce and poorly titanosauriform and relationship with the preserved in the coprolitic mass. This can be evolution of Mesozoic plants in India is owing to corrosion of the material in the guts presently difficult to establish due to absence of and alimentary canals of the animals (Waldman any early Cretaceous dinosaurian bearing and Hopkin, 1970). The plant tissues in the sediments in India and inadequate sampling. coprolites are perminerlised, comminuted and Clusters of Type-A coprolites in coarsely chewed. The tissues are exclusively association with the other types of coprolites soft and tender consisting of inflorescence, occur as a discrete layer within the over-bank fertile shoots, apical shoots, tender leaves with sediments. They are associated with the petioles, flowers and small fruits with thin skeletal remains of titanosaurs and other pericarps. Hard woody tissues are rare. This vertebrates and are interpreted as lag suggests that the titanosauriform sauropods accumulate in the over-bank areas (Mohabey et preferred to eat the soft foliage of higher plants al. 1993). The coprolites show desiccation by cropping as supported by their narrow cracks suggesting their drying and hardening crowned teeth. The titanosauriform teeth after defecation and exposure to sun in the collected from the Lameta Formation represent overbank areas of their habitat and week dentition comprising narrow crowned subsequently deposited as lag accumulates. peg-like teeth with Slender Index (SI, Positioned at palaeolatitude 290 south, Height:Width>4) and with a lot of wear. The the Indian subcontinent during the Late jaw structure possibly could not effectively Cretaceous (Mastrichtian, C30n to C29r) in occlude like those of ornithischian herbivores. central and western India offered ideal It is strongly suggested that the India Late environmental and ecological niches for the Cretaceous sauropod were more adapted to preferred habitat of titanosauriform sauropods cropping of soft plant issues of angiosperms, and their breeding and large scale nesting. The gymnosperms and pterodophytes as their solid evidence suggests that during the Lameta time diet. The ornithischian herbivores known for under semiarid climatic conditions with strong their complex mastidentary adaptations are not seasonality, the overbank areas of the low land known from the Indian Late Cretaceous alluvial-limnic environments were inhabited by excepting doubtful reports of Dravidosaurus herds of titanosauriform sauropods and blandfordi and Brachypodosaurus gravis. abelisaurid theropods. Existing lakes and water Presence of phytoliths of grasses including rice pools were surrounded by patchy but tribe in the Pisdura coprolites (Prasad et al. diversified flora comprising varied plant 2011) is suggestive that the titanosauriform species of pteridophytes, conifers and sauropods were also adapted to browsing other angiosperms including grasses representing tall than cropping the foliage of trees. In the Late leafy trees, shrubberies and abundant aquatic Cretaceous of India the angiosperm plants and vegatation that provided main solid d of lakes narrow crowned titanosauriform sauropods and ponds to the herbivore sauropods. In the appear simultaneous for the first time in the semiarid conditions with strong seasonality magnetic chron C30n of the Mastrichtian. (Mohabey et al. 1993, Mohabey and Samant, However, based on the existing state of 2005) the availability of the plant as food knowledge it is difficult to suggest any resources could be controlled by the seasonal co-evolutionary relationship between the variations. The impact of Deccan volcanism on narrow-crowned titanosauriform herbivores the existing environments and availability of and the origin and evolution of angiosperms on plant resources food influencing the life and the Indian subcontinent. Community structure death of the Indian Late Cretaceous sauropods and migratory behaviour for Indian titanosaurid still need to be properly assessed. It is currently is well known (Mohabey, 1998) and the considered (Mohabey and Samant, 2013) that dispersal of flora through seed and pollen-spore the history of Late Cretaceous dinosaurs on the in the coprolites is not be ruled out. The older Indian subcontinent only spanned 500 KY to prosauropods (Barapasurus) and early 350 KY before the Cretaceous-Paleogene sauropod (Kotasaurus) are known to have boundary (K-Pg) and affected by the Deccan broad crowned spatulate teeth. Their evolution volcanic eruptions they never reached the K-Pg to the Late Cretaceous narrow crowned boundary.

105 References: Ghosh, P., Bhattacharya, S.K., Sahni, A., Kar, R.K. and Mohabey, D.M., 2004. Dinosaur coprolites from the Late Cretaceous (Maastrichtian) Lameta Formation of India: isotopic and other markers suggesting a C3 plant diet. Cret. Res., 24, 743-755. Hislop S., 1860. On the Tertiary deposits associated with trap-rocks in the East Indies. Quart. J. Geol. Soc. London, 16, 154-166. Jain, S. L. and Bandyopadhyay, S., 1997. New titanosurid (Dinosauria; Sauropoda) the Late Cretaceous of Central India. Jour. Vert. Pal., 17, 114-136. Lydekker, R., 1877. Notices of new and other vertebrata from Indian tertiary and secondary rocks. Rec. Geol Surv. India, Pal. Ind., 4, 1-35 Mathur, U.B. and Srivastava, S., 1987. Dinosaur teeth from Lameta Group (Upper Cretaceous) of Kheda District, Gujarat. J. Geol. Soc India, 29, 554-566. Matley, C. A., 1939. The coprolites of Pijdura, Central Province. Rec. Geol. Surv. India, 74, 535-547. Mohabey, D.M., 1987. Juvenile sauropod dinosaur from Upper Cretaceous Lameta Formation of Panchmahals District, Gujarat, India. Jour. Geol. Soc. India, 30, 210-216. Mohabey, D. M., 1996. Depositional environment of Lameta formation (Late Cretaceous of Nand-Dongargaon inland basin, Maharashtra: the fossil and lithological evidences. Mem. Geol. Soc. India, 37, 363-386. Mohabey, D.M., 1998 Systematic of Indian Upper Cretaceous dinosaur and chelonian eggshells. J. Vert. Pal., 18, 348-362. Mohabey, D. M., 2001. Dinosaur eggs and dung mass (fecal mass) from Late Cretaceous of central India: dietary implications. Geol. Surv. India, Spl. 64, 605-615 Mohabey, D.M. and Samant Bandana, 2003. Floral remains from Late Cretaceous faecal mass of sauropods from central India: implication to their diet and habitat. Gond. Geol. Magz., Spl. 6, 225-238. Mohabey, D.M. and Samant Bandana, 2013. Deccan Continental Flood Basalt Eruption terminated Indian Dinosaurs before Cretaceous-Paleogene Boundary. Geol. India, Spl. 1, 260-267. Mohabey, D. M., Udhoji, S. G. and Verma, K. K., 1993 Palaeontological and sedimentological observations on non-marine Lameta Formation (Upper Cretaceous) of Maharashtra, India: their palaeoecological and palaeoenvironmental significance. Palaeo-3, 105, 83-94. Mohabey, D. M., Head, J. J. and Wilson, J. A., (2011) A new species of the snake Madtsoia from the Upper Cretaceous of India and its paleobiogeographic implications. J. Vert. Pal., 31, 588-595. Novas, F.E., Chatterjee, S., Rudra, D.K. and Dutta, P.M. 2010. Rahiolisaurus gujaratensis, n. gen. n. sp., a new abelisaurid thropod from the late Cretaceous of India. In: S. Bandyopadhyay (eds.) New aspects of Mesozoic biodiversity, lecture notes in earth Sciences, 132, DOI 10, 1007/978-3-642-10311-7-3. Sarkar, A., S. K. Bhattacharya and D.M. Mohabey.(1991). Stable isotope analysis of dinosaur eggshells: Palaeoenvironmental implications, Geology, 9, 1068-1071. Srivastava, A.K. and Mankar R. 2013.Dinosaurian ulna from a new locality of Lameta succession, Salbardi area, districts Amravati, Maharashtra and Betul, Madhya Pradesh Curr. Sci., 105, 900-901. Prasad, V., Stromberg, C.A.E., Leach, A.D., Samant, B., Patnaik, R., Tang, L., Mohabey, D.M., G,S., Sahni, A., 2011. Late Cretaceous origin of the rice tribe provides evidence for early diversification in Poaceae. Nature Commun. 2:480, 1-9. Von Huene, F.B. and Matley, C.A., 1933. Cretaceous-Saurischia and Ornithischia of Central Provinces of India, Geol. Surv. India, Mem. 1, Pal. India, 21, 1-24. Waldman, M. and W.S. Hopkins. 1970. Coprolites from the Upper Cretaceous of Alberta, Canada, with a description of their microflora. Cand. Jour. Ear. Sci., 7, 1295-1303. Wilson, J.A., Paul, C.S., Bhatt, D.K., Khosla, A. and Sahni, A. 2003. A new abelisauid (Dinosauria, Theropoda) from the Lameta Formation, (Cretaceous, Maastrichtian) of India. Contrib. Mus.Pal., Uni. Michigan, 31, 1-42

106 Wilson J.A., Mohabey, D.M., Peter., S.E., and Head, J. J., 2010. Predation upon Hatchling Dinosaurs by a New Snake from the Late Cretaceous of India. PLoS Biol 8, e1000322. Wilson, J. A., D’emic Michael, D., Curry Rogers, K.A., Mohabey, D. M. and Sen, S., 2009. Reassessment of sauropod dinosaur Jainosaurus (=Antarctosaurus) septentrionalis from the. Upper Cretaceous of India. Contrib. Mus. Pal. Uni Michigan, 32, 17-40.

107

Titanosaurian sauropod dinosaurs from the Latest Cretaceous of Pakistan

Malkani, M. S.

Paleontol. Stratigr. Bran., Geol. Sur. Pakistan, Sariab Road, Quetta, 87300, Pakistan ([email protected])

Recent geological and paleontological and large bodied with stocky limbs. It has a exploration in the Latest Cretaceous strata of short and stocky tail. Sulaiman basin (Pakistan) yielded many Gspsaurus Pakistani diagnostic and significant Latest Cretaceous Previously the skull specimens titanosaurian sauropod dinosaurs which show MSM-79-19 and MSM-80-19 to Marisaurus close affinity to Gondwanan landmasses and jeffi (titanosaurian sauropod). Due to isolated far affinity to Laurasia. These discoveries put finding it is being established as holotype of the Pakistan first time in the world dinosaur Gspsaurus pakistani-a new genus and species map. Some endemic character and taxa show of titanosaurian sauropod dinosaur (Fig.1). isolation of Indo-Pakistan as big island during Gspsaurus pakistani (after Geological Survey most of the Cretaceous and its northward of Pakistan, saurus mean Lizard, species name journey. after Pakistan) is found from red muds of Vitakri Formation of Alam Kali Kakor locality Titanosaurian sauropods from the Latest of Vitakri area, Barkhan district, Balochistan, Cretaceous of Pakistan Pakistan. Holotypic specimens MSM-79-19 Khetranisaurus barkhani consists of articulated upper and lower jaws The Khetranisaurus barkhani were with teeth, palatal processes, left quadrate, plant eater, slender and medium size (Fig.1) partial quadratojugal, possibly lowermost titanosaurs. These have one holotypic and portion of squamosal, mandible rami and teeth many attributed caudals. Some vertebrae and while MSM-80-19 shows palatal bones like limb bones were located in holotypic Kinwa posterior vomerine, fused palatine and mid locality. pterygoid. The exposed part of skull and Sulaimanisaurus gingerichi dentary are pneumatic. The skull has mid line It is based on seven fragmentary but contact. The right premaxillary and right associated caudal vertebrae (long and squarish maxillary teeth are cemented on the anterior mid caudals; Fig.1). and lateral side of right dentary ramus. Left Pakisaurus balochistani dentary ramus is covered by quadrate, Pakisaurus balochistani were based quadratojugal, possible squamosal and matrix. on four associated tall caudal centra (Fig.1) Dentary symphysis seems to be weak. The and also attributed by many fragmentary, available dentary ramus shows length 12 cm, associated and articulated bones and pieces of depth 4.5-5cm and width (with splenial) 1.8 bones. cm. The anteroventral marginal shape of Marisaurus jeffi dentary is gently rounded. Dentary symphysis Marisaurus jeffi (Balochisauridae) is almost V shape or sub V shape. Palatine were thick and long necked and relatively lateral ramus is rod shaped and has narrow short tail with trispinous distalmost tail special maxillary contact. The palatal process is may be used for support to eat/mat/defend reverse V shape which is hanged/hooked by (Fig.1). small v shape dorsal palatal process. The Balochisaurus malkani ventral palatal processes are also bifurcated. Balochisaurus malkani The maximum thickness of palatal process is (Balochisauridae) were relatively most stocky 8mm and width is about 2 cm. Maxilla has 1.5 cm thick alveolus ramus and the upper/dorsal 108 portion which is about 0.5 cm thick. Preserved rostrum represents generally long, narrow and quadrate plate is about 1cm thick and 10 cm moderate shallow shape (with 400 inclinations long and 7 cm wide. On the dorsal of quadrate from horizontal). Generally this rostrum is seems to be partial squamosal which is also tilted towards right. The anterior portions of about 1 cm thick. Quadratojugal is thick about upper and lower jaws are broadly arched 1-2.5cm and dorsal process rotate at an angle forming U shape. The right and left of about 40-50 degree from anterior process of Premaxilla form a greatly elongated quadratojugal. Right premaxillary teeth are rostrocaudally belt. Laterally it has a long about 4 and available maxillary teeth are about contact with maxilla. Its each preserved fellow 5 or 6. The upper teeth row broadly arched is 8.5 cm long, and 1 cm wide on each side forming U shape. Teeth cross-sections vary measured at the cross section just behind the from circular to subelliptical. The lengths of ending of teeth row. The both fellow are about premaxillary teeth vary from 10 mm to 18 mm, 2 cm wide. It goes backward with about 400 width varies from 4mm to 6mm. The first inclinations from the anterior most point of maxillary tooth length is 28mm and width is premaxilla. There are 4 premaxillary teeth. 7-8mm. Other tooth at a distance of about 2 The shape of premaxillary anterior margin cm (from first maxillary tooth) is again long seems without step or with feeble step. The and thick like first maxillary tooth. After this premaxillary teeth are 1 cm to 2 cm. long and one or two small tooth seems to be fixed in possible maximum width is 0.4 cm. The dorsal matrix. The alternating small and large teeth process and lateral process bifurcate of may represent the replacement phenomena of maxilla at the start of antorbital fenestra. The teeth. Maxillary teeth are articulated with antorbital fenestra is starting at about 8 cm maxilla. However spacing between teeth is length from anterior most premaxilla junction. increasing toward posterior/back. Premaxillary Tentatively the antorbital fenestra started at the tooth crowns apex is slightly curved toward ending of maxillary teeth row. The teeth have lingual side. Some teeth are cone forming and little gap less than 2 mm among each other. some are blunted or having wear facet. Pulp The larger teeth are observed in the middle of cavity of 3 fragmentary teeth found in matrix teeth row i. e., the fifth and sixth maxillary associated with skull measured at base as 3mm, teeth. However distal parts of the most of the 4mm, and 7mm maximum diameter on the teeth are eroded. The length and width of basal part of crown, with total teeth thickness longest teeth is 1.5 cm and 3 to 4 mm. The 7mm, 8mm, 9mm and width 8mm, 9mm, 10 smallest teeth are less than 1 cm. There are 13 mm respectively. A tooth slenderness index is maxillary teeth. The maxillary teeth bearing 4-5. Dentary teeth are covered by anterior part is 7 cm long and preserved backward upper skull. Teeth are long, narrow, slender, portion without teeth is 4.5 cm. Backward to circular peg and pencil shaped. teeth row the upper jaw showing concavity Saraikimasoom vitakri and the lower jaw showing upward convexity. Previously the skull specimen There are anteroposteriorly parallel lamination MSM-142-4 was referred to Balochisaurus on the maxilla and premaxilla. The dorsal malkani (titanosaurian sauropod). But due to palatal processes are bifurcated forming v its isolated finding in excavation it is being shape hook. It forms a hook which supports established Saraikimasoom vitakri-a new the ventral palatal process. The ventral palatal genus and species of titanosaurian sauropod processes are also bifurcated and trends gently dinosaur (Fig.1). Saraikimasoom vitakri towards maxilla. The ventral most part of (named after Saraiki language of the area; palatal is forming vaulted shape. Ventral masoom is Urdu and Saraiki word meaning palatal flange is more than 4 cm wide, and innocent; Vitakri is host locality) is found thickness is about 1 cm. Dentary depth of from red muds of Vitakri Formation of Kinwa ramus is nearly equal and anteroventral margin Kali Kakor locality of Vitakri area, Barkhan shape is gently rounded (no chin). The anterior district, Balochistan, Pakistan. This partial portions of dentary are broadly arched forming skull includes articulated upper and lower jaws U shape. Dentary along with available consisting of left and right premaxillae, left possibly surangular measurement is 8 cm. The and right maxillae, dorsal and ventral palatal best preserved impressions of three teeth of process, left and right dentary and teeth. The right dentary are found. The impression of 109 central tooth (among these three teeth) is about after the Pashto language of local peoples, and 1.5 cm long, and 5 to 6 mm wide. The exposed species name from host Zhob district) based part of dentary rami is pneumatic with large on footprints and trackway. There is also open internal cells, showing this partial skull is danger that these trackways may be destroyed highly vascularised. Surangular at the during future construction materials required anterior portion is interpreted due to coronoid for road construction. The strike of sandstone process i. e., the convexing upward. The teeth bed is North 65o East and its dip is 70o are long and slender. Long teeth preserved in Northwest. This ichnocoenosis consists of the middle of jaw seem like 3rd to 6th while exposed more than 14 footprints, and 3 or 4 most of the tips of teeth have eroded. Teeth short trackways. The width of pes footprint is seem to be generally straight while middle to about 0.7-0.8 meter while the length is about distal part is slightly recurving towards 0.7-0.9 meter. The separation of manus and posterior/back side. Tooth crown pes is about 0.5-1m. The internal trackway cross-sectional shape at mid crown is width is about 20-25cm indicating less wide subcircular. Tooth crown is subcircular. A gauge locomotion of track maker. The tooth slenderness index seems to be 3-5. The maximum depth of footprint is more than Saraikimasoom vitakri represents possible 12cm. Some footprints show glide (slipped) dental formula 4, 13/11-17? and it gives the mark due to slippery muddy surface of thick best information for the Titanosauria. sandstone bed. These trackways of Generally the titanosaurs were considered as titanosaurian sauropods mostly trend in a bearing a Diplodocus-type skull but now northwest direction and are parallel to each Pakistan has represented moderate incline and other (Fig.1), however there are some signs of moderate long well developed skulls. opposite tracks. These are indicative of a less Nicksaurus razashahi: The associated axial wide gauge titanosaurian sauropods herd and limb elements of Nicksaurus razashahi-a composed of 3 or more individuals. The saltasaurids due to very broad caudal are exposed area is small and excavation in depth shown in Fig. 1. inclination may reveal best results. The New trackways of titanosaurian sauropod footprints belong to titanosaurs are diagnosed dinosaurs from Pakistan on the basis of large size, the oval manus The new footprints and trackways of impression and there is no indication of manus titanosaurian sauropod dinosaurs are found on claw on digit I or on any digit (Fig. 1). Three the thick sandstone bed (freshly cut for road stocky digit traces may correspond to digits II construction) of Latest Cretaceous Vitakri to IV are well observed on pes prints. These Formation of Sor Muzghai locality (300 digits are not equidimensional, and the central 57’.36”; 690 08’ 24”; northeast of Moor Pump digit (III) is largest and longest. The posterior bus stop; southeast of Bali Railway station; side of pes also shows a median concavity. also on the eastern bank of Zhob-Quetta road), This discovery is significant due to occurrence Zhob District, Balochistan (Fig.1). The of titanosaurs body fossils in coeval strata and trackmakers Pashtosaurus zhobi (genus name also in the same middle Indus/Sulaiman basin.

110 A uj

ph B mr

p C

A B C D E

Figure 7. Generalized morphology of diverse middle caudal centra of Khetranisaurus barkhani (A), Sulaimanisaurus gingerichi (B) and Pakisaurus balochistani (C) of Pakisauridae (A,B,C), and Marisaurus jeffi (D) and Balochisaurus malkani (E) of Balochisauridae (D,E) from the latest Cretaceous terrestrial strata of Sulaiman Basin, Pakistan. Figure 1. Map of Pakistan showing bone fossil localities by black circle and Sor Muzghai ichnosite by white circle. (A); holotype skull MSM-79-19 and MSM-80-19 in ventral (B) and posterior (C) views of Gspsaurus pakistani-a titanosaurian sauropod found from Alam Kali Kakor locality of Vitakri area, Barkhan district, Balochistan. D Row holotype skull MSM-142-4 in anterior, lateral, ventral and posterior views of Saraikimasoom vitakri-a titanosaurian sauropod found from Kinwa locality of Vitakri area, Barkhan district, Balochistan, footprints and trackways of titanosaurian sauropod dinosaurs (Pashtosaurus zhobi) from the Latest Cretaceous Vitakri formation of Sor Muzghai locality, Western extremity of Sulaiman basin adjoining Western Indus Suture, Zhob District, Balochistan. E (upper and lower rows) referred, associated axial and limb elements of Nicksaurus razashahi from Kinwa north locality of Vitakri area. upper row 1st column MSM-190-4n left full femur; 2nd column MSM-346-4n distal tibia stocky, MSM-345-4n distal tibia stocky, MSM-378-4n and MSM-270-4n femur sections, MSM-192-4n distal femur; 3rd column MSM-380-4n, MSM-377-4n, MSM-379-4n and MSM-438-4n humerus parts; MSM-190-4n and MSM-192-4n a pair of distal femora in ventral view, and MSM-344-4n proximal radius in 3 views; and MSM-138-4n five teeth in jaw ramus in two views. Lower row MSM-315-4n and MSM-314-4n skull and teeth fragments in matrix, MSM-313-4n chevron in three views; MSM-212-4n cervical/dorsal centrum, MSM-381-4n, MSM-382-4n and MSM-383-4n cervical centra; line drawing of Pakisauridae (A,B,C) and Balochisauridae (D,E) titanosaurian sauropods. Scale each black or white digit is 1cm.

111 New elasmobranch fauna from the Bagh Group, Narmada Valley, India - Palaeobiogeographic context

Prasad, G. V. R.1, Verma, V.2, Sahni, A.3, Priyadarshini, R. K.1 and Singh, L. R.1

1Dept. Geol., Cent. Adv. Stud., Univ. Delhi, Delhi 110007, India ([email protected]) 2D.No.56, Manawar, Dhar District, Madhya Pradesh, India 398, Mahatma Gandhi Marg, Lucknow – 226001, India

In India, until now Cretaceous Limestone (Roy Chowdhary and Sastri, 1962) elasmobranchs have been recorded from the and as such currently the Bagh Group is Albian-Turonian Karai Formation of Cauvery considered to consists of Nimar Sandstone, basin (Underwood et al., 2011), from the Nodular Limestone and Coralline Limestone Deccan volcano-sedimentary sequences (Jain (Tripathi, 2006; Jaitly and Ajane, 2013). The and Sahni, 1983; Prasad and Cappetta, 1993) Nimar Sandstone overlies the Precambrian and Turonian-Campanian Bagh Group (Verma, basement rocks with an angular unconformity. 1965; Das Sarma and Sinha, 1975). The Karai The lower part of the Nimar Sandstone was Formation has yielded squaliform interpreted to have been deposited in a (Protosqualus sp.), hexanchiform freshwater environment, while the upper part (Gladioserratus magnus, ?Notidanodon sp.) was considered as a shallow marine sequence and lamniform sharks (Cretalamna (Tripathi, 2006) or deposited in an intertidal to appendiculata, Dwardius inner subtidal environment (Singh and sudindicus, ?Eostriatolamia sp., Squalicorax Srivastava, 1981). The overlying Nodular aff. baharijensis, Cretodus longiplicatus) Limestone and Coralline Limestone yielded which indicated cool-water depositional marine invertebrate fossils such as gastropods, environment and antitropical distribution bivalves, brachiopods, echinoids, corals, (Underwood et al., 2011). Only skates (Raja) bryozoans, ammonites, foraminifers, algae and and rays (Igdabatis, Rhombodus) have been trace fossils indicating shallow marine reported from the Upper Cretaceous environment of deposition for these units. A (Maastrichtian) Lameta Formation (Jain and wide range of ages from Albian to Campanian Sahni, 1983) and the Deccan intertrappean beds have been suggested for the Bagh Group (Prasad and Cappetta, 1993). Previously, shark (Chiplonkar et al., 1977; Jafar, 1982; Taylor teeth were documented from the uppermost and Badve, 1992; Kennedy et al., 2003; gritty sandstone (oyster bed) of the Nimar Gangopadhyay and Bardhan, 2007). In a more Sandstone from a number of localities, recent synthesis of the age of Bagh Group, particularly from the western part of lower Jaitly and Ajane (2013) suggested Turonian, Narmada valley (Verma, 1965; Das Sarma and Cenomanian, and Coniacian ages for the Nimar Sinha, 1975). Sandstone, Nodular Limestone, and Coralline The Cretaceous sediments of lower Limestone, respectively. Narmada valley, generally known as ‘Bagh Though as many as 12 species of Beds’, occur as detached outcrops following sharks were reported from the upper part of the the erosion of overlying Lameta Formation and Nimar Sandstone, no detailed descriptions are Deccan lava flows. Bose (1884) divided the available, the illustrations are poor, and the Bagh Beds into formal lithostratigraphic units identifications were based on limited and viz., Nimar Sandstone, Nodular Limestone, poorly preserved specimens. During recent Deola-Chirakhan Marl, and Coralline field investigations of the Bagh Group, a large Limestone in this order of superposition. number of shark teeth have been recovered However, Deola-Chirakhan Marl was later from the upper part of the Bagh Group. The considered as a weathered product of Nodular new fossil material recovered from a green 112 sandstone (oyster bed) capping the Coniacian geographic distribution with fossil records Coralline Limestone is the first record of known from North America, Europe, elasmobranchs from this formation. So far, Madagascar and Africa. Scapanorhynchus, more than 500 teeth have been collected in the Cretalamna, and Squalicorax are known to field by surface prospecting, predominantly occur abundantly both in shallow and deep from two sites viz., Phuti Bawri and Rati Talai water environments. On the other in Dhar District, Madhya Pradesh (India). hand ?Cretoxyrhina mantelli, and Ptychodus sp. Preliminary identification reveals the presence are restricted to deep water environments. The of five elasmobranch genera. Scapanorhynchus occurrence of these taxa in association with raphiodon, Cretalamna appendiculata, Scapaonorhynchus, Cretalamna, and Squalicorax pristodontus, ?Cretoxyrhina Squalicorax in a sandstone horizon implies mantelli, and Ptychodus sp. A vast majority of that ?Cretoxyrhina and Ptychodus might have the specimens recovered belong to the genus been reworked into shallower environments. Scapanorhynchus. The elasmobranch fauna from the Acknowledgements: GVRP is thankful to the Bagh Group is not as diverse as that of Department of Science and Technology (DST), Albian-Turonian Karai Formation of the Govt. of India, New Delhi for a grant under Cauvery basin in South India. The selachian J.C.Bose National Fellowship to carry out this fauna from the Karai Formation has an work. RKP and LRS acknowledge the financial antitropical distribution (Underwood et al., support from the University of Delhi, Delhi in 2011). In contrast, the selachian fauna from the the form of University Fellowship. upper part of Bagh Group demonstrate wide

References: Bose, P.N. (1884). Geology of Lower Narbada Valley between Nimavar and Kawant. Mem. Geol. Surv. India 21: 1-72. Chiplonkar, G.W., Ghare, M.A. and Badve, R.M. (1977). Bagh Beds – their fauna, age and affinities: a retrospect and prospect. Biovigyanam 3: 33-66. Das Sarma, D.C. and Sinha, N.K. (1975). Marine Cretaceous Formation of Narmada valley, Bagh Beds, Madhya Pradesh and Gujarat. Palaeontol. Indica (N.S.) 42: 10. Gangopadhyay, T.K. and BARDHAN, S. (2007). Ornamental polymorphism in Placenticeras kaffrarium (Ammonoidea; Upper Cretaceous of India): Evolutionary implications. In: N.H. Landman, R.A. Davis and R.H. Maps (Eds.), Cephalopods: Present and Past. New Insights and fresh perspectives. Springer, pp.97-120. Jafar, S.A. (1982). Nanoplankton evidence of Turonian transgression along Narmada Valley, India and Turonian-Coniacian boundary problem. J. Pal. Soc. India 27: 17-30. Jain, S. L. and Sahni, A. (1983). Some Upper Cretaceous vertebrates from central India and their paleogeographical implications, in Maheshwari, H. K., ed., Cretaceous of India: Indian Association of Palynostratigraphers Symposium, Lucknow, p. 66-83. Jaitly, A.K. and Ajane, R. (2013). Comments on Placenticeras mintoi (Vredenburg, 1906) from the Bagh Beds (Late Cretaceous), Central India with special reference to Turonian Nodular Limestone horizon. J. Geol. Soc. India 81: 565-574. Kennedy, W. J., Phansalkar, V.G. and Walaszczyk, I. (2003) Prionocyclus germari (Reuss, 1845), a Late Turonian marker fossil from the Bagh Beds of central India. Cret. Res. 24, 433-438. Prasad, G. V. R. and Cappetta, H. (1993). Late Cretaceous selachians from India and the age of the Deccan Traps. Palaeontology 36: 231–248. Roy Chowdhary, M.K. and Sastri, V.V. (1962). On the revised classification of the Cretaceous and associated rocks of the Man River section of lower Narbada Valley. Rec. Geol. Surv. India 91: 283-301. Singh, S.K. and Srivastava, H.K. (1981). Lithostratigraphy of the Bagh Beds and its correlation with Lameta Beds. J. Pal.Soc. India 26: 77-85. Taylor, P. and Badve, R.M. (1995). A new cheilostome bryzoan from the Cretaceous of India and Europe: A cyclostome homeomorph. Palaeontology 38: 627-657. Tripathi, S.C. (2006). Geology and evolution of the Cretaceous Infratrappean Basins of Lower 113 Narmada Valley, western India. J. Geol. Soc. India 67: 459-468. Underwood, C.J., Goswami, A., Prasad, G.V.R., Verma, O. and Flynn, J.J. (2011). Marine vertebrates from the ‘Middle’ Cretaceous (Early Cenomanian) of South India. J. Vertebr. Paleontol. 31: 539-552. Verma, K. K. (1966). On the fossil shark-teeth from the Bagh Beds of Amba Dongar area, Gujarat State. Current Sci, 34: 289-290.

114 Description of the Late Cretaceous Crocodylomorph, Shamosuchus from Mongolia

Takekawa, A.1, Hirayama, R.2 and Aoki, R.3

1Grad. Schl. Internat. Cult. Comm. Stud., Waseda Univ., 169-8050, Tokyo, Japan ([email protected]) 2Schl. Internat. Liberal Stud., Waseda Univ., 169-8050, Tokyo, Japan 3Yokosuka City, Japan

Crocodilians first appeared on the morphology and phylogeny of Shamosuchus Earth during the Triassic period, about 235 will be discussed. million years ago. Cretaceous period is an Shamosuchus djadochtaensis was important era for crocodilians since it is when initially described by Mook (1924) based on an the modern crocodilian, Eusuchia, began to incomplete skull and mandible discovered in evolve. As Shamosuchus is a genus, which the Djadochta Beds of lower Cretaceous, belongs to the basal Eusuchia, it plays a Mongolia, pointing out on its distinctive significant role as an intermediate form characters such as, absence of mandibular between the mesosuchians, more primitive fenestra, noticeable posteroexternal process of group, and the eusuchians. squamosal and exoccipital, which comprises a significant portion of the condyle. Thenceforth, six species those belong to the same genus were discovered from Mongolia and Uzbekistan including S. borealis, S. major, S. occidentalis, S. tarsus, S. ulanicus, and S. karakalpakensis (Efimov, 1975, 1981, 1982, 1983,1988; Nesov et al., 1989). While S. occidentalis was synonymized with S. borealis, species those originally belonged to the genus Paralligator, such as, Paralligator ancestralis and Paralligator gradilifrons (Konzhukova, 1954) from the Late Cretaceous of Mongolia, were later considered to be Shamosuchus along with Paralligator sungaricus (Sun, 1958) from the Early Cretaceous of China. Yet, as recently FIGURE 1. RHg122 before preparation indicated by Storrs and Efimov (2000), some of Shamosuchus is a neosuchian genus the species of this genus may be synonymous. with sufficient amount of materials especially Recently, Pol et al. (2009) described a more discovered from Mongolia. In spite of the complete specimen of the type species, number of specimens, much was unknown until Shamosuchus djadochtaensis. The referred recently, a more complete specimen of the specimen preserves nearly complete skull and holotype species, Shamosuchus djadochtaensis, mandible, all eight cervical vertebrae, three was described by Pol et al. (2009). Furthermore, dorsal vertebrae with four right dorsal ribs, five an articulated specimen discovered in anterior caudal vertebrae, two haemal arches, Mongolia, RHg122, indicates additional complete right humerus, distal half of the left information regarding this genus, through its humerus showing association with complete well-preserved vertebrae and articulated left radius, proximal portion of the right radius, osteoderms. While comparing with the complete left ulna, fragmentary right ischium, previous description and related taxa, partial right femur, complete right fibula, 115 partial left fibula, single left metatarsal and vertebrae. In addition, left femur, left fibula, phalanx. Furthermore, osteoderms partial partial right humerus, partial left radius, left articulated were also reported. Through this ulna, dorsal and ventral osteoderms are present. additional information, distinctive characters RHg122 shows characters including were diagnosed including the autapomorphic autapomorphic features of Shamosuchus such features of this genus such as the depression as the lacrimal and prefrontal ridge, elevated constrained by the ridge at the lacrimal and frontal margin which contributes to the prefrontal, groove along the lateral edge of the supratemporal fossa, shallow and broad posterolateral process of the squamosal, ridge squamosal groove, closed external mandibular at the narrow anterior process of the fenestra, lateral longitudinal groove formed by quadrojugal, and overlapping dorsal angular and surangular, procoelous cervical osteoderms with convex anterior margin, vertebrae, amphicoelous caudal vertebrae, bearing keels only at the posterior portion. In overlapping dorsal osteoderms with convexities addition, through shared features of sagittal at the anterior margin and exceptional keel only ridge at the frontal, merged openings for the at the posterior portion, and appendicular cranial nerves IX-XI, posteriorly flaring osteoderms. As sufficient quantity of posterior palatine bar, and ridge on the lateral surface of cervical osteoderms and anterior dorsal the angular, with neosuchian genus from late osteoderms are preserved, the configuration of Early Cretaceous Nenjiang Formation from osteoderms is clearly seen. Two articulated China, Rogosuchus nonganensis (Wu et al, rows with deeply ornamented pits and 2001a), S. djadochtaensis was placed as its prominent keels at the posterior portion sister group. develop along the cervical region, and forms R. nonganensis, was discovered by four lateral osteoderms by the dorsal vertebrae. Petroleum Geological Survey of the Song-Liao Neurocentral suture provides relevant Basin from the Nong’an Country in 1958, and information regarding aging since crocodilian characterized by a unique set of fossae of the vertebral column shows a distinctive pattern of lateral portion of the flattened dorsal surface of caudal to cranial sequence during Ontogeny maxilla, concavity of frontal and parietal, and (Brochu, 2010). As for S. djadochtaensis widely spaced crown. It is distinguished from according to Pol et al, 2009, major neurocentral Shamosuchus sungaricus, which was originally sutures are completely closed on the lateral assigned to ‘Paralligator’ sungaricus (Sun, surface and merely the internal surface of the 1958), by the pit and the keel on dorsal eighth cervical vertebra is visible, where as osteoderms as well as the proximal shaft of most of the anterior caudal vertebrae are not femur, since cranial material lacks for S. fused for RHg122. This suggests that RHg122 sungaricus. is a juvenile individual reaching to RHg122 preserves wide variety of approximately one meter. information especially regarding vertebrae and In relation to S. djadochtaensis, the osteoderms along with partially displaced skull. taxon of Shamosuchus will be discussed in Most of the dorsal vertebrae remain, together relation to the species described by Efimov, with one cervical vertebra, one sacral vertebra, while describing the characteristic of RHg122 eight caudal vertebra and three isolated and suggesting on the importance of ontology.

Reference: Brochu, C. A. 1996. Closure of neurocentral sutures during crocodilian ontogeny: implications for maturity assessment in fossil archosaurs. J. Vert. Paleontol. 16: 49–62. Efimov, M.B. 1988. Fossil crocodiles and champsosaurs of Mongolia and the USSR. Trudy Sovmestnoi Sovetsko-Mongol’skoi Paleontologicheskoi Ekspeditsii 36: 1–108. Mook, C.C. 1924. A new crocodilian from Mongolia. Amer. Mus. Novitates 117: 1–5. Pol, D., Turner, A. H. & Norell, M. A. 2009. Morphology of the Late Cretaceous crocodylomorph Shamosuchus djadochataensis and a discussion of neosuchian phylogeny as related to the origin of Eusuchia. Bull. Amer. Mus. Nat. Hist. 324: 1–103. Storrs, G.W., and M.B. Efimov. 2000. Mesozoic crocodyliforms of north-central Eurasia. In M.J. Benton, M.A. Shishkin, D.M. Unwin, and E.N. Kurochkin (editors), The age of dinosaurs in Russia and Mongolia: 402–419. Cambridge: Cambridge University Press. 116 Sun, A.-L. 1958. A new species of Paralligator from Sungarian Plain. Vertebrata PalAsiatica 2: 277–280. [in Chinese, English summary] Wu, X.-C., Z.-W. Cheng, and A.P. Russell. 2001a. Cranial anatomy of a new crocodyliform (Archosauria: Crocodylomorpha) from the Lower Cretaceous of Song-Liao plain, northeastern China. Canadian J. Earth Sci. 38: 1653–1663.

117 Cranial morphology of a giant marine side-necked turtle (Pleurodira: Bothremididae) from the upper Cretaceous of Morocco

Yoshida, M.1 and Hirayama, R.2

1Grad. Schl. Internat. Culture Comm., Waseda Univ., 169-8050,1-6-1, Nishi-waseda, Shinjuku-ku, Tokyo ([email protected]). 2Schl. Internat. Liberal Stud., Waseda Univ., 169-8050,1-6-1, Nishi-waseda, Shinjuku-ku, Tokyo.

Sea turtles (Cryptodira: Chelonioidea) Morocco. Its skull shows jugal pits which are are the only turtle group adapted to life in one of the most characteristic synapomorphies oceanic environments today. However, during in the tribe Bothremydini. Associated with the Cretaceous and Paleogene, they were not skull and jaw, there are left forelimb bone the only turtle in the marine ecosystem. There elements and several peripheral plates of the were several marine side-necked turtles carapace are preserved. We refer the aquatic (Pleurodira: Bothremididae) reported (Gaffney adaptations of Bothremydini turtles using its et al.,2006) from North America, North and forelimb anatomy in comparison with extant Central Africa, Europe and India. Both turtles. cryptodiran and pleurodiran marine turtles Stupendemys geographicus from the successfully survived the K/P boundary Paleogene of Venezuela (Wood, 1976) with without significant damage in their 250cm long carapace is the largest known diversification at Paleogene era. Nonetheless, pleurodiran turtle, and Puentemys comparing to cryptodiran sea turtles, these mushaisaensis from the Paleogene of Columbia marine side-necked turtles are remained is the largest known bothremidid turtle with unclear in their marine adaptation in life. 151cm long carapace (Cadena et al.,2012). ryptodira sea turtles, these marine side-necked RHg 519 remains remarkable in size of its skull turtles are remained unclear in their aquatic (at least 30 cm long). adaptation in life. The functional morphology of unique In this presentation, we report a giant jugal and mandibular pits of the lower jaw will side-necked turtle of the family Bothremydidae be discussed in the poster presentation. from the Maastrichitian phosphates bed of

Figure: Ventral and dorsal views of WSILS-RHg519 before preparation. Scale-bar is 10 cm long.

118 References: Cadena, E. A., D. T. Ksepka, C. A. Jaramillo, and J. I. Bloch. 2012.New pelomedusoid turtles (Testudines, Panpleurodira) from the late Palaeocene Cerrejo´n Formation of Colombia and implications for phylogeny and body size evolution. J. System. Palaeontol., 10:313–331. Gaffney, E. S., Tong, H. and Meylan, P. A. 2006. Evolution of the side-necked turtles: the families Bothremydidae, Euraxemydidae, and Araripemydidae. Bull. Amer. Mus. Nat. Hist. 300, 1–698. Gaffney, E. S. and Zangerl, R. 1968. A revison of the chelonian genus Bothremys (Pleurodira: Pelomedusidae). Fieldiana: Geology 16, 193–239. WOOD, R. C. 1976. Stupendemys geographicus, the world’s largest turtle.Breviora, 436:1–32.

119 Cranial morphology of Mesodermochelys (Testudines; Dermochelyidae) from the Upper Cretaceous Japan, with special reference to its feeding habitat

Hirayama, R.

SILS, Waseda Univ., Nishiwaseda 1-6-1, Shinjuku-ku, Tokyo 169-8050, Japan ([email protected])

Mesodermochelys unduratus is a from living leatherback turtle, Dermochelys basal dermochelyid (family Dermochelyidae) coriacea, mainly catching jellyfishes. turtle from the Late Cretaceous of Japan An isolated partial skull (HMH (Hokkaido, Hyogo, and Kagawa Prefectures), 151807, housed in the Historical Museum of characterized by especially massive peripherals Hokkaido, Sapporo) from the Santonian epoch of carapace (Hirayama et al., 1996; Sato et al., of Tomamae-cho, Hokkaido Prefecture have 2012). Although postcranial remains of this been prepared by formic acid, showing detailed taxon are rather abundant in the type locality, structures of braincase (Hirayama et al., 2007). Hobetsu district of Mukawa-cho, Hokkaido Some derived features such as the well Prefecture, its cranial element had been hitherto developed processus trochelaris oticum are poorly unknown except for lower jaw. shared by both the Maastrichtian and Santonian A nearly complete skeleton of M. materials. Thus, this Santonian skull is unduratus was collected from the Kitaama identified as Mesodermochelys sp. This skull Formation of Izumi Group (early shows the following derived features; 1) Maastrichtian) of Sumoto City of the foramen posterius canalis carotici interni Awajishima Island, Hyogo Prefecture in 2009 incompletely covered by bones on ventral by Mr. H. Matsumoto and Kishimoto surface of pterygoids as in Protostegidae; 2) (Hirayama et al., 2014). This material contains basisphenoid has a V-shaped crest on its the first known perfect skull, about 160 mm ventral surface, deeply emarginated from the long as preserved, of M. unduratus. This posterior as in Cheloniidae. Another isolated specimen shares some derived characters, such skull of Mesodermochelys sp. was recently as extremely large parietal bone and the loss of collected from also the Santonian of scute sulcus, with Cenozoic dermochelyids. Tomamae-cho. These cranial features suggest Both upper and lower triturating surfaces have Mesodermochelys was a mosaic of different prominent lingual ridges. These characters families, whereas its limb morphology shows suggest M. unduratus fed on omnivorous diets, dermochelyid affinity. including hard shell animals, largely different

References: Hirayama, R. 2007. Cranial morphology of Mesodermochelys (Chelonioidea; Testudines) from the Late Cretaceous of Japan. J. Vert. Paleontol., 26, Suppl. to No.3, Abst. Pap., 83A. Hirayama, R. and Chitoku, T. 1996. Family Dermochelyidae (Superfamily Chelonioidea) from the Upper Cretaceous of North Japan. Trans. Proc. Palaeontol. Soc. Japan, N. S., 184:597-622. Hirayama, R., Kishimoto, S., Saegusa, H. and Ikeda, T. 2014. Skulls of fossil marine turtles from the Late Cretaceous Izumi Group in Sumoto, Hyogo Prefecture, western Japan. Abstracts of the 2014 Annual Meeting of the Palaeontological Society of Japan, p. 21. (in Japanese) Sato, T., Konishi, T., Hirayama, R. and Caldwell, M. 2012. A review of the Cretaceous marine reptiles from Japan. Cretaceous Research 37: 319-340.

120 Discovery of the first dinosaur fossils from Malaysia: spinosaurid theropod teeth from the non-marine Cretaceous of Pahang

Sone, M.1, Hirayama, R.2, Teng, Y. H.1, Yoshida, M.2, Komatsu, T.3

1Department of Geology, University of Malaya, Kuala Lumpur 50603, Malaysia ([email protected]) 2School of International Liberal Studies, Waseda University, Tokyo, Japan 3Faculty of Science, Kumamoto University, Japan

As released at a press conference held display the ‘globular’ or veined micrornament in Kuala Lumpur on 18 February 2014, our over the surface, typical of spinosaurid teeth. international team of The best preserved tooth UM10575 is about 23 geologists/palaeontologists from Malaysia and mm long and 10 mm wide in preserved Japan has discovered several isolated teeth of condition; it was originally longer, as its crown carnivorous dinosaur(s) from the state of tip has been lost. Pahang, Peninsular Malaysia. This is the first Besides the spinosaurid material, some confirmation of dinosaur remains, and even of fossils of fresh-water bivalves and fish teeth any Mesozoic terrestrial vertebrates, in have also been found; the fish teeth belong to Malaysia. hybodont sharks and bony fish. Similar A find of a dinosaur fossil, despite bivalves and fish faunas have been known from decades of searching, had long been wanted in the Early Cretaceous of Thailand. Some trace Malaysia since such fossil was already fossils of grazing/crawling trails (of unknown confirmed in the Khorat Group of the animals) are also present. neighbouring country Thailand some 40 years No palynological age is determined for ago. Jurassic–Cretaceous non-marine sediments, the fossil-bearing sediment; nevertheless, most importantly the Tembeling Group, are considering from the occurrence of the widely distributed in the interior of Peninsular spinosaurid remains and associated Malaysia, and this has traditionally been non-dinosaur fossils, it is interpreted to be correlated and compared to the Khorat Group. Early to early Late Cretaceous in age. The Potential of a local dinosaur deposit has present find extends known distribution of therefore been undoubted. Our team has started Asian spinosaurids, and this marks, so far to make expeditions to targeted areas since defined, the possible southeasternmost 2012, and has now achieved the first mission. occurrence of dinosaurs in Cretaceous Asia, as The present find is a landmark in natural in the southern end of Sundaland. history of Malaysia; it is described in the local The location of the dinosaur fossil site media as “a small find, a big discovery”. has been kept confidential, and it will not be The teeth are identified to be of disclosed until the local government takes spinosaurid theropod, often known as a largely necessary measures for protection and piscivorous (fish-based diet) and/or conservation of the area. A potentially large semi-aquatic predatory dinosaur. Most of the fossil deposit is expected to remain unearthed, well-preserved teeth have sharp vertical ridges and we have currently tried to find the best plan and serrated carinae with minute denticles, and to cope with the situation.

121

Poster session 5-6 September 2014

122 Land-ocean linkage: Correlation, sedimentology and paleoenvironments

P1: The Lower Cretaceous deposits of southeastern Transbaikal

Kurilenko, A. V. and Yadrishchenskaya, N. G.

Public corporation «Chitageolsyomka», 672000, Chita, Russia ([email protected])

Introduction and tuffaceous-terrigenous deposits Southeastern Transbaikal in Eastern (Turga-Haranor, West-Urulunguy and Daur Siberia extends from west to east from the depressions). The Gazimur-Argun facial zone is middle reaches of the Onon River to the upper dominated by volcanogenic rocks which are reaches of the Amur River. Lower Cretaceous deposited in the several volcanic cycles deposits are widely distributed in the (East-Urulunguy, South-Argun, North-Argun, intermountain rift depressions. The lower part of Urov-Motogor and others). We consider only them was classified as Turga Suite and upper the Lower Сretaceous deposits of the Turga part as Kutya Suite for all region by previous zone must be named as Turga Suite. Its researchers (Ozersky et al., 2001, Rutshtein et al. stratotype is situated in the Turga-Haranor 2001 and others). In our mind there are two depression. The upper part of Lower Сretaceous types of sections in the lower part of deposits both zones corresponds Kutya Suite. Southeastern Transbaikal Lower Cretaceous Here we present new information from deposits, each consists different rocks. They investigations of Сretaceous stratigraphy in the were divided on the two facial zones by authors Transbaikal and summarize previous (fig.). One of them called Turga zone has stratigraphic and paleontological data (The formations which are composed of terrigenous Decision... 1994, Ozersky et al. 2001, Rutshtein et al. 2001, Kurilenko et al. 2002, Shatkov et al. 2010, Yadrischenskaya et al. 2010 and others).

Results of investigations Lower Сretaceous of the Turga zone Lower Сretaceous deposits of the Turga zone (fig.) are comparatively homogeneous in lithologic composition and characterized by very numerous remains of fauna. They bed in discordance on the Middle-Upper Jurassic volcanogenic rocks and are named Turga Suite. The stratotype of the Suite is described by S.A. Muzylev on the right bank of the Turga River (the Turga-Haranor depression). This section consists of terrigenous rocks ("paper" or "fish" slate) with numerous organic remains which have been known since the mid-19th century. Now this section corresponds with the upper part of Suite. The lower part of section of the Turga Suite in the Turga-Haranor hollow (80-120 m) 123

Fig. Scheme of rift depressions in the southeastern Transbaikal consists of conglomerates, tuff conglomerates, cerebriformis Naum. et Il., Vitreisporites gravelstones, sandstones, aleurolites, argillites pallidus (Reis.) Nilson. и др. with rare fishes and mollusks Limnocerena, The Upper Turga Subsuite (630 m) has rarely basalt covers (alternating currents of sandstones, aleurolites, tuffaceous sandstones trachyandesite-basalts and trachybasalts). In the and aleurolites, gravelstones, rare base of basalt covers brecciated lavas and clastic conglomerates, tuffas of rhyolites, zeolite lavas are situated. This part of section was sandstones. A complex of fossil as follows: named Lower Turga Subsuite (Ozersky et al. fishes Stichopterus sp., Irenichthys sp.; 2001, Rutshtein et al. 2001). mollusks Limnocyrena wangshihensis (Grabau), The upper part of the section (400-900 L. cf. sibirica (Ramm.), Probaicalia cf. m) is characterized by finer granulometric elongata Mart., Valvata sp.; ostracodes composition. Only terrigenous rocks are located Darwinula cf. nimia Sin., D. cf. contracta in the part. Interbedded argillites and aleurolites Mand.; flora Archaeolarix argunensis Tesl., prevail, inequigranular sandstones are rarely Pityospermum sp., Pseudolarix sp., Baisia presented. In the base of the section low-width hirsuta Krassil., Kutiella transbaicalica Srebr. layers of conglomerates are known. Number of The covers of basalts are timed the great clastic rocks increases to the sides of the Upper Turga Subsuite of the Torey hollow. The basin. This part of the section more corresponds absolute age of them identified of K-Ar method of the Turga Suite in its first understanding. We are 129 - 119 Ma (Yadrischenskaya et al. 2010). consider this part of the section should be named Upper Turga Subsuite. Lower Сretaceous of the Gazimur-Argun It is characterized by very numerous zone remains of the freshwater fauna and flora. The Depressions located in the assemblage contains the remains of insects Gazimur-Argun area (fig.) were made up by Ephemeropsis trisetalis Eichw., Coptoclava facialy variable tuffaceous-terrigenous deposits longipoda Ping, Mesogyrus striatus Ponom., and effusive rocks trachybasalt-trachyrhyolite Terrindusia reisi (Cock.), Ostracindusia formation. Lower Сretaceous rocks were sibirica Vial., Folindusia turga Suk.; fishes deposited in the several volcanic cycles. Their Lycoptera middendorfii Mull., Stichopterus thickness is 2100-2800 m. woodwardii Reis.; conchosrtacan Bairdestheria In our mind Gidar and Godimboy middendorfi (Jones), Estherites dahuricus Suites can be identified in this area. The (Tshern.); mollusks Calba obrutschewi (Reis), stratotype of the Gidar and Godimboy Suites Viviparus fusistomus Chi Ping; ostracodes was described in the Gidar hollow. The most Ussuriocypris ussurica Mand., flora complete their section is situated in the Pseudolarix erensis Krassil., Baisia hirsuta Urov-Motogor depression. Krassil., Otozamites lacustris Krassil. and The lower part of the Gidar Suite others. (750-1400 m) is characterized by covers of The most complete section of intermediate and basic rocks, their tuffs and Cretaceous deposits is in West-Urulunguy volcanic breccias, rare terrigenous rocks. In the depression. It differs from the section described base of the Suite tuffaceous conglomerates above a little. There are more tuffaceous overlie. Lavas and tuffs of rhyolite are observed deposits, rocks with carbonate cement and above. layers of limestones. Authors have studied this In the base of upper part of the Gidar section on borehole which has depth 1607 m. Suite (to 600 m) we can see basic and The Lower Turga Subsuite (270 m) is intermediate volcanogenic rocks with beds of presented by breccias, conglomerates, sandstones, tuffaceous sandstones and gravelstones, sandstones, aleurolites and rare conglomerates. The tuffaceous, sedimentary tuffas of rhyolites. The fossil assemblage has rocks and acidic effusive rocks make up upper. mollusks Valvata transbaicalensis Mart.; flora The assemblage of the Suite contains Archaeolarix argunensis Tesl., Pseudolarix sp., the remains of insects Ephemeropsis trisetalis Brachyphyllum sp. and palynocomplex Eichw., Uroperla karabonensis Sinitsh., Neoraistrickia truncata (Cooks) Pot., Positocoris sibiricus Yu.Pop., Coptoclava Leiotriletes pallescens Bolch., Camptotriletes longipoda Ping., fishes Lycoptera middendorffii Müll., Stichopteris reissi Jak.; conchosrtacan 124 Bairdestheria middendorfi (Jones), B. sinensis mainly sandstone-aleurolite composition. In the (Chi), B. elongata (Kob. Et Kus), Brachygrapta upper part interbedded aleurolites and argillites curta Novoj., Defretinia asiatica (Novoj. et dominate, layers of sandstones are rare. Beds of Kap.), D. argunica Novoj.; mollusks carbon shale and brown coal are characterized Limnocyrena wangschihensis (Grab.), for Suite. It consists of brown coal deposits. Arguniella uruljunguica Kol.; ostracodes There are fossil remains in the Kutya Daurina eggeri Sin., Torinina divina Sin.; flora Suite: mollusks Leptesthes angulatus Kol., Equisetum cf. argunense Srebr., Sphenobaiera Limnocyrena ovalis (Ramm.), L. hupehensis angustiloba (Heer) Fl., Archaeolarix (Grab.), Unio obrutschewi Mart., flora argunensis Tesl., Pseudolarix sp. and others. Equisetum argunense Srebr., Birisia The absolute age of the lower part of onychioides (Vassil. et K.-M.) Samyl., the Gidar Suite is identified as 127-138 Ma Coniopteris prynadae Srebr., Nilssoniopteris aff. (Kurilenko et al. 2002, Shatkov et al. 2010). prynadae Samyl., Ginkgo ex gr. huttonii (Stern.) The Godimboy Suite (to 850 m) is Heer, Sphenobaiera aff. longifolia (Pom.) characterized by interbedded sedimentary and Florin, Pseudotorelia kharanorica Bugd., volcanogenic rocks of basic and acidic Pagiophyllum sp. and others, palynocomplex of composition. There are also two full rhythms Lower Cretaceous. which start basic rocks and finish acidic and one represented only basic volcanic rocks. Summary Conchosrtacan Bairdestheria sp., The lower part of Southeastern Estherites sp., mollusks Limnocyrena rotunda Transbaikal Lower Сretaceous deposits are Mand., L. retrorostrum (Grab.), L. represented by two lithofacies of the geological wangschihensis (Grab.), Daurinia marginata section: terrigenous and tuffaceous-terrigenous (Kol.), D. ovalis Kol., Unio grabaui Mart., deposits (Turga facial zone, Turga Suite) and Viviparus sp., Planorbis sp., ostracodes predominantly volcanogenic rocks Ussuriocypris sp., Limnocypridea modesta Sin., (Gazimur-Argun facial zone, Gidar and Daurina eggeri Sin., insects Folindusia Godimboy Suites). For the upper part of Lower retratata Suk., fishes Lycoptera sp., flora Сretaceous (Kutya Suite) terrigenous coal Equisetum aff. toromense (E. Leb.) Srebr., E. cf. deposits without volcanogenic rocks are semenenses Srebr., Scleropteris dahurica Pryn., characterized. All strata have abundant fossil Neozamites verchojanensis Vachr., Ginkgo ex remains. gr. digitata (Brongn.) Heer, Pseudotorellia ex gr. ensiformis (Heer) Dolud., Schizolepis Acknowledgements burjatica Srebr. characterize Godimboy Suite. The authors are grateful to N. Chaban, The Kutya Suite beds on the Turga and the director of “Chitageolsyomka” for constant Godimboy Suites in discordance. It has only support of our investigations and thank E. terrigenous coal deposits, which are situated in Bugdaeva, Ch. Kolesnikov, G. Martinson, A. Turga-Haranor, Daur, South-Argun and Oleynikov, Yu. Popov, A. Ponomarenko, N. East-Urulunguy hollows. The stratotype is Podlesnich, S. Sinitsa, N. Sinichenkova, I. described by Y.P. Pistsov on a core hole in Srebrodolskaya, E. Sychevskaya, E. Trusova, V. South Argun depression (Pistsov 1966). The Yakovlev for their identifications. This work lower part of Suite consists of sandstones, was supported by E. Bugdaeva. conglomerates and breccia, the middle has

References: KURILENKO, A.V., KOTLYAR, G.V., KULKOV, N.P. et al. 2002. Atlas of fauna and flora of Paleozoic-Mesozoic in the Transbaikal. 714 pp. Novosibirsk (in Russian). OZERSKY, A.F., KRIVICKY, A.V., VINNICENKO, E.L. et al. 2001. The State geologic map of Russian Federation of scale 1:200000. List M-50-VI (Bol. Zerentuy). Publishing house VSEGEI. 168 pp. (in Russian). PISTSOV, YU.P. 1966. The stratigraphy of the Upper Mesozoic freshwater-continent deposits of Eastern Transbaikal. Nedra, Moscow. 20 pp. (in Russian).

125 THE DECISIONS of the forth regional stratigraphic conference of Precambrian and Phanerozoic of the Far East south and Transbaikal (Chabarovsk, 1990). 1994. 124 pp. Chabarovsk (in Russian). RUTSHTEIN, I.G., BOGACH, G.I., VINNICHENKO, E.L. et al. 2001. The State geologic map of Russian Federation of scale 1:200000. List M-50-IX (Kalanguy). Publishing house VSEGEI. 156 pp. (in Russian). SHATKOV, G.A., BEREZHNAYA, N.G., LEPECHINA, E.N. et al. 2010. U-Pb (SIMS SHRIMP-II) age of volcanic rocks of Tulukuy caldera (Strelstsovsky uranium ore, Eastern Transbaikal). Report RAS P. 587-592 (in Russian). YADRISCHENSKAYA, N.G., KURILENKO, A.V., KOROSTOVSKY, R.A., RAITINA, N.I. 2010. New data in studying of the Torejsky hollow (Eastern Transbaikal). Ulyanovsk. P. 356-360 (in Russian).

126 P2: CRETACEOUS OF MONGOLIA

R. Barsbold and Y. Khand

Paleontol. Cent. Mongolian Acad. Sci., Enkhtaivan Avenue 63, Ulaanbaatar 13343, Mongolia

Non-marine Cretaceous of Mongolia and yielding a lot of the fossil material too, is is one of the unique phenomena in the the most similar to the Mongolian geological history of Asia. In comparison with Cretaceous.But the area of the Mongolian Gobi the Cretaceous of other areas the Mongolian Desert with wide-spread Upper Cretaceous is Cretaceous differs by a high level of much smaller than the Upper Cretaceous the non-marine features, although the probable areas of North America. Though a density of brackish-water deposits were spread in the fossil contents, especially connected with the corresponding geological formations, dinosaur burials, seems to be more high (Ryan, especially in the south-east of the country. The 2013; Currie, 2014) per the comparable square Mongolian Cretaceous is characterized by unit in Mongolia. respectively completeness of the stages over Non-marine Lower Cretaceous is the territory of the country, although the real wide-spread in Mongolia. In comparison with geological formations have been divided into the Upper Cretaceous, sparcely distributed many separate parts and until now needed to be mainly in the southern part of the country, in correlated in detail. Within Central Asia (and the regions of the Gobi Desert, the Lower the Asian territory, as a whole) Mongolian Cretaceous is widely extended almost in all Cretaceous is one of the most complete, and simultaneous basins over the country. more or less similar to the units of European Thus,there are limited areas of Upper standardized stratigraphy. Also, Mongolian Cretaceous, which contain almost all known Cretaceous contains its most upper fossiliferous Mongolian dinosaurs, and large areas of Lower horizons,wich is not often found in Asia.Other Cretaceous, until now seem to be almost free of notable characteristicks of the Mongolian a dinosaur fossil record. This phenomenon is Cretaceous are the multifacial structure of the connected with the big difference in non-marine deposits, including a large diversity paleogeography and, as a result, in burial of alluvial, fluvial and lacustrian facies of all conditions during the Early and Late types, and eolian and pedogenic deposits, as Cretaceous of Mongolia and Central Asia, as well (Gradzinski 1970; Gradzinski et al. 1977; well. Loope et al.1998; Barsbold et al. 2011). This The Early Cretaceous is known as the explains to some extent the high variety of the “period of basins”, because during this time the burials,met in the Mongolian great lakes were wide-spread on the territory of Cretaceous,beginning with respectively usual Mongolia. This name dates from the initial ones in shallow lake shores up to sandy dune “heroic” stage of paleontological research in surroundings, which, as a rule, illustrated an Mongolia, carried out by the Central Asian unusual state of preservation in the fossil expeditions in the 1920’s (Berkey& Morris, vertebrate record. The richness and variety of 1927). Also, F.K. Morris (1936) was the first the fossil record is the main characteristic, who referred the fossiliferous red-colored distinguishing the Mongolian Non-marine sandy deposits of the famous Flaming Cliffs, Cretaceous from the same and simultaneous the rich dinosaur locality discovered in the deposits, widely spread over enormous areas in Gobi Desert, to the ancient dunes of the Late Central Asia, as a whole (Dingus et al. 2008; Cretaceous time. Badamgarav et al. 1995). It seems, well-known The Early and Late Cretaceous of Non-marine Cretaceous of North America, Mongolia corresponded respectively to the sometimes alternating with the marine strata, successive different stages in paleogeography 127 at the end of Mesozoic. Each epoch was lizards, primitive mammals, birds, and some characterized by the formation of different groups of limnic Invertebrates (Ostracods, sedimentary basins, corresponding landscapes Pelecypods). Plants, spores and pollen, so and particular climatic conditions as well abundant in the Lower Cretaceous, practically (Shuvalov 1982) During the Early Cretaceous a are absent in Upper Cretaceous, though these development of the extensive lake basins and fossils are rarely preserved in corresponding humid climatic conditions were the most sedimentary facies (Barsbold 2008) characteristic for the territory of Mongolia. The Lower Cretaceous non-marine During the Late Cretaceous all conditions deposits are wide-spread over extensive areas changed in sharp contrast to the previous time. in Central and Eastern Asia, including China, Lake basins were strongly reduced,the climate Russian Siberia, Middle Asia, the Indo-Chinese became more arid, with clear seasonal Peninsula etc. The Upper Cretaceous is much alternation, and sandy dunes had been formed more restricted in its distribution in those areas along the lake coasts. Dispersed sand dunes and not so complete in comparison with the formed the most favorable conditions for Lower Cretaceous, being more connected with dinosaur burials. Evidently the sand dunes were the inner regions of Central Asia, and one of the main reasons,why the Upper dominantly filling up the sedimentary basins of Cretaceous of Mongolia contains almost all the Gobi Desert. By the end of the Early dinosaurs, discovered in the country,and other Cretaceous extensive areas of Central Asia had Vertebrates including the ancient mammals as undergone intercontinental deformations, well. having transferred into a more quiet regime, The Early Cretaceous non-marine continued over the Late Cretaceous. sedimentation and corresponding environments Correspondingly the previous were mainly characterized by reduction paleobiogeographical conditions and patterns conditions,whereas in the Late Cretaceous throughout the country had been strongly oxidizing environs definitely dominated.During changed in the subsequent stage. the Early Cretaceous the coal formations were The Early Cretaceous fossil groups of widely accumulated, but the Upper Cretaceous Mongolia are quite similar to the famous Jehol has no traces of coal. The Early Cretaceous Biota of Liaoning province, China, preserved in burials: diverged plants including representing only its separated parts dispersed big wooden trunks,as well as spores and pollen. in this interval over the territory of Mongolia. During the Cretaceous period the terrigenous No doubt, this similarity shows a close deposits strongly prevailed in sedimentary connection of the dinosaur groups of both areas basins. Lower Cretaceous includes respectively during the Early Cretaceous. Whereas during more thin-granulated lacustrine deposits, the Late Cretaceous time the dinosaur faunas of whereas Upper Cretaceous consists of more Mongolia were closely connected with the coarse-granulated facies of alluvial-lacustrine North American groups, and faunal exchange origin, including remarkable sandy dunes and took place through the hypothetical, though their dispersible analogies. The Lower quite probable, Beringean continental bridge. Cretaceous of Mongolia contains many organic There are many ancient animals and plants in groups--mostly limnic Invertebrates (a number Mongolian analogue (Barsbold 2008) of the of Ostracods, Phylopods, Early Cretaceous Jehol Byota: among the Pelecypods,Insects),from Vertebrates--a few dinosaurs – well-known Psittacosaurus, (first Dinosaurs species,many fishes including an discovered in Mongolia well in advance of the Asian famous Lycoptera,quite rare Jehol Byota was established), one of the most sturgeons,very rare shark teeth,and furthermore, common dinosaurs in Mongolia and China; also, turtles, birds and bird feather prints and Lycoptera, famous Asian fish of the continental primitive mammals. Plentiful fossil plants, distribution, often found in Lower Cretaceous of spores and pollen testify to their suitable burial Mongolia; many kinds of Insects, including the conditions and rich vegetation during this time. water beetles and their larvae; a lot of plants, The Upper Cretaceous contains the main spores and pollen of common distribution in the Vertebrates discovered in Mongolia: most Lower Cretaceous of Mongolia and China. dinosaurs (about 95% of all found species), Indeed, the evidence presented above, definitely dinosaur and fossil bird eggs, also, turtles, shows -- the Early Cretaceous fossil organic 128 groups in Mongolia almost completely seem to be interest, as follows: they were correspond to the Jehol Biota of north-eastern distinctive in all extents, first of all, in size, China. Additionally, the Lower Cretaceous which is evidently very important for deposits of Mongolia contain volcanic ash, as it taphonomy (and reconstruction of paleoecology, is in the Lower Cretaceous of Liaoning, China. hidden behind or within taphonomy). But the main important elements of the Jehol In spite of the big differences of the Biota -- feathered dinosaurs and birds have not mentioned groups, their burials could often yet been discovered in Mongolia. coincide in the burial conditions. In some cases The Late Cretaceous fossil record the burials were quite separated, clearly contains respectively mass-burials of the emphasizing the specific conditions, (as dinosaurs, which evidently means that the mentioned above, dry climatic conditions at corpses of the dead animals, as a rule, had been Flaming Cliffs), in which the animals inhabited, speedily buried in situ with the expressed and were buried in full accordance with their intensive sedimentation. Sometimes, probably, ecology and taphonomy. Evidently these the limited transportation of the buried objects coincidences and non-coincidences express not took place, and contributed to their higher complete, but quite real relationships between concentration in the localities. Transportation, ecology and taphonomy, characteristic for such no doubt, was quite short and limited in time different animal groups, as the Dinosauria and and space, and, most dinosaur corpses were Ostracoda. It seems,more profound knowledge buried in situ. It`s very probable, that the of these relationships could promote to more specific characters of the Late Cretaceous local exact reconstructions of the ancient sedimentation formed the most favorable environments and ecosystems, especially, when conditions, very suitable for and corresponded different organic groups were integrated to the mass-burials of the dinosaurs. In contrast together into joined burials, in which the to dinosaurs, the huge animals, the Ostracoda, possible ecological and taphonomical notably microscopic animals, highly tolerant of conditions seem to be excluding each other.The different environs, did not demand a quick and high organic divergence of the great burials in intensive sedimentation, and might be buried the Mongolian Cretaceous can not be formed during “normal’, sands not fast sedimentation, accidentally,only as the result of mechanic and were wide-spread almost in all facies transportation and concentration of the (excluding sand dune) Well-known dinosaur different animals, for example, water Ostracoda localities, like the Flaming Cliffs, Tugregeen and mostly terrestrial Dinosauria, both buried Shire and their analogies, being formed in dry together. The “big taphonomy” probably climatic conditions, express quite selective indicates quite big and general regularities in fossil records in particular environments, often the formation of the great burials, which are, as with strongly reduced water basins necessary a rule, complex and divergent in their for ostracods (Khand 2000). In these cases, composition. Mass death of gigantic seemingly pressed dinosaur faunas, for dinosaurs,noted in USA,Canada and Mongolia example, the monotypic dinosaur species (Curry 2014), is a good example to take into (Protoceratopses), were buried, and ostracods consideration the possible relationships came down to the reduced number of between ecology and taphonomy, what seems specialized forms, as Talicyprididae, probably to be not so simple. Probably, more adapted to the air-less waters of little ponds and understading of profound adequacy of these even pools (Khand 2000).The joint burials of relationships could open, step by step, the two organic groups–the dinosaurs and mystery of regularities in formation of the great ostracods, both widely represented almost in all Cretaceous dinosaur localities, including those divergent burials of the Mongolian Cretaceous, of Mongolia.

References: Berkey Ch., Morris F.K, 1927. Geology of Mongolia,Amer.Mus.Nat.Hist., New-York, V.2, 475p. Badamgarav D., Khand Yo & Barsbold R., 1995. Nonmarine Cretaceous of Mongolia. The Cretaceous System in East and Southeast Asia, Newsletter Special Issue 2, IGCP 350, Kyushu Univ, Japan:17-23.

129 Barsbold R. 2008. Non-marine Lower Cretaceous of Mongolia and Necessity of Dinosaur Hunting. – Recent progress of the study on Asian Dinosaurs and paleoenvironments. Internat. Dinosaur Symp. Fukui 2008, Japan, abstr. 23-26. Barsbold R., D. Badamgarav, Yo. Khand. 2011. Late Cretaceous Dunes in the Gobi Desert (Mongolia). Abstr., Bull. IGCP 507, pp.34-35., Beijing, China. Dingus L., D.B.Loope, D.Dashzeveg, C.C.Swisher III, Ch. Mingin, M.J.Novacek, M.A.Norell. 2008. The Geology of Ukhaa Tolgod (Djadokhta Formation, Upper Cretaceous, Nemegt Basin, Mongolia). – Amer. Mus. Novitates, 3616, 40 pp. Fastovsky D.E., D.Badamgarav, H. Ishimoto, M.Watabe,D.Weishampel. 1997. The paleoenvironments of Tugrikin-Shireh (Gobi Desert, Mongolia),and aspects of the taphonomy and paleoecology of Protoceratops (Dinosauria:Ornithischia).Palaios12:59-70. Gradzinski R. 1970. Sedimentation of dinosaur-bearing Upper Cretaceous deposits of the Nebegt basin, Gobi Desert.- Paleontol. Pol.,21:147-229. Gradzinski R., Z.Kielan-Jaworowska & T.Maryanska. 1977. Upper Cretaceous Djadokhta, Barun Goyot and Nemegt formations of Mongolia, including remarks on previous subdivisions. – Acta Geologica Polonica, vol. 27, 3:281-318. Khand Yo. 2000. The origin of Modern Non-marine Ostracod Fauna: Evidence from the Late Cretaceous and Early Paleogene of Mongolia. –Evolutionary Biology and Ecology of Ostracoda. Hydrobiologia, 419:119-124. Loope D.B., L.Dingus, C.C.Swisher III, Ch.Mingin. 1998. Life and death in a Late Cretaceous dune field, Nemegt basin, Mongolia. – Geology 26:27-30. Morris Fr.K. 1936. Central Asia in Cretaceous time. – Bull. Geol.Soc.Amer.47:1477-1533. Shuvalov V.F., 1982. Paleogeography and history of development of the lake system of Mongolia during Jurassic and Cretaceous time. – Mesosoic lake basins of Mongolia. “Nauka”, pp. 18-80. (in Russian).

130 P3: GEOLOGICAL AND PALINOLOGICAL PRELIMINARY RESULTS OF

KHETSUU TSAV AREA IN SOUTH MONGOLIA

A. Eviikhuu, N.Ichinnorov, and Ch.Gankhuyag

([email protected], [email protected], [email protected])

Introduction Palynology Studies The study area labeled Khetsuu Tsav The newly revealed oil shale bed is located on South Mongolia, in 780 km to SW forms outcrop in 25 to 150 m width, starting its from Ulaanbaatar, in 230 km to the South from distribution from SW corner of the study area, Dalanzadgad Town, Umnugobi Aimak and in continuing to the East for a while and then 130 km to SW from Nomgon Soum center. turning to the North up to northern border of There are observed mainly Lower Cretaceous the area in length about 1 km. The oil shale bed volcanogenic –sedimentary and terrigenic rocks, plunges to the N on SW corner, and plunges to and Holocene-Pleistocene, Holocene loose NW on the West, central and north-central sediments of deluvial-proluvial and parts of the area dipping at 10 degrees. alluvial-proluvial origin. There were taken 5 samples from the In 1995, there was carried out Complex drill core and sent to laboratory on proximate geological survey at scale 1:200 000 under analyses and palynology. Only one sample leading of geologist E. Burenkhuu and contains spore labeled Foraminisporis A.Gotovsuren to the region including the assymmetricus, Baculatisporites sp., and some current study area, and classifying the pollens Gymnosperm of following species: volcanogenic sedimentary rock unit covering Podocarpidites multiformis, Podocarpidites the area into Lower Cretaceous Tsagaantsav luteus, Podocarpidites multesimus, Formation, which has been composed of Podocarpidites, Cedripidites Iibaniformis, mainly conglomerate, conglomerate-breccia, Cedripidites sp, Piceapollenites sp, gritt stone, yellowish green and light grey Protopiceapollenites sp, Pinuspollenites colored sandstone, tuffaceous siltstone, eqisitae, Pinuspollenites sp, andesite basalt, and basalt containing lenses of Protopinuspollenites sp, Disaccites sp, light grey sandstone. Protoconiferus funarius, Disaccites sp.1, During 2012 to 2013, geologists of Araucariacidites sp., Cycadopytes sp., Etugen Eye LLC have carried out prospecting Piceapollenites variabilis., Piceapollenites sp., works for coal including mapping at scale 1:25 Inaperturapollenites sp., Piceapollenites 000, some drill holes and trenching works to exiloides., Podocarpidites decorus, the study area and revealed oil shale bed, which Podocarpidites sp., Cycadopites reticulate. outcropped on two areas (about 150 x 800 m According to palynology descriptions, spore and 73 x 510 m) within the study area. The oil observed very rarely (only Foraminisporis shale unit is preliminarily classified into Lower assymmetricus, Baculatisporites sp), while Cretaceous Shinekhudag Formation on Gymnosperm pollens were in significant basements of preliminary palynological data amount. However, spores and pollens of that obtained from the rock unit. The sediment ancient vegetation have large distribution in of Shinekhudag Formation is outcropped on wide spectrum in whole Lower Cretaceous SW, central and north-central parts of the study period, the above mentioned species of spores area and composed of red and green and pollens are typical for Barremian to Aptian conglomerate, light grey, greenish grey stage, therefore, the oil shale, which contains sandstone, siltstone, dark grey papery shale, the spore and pollen are preliminarily classified and clayey shale. into Lower Cretaceous Shinekhudag Formation, by authors of the current abstract. 131 Conclusion two formations; and its some part has to be The geological-palynological studies re-classified into younger (Barremian to Aptian that carried out to Khetsuu Tsav Area that stage) unit like as Lower Cretaceous located in southern most part of Umnugobi Shinekhudag Formation, and the rest of the Aimak (Mongolia) revise the sediments, which sediments is still classified into Tsagaantsav have been entirely classified into Lower Formation. In further, it has to be carried out Cretaceous volcanogenic-terrigenic units of detailed studies onto age determination of the Tsagaantsav Formation by the previous newly classified Shinekhudag sediments using researchers, shall be divided into sediments of more types of studies.

132 P4: Paleobotanical and Palynological characteristics of the Shivee-ovoo coal deposit,

Central Mongolia

Tsolmon G., Uranbileg L. and Ichinnorov N.

Paleontol. Cent. Mongolian Acad. Sci., Enkhtaivan Avenue-63, P.O.Box-260, Ulaanbaatar 13343, Mongolia ([email protected], [email protected], [email protected])

Summary generally includes the Lower Cretaceous age The fossil plants from the Shivee-ovoo (aptian-albian) and which has also been written locality (coal deposits) discovered and the in several references of Ichinnorov N., such as Lower Cretaceous flora of this locality has (Ichinnorov N., 2003а, 2005, Jargal L., been studied for the first time and which Ichinnorov N., Enkhtuya A., 2008; Ichinnorov includes the leaves, stems and seeds. The N., Tsolmon G., Odgrerel N., 2013). purpose of this paper is to show the result of The fossil pollen and spores were the systematic composition study. obtained from the siltstone end argillite-like The fossil plants collecting in the clay of the lower part and bed of upper part, Shivee-ovoo coal deposit by Ichinnorov N., assigned to 59 genus and 62 species.The Tsolmon G., Odgerel N., Patrick S. Herendeen, assemblage abounds in gymnosperm pollen in Masamichi Takahashi, Peter R. Crane et all, on which Coniferalis predominates (29-63%). 2012 in their field work. Shivee-ovoo coal Bisaccate conifer pollen of the genus deposit located about 260 km south-east of Protoconiferus (P.funarius, P.asaticus), Ulaanbaatar. By the our first study (Uranbileg Pinuspollenitus (P.divulgatus, P.similes, L., Tsolmon G.) we have found out that several P.insignius, P.oralicus), Piceapollenites following taxanomic composition: (P.exilioides, P.variabilis, P.singularis), Sphenopteris sp., Asplenium sp., Phoenicopsis Podocarpidites (P.decorus, P.multesimus) are sp., Nillsonia sp., Ginkgo sp., Ginkgoite sp., always present. Less freguent is monosaccate Podozamites ex gr. еichwaldii Shimper, conifer pollen Cycadopites sp., Pityophyllum sp., Pityospermum sp., Sciadopityspollenites macroverucatus, Carpolithes sp. (figures 1-13), but elements Retimonosulcites sp., Classopollis classoides, of Czekanowskiales are did not find in this C. echinatus and Inaperturapollenites sp. The study. From the types of conifers the spores (22-47%) are characterized by Pityophyllum is predominate here and in terms abundance of Cyathidites (C. australis, of number, there are the conifers are C.minor), Osmundacidites (O. wellmanii, O. (Pityophyllum, Podozamites) also much higher granulates) and various type: than ferns. There are also Ginkgo and Cicatricosisporites (C. australiensis, C. hallei, Ginkgoites are found and however, Nillsonia C.exiloides, C. ludbrooki), Pilosisporites was found in small amount. According to the (P.notensis, P. trichopapillosus), Rousesporites general spread of Podozamites еichwaldii is reticulates, Cooksonites (C.irregularis, explored in the Russia and most commonly C.variabilis), Aequitriradites spinulosus, researched in Asian part of Russia. Foraminsporites, Laevigatosporites and ets. To sum up this study, the ancient Among the Angeosperm pollen (2%) plants of Shivee ovoo is Mongolian Upper part Asteropollis sp., Clavatipollenites rotundus, of the Lower Cretaceous and which similar to Fraxinopollenites constrictus and Ttricolpites time, which can demonstrate the period of the sp. were present. Lower Cretaceous. However, we are consider that the further study should be made in the Conlusions future. The coal researches of this place is 133 The spores and pollen assemblage is Therefore the composition of the plants in similar to a spore-pollen assemblages from the Shivee-ovoo which illustrates the similar time Lower Cretaceous formations (Transbaikaila, of the Lower Cretaceous. Preliminary results Russia) Aptian and Albian age and to Dalazi of the floral study of systematic composition of Formation (Jilin, China) of Albian age. Shivee-ovoo locality are may be discussed.

Refrences: Ichinnorov N., 2003а, Pollen and Spore assembleges of Lower Cretaceous East Mongolia and their stratigraphy, 20 (in Russian). Ichinnorov, N. 2005. Pollen and Spore assemblages and ther stratigraphic significances. Mongolian Geoscientist.P.160-163. Jargal L., Ichinnorov N., Enkhtuya A., 2008. Petrology and Palynology of the Shivee-Ovoo deposit //3rd International Symposium of the IGCP project 507/ Abstract Volume. P. 100-102. Ichinnorov, N. Tsolmon, G. Odgerel, N. 2013. New data of Cretaceous (Shivee-Ovoo, Togrog lake) fossil plants and spores-pollen //”Mongolia Mineral Exploration Roundup-2013”, P. 33-50.

Plants from the Shivee-Ovoo coal deposits, Lower Cretaceous, aptian-albian, Central Mongolia. 1-3: Sphenopteris sp., 4-5: Conifers., 6-Podozamites ex gr. eichwaldii Shimper., 7- Pityophyllum sp., 8- Nillsonia sp., 9.10: Ginkgoites sp., 11-Carpolithes sp., 12,13: Pityospermum sp..

134 P5: Fossil Fuels Hosted in Mesozoic Sequences of Mongolia

Erdenetsogt, B.* and Jargal, L.

Dept. Geol. Geophy., Schl. Sci., Nat. Univ. Mongolia, Sukhbaatar District, Ulaanbaatar, Mongolia, ([email protected])

Mesozoic fossil fuel of Mongolia, coal, 4.5% hydrogen, 16.6% ash, and 1.2% total oil shale and petroleum, has great importance sulfur. Average calorific value is 26.4 MJ/kg. from the point of view of both economics and Mean vitrinite reflectance of Jurassic and geological studies. The deposition of fossil fuel Cretaceous coals are 0.48 and 0.33%, commenced with Pennsylvanian sequences, respectively. The results show that coal rank is and continued with Upper Permian, mainly controlled by the age of coal bearing Lower-Middle Jurassic, and finally with Lower sequences (Erdenetsogt et al., 2009). Cretaceous units. Pennsylvanian and Upper Petrographically, Mongolian coals are Permian coal seams were deposited mainly in classified as humic type. The concentration of western and southern Mongolia, respectively. huminite maceral groups of Creatceous coal Lower-Middle Jurassic coal and oil shale ranges from 54.9 to 82.9% on mineral matter accumulated in western, northern and eastern free basis. The concentration of inertinite group Mongolia. In the Early Cretaceous, thick and varies between 15.0 and 44.0%. The extensive oil shale, which is also considered as concentration of liptinite group does not exceed source rock of petroleum, and coal were more than 4.2%. Jurassic coals are distinct formed mostly in eastern Mongolia. At the from other coals, characterized by high same time oil shale and coal seams were concentration of vitrinite (87.3-96.6%) and accumulated in the western Mongolia, as well. liptinite groups (up to 11.7%), and by low Mongolia is favored by large coal recourses, concentration of inertinite groups (1.0- 6.0%) estimated at more than 170 billion tons, of (Erdenetsogt et al., 2009). which predominant portions are Mesozoic Oil shale resources were estimated to bituminous coal and lignite (Fig 1a). be 788 billion tons with 22.7 billion tons of Lower-middle Jurassic coal measures are shale oil (Bat-Erdene and Jargal, 1994). Oil hosted in Jargalant (western Mongolia), Bakhar shale is hosted in Middle Jurassic unit and (western part of central Mongolia), Saikhan Lower Cretaceous oil shale bearing formations (north Mongolia), while Lower Shinekhudag Formation. Jurassic oil shale has Cretaceous coals are in Andkhudag formation been identified in central and northern (central Mongolia) and in coal-bearing Mongolia, while Lower Cretaceous oil shale is Khukhteeg formation of Zuunbayan group distributed almost entire Mongolia (Fig 1b). (eastern Mongolia) (Erdenetsogt et al., 2009). Previously, it was thought that all oil shale in Based on the results of ultimate, proximate Mongolia is related to Lower Cretaceous analyses, calorific value, vitrinite reflectance (Bat-Erdene and Jargal, 1994), but recently the and maceral group concentration, coal quality age of some oil shale is revised from Lower has been determined. For Jurassic coals, Cretaceous to Middle Jurassic (Li et al., 2014). average carbon and hydrogen contents are Both Jurassic and Cretaceous oil shale have 73.3% and 5.0%, respectively. Ash yield and Type I kerogen and low sulfur content, ranging total sulfur contents are low, 16.1% and 1.0%, from 0.1% to 1.5 %. Jurassic oil shale has up to respectively. Average calorific value is 28.4 33.2 % TOC, whereas Lower Cretaceous oil MJ/kg. Cretaceous coals contain 66.2% carbon, shale has 35.6 %TOC (Bat-Erdene and Jargal 135 1994; Yamamoto et al.,1998; Sladen and events. In contrast, Lower Cretaceous coal-, oil Traynor, 2000; Johnson et al., 2003; shale-, and oil-bearing rocks were accumulated Bat-Erdene, 2012). in rift valleys, caused by extensional tectonic According to Pentilla (1993) and events. Jurassic coals, distributed throughout Traynor and Slayden (1995), conventional oil north, central and eastern Mongolia, with high reserves can be found from Cretaceous vitrinite and liptinite contents formed under sequences. Four oil fields, Zuunbayan, raised water table condition due to much higher Tsagaan-Els, Toson-Uul and Tamsag, hosted in rainfall than the rainfall in Lower Cretaceous Lower Cretaceous sequences, have been (Erdenetsogt et al., 2009). It is known that most, discovered in eastern and south eastern if not all, Jurassic oil shale lies under coal Mongolia so far. In addition, several tar sand measures, indicating that water level was and oil seepage were catalogued (Fig 1c). increased continuously and oil shale was Penttila (1993) estimated that Mongolia has 3 accumulated instead of peat due to increased to 6 billion barrels oil equivalent of water depth in lakes. During Late conventional recoverable oil and gas resources. Jurassic-Early Cretaceous, when extension took The expected most likely oil field size ranges place, sediments of Shinekhudag oil from 100 to 170 million barrels o.e. According shale-bearing formations accumulated in rift to Uuganbayar (2014), proved oil reserves of valleys on top of the older synrift sequences. the above mentioned four oil fields are 2.1 Within the troughs, relatively large lakes billion barrels with 271.6 million barrels of formed (Sladen and Traynor, 2000; Johnson recoverable reserves. API gravity and sulfur and Graham, 2004), where thick mud and oil contents of Tsagaan-Els and Tamsag fields are shales accumulated. With decreasing 300 and 360, and 0.14% and 0.01%, subsidence rates, water levels decreased and respectively. paleoenvironmental condition became more Early-Middle Jurassic non-marine suitable for peat accumulation. The shallow sedimentary sequences, which host coal and oil lakes/swamps were filled with Khukhteeg shale, were deposited in foreland intermontane coal-bearing formations (Erdenetsogt, 2009). basins, formed under compressional tectonic

References: Bat-Erdene, D., 2012. Fossil fuel. In: Byamba, J. (Ed. in chief), Mongolian Geology and Mineral Resources, Mem. Vol. 70th year anniv. Mongolian Geol. Sur., vol. 5, pp 247-266 [in Mongolian]. Bat-Erdene and Jargal, 1994. Mongolian oil shale and its potential. Ministry of Energy and Mining, ‘Mongol Gazriin tos tovchoo’, Open file report. Ulaanbaatar [in Mongolian]. Erdenetsogt, B., Lee, I., Bat-Erdene, D., Jargal, L., 2009. Mongolian coal-bearing basins: Geological settings, coal characteristics, distribution, and resources. Internat. J. Coal Geol. 80, 87–104. Johnson, C.L., Greene, T.J., Zinniker, D.A., Moldowan, J.M., Hendrix, M.S., Carroll, A.R., 2003. Geochemical characteristics and correlation of oil and nonmarine source rocks from Mongolia. AAPG Bull. 87, 817–846. Johnson, C.L., Graham, S.A., 2004. Cycles in perilacustrine facies of Late Mesozoic rift basins, Southeastern Mongolia. J. Sediment. Res. 74, 786–804. Li, G., Ando, H., Hasegawa, H., Yamamoto, M., Hasegawa, T., Ohta, T., Hasebe, N., Ichinnorov , N., 2014. Confirmation of a Middle Jurassic age for the Eedemt Formation in Dundgobi Province, southeast Mongolia: constraints from the discovery of new spinicaudatans (clam shrimps), Alcheringa, DOI: 10.1080/03115518.2014.870834. Pentilla, W.C., 1993. The recoverable oil and gas resources of Mongolia. J. Petrol. Geol. 17, 89–98. Sladen, C., Traynor, J.J., 2000. Lakes during the evolution of Mongolia. In Gierlowski-Kordesch, E.H. and Kelts, K.P. (Eds), Lake basin through space and time: AAPG Studies in Geology 46, pp 35-57. Traynor, J.J., Sladen, C., 1995. Tectonic and stratigraphic evolution of the Mongolian People's Republic and its influence on hydrocarbon geology and potential. Marine Petrol. Geol. 12, 35–52. 136 Uuganbayar, 2014. Outline of petroleum exploration in Mongolia. Petroleum Authority of Mongolia, Proceedings of GIMAR-2014 conference. Ulaanbaatar [in Mongolian]. Yamamoto, M., Bat-Erdene, D., Ulziihutag, P., Watanabe, Y., Imai, N., Kajiwara, Y., Takeda, N., Nakajima, T., 1998. Organic geochemistry and palynology of Lower cretaceous Zuunbayan oil shales, Mongolia. Geol. Sur. Japan Bull. 49, 257–274.

137 Fig 1. Distribution schema of Mesozoic fossil fuel deposits and occurrences of Mongolia. 1a. Location map of Mongolian coal-bearing provinces, basins and deposits (modified after Erdenetsogt et al., 2009). Province: WM - Western Mongolian; EM - Eastern Mongolian; Basins: KHB - Kharkhiraa; MAB – Mongol-Altai; SGB - South Gobi; UHB - South Khangai; IBB - Ikh Bogd; ORB - Ongi river; CNB – Choir-Nyalga; CHB - Choibalsan; TAB - Tamsag; SHB - Sukhbaatar; EGB - East Gobi; CGB - Central Gobi basin; Areas: BUA – Bayan-Ulgii; TAA - Trans-Altai; OSA – Orkhon-Selenge; Coal deposits: 1 - Mantag; 2 - Jargalant; 3 - Minguush; 4 – Egiin gol; 5 - Murun; 6 - Jilchigbulag; 7 – Saikhan-Ovoo; 8 - Ereen; 9 - Bayantsagaan; 10 - Unjuul; 11 - Khuden; 12 - Bayanduurekh; 13 - Alagtsakhir; 14 - Khotgor; 15 - Bayanteeg; 16 - Tsagaan-Ovoo; 17 - Nariin sukhait; 18 - Tsogt; 19 - Mogoin gol; 20 - Ulaan-Ovoo; 21 -Shariin gol; 22 - Nalaikh; 23 - Baganuur; 24 - Maint; 25 - Tsaidam; 26 - Tugrug; 27 - Khumuult; 28 - Tsaidam nuur; 29 - Olongiin Ukhaa; 30 - Alagtogoo; 31 - Shivee-Ovoo; 32 - Ulaan nuur; 33 - Ikh Ulaannuur; 34 - Uvdugkhudag; 35 - Tevshiin gobi; 36 - Khulstnuur; 37 - Aduunchuluun; 38 -Utaat minjuur; 39 - Talbulag; 40 - Ulziit; 41 - Zuunbulag; 42 - Bulangiin khooloi; 43 - Bayantsogt; 44 -Taliin khudag; 45 - Nukhet; 46 - Khootiin khonkhor; 47 - Khamriin khura. 1b. Location map of Mongolian oil shale-bearing basins, deposits and occurrences (modified after Bat-Erdene, 2012). Basins: LAB – Nuuruudiin Khotgor, GAB – Gobi-Altai, ORB – Ongi River, TGB – Tugrug, ULB – Ugii Lake, UJB – Uvurjargalant, NGB – Nyalga, MGB – Middle Gobi, SGB – South Gobi, EGB – East Gobi, SBB – Sukhbaatar, TAB – Tamsag, CHB – Choibalsan; Deposit/occurrence: 1 – Bayanteeg, 2 – Tsagaan-Ovoo, 3 – Khuut, 4 – Shariin Gol, 5 – Erdene Uul, 6 – Bayantsagaan, 7 – Gashuun Gol, 8 – Sukhai, 9 – Bakhar Uul, 10 – Andkhudag, 11 – Tugrug, 12 –Erdene Uul, 13 – Khugshin Gol, 14 – Zuunbulag, 15 – Uvurjargalant, 16 – Tuhum Nuur, 17 – Ereen Gobi, 18 – Nariin Uul, 19 – Tsarsan Chuluut, 20 – Uvdug Khooloin Gashuun, 21 – Nalaikh, 22 – Ereen gobi, 23 – Ulziin Lake, 24 – Beeliin jas, 25 – Shavart-Ovoo, 26 – Nukht, 27 – Khukhtsaa, 28 – Nergui, 29 – Khashaat khudag, 30 – Jirmiin khudag, 31 – Shine Us, 32- Khavkhastai, 33 – Nergui, 34 – Zamiin Uud, 35 – Khar Ereg, 36 – Shorvog Nuur, 37 – Tugrug, 38 – Bayan-Erkhet, 39 – Bayanjargalan, 40 –Ovoo sum, 41 – Khulun Buir, 42 – Bukhiin khhudag, 43 – Melkhii khudag, 44 – Tsagaan nuur, 45 – Amnii khudag. 1c. Location map of Mongolian petroleum blocks, oil fields and tar sand deposits/occurrences. Block: I - Uvs, II - Khar-Us Lake, III - Sharga, IV - Bogd, V - Ongi, VI - Nemegt, VII – Borzon, VIII - Khongor, IX – Nomgon, X_S – South Tukhum, X_N – North Tukhum, XI – Galba, XII - Ergel, XIII – Tsagaan-Els, XIV – Zuunbayan, XV – Tariach, XVI – Nyalga, XVII – Bayantumen, XVIII – Khukh Lake, XIX – Toson Uul, XX – Matad, XXI – Tamsag, XXII – Buir, XXIII – Sulinkheer, XXIV – Dariganga, XXV – Choir, XXVI – Tsaidam, XXVII – Sukhbaatar, XXVIII – Kherlentokhoi; Oil field: 1 – Tsagaan-Els, 2 – Zuunbayan, 3 – Toson Uul, 4 – Tamsag; Tar sand occurrence: 5 – Zuunbayan, 6 – Bayan-Erkhet, 7 – Khugshingol.

138 P6: Stratigraphic succession of Conchostracan fossils from the lacustrine deposits in the

Shinekhudag area (Lower Cretaceous), Eastern Gobi basin, Southeast Mongolia

Murata, T.1, Li, G.2, Ando, H.3, Hasegawa, H.4, Hasegawa, T.5, Ohta, T.6, Yamamoto, M.7, Hasebe, N.8 and Ichinnorov, N.9

1Grad. Schl. Sci. and Tech., Ibaraki Univ., Mito 310-0056, Japan ([email protected]) 2Nanjing Inst. Geol. Palaeont., Chinese Academy of Science, Nanjing 210008, China 3Dept. of Earth Sci., Fac. Sci., Ibaraki University, Mito 310-0056, Japan 4Nagoya Univ. Mus., Nagoya University, Nagoya 464-8601, Japan 5Dept. Earth Sci., Fac. Sci., Kanazawa Univ., Ishikawa 920-1192, Japan 6 Fac. Edu., Int. Arts, Sci., Waseda University, Tokyo 169-8050, Japan 7Fac. Env. Earth Sci., Hokkaido University, Sapporo 060-0810, Japan 8Div. Ear. Env. Tech., Kanazawa University, Ishikawa 920-1192, Japan 9Paleont. Center, Mongolian Acad. Sci., Ulaanbaatar-210351, P.O. Box 260, Mongolia

Clam shrimps (spinicaudatans, morphological, paleoecological and so-called ‘conchostracans’) are small, taphonomical analyses of the spinicaudatan fresh-water branchiopod crustaceans with fauna. bivalved chitinous carapace. Although they The Shinekhudag Formation, well have a long geologic history from the Devonian exposed in the Shine Khudag locality, is Period to the Recent, they were more composed mainly of dark grey paper shale, prosperous during the Mesozoic Era. Their light grey calcareous shale, and whitish, fossils often occur in lacustrine mudstone yellowish and brownish dolomite. The shale deposited in quiet fresh-water environments and dolomite successions are rhythmically abundantly. Therefore, they are alternated (decimeter-, meter-, tens of biostratigraphically useful for the correlation meter-scale), which might be controlled by and zonation of the Mesozoic non-marine orbital cycles. Strata are continuously exposed successions. about 300 m in thickness. The age of the The Gobi Basin of southern Mongolia formation is estimated as Aptian based on the contains widespread non-marine Cretaceous floral and molluscan evidence (e.g., deposits that yield abundant vertebrate remains, Jerzykiewicz and Russell, 1991), and Ar40/Ar39 including dinosaurs, mammals, etc. age data from basaltic rocks of the uppermost (Jerzykiewicz and Russell, 1991; Khand et al., part of the underlying Tsagantsav Formation 2000; Hasegawa, H., et al., 2009). We (ca. 121-125 Ma: Graham et al., 2001). investigated thick lacustrine shale and Stratigraphic occurrences of mudstone sequences represented by the conchostracans and associated ostracods, mid-Cretaceous (Aptian) Shinekhudag bivalves, insects and plant remains were Formation for evaluating terrestrial examined by careful observation along the paleoenvironments in the eastern Gobi basin, outcrop and trench successions of the middle Southeast Mongolia. As abundant part of the Shinekhudag Formation. Only two spinicaudatan fossils successively occur in the previously described species, as Neodiestheria studied section, the Shinekhudag Formation is mongolensis Chen, 2005 and Yanjiestheria suitable to undertake taxonomical, gobiensis Chen, 2005 occur from the interval 139 over 100 m thick. On the basis of their size, in grey laminated shale, apparently showing outline and surface ornamentation of carapace, periodic intercalations and zones, especially N. mongolensis is elliptical and larger frequent above and below dolomite layers. (9-27mm) with well-developed growth lines Furthermore, ostracods are contained and reticulated growth bands, and Y. gobiensis in poorly laminated calcareous shale in the has round-shaped and smaller (ca. 4 to 16mm middle part of the entire section, and they may in shell length) carapace. be also exclusive with two conchostracans. In N. mongolensis occurs from dark grey well-exposed successions in the middle part of paper shale and light grey calcareous shale the entire section, we identified the following abundantly, and whitish dolomite rarely of characteristic types of layers: 1) conchostracans most fossil horizons spanning over 100 m thick abundant layer, 2) ostracods abundant layer, 3) except the lowermost and uppermost parts of poorly fossiliferous layer. These types occurs the entire section. Density of conchostracan somewhat periodically depending upon the fossils decreases in the interval of the lithological changes. less-frequent alternation of shale and dolomite These modes of fossil occurrence beds. On the other hand, Y. gobiensis occurs suggest the relationship between paleoecology mainly from dolomitic light grey shale of some and lake environmental changes such as lake certain horizons in the middle part of the entire levels, bottom-water condition and primary section. Both species are exclusive on the same production in large and deep lakes within an lamina plane, even though they are contained interior portion of the large Eurasian Continent. within the same bed. Although they often occur Further taphonomical studies are necessary to sporadically, a few milli- to centimeters understand the relationship between the lake swarmed lamina or thin beds are very common ecosystem and physical condition.

References: Graham, S.A., Hendrix, M.S., Johnson, C.L., Badamgarav, D., Badarch, G., Amory, J., Porter, M., Barsbold, R., Webb, L.E., Hacker, B.R., 2001, Geol. Soc. Amer. Bull., 113, 1560–1579. Hasegawa, H., Tada, R., Ichinnorov, N., Minjin, C., 2009. J. Asian Earth Sci., 35, 13–26. Jerzykiewicz, T., Russell, D.A., 1991. Cretaceous Res., v.12, p.345–377. Khand, Y., Badamgarav, D., Ariunchimeg, Y., Barsbold, R., 2000. Cretaceous Environments of Asia. p.49–79. Yamamoto, M., Bat-Erdene, D., Ulziikhishig, P., Watanabe, Y., Imai, N., Kajiwara, Y., Takeda, N., Nakajima, T., 1998, Bull. Geol. Sur. Japan, 49, p.257–274. Yuan, F., Chen, P., 2005. Acta Palaeontol. Sinica, v.44, p.25-35.

140 P7: TEX86-based lake water temperatures in Jurassic and Cretaceous Mongolia

Yamamoto, M.1, Ando, H.2, Hasegawa, H.3, Hasegawa, T.4, Ohta, T.5, Hasebe, N.6, Murata, T.2, Li, G.7 and, Ichinnorov, N.8

1Fac. Env. Earth Sci., Hokkaido Univ., Kita-10, Nishi-5, Kita-ku, Sapporo 060-0810 ([email protected]) 2Dept. Earth Sci., Ibaraki University 3Nagoya University 4Dept. Earth Sci., Kanazawa University; 5Fac. Edu., Int. Arts, Sci., Waseda University 6Div. Ear. Env. Sci., Kanazawa Univ. 7Nanjing Inst. Geol. Palaeont., China 8Paleontol. Center, MAS, Mongolia

H Introduction Temperature was calculated from TEX86 The surface temperatures and their according to the equations based on a global latitudinal gradient in the Greenhouse Earth are core top calibration (Kim et al., 2010). The a current topic in paleoclimatology to analytical accuracy was 0.45°C in our understand the climate sensitivity and polar laboratory. amplification for future climate prediction. TEX86 is a powerful tool of paleo-sea and lake Results and discussion surface temperature reconstruction. In this Five Jurassic and ten Cretaceous study, we reconstructed lake water sediments yielded reliable lake water H temperatures in Mongolia during the Jurassic temperatures. TEX86 -based temperatures and Cretaceous periods by analyzing the TEX86 ranged from 23 to 32°C. The averages and H values of GDGTs in sediments from the standard deviations of TEX86 -based Jurassic Eedemt Formation and the Cretaceous temperature were 28.1°C and 2.4°C in the Shine Kuhag Formation. Jurassic Eedemt Formation and 28.4°C and 3.4°C in the Cretaceous Shinekhudag Formation, Samples and Methods respectively. The Mongolia was located at about The sediment samples were collected 50°N in the Jurassic and Cretaceous periods. at outcrops of the Eedemt locality of central The estimated temperatures are much higher Mongolia and the Shinekhudag locality of than the modern mean annual temperatures at southern Mongolia during the expeditions in the same latitude (Figure 1). Theses new data 2010 leaded by Hisao Ando. The sediment was are consistent with a view that temperature extracted with dichloromethane/methanol gradient was smaller in the Cretaceous period, mixture and chromatographed into four suggesting that polar amplification responds to different fractions. GDGTs in the polar fraction radiation forcing. The estimated Jurassic were analyzed on a liquid chromatograph-mass temperatures are not different from Cretaceous H spectrometer. TEX86 (derived from TEX86) temperatures. This finding contradicts the result were calculated from the concentrations of of previous studies suggesting that Jurassic GDGT-1, GDGT-2, GDGT-3 and a worlds were cooler than Cretaceous ones (e.g., regioisomer of crenarchaeol (Schouten et al., Frakes et al., 1992). This question is open. More 2002 EPSL; Kim et al., 2010 GCA). data are required for understanding this issue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

P8: Base level and paleotemperature changes of Cretaceous lacustrine succession in

southeast Mongolia

Fujita, Y.1, Ohta, T.2 and Shinya, H.1

1Department of Geosciences, Waseda University, Tokyo, Japan 2Department of Geosciences School of Education, Waseda University, Tokyo, Japan email:[email protected]

The Shinekhudag Fomation is a (e.g. kaolinite) and the geochemical hinterland Cretaceous lacustrine succession distributed in weathering indices covary with PC2. PC3 the East Gobi Basin of southeast Mongolia, correlates with the amount of the mafic which is characterized by rhythmically minerals: it is characterized by positive alternating beds of mudstone and dolomite. correlation with smectite and illite components Mudstone layers comprise sediment discharge and negatively with kaolinite and quartz. The from the eroded continental crust (such as former mineral assemblage represents sediment detrital illite), while dolomite indicates input from mafic source, while latter represent intervals of hypersaline and significant felsic source. Consequently, PC3 can be microbial activities. Therefore, these alterations interpreted as a measure of source rock can be interpreted to reflect base-level changes lithology. of the lacustrine. In addition, the hinterland The result of PCA suggests that PC1 weathering indices show a significant increase and PC2 can stand as the individual measures from the lower to the upper part of the of the base-level and paleotemperature changes Shinekhudag Formation, which indicates that in the inland region of East Asia. The overall the paleoclimate of mid-latitude in Asian changes of the base-level inferred from the PC1 region gradually shifted to more humid and score profile indicates that water depth slightly temperate condition in Aptian. Principal increased in the middle part of the Shinekhudag component analysis (PCA) of the major Formation. In contrast, the paleotemperature mineral composition (smectite, illite, kaolinite, implied by the PC2 score profile increased quartz and carbonate) and the hinterland continuously, which is concordant with the weathering indices (W index and CIA) has global warmth trend during the Aptian deduced been performed in order to deduce the climate from oxygen isotope data. Moreover, the changes recorded in studied lacustrine deposits. present analysis revealed a high frequency PCA extracted three principal components change in the both base-level and (PC1, PC2 and PC3), which captured 40.74%, paleotemperature. The wavelet spectral 26.26% and 17.03% of total variability, analysis revealed that respective cycles of these respectively. The absolute values of PC1 scores variations are in the order of 113 ± 21 kyr, are governed by the increase or decreases in which is concordant with an eccentricity cycle. carbonate content against detrital minerals. Therefore, the results suggest that Therefore, PC1 can be interpreted as latent mid-Cretaceous paleoclimate change preserved variable recording changes in base-level which in the Shinekhudag lacustrine succession had been controlled by the balance between records both global high-amplitude climate precipitation and evaporation. On the other change in the mid-Cretaceous, as well as hand, PC2 is regarded to be the proxy of the high-frequency climate change deduced by the paleotemperature because weathered minerals Milankovitch orbital forcing.

143 P9: Paleoenviromental of Cretaceous lacustrine succession

in Xinjiang-Uygur Autonomous Region: Development of mega-monsoon climate regime as a cause of high-frequent reversals of redox conditions in the lacustrine environment

Arai, K.1, Ohta, T.1, Hirano, H.1, Harigaya, S.2, Sakai, T.3, Kozai, T.4 and Li, G.5 1Waseda University, Japan ([email protected]) 2Tokyo Institute and technology, Japan 3Kyushu University, Japan 4Naruto University of Education, Japan 5Nanjing Institute of Geology and Palaeontology, China

Mesozic non-marine systems are focuses on analysis of Aptian to Albian widely distributed in the Junggar basin of Lianmqin Formation, which occupy the Xinjiang-Uygur Autonomous Region, stratigraphically highest position of Taguru northwest, China. The Junggar basin developed Group. as a continental basin of the southern margin of Visual light spectra and L*a*b* color the Asian continent that faced paleo-Tethys index values were measured by optical Ocean during the early Mesozoic. However, the colorimeter. Spectra were futher analyzed by Junggar basin turned out to be a foreland basin principal component analysis (PCA) in order to after J/K boundary, due to the accretion of the identify latent variables, which produced color Tibet Plateau and succeeding uplift of Tianshan variation of mudstone. Also, major elements of Mountains. After this collisional event, mudstone sample were analyzed by x-ray sediments of the Junggar basin. fluorescence spectroscopy and clay mineralogy Among them, the Lianmuqin Fomation, of mudstones was identified by x-ray comprising mid-Cretaceous lacustrine diffractometer. succession is characterized by a high-frequent PCA results of raw visual light spectra alternating layers of red and dark gray data indicate that colors of the Lianmqin mudstone. In this study, we analyze Formation are controlled by the three specific paleoenvironment factors which produced these types. A comparison with the reference characteristic layers by using visible light spectrum data of mineral spices identify that spectrometer and chemical composition of these latent spectra represent presence of mudstone samples. hematite, chlorite and calcite. However, the The Jungger basin is a foreland sedimentary main factor that determines the color variation basin developed by the obduction and uplift of is attributed to the content of hematite, because Tianshan Mountains which fringe on the south the variation of visual light spectra data that limit of the Junggar basin. The lower hematite attributed was significantly high Cretaceous system of the Junggar basin is (97.4%). Within the lacustrine environment, named as the Taguru Group, which is further hematite is known to be produced in subdivided into four formation(Eberton et al, oxygenated conditions. Therefore, the color 2001). These formations are consisted of variation of the Lianmqin Formation sandstones and mudstones exhibiting red or demonstrates the variation in redox condition light gray-green colors. The paleo-depositional of lacustrine environment; red hematite-rich environments were mainly lacustrine with bed and light gray hematite-poor beds comprise minor alluvial to fluvial intrusions in some oxygenated and anoxic conditions, respectively. localities(Zhou and Dean, 1996). This study In addition V/Cr and Ni/Co ratios, which are

144 the geochemical indices that can also monitor increases of the bioproductivity. Therefore, the oxidation-reduction state (Jones and reductive but high-productive phase recorded Manning, 1994) showed stratigraphic in the Lianmqin Formation indicate warm variations concordant PC1 variations. All of paleoenvironment. our results suggest that the prominent factor, On the other hand, during the which produced alternating layers of red-light cool-season, a stable thermocline would not gray mudstones in the Lianmqin Formation is a develop, making it easy for water column reflection of the oxidation-reduction state of the circulation, and thus, oxygenation of lacustrine lacustrine bottom water conditions. Meanwhile, environment. At the time, cooler climate that data regarding bioproductivity (fossil and are unsuitable for biota hinters bioproductivity. CaCO3 content) shows an apparent This makes oxygenated but low bioproductivity contradiction to the above interpretation. In horizons recorded in the Lianmqin Formation. general one can assume that the fossil record In summary, lacustrine sediments with PC1 and amount of carbonate in lacustrine would values were deposited under the oxidized and increase in high PC1 strata, namely the cool climate regime, and in contrast, those with bioproductivity is expected to increase if the low PC1 values were deposited under the dissolved O2 was abundant. However, the reduced and warm climate regime. In Central redox indices and bioproductivity of the Asian region, these two contrasting Lianmqin Formation are inversely correlated. paleoclimate modes were alternatively This apparent contradiction can be explained developed with a frequency of c.a. 10 to 100ky. by the following scenario. Probably, such periodic climate that was not During the warm-seasons, a firm thermocline seen before the Cretaceous may have emerged would develop, which hinders lacustrine water by the development of mega-monsoon climate column circulation and oxygenation. caused by the uplift of Tianshan Mountains, Meanwhile, warm and suitable climate would wich intitated in latest Jurassic.

References: Jones, B. and Manning, D.A.C., 1994. Comparison of geochemical indices used for the interpretation of palaeoredox conditions in ancient mudstones. Chem. Geol. 111, 111–129. Zhou, Z. and Dean, W.T., 1996. Phanerozoic Geology of Northwest China. Science Press, 316pp. Eberth, D.A., Brinkman, D.B., Chen, P.J., Yuan, F.T., Wu, S.Z., Li, G. and Cheng, X.S., 2001. Sequence stratigraphy, paleoclimate patterns, and vertebrate fossil preservation in Jurassic Cretaceous strata of the Junggar Basin, Xinjiang Autonomous Region, People’s Republic of China. Can. J. Earth Sci. 38, 1627–1644.

145 P10: Laboratory experiments for attesting the “weathering hypothesis” as a possible cause

of the mid-Cretaceous Oceanic Anoxic Events

Sasaki, G.1 and Ohta, T.2

1Grad. Schl. Creat. Sci. Eng., Waseda University, Japan ([email protected]) 2Dept. Earth Sci., Fac. Edu. Arts Sci., Waseda University, Japan ([email protected])

The “Weathering hypothesis” compared to those under the ordinary meteoric (Weissert et al., 1998) that might have occurred water during the volcanically quiescent phase. during the middle Cretaceous has received Materials used for weathering wide attention because it may have played a experiments are granite and basalt, which can crucial role in causing the Oceanic Anoxic be seen as representative materials of Events (OAEs). In this model, the cause of continental crust and LIPs. Samples were kept OAEs is explained by a following chain in reaction container filled by acidic solution reaction, (1) global warmth and increase in and several samples were simultaneously batch atmospheric CO2 by the Large Igneous processed within the heated thermobath, The Provinces (LIPs) enhanced weathering of acid employed was HCl solution, because it is continental crust, (2) enhanced land weathering the main acid present in volcanic gas. led excessive influx of nutrients from Concentrated and dilute acidic solutions were continents to oceans, (3) eutrophication used, which were adjusted in order to represent enhanced primary productivity, (4) the fact, artificial meteoric water during volcanically several numerical simulations have revealed active and quiescent periods. After reacting 168, that elevated rates of continental crust 504, 840 and 1344 hours chemical weathering were one of the most important compositions of the solution were analyzed by factors involved in triggering global anoxic ICP-MS. events (Misumi et al., 2009;Ozaki et al., 2011; The quantity of elemental elution of Monteiro et al., 2012). In addition, several lines both rock types increased in the volcanically of direct field-based evidence of the weathering active period compared to those of the hypothesis have recently been provided, which quiescent period. The amount of Na, Mg, K demonstrates that enhanced hinterland and Ca were 1.4 to 4.5 times higher during weathering was the actual cause of OAEs (e.g., volcanically active phase, and those for P was Weissert et al., 1998; Frijia and Parente, 2008; at least 4.0 to 12.8 times higher. Particularly, Tejada et al., 2009). among these elements, the eutrophication of the Therefore, both the simulation-based Ca known as a main factor for blooming of and geochemistry-based studies revealed that dinoflagellate (Iwane et al,.2008), and P is one the process (2) of above mentioned weathering of the important nutrient supplied to the hypothesis actually occurred during OAEs. biosphere by rock weathering. The result However, the relationship between LIPs suggests that the acidified meteoric water activity and enhancement of continental induced by the activity of LIPs escalated 1.4 to weathering remains unknown, i.e., the process 12.8 times higher nutrient supply to the ocean, (1) of the weathering hypothesis. In this regard, which was in an order sufficient to promote the purpose of this study is to determine the marine bioproductivity. extent of weathering enhancement by the LIPs Recently, Courtillot et al. (2003) and activity. We quantitatively measured the degree Kuroda et al. (2007) revealed the simultaneity of weathering under the acidified meteoric of LIPs activities and OAEs. They further water induced by the activity of LIPs, and revealed that activities of LIPs consistently predated oceanic anoxic events. Present 146 experiment suggests that acidified meteoric temperature in order to accelerate weathering water by the intense LIPs activity possibly reaction in laboratory environment. The result promoted the weathering of continental crust, only demonstrates the relative tendency of and this raised oceanic eutrophication. elemental elution during in-phase LIPs and Therefore, LIPs activity may have been the out-phase volcanism. It is necessary to design a triggering event of OAEs. However, the present laboratory experimental condition analogous to experiment is only a simplified comparative natural in-phase LIPs and out-phase LIPs in experiment, which employed unnaturally future work. concentrated acid under overly high

Reference: Courtillot et al., 2003. Geoscience 335. 113–140. Frijia and Parente., 2008. Palaeogeography, Palaeoclimatology, Palaeoecology, 261, 15–29. Iwane et al., 2008. Annual Jounal of Hydraulic Engineering. 52, 1303-1308. Kuroda et al., 2007. Earth Planet. Sci. Lett. 256, 211-223. Misumi et al., 2009. Earth Planet. Sci. Lett. 286, 316-323. Monteiro et al., 2012. Paleoceanography, 27, PA4209. Ozaki et al., 2011. Earth Planet. Sci. Lett. 304, 270-279. Tejada et al., 2009. Geology, 37, 855-858. Weissert et al., 1998. Paleo3, 137, 189-203.

147 P11: Evidence of enhanced continental weathering during oceanic anoxic event 2 (OAE 2) in eastern continental margin of Asia

Ohta, T.1, Kamigata, Y.2 and Takagi, H.2

1Dept. Earth Sci., Fac. Edu. Integ. Arts and Sci., Waseda Univ., 1-6-1 Nishiwaseda, Shijuku-ku, Tokyo 169-8050, Japan ([email protected]). 2Grad. Schl. Creat. Sci. Eng., Waseda Univ., 1-6-1 Nishiwaseda, Shijuku-ku, Tokyo 169-8050, Japan.

Mid-Cretaceous is characterized by value increases from the Aptian to the intensified oceanic anoxia (Oceanic Anoxic Cenomanian, and then decreases towards the Events: OAEs) that raised global deposition of Campanian. The fluctuations in the W values organic black shales. The “Weathering are concordant with paleotemperature hypothesis” that might have occurred during fluctuations (oxygen isotope) reported from the the middle Cretaceous has received wide Exmouth Plateau. This agreement indicates that attention because it may have played a crucial the change in paleotemperature governed the role in causing the OAEs. In this model, the weathering rates of the East Asian continental cause of OAEs is explained by a following crust. In addition, high-resolution chain reaction, (1) global warmth and increase measurements of W values around the OAE 2 in atmospheric CO2 enhanced weathering of interval revealed an abrupt increase in continental crust, (2) enhanced land weathering hinterland weathering rates during OAE 2 that led excessive influx of nutrients from ceased simultaneously with the termination of continents to oceans, (3) eutrophication OAE 2. Moreover, the increase in the W value enhanced primary productivity, (4) the slightly predates the onset of OAE 2 (ca. excessive primary producers consumed 100–500 ka). Therefore, this preliminary result dissolved oceanic oxygen that finally led to the is consistent with the weathering hypothesis in OAEs. Several studies, in fact, revealed a two respects. As assumed in the weathering causal relation between enhanced weathering hypothesis, enhanced hinterland weathering is and OAEs in northern Tethys region. This actually linked with the OAEs, and hinterland study explores, for the first time, the degree of weathering did precede the onset of the OAEs. continental paleoweathering during OAE 2 in Previous studies revealed that weathering of the Panthalassa Ocean. The extent of hinterland continental crust increased during OAEs in the paleoweathering was determined using the Tethys and proto-North Atlantic oceans. Our geochemical weathering index (W values) of data suggest that a similar phenomenon also mudstones from the Aptian to Campanian Yezo operated in the open ocean; i.e., in the Group, exposed in Hokkaido, northern Japan. Panthalassa Ocean. This indicates that The W values obtained for the Yezo Group enhanced hinterland weathering during the were in the range 30–50, which is equivalent to Middle Cretaceous was a global and pervasive the W values of recent soils that developed event that caused OAEs. under temperate mid-latitude climates. The W

148 P12: Bottom water paleothermometry: screening late Cretaceous calcareous nodules for

application of oxygen isotope method

Kobiyama, Y. 1, Yonezawa, S.1,2, Suzuki, T.1,3 and Hasegawa, T.1,4

1Schl. Nat. Sys., Coll. Nat. Sci. Tech., Kanazawa Univ., Kakuma-machi, Kanazawa 920-1192, Japan ([email protected]) 2Now at Mitsui Mineral Develop. Eng. Co., Ltd. 3Now at Itochu Oil Expl. Co. Ltd. 4Dept. Earth Sci., Fac. Nat. Sys., Inst. Nat. Sci. Eng., Kanazawa University

Paleothermometry is one of the most XRD analyses showed carbonate important proxies for paleoceanographers. mineral of the nodules studied here was calcite. Oxygen isotope paleothermometry has been a Structure suggesting consolidation just below major strategy for paleoceanographers. Benthic the sea floor includes burrows that eject foraminifers have been used for reconstructing calcareous material from site of nodule bottom water temperature through Cenozoic formation. The nodules consolidated associated and Cretaceous. Calcareous ooze from deep sea with anaerobic oxidation of methane with sediments are excellent material to extract them sulfate reduction appear to be “just below the while mudstone sequences including sediments sea bottom” origin. Such nodules show exactly distributed around Pacific shows substantial same oxygen isotope values with that of difficulty to apply this technique in terms of benthic foraminifers. A bivalve fossil found on preservation. Calcareous nodules are one of the methane seep nodules preserved commonly observed in mudstone sequences; shell aragonite and yielded close oxygen however, no study discussed potential isotope paleotemperature with that of host paleothermometry based on calcareous nodules. nodule. Carbonate content and oxygen isotope They are concretions formed in sediment, values had positive relation suggesting spherical, sub-spherical, plank-like, or irregular carbonate content was controlled by the depth in shape. Their physical and chemical of nodule production. Nodules with lower properties contrast well with those of host carbonate content (<50%) exclusively show mudstones and appear to better preserve low oxygen isotope values and inappropriate chemically fragile proxy signal. As the role for the sea bottom paleothermometry. supplementing benthic foraminifers for oxygen Study on nodules from the Haboro isotope thermometry is expected, calcareous area showed that selections in front of outcrops nodules were investigated as target meterials. and at laboratory enable us to select "high The nodules were collected from quality nodules" for oxygen isotope Cretaceous strata of several regions in paleothermometry. As the procedure of Hokkaido including Haboro area. We described oxygen/carbon isotope analysis of nodule their occurrences at outcrops, shape and surface material is simple, large number of analysis on structure of irregularity, internal structures and the selected nodules are available. The colors under vertically cut sections, SEM cross-plot of the data can emerge "upper limit observations, XRD characters, carbonate line" of oxygen isotope values. The content and total organic carbon content, then paleotemperature based on that value could analyzed carbon and oxygen isotopes using provide reliable temperature for the sea bottom. GasBench II preparation system connected to On the other hand, SEM observation showed Delta V advantage at Kanazawa University. that nodules with similar condition from the

149 Oyubari area appeared to be recrystalized and recrystallization of calcite with oxygen isotopes inappropriate for paleothermometry. It might as low as -10 permil in the nodule. be derived from the difference of burial depth Calcareous nodules with following between sediments of the Haboro and Oyubari characters provide materials to be investigated areas. Even if it was originally consolidated for oxygen isotope paleothermometry: near the bottom of the sea, strong compaction ichnofossils on the surface, with dark grey during burial would have caused permeation of color on the cut section, higher mud content, pore water into the nodule. Carbon dioxide or over 70% carbonate content, with no fossil bicarbonate ions derived from decomposed inside. Depositional history over Ro=0.6% organic matter would have caused would cause secondary cementation that mask original paleoceanographic signal

150 P13: Denudation stages of mid-Mesozoic accretionary complexes in East Asia based on

microfossil-bearing clasts within the Upper Mesozoic strata

Ito, T.1, Sakai, Y.2 Feng, Q.L.1 and Matsuoka, A.2

1China Univ. Geosci., Wuhan, 430074, China ([email protected]) 2Niigata Univ., Niigata, 950-2181, Japan

Upper Mesozoic neritic–terrestrial originated from the mid-Mesozoic ACs (Saida, strata in East Asia interbed conglomerates 1987). This occurrence suggests that the including microfossil-bearing clasts (e.g. Ishida initiation of denudation of the mid-Mesozoic et al., 2003; Ito et al., 2012). Some clasts were ACs started in the Tithonian. However, there assumedly derived from mid-Mesozoic are a few reports of mid-Mesozoic-AC-derived accretionary complexes (ACs) in East Asia (inc. clasts in previous studies, suggesting the the Tamba-Mino-Ashio, Chichibu composite, denudation in the term is narrow in extent. Samarka, Khabarovsk, Taukha and other Meanwhile, the stratigraphic position of the terranes). Some researchers have discussed the interbedded microfossil-bearing clasts and its initiation of the denudation of the age is not fully elucidated. Further studies of mid-Mesozoic ACs (Takeuchi et al., 1991; the clasts within the Kamihambara Formation Matsukawa and Takahashi, 1999; Kamata et al., together with the age assignment of the 2000), whereas few studies have highlighted formation are important for the estimation of staged denudation of the mid-Mesozoic ACs. the timing of the initial denudation in more We have researched microfossil-bearing clasts detail. within the Tetori Group in the Inner Zone of Stage B (Barremian–early Albian) is Southwest Japan in recent years (e.g., Ito et al., characterized by wide denudation and supply of 2012, 2014, in press). This study compiles Jurassic clasts. This stage is characterized by previous reports of microfossil-bearing clasts wide denudation. Microfossil-bearing clasts within the Upper Mesozoic in the Inner Zone of presumed to be originated from the Southwest Japan and in the southeastern mid-Mesozoic ACs have occurred in the Korean Peninsula, in addition to our data. As a following formations corresponding partially to result, three denudation stages (Stages A, B and the Barremian–early Albian: the Mizukamidani, C) are recognized. Itsuki, Donghwachi, and Kumidong formations, A pre-stage (–Kimmeridgian) is the Lower Formation of the Sasayama Group, characterized by no-denudation. the Yakushizawa-migimata Conglomerate Microfossil-bearing clasts have occurred in Member, and the Kurobishiyama Conglomerate. some pre-Kimmeridgian strata in the Inner Additionally, this stage is characterized by Zone of Southwest Japan, such as the Kuruma, supply of Middle Jurassic clasts. Middle Nariwa and Maizuru groups. However, these Jurassic radiolarians occurred in chert clasts clasts have yielded only Permian radiolarians within the Itsuki Formation (Ito et al., in press) which are able to be originated from (Fig. 1A) and a siliceous mudstone clast within pre-Mesozoic units (e.g. Akiyoshi and Maizuru the Mizukamidani Formation (Ito et al., 2014) terranes). (Fig. 1B). Based on a zircon U–Pb dating, the Stage A (Tithonian–Hauterivian) is youngest zircon grain from the sandstone of the characterized by initial and narrow denudation. lower Itsuki Formation has a concordant age of The Kamihambara Formation, which 127.2 ± 2.5 Ma (Kawagoe et al., 2012); the corresponds at least partially to the Tithonian youngest zircon grain extracted from sandstone based on the ammonoid occurrence, interbeds of the Mizukamidani Formation has a microfossil-bearing clast presumed to be concordant age of 128 Ma (Takeuchi et al., 151 2013). Based on the general features of the these radiolarian origins are uncertain. mid-Mesozoic ACs, the former clast was Tithonian radiolarians have occurred in the derived from Middle or early Late Jurassic ACs Early Cretaceous ACs in the mid-Mesozoic and the latter clasts were derived from the late ACs (e.g. Matsuoka et al., 1998), which are Middle Jurassic or younger ACs. nearly the youngest in the mid-Mesozoic ACs. Stage C (late Albian–) is characterized Consequently, if the Tithonian radiolarians by denudation of all-age of the mid-Mesozoic were not derived from a matrix but a clast, accretionary complexes. This stage is Tithonian microfossil-bearing clasts started to characterized by denudation of almost-all-age be supplied by the depositional time of the of the mid-Mesozoic ACs. Clasts within the Kisadong Formation in the provenance of the Kisadong Formation yielded Tithonian Hayang Group. radiolarians (Kamata et al., 2000), although

Figure 1. Scanning electron microscope images of etched surfaces of siliceous rock clasts including radiolarian tests of

the Tetori Group in the Inner Zone of Southwest Japan (after Ito et al., 2014, in press). A: Middle Jurassic chert clast (IT13050313-2) of the Itsuki Formation in the Taniyamadani valley. B: Middle Jurassic siliceous mudstone clast (IT12050102-1) of the Mizukamidani Formation in the Itoigawa area. White arrows indicate conspicuous radiolarian tests.

References: Ishida, K., Kozai, T., Park, S.O., Mitsugi, T., 2003. Gravel bearing radiolarian as tracers for erosional events: a review of the status of recent research in SW Japan and Korea. J. Asian Earth Sci., 21, 909–920. Ito, T., Sakai, Y., Feng, Q.L., Matsuoka, A., in press. Middle Jurassic radiolarians from chert clasts within conglomerates of the Itsuki Formation of the Itoshiro Subgroup (Tetori Group) in the Taniyamadani Valley, Fukui Prefecture, central Japan. Sci. Rep. Niigata Univ. (Geol), 30. Ito, T., Sakai, Y., Ibaraki, Y., Matsuoka, A., 2014. Middle Jurassic radiolarians from siliceous mudstone clast within the Tetori Group in the Itoigawa area, Niigata Prefecture, central Japan. Sci. Rep. Niigata Univ. (Geol.), 29, 1–11. Ito, T., Sakai, Y., Ibaraki, Y., Yoshino, K., Ishida, N., Umetsu, T., Nakada, K., Matsumoto, A., Hinohara, T., Matsumoto, K., Matsuoka, A., 2012. Radiolarian fossils from siliceous rock pebbles within conglomerates in the Mizukamidani Formation of the Tetori Group in the Itoigawa area, Niigata Prefecture, central Japan. Bull. Itoigawa City Mus., 3, 13–25 (in Japanese with English abstract). Kamata, Y., Hisada, K., Lee, Y.I., 2000. Late Jurassic radiolarians from pebbles of Lower Cretaceous conglomerates of the Hayang Group, southeastern Korea. Geosci. J., 4, 165–174. Kawagoe, Y., Sano, S., Orihashi, Y., Obara, H., Kouchi, Y., Otoh, S., 2012. New detrital zircon age data from the Tetori Group in the Mana and Itoshiro areas of Fukui Prefecture, central Japan. Mem. Fukui Pref. Dinosaur Mus., 11, 1–18. 152 Matsukawa, M., Takahashi, O., 1999. Radiolarian fossils occurred from the Itoshiro Subgroup of the Tetori Group and its geological significance. Abst. 106th Ann. Meet. Geol. Soc. Japan, 165 (in Japanese). Matsuoka, A., Yamakita, S., Sakakibara, M., Hisada, K., 1998. Unit division for the Chichibu Composite Belt from a view point of accretionary tectonics and geology of western Shikoku Japan. J. Geol. Soc. Japan, 104, 634–653 (in Japanese with English abstract). Saida, T., 1987. Triassic and Jurassic radiolarians in chert clasts of the Tetori Group in Tamodani area of Izumi Village, Fukui Prefecture, central Japan. J. Geol. Soc. Japan, 93, 57–59 (in Japanese). Takeuchi, M., Kawahara, K., Tomita, S., 2013. Development of sedimentary basin of the Lower Cretaceous Tetori Group in the northeast Toyama Prefecture, based on clast composition and age distribution of detrital zircon. Abst. 120th Ann. Meet. Geol. Soc. Japan, 81 (in Japanese). Takeuchi, M., Saito, M., Takizawa, F., 1991. Radiolarian fossils obtained from conglomerate of the Tetori Group in the upper reaches of the Kurobegawa River, and its geologic significance. J. Geol. Soc. Japan, 97, 345–359 (in Japanese with English abstract).

153 P14: New view of the Tetori Group in Central Japan: clues to the interregional correlation

among the Early Cretaceous strata in East Asia?

Sano, S.

Fukui Pref. Dinosaur Mus., Katsuyama, Fukui 911-8601, Japan ([email protected])

The Tetori Group, mainly composed 100 Ma volcanism (e.g., Hayashidani Andesite: of Late Mesozoic siliciclastic rocks deposited Tanase et al., 1994) in this region are in shallow marine to terrestrial environments, is summarized as below, and divided into four sporadically but widely distributed in the depositional stages (DS1 to 4, in ascending northern Central Japan, which was located in order) here. the eastern margin of the Asian Continent at DS1 (Bathonian–Oxfordian), is that time. Recently its rich vertebrate fauna and represented by the Kuzuryu Subgroup (Maeda, flora in the Early Cretaceous attract much 1961) in the Itoshiro area, which is mainly attention to reveal the evolution of Mesozoic composed of marine deposits corresponding to terrestrial ecosystem in East Asia. Most parts of transgression stages Ia (late Bathonian–Early the Tetori Group deposited in the Hida Belt Callovian) and Ib (Oxfordian) of Sano et al. (North China Block), and some parts in the (2013). Hida Gaien Belt (un-metamorphosed DS2 (Berriasian–Barremian) is almost Ordovician to Triassic strata, high pressure represented by the Itoshiro Subgroup (Maeda, metamorphic rocks, serpentine, etc., forming 1961), which is composed of marine to tectonic zone: the Hida Gaien Belt). Its age has freshwater deposits, and characterized by the been considered as Middle Jurassic (Bathonian) occurrence of endemic brackish bivalves, to Early Cretaceous (Aptian?) based on the Myrene (Mesocorbicula) tetoriensis and ammonite fossils in its lower part and Tetoria yokoyamai. Transgression stages IIb non-marine bivalves in its uppermost part. (Berriasian) and III (Hauterivian–Barremian) Previously, threefold division of the Tetori of Sano et al. (2013) are recognized in this Group, namely Kuzuryu, Itoshiro and Akaiwa stage. U-Pb age data in the Tedori-gawa subgroups in ascending order, were proposed, (Setono) and Itoshiro areas indicates about and applied to the strata in all the distributional 131–127 Ma for the late stage of DS2 areas of the Tetori Group (e.g., Maeda, 1961; (Kusuhashi, 2008; Kawagoe et al., 2012). Kusuhashi et al., 2002; Fujita, 2003). New DS3 (Barremian–Aptian?) is almost discoveries of ammonoid fossils and applying represented by the Akaiwa Subgroup (Maeda, detrital zircon LA-ICPMS U-Pb dating revise 1961), which is composed of freshwater the age of the lower and middle part of the deposits only, and is characterized by the Tetori Group (Sano et al., 2013 and references freshwater bivalves, similar to those of the therein). Furthermore, it is revealed that Kwanmon (Southwest Japan) and Gyoengsang stratigraphy of the Tetori Group in the Hida (southern Korea) areas. Famous terrestrial Belt and that in the Hida Gaien Belt is biota-bearing horizons in the Tetori Group significantly different from each other, though occur in the early stage (Kuwajima, Okurodani it was previously considered that same and Itsuki formations) and also in the late stage formations are distributed in both tectonic (Kitadani Formation) of DS3. Age of DS3 is belts. not well-established. Paleomagnetic study in This study mainly focuses on the the Tedori-gawa (Shiramine) area suggested stratigraphy of the Tetori Group in the Hakusan early stage of DS3 predated the Long Region, where type localities of the subgroups Cretaceous Normal (C34n) (Kunugiza et al., of the Tetori Group are located. The 2002). Charophyte zygote fossils from the stratigraphy and age of the Tetori Group and ca. Kitadani Formation indicated its Barremian age 154 (Kubota, 2005). On the other hand, a 100Ma age are recognized widely in the whole trigonioidid bivalve, Plicatounio (Plicatounio) Tetori area. naktongensis, known from the Kitadani Stratigraphy of the Tetori Group in the Formation, is considered to appear in the Hakusan Region of the Hida Belt and that in Aptian of East Asia (Sha et al., 2012). Thus it the Hida Gaien Belt is significantly different is suggested that the late stage of DS3 possibly from each other. The traditional Tetori Group extends to the Aptian age. can be divided into several groups and The boundary between DS2 and DS3 formations: e.g., the Kuzuryu Group are here defined based on the last horizon of (Bathonian–Oxfordian) and the Tetori Group brackish or marine deposits or the last (Berriasian–Aptian?) in the Hakusan Region, occurrence of brackish water bivalves in each and the Managawa Group (Oxfordian–Aptian?) depositional area. The timing of separation in the Hida Gaien Belt (Kobayashi, 1954; Sano from marine or brackish environment is et al., 2013). A long term change of probably slightly different among the depositional environments and also the depositional areas, but can be considered as presence of several geological events are almost same or similar in the broad sense in the clearly recognized in the “Tetori Group” in the whole Tetori area, because no unambiguous Hakusan Region: a few transgressive stages marine and brackish records after (TS Ia, Ib, IIb, III) in DS1 and DS2; relatively Hauterivian–Barremian time has been small-scale basin formation in DS1a and DS1b; recognized, and fluvial environment with hiatus in the Kimmerigdian-Tithonian; abundant quartzose sandstone gravels is expansion of brackish environment in DS2a; prevailed in the upper part of the Tetori Group start of basin formation in many areas of whole Tetori area. In addition, there is the (including the wide distribution in the controversy of the affinity of some formations, Shiramine and Takinamigawa areas) in DS2b; such as the Amagodani Formation in the and uplift (corresponding to the change from Shokawa area, to the Itoshiro or Akaiwa brackish to freshwater environments) in the subgroups. In the definition here proposed, the Barremian-Aptian; the presence of TPN boundary between DS2 and DS3 does not freshwater bivalve assemblage, thermophilic correspond to the boundary between Itoshiro plants and pedogenetic calcareous nodules in and Akaiwa subgroups of Maeda (1961), and is DS3. Furthermore, DS4 represents located within the Kuwajima Formation in the Albian–Cenomanian volcanic episodes, Tedori-gawa (Shiramine) area and the recognized in the whole Tetori area. Such Okurodani Formation in the Shokawa area. geological events in the Tetori area can be DS4 (late Albian to early compared to those in the coeval basins in East Cenomanian) is represented by the Hayashidani Asia, and thus possibly provide useful clues to Andesite in the Itoshiro area, which their interregional correlation, and unconformably overlies the Tetori Group. subsequently contribute to the discussion of the Similar volcanic and intrusive rocks of ca. evolution of Mesozoic terrestrial biota in East Asia.

References: Kawagoe et al., 2012. Mem. Fukui Pref. Dinosaur Mus. 11: 1‒18. Kobayashi, 1954. Res. Bull. Geol. Mineral. Inst., Tokyo Univ. Edu. 3: 35‒42. Fujita, 2003. Mem. Fukui Pref. Dinosaur Mus. 2: 3‒14. Kubota, 2005. Paleont. Res. 9: 203‒213. Kunugiza et al., 2002. Report of the Researches of the Mesozoic Tetori Group in the Tedori River Area, Ishikawa Prefecture. 71‒87. Kusuhashi, 2008. Acta Palaeont. Polonica 53: 379‒390. Kusuhashi et al., 2002, Mem. Fac. Sci. Kyoto Univ., Ser. Geol. Mineral. 59: 9‒31. Maeda, 1961. J. Coll. Arts Sci., Chiba Univ. 3: 369‒426. Sano et al., 2013. Mem. Fukui Pref. Dinosaur Mus. 12: 1‒16. Sha et al., 2012. J. Strat. 36: 357‒381. Tanase et al., 1994. J. Geol. Soc. Japan 100: 635‒638. Yabe et al., 2003. Mem. Fukui Pref. Dinosaur Mus. 2: 23‒42. 155 Yamada and Uemura, 2008. Paleont. Res. 12: 1‒17.

P15: Provenance analysis of Lower Cretaceous Sindong Group sandstones in the

Gyeongsang Basin, Korea using integrated petrography, quartz SEM-cathodoluminescence, and zircon Zr/Hf analysis

Lee, Y.I.1, Yi J.*1,2 and Choi, T.3

1Schl. Earth Env. Sci., Seoul Nat. Univ., Seoul 151-747, Korea 2KEPCO Eng. & Constr. Comp., Inc., Yongin, Gyeonggi-do 446-713, Korea 3Dept. Energy and Res. Eng., Chosun Univ., Gwangju 501-759, Korea

The Sindong Group (Aptian-Albian) episodic increasing in volume of plutonic in southeastern Korea is a 2-3 km thick quartz content in the sequence, especially in the fluvio-lacustrine sedimentary package northern part of the basin, suggest that episodic deposited in an elongated basin (Nakdong tectonic activities occurred in the catchment. Trough), which was formed by extension in an The increasing feldspar content up sequence active continental margin setting. The could support the occurrence of tectonic provenance of the Sindong Group was studied activity in the catchments. Thus, the Zr/Hf to understand spatial and temporal variation in analysis of detrital zircons revealed that the composition in three different parts of the basin majority of zircons are of continental crust by using integrated data of petrography, quartz origin formed in orogenic settings, but zircons SEM-cathodoluminescence (CL) analysis, and in the lowest strata in the northern part of the zircon Zr/Hf analysis. Although Sindong Group basin were largely derived from anorogenic sandstones display wide variation in the magmatic rocks of mantle origin. Our results composition of framework grains, they demonstrate that source terrains for the generally have increasing amounts of feldspar Sindong Group were mainly composed of and decreasing amounts of quartz up sequence. Precambrian basement and Triassic-Jurassic Significant amounts of volcanic rock fragment granitic rocks, with minor (meta)sedimentary and volcanic quartz are observed in the rocks and syndepositional volcanic rocks. The late-stage sediments. Metamorphic quartz is detritus derived from syndepositional volcanic predominant in all Sindong Group sandstones, rocks became significant in the late stage of indicative of the exposure of metamorphic basin-filling. The spatial distribution of these rocks in the source terrain, mostly from source-rock types was heterogeneous, with Precambrian basement and Triassic granites. slight temporal variation. The differences in The occurrence of significant amounts of quartz SEM-CL and zircon Zr/Hf ratio plutonic quartz from early-stage sediments characteristics in different parts of the basin are suggests that Jurassic granites were widely best explained by deposition on different exposed in the source terrains. In addition, the alluvial fans and river systems.

156 P16: Provenance analysis of clastic sediments of the Chichibuand Shimanto Belts in

Okinawa Prefecture using modal and whole-rock chemical compositions

Hirose, K.1 and Ohta, T.2

1Graduate School of Creative Science and engineering, Waseda University, Tokyo, Japan 2Faculty of Education and Integrated Arts and Science, Waseda University, Tokyo, Japan Email: [email protected]

Clastic compositions of the Jurassic abundant quartz grains than do sandstones of Chichibu Belt and the Cretaceous Shimanto the Shimanto Belt distributed in other areas of Belt in Okinawa Islands had not been fully Japan. In contrast, plagioclase grains and investigated, and their provenance had been K-feldspar grains are scarcer than those results. unknown. In this regard, the present study aims From the amount of rock fragments, it was hard to unravel provenance of the Iheya and Motobu to find out the differences. Particularly, Complexes of the Chichibu Belt, and the Nago sandstones of the upper Albian unit were the and Kayo Complexes of the Shimanto Belt, most quartzose and matured. Similarly, the which are distributed in eastern regions of Nago and Kayo complexes have high SiO2 Okinawa and Iheya Islands. Provenances of amounts. On the Al2O3/SiO2-Basicity Index these sediments were analyzed by sandstone diagram (Kiminami et al., 2000), a tendency of modal and whole-rock chemical compositions. maturation during the late Albian was obscure. The Chichibu Belt in Okinawa Islands Sandstones of the Shimanto Belt except for the is subdivided into the Iheya Complex (Early upper Albian sediments indicate a mature Jurassic to Middle Jurassic; Takami et al., sedimentary provenance on 1999) and the Motobu Complex (Valanginian SiO2/Al2O3-NaO2/K2O diagram (Ohta, 2004). to Hauterivian; Fujita, 1989). The Nago and From the results of the present Kayo Complexes are distributed further south analyses, the Shimanto Belt in the Okinawa bounded by the Butsuzo Tectonic Line. The area showed relatively matured compositions. accretionary age of the Nago Complex is These results possibly indicate that continental poorly determined owing to the high arc in Oknawa area had been uplifted, allowing metamorphic grades and lack in fossil records supply of mature basement derived-detritus (Osozawa and Watanabe, 2011). However, the into the trough during late Albian stage. Also, accretionary of the Nago Complex is estimated volcanic activities should have been quiescent to be Albian (Chinen et al., 2004). Nummulites during the formation of the late Albian found from the Kayo Complex indicates accretionary wedge, because upper Albian Eocene age of accretion (Konishi et al., 1973). sediments lack volcanic lithic grains. Therefore, The results of point-counting of our result suggests a prominent event of sandstones were examined by the Dickinson’s basement uplift and volcanic quiescent during triangular diagrams. Modal compositions of the the late Albian in the southern continental Nago and Kayo Complexes indicate that margin of Asia. Further studies are necessary to sandstones were derived from recycled orogeny. reveal the actual cause of such event. These complexes generally contain more

References: Chinen, T., Shinjo, R.and Kato, Y. 2004. Occurrence and geochemistry of in-situ greenstrones from the Shimanto Belt in the Ryukyu Islands. Jour. Mineral. Petrol. Sci. Japan, 33, 208-220.

157 Fujita, H. 1989. Stratigrphy and geologic structure of the pre-Neogene strata in the central Ryukyu Islands. Jour. Sci, Hiroshima Univ. [C], 9, 237-284. Kiminami, K., Kumon, F., Miyamoto, T., Suzuki, S., Takeuchi, M. and Yoshida, K. 2000. Revised BI diagram and provenance types of the Permian-Cretaceous sandstones in the Japanese Islands. Mem. Geol. Soc. Japan, no. 57, 9-18. Konishi, K., Ishibashi, T. and Tsuruyama, K. 1973. Find of Nummulites and orthoquartzitic pebbles from the Eocene turbidites in Shimajiri Belt, Okinawa. Sci. Report. Kanazawa Univ, 18, 43-53. Ohta, T. 2004. Geochemistry of Julassic to earliest Cretaceous deposits in the Nagato Basin, SW Japan: implication of factor analysis to sorting effects and provenance signatures. Sediment Geol, 171, 159-180. Osozawa, S. and Watanabe, Y. 2011. Chapter 9: Cretaceous Nago complex, Inogama Unit. In Osozawa, S. and Watanabe, Y. (Eds), Geology of Nago and Yambaru District (pp. 67-74). Okinawa, Japan: Nago Museum. Takami, M., Takemura, R., Nishimura, Y., Kojima, T. 1999. Reconstruction of oceanic plate stratigraphies and unit division of Jurassic-Early Cretaceous accretionary complexes in the Okinawa Islands, central Ryukyu Island Arc. Jour. Geol. Soc. Japan, 105, 866-880.

158 P17: Provenance and paleoclimate during Cretaceous in northeastern Thailand:

Mineralogy and geochemistry of the Khorat Group

＊ Oe, K.1 and Ohta, T.2

1 Grad. Schl. Creat. Sci. Eng., Waseda University, Tokyo, Japan ([email protected]) 2Fac. Edu. Integ. Arts Sci., Waseda University, Tokyo, Japan ([email protected])

The Upper Triassic to Upper Result of provenance analysis Cretaceous Khorat Group is a non-marine conducted by the MFW diagram suggests that deposit widely distributed in the Khorat Plateau, clastics of Khorat Group were supplied from northeastern Thailand. It mainly consists of andesitic volcanic rocks. Consequently, the red-beds and characteristically includes most probable candidate of the provenance of evaporite minerals (e.g. calcrete and gypsum). the Khorat Group was the Permian to Triassic This fact suggests that although Thailand Had Sukhothai volcanic arc. been located in a tropical rainforest climate The W values of the Upper Jurassic region, several aridification events occurred Phu Kradung Formation shows wide range of during the Late Mesozoic era. The purpose of scatter, but the values suggest a humid-arid this study is to unravel climate system at Asian climate regime. Those of the Lower Cretaceous low-latitude areas during the Late Mesozoic. Phra Wihan Formation retain high values and For this, we utilized the whole-rock chemical suggest a tropical rainforest climate. Therefore, composition of Khorat Group to reconstruct its the Mesozoic climatic system in Thailand had provenance and paleoclimate. generally been tropic and humid. However, the The Khorat Group consists of Lower Cretaceous Sao Khua Formation shows following 8 formations in the ascending order: low W values, which are suggestive of an arid The Upper Triassic Nam Phong Formation, the climate. The clay mineral compositions of the Jurassic Phu Kradung Formation, the Lower Sao Khua Formation detected by the XRD also Cretaceous Phra Wihan Formation, Sao Khua implied an arid climate, as suggested by the W Formation and Phu Phan Formation, the middle values. Mudstones of the Phu Kradung Cretaceous Khok Kruat Formation and Maha Formation and Sao Khua Formation include Sarakham Formation, the Upper Cretaceous substantial amounts of carbonate minerals, Phu Thok Formation. These formations are which imply an arid climatic regime. Whereas mainly fluvial red beds. However, the Phu those of the Phra Wihan Formation included Thok Formation consists of both fluvial and kaolinite, normally produced in highly aeolian deposits (Meesook, 2011). weathered tropical rainforest environment. In We analyzed whole-rock chemical summary, our results indicate that the compositions of mudstone and sandstone paleoclimate in Thailand area during Late samples by X-ray fluorescence (XRF) and Jurassic-Early Cretaceous had a cyclic turnover evaluated conditions of hinterland being arid-humid climate. The results further paleoweathering using the W index (Ohta and indicate that mid-Cretaceous was the time of Arai, 2007). In addition, we compared the W severe aridification. values of the Khorat Group with those of the Similarly, Hasegawa et al. (2012) present soil in order to determine paleoclimate recently reviled the arid-humid climatic cycle in Thailand. Furthermore, clay mineral in Thailand during Early Cretaceous by the compositions of mudstone samples were sedimentary facies analysis and especially determined by X-ray diffraction (XRD) suggested that paleoclimate during middle analysis. Cretaceous was arid corresponding to the desert environment. They further introduced a 159 hypothesis called “shrinkage of Hadley mid-Cretaceous probably arose perturbation to circulation” during mid-Cretaceous global the atmospheric general circulation regime. warmth period to explain desertification of Consequently, paleoclimate reconstruction low-latitude areas. The results of present study during middle Cretaceous in low-latitude Asian is concordant with those proposed by areas is important to understand peculiar Hasegawa et al. (2012) by the facies analysis responses of the climate system during global and supports “shrinkage of Hadley circulation greenhouse periods. hypothesis”. The extreme global warmth during

References: Hasegawa, H., Tada, R., Jiang, S., Suganuma, Y., Imsamut, S., Charusiri, P., Ichinnorov, N., Khand, Y., 2012. Drastic shrinking of the Hadley circulation during the mid-Cretaceous Supergreenhouse. Climate of the Past., 7, 119-151. Meesook, A., 2011. Cretaceous. In: Ridd, M.F., Barber, A.J., Crow, M.J. The Geology of Thailand. Geol. Soc., London, pp. 169–184. Ohta, T. and Arai, H., 2007. Statistical empirical index of chemical weathering in igneous rocks： A new tool for evaluating the degree of weathering. Chem. Geol., 240, 280-297.

160 Biotic evolution: Asian and western Pacific fauna and flora

P18: Litho- and biofacies association of two Maastrichtian lakes across the earliest Deccan

volcanic flow: environments and biota

*Mohabey D. M. and Samant, B.

Postgrad. Dept. of Geol. RTM Nagpur Univ., Amravati Road, Nagpur-440001, India.

Email- [email protected]; [email protected]

* Ex. Geol. Surv. India

The integrated study of volcanic and well-developed lake sequence in from the associated sedimentary and biotic processes is Nand-Dongargaon basin (Mohabey, et al., important for assessing the impact of Deccan 1993). volcanism on the contemporary environments. The present investigation was taken up The studies of lake sequences in this context in the N-D basin for the study of the well are critical as they are considered as archives of preserved lake sequence of the Lameta continental and climatic history. The Formation and the Daiwal lake sequences non-marine Late Cretaceous sediments of the developed across the basal most Deccan Lameta Formation which are associated with volcanic flow in the area. The sediments of the the Deccan volcanism (69-62 MY, Sheth et al. two lakes are separated in time by the first 2001, 2014) represent the deposits just before Deccan basalt flow arriving in the basin and are the arrival of first volcanic flows in the basin. geographically separated by a distance of 16 The Lameta sediments are mainly deposited in km. The investigation was focused on different geographically separated inland basins, detailed litho-facies and bio-facies analysis of viz. Nand-Dongargaon (N-D) in (Maharashtra); the Lameta Formation for depositional and Jabalpur, Sagar, Ambikapur-Amarkantak in environmental interpretation of the sediments Madhya Pradesh, Balasinor-Jhabua-Bagh resulting in delineating different lithofacies viz. (Gujarat and adjoining Madhya Pradesh) and over-bank, channel, lake and paludal deposits Salburdi (Amravati-Maharashtra and under semi-arid to arid conditions having Betul-Madhya Pradesh). The detailed strong seasonality. The Lameta sediments of sedimentary analysis is available through the the N-D basin are considered as deposits of work of (Brookfield and Sahni, 1987, Mohabey magnetochron C30n-C29 of Maastrichtian et al. 1993, 1996, Mohabey and Udhoji, 1996, (Hansen et al. 2005). The sediments are Mohabey and Samant, 2005, Tandon et al. pedogenically modified with presence of 1995). The sediments are deposits of characteristic calcrete profiles and red beds in alluvial-limnic environments under semiarid the Lameta sequence. This study was followed climate and are time-transgressive that are by the detailed analysis of the two lake deposited during the Maastrichtian sequences designated as the Dongargaon lake magnetochron C30n to C29r in different basins (Lameta, below the first flow) and the Daiwal (Hansen et al. 2005). However, the lake lake (intertrappean sedimentary bed between sequences from the Late Cretaceous Lameta the first two Deccan volcanic flows). Formation remained eluding excepting a 161 1. Dongargaon Lake deccanes. The palynomorphs recovered from It is developed over an area ca. 60 km2 the lake facies, include Araucariacites, (200 00' 00"-200 15' 30" N:790 04' 00"-790 09' 00" Cycadopites, Palmepollenites and a few E) in the southern extremity of the N-D basin tricolpate. A monogeneric diatom assemblage that occupies a little over 700 km (200 10' dominated by a couple of Aulacoseira species 00"-210 10' 00'' N: 790 00' 00"-790 30' 00" E) in (Mohabey, 2001) are present in the varved the state of Maharashtra in central India. couplets (FVC) deposited during the (a) Lithofacies association: The magnetochron C30n, Mastrichtian. This is the sediments are indicated to be deposits of a large oldest record of the freshwater diatoms from open shallow water lake. The different the Late Cretaceous of India from the Indian lithifacies of the 20m thick cyclically bedded subcontinent. Associated bones of lake sequence are i) Clay-silt facies (FSC), ii) titanosauriform sauropods are found in the lake Limestone-carbonate mud facies (FLC), iii) in the FSCN (Mohabey and Samant 2005). Septerian concretionary facies (FSCN), iv) Seventeen species of freshwater ostracods have Varved/rhythmite clay facies (FVC), v) been described (Khosla et al. 2005) from the Fibrous/radial calcite (crypalgal) facies (FRC) FSC facies of the lake deposited during C30n. and vi) Sandy gravel facies (FSG). Two types The Dongargaon lake ostracods show no of cyclic patterns observed in the sediments are affinity with the ostracoda fauna from the i) varved clays (FVC) facies separated at least younger Lameta sediments at Jabalpur at four levels by mudstone-green clay partings deposited during the magnetochron C29r. in the lower part of the sequence and ii) Fine The evaporite facies is almost absent silici-clastic (FSC) and carbonate (FLC) cycles in the lake sequence, though minor evaportic mostly observed in the upper part of the phases of the lake is indicated by presence of sequence. Deposition of fine silici-clastic gypsum pyramid in the silici-clastics (FSC). (FSC) is interrupted at multiple levels by thin Algal domal tuffa like structures (FRC), limestone-carbonate mud facie (FLC). The FSC mud-cracks and septerian concretions and case associated with the gypsiferous clays is hardening may have formed during the lake interpreted as deposits of open shallow water transgression and its subsequent prolonged lake during the high strand (wet season) of the emergence. The lake sealing by aggrading lake was periodically witnessed deposition of alluvial system is evident as observed in the the carbonates (dry season). The carbonates are Dongargaon Hill sections. The contraction of interpreted as deposits of the lake having an the Dongargaon lake is related to the alkaline and excessive evaporative condition. simultaneous Deccan volcanic activity. The presence of well-defined cyclic pattern and 2. Daiwal Lake the rhythmites (varved clays) in the sediments The lake deposits at Daiwal occur are suggestive that they are related to seasonal between the two lowermost Deccan volcanic changes. flows outpoured with the initiation of the in (b) Palynology of Lake Sediments: Of Deccan volcanism in the N-D basin. Of this the all the lithofacies of the Dongargaon lake basal most flow covers the sediments of the sequence only palustrine carbonates comprising Lameta Formation. The Daiwal lake gray nodular marl and marlite from Polgaon geographically located nearly 16 km WNW of and Pisdura have yielded relatively a rich the Dongargaon lake. pollen and spore assemblage and megaflora (a) The outcrops of the Daiwal lake (Samant and Mohabey, 2003). The presence of sediments are spread over an area of ca. 6 km 2 the megaflora as well as the microflora from exposed along the Daiwal river section the Lameta sediments of the N-D is poor. The between the villages of Panjurni and Nandra. overbank green and red clays and channel The sediment thickness varies between less related facies has hardly yielded any significant than 10 cm along the flanks (shore area) to 400 palynomorphs. from the palustrine facies. The cm in the central and deeper part of the lake. megaflora comprise (Araucarites, The basal contact of the Daiwal lake sequence Brachiophyllum, Pagiophyllum, Equisetites) with the lowest flow (F-1) is undulating and angiosperms- palm and dicot leaf suggesting weathered and draping lava surface impressions and wood fragment of palms, over which the lake formed and sediments were Euphorbioxylon and Barringtonioxylon deposited. The upper contact shows truncated 162 top with caught-up sediments of the lake. The scarce or few in the assemblage. The section comprises white and cream porcellinite, palynotaxa recovered comprise shales, biscuity laminated clays and dark gray Cicatricososporites sp., Gabonisporis to black inter-banded cherts in the basal part vigouroxii, Osmundacidites sp., and massive pink and buff chert at the top. The Lygodiumsporites sp., Triporoletes reticulates, sediments are buckled and folded. The thin Azolla cretacea, Callialasporites sp., bandings in the chert and porcellinitic shales Aquilapollenites bengalensis, Echitricolpites, also show microfaulting. This probably sp., Echimonocolpites sp., Palmaedites sp., suggests that the intertrappean lake sediments Proxapertites operculatus, Racemonocolpites were deposited under tectonically stressed maximus, Racemonocolpites sp., Tricolpites sp. condition possibly induced by Deccan volcanic and Tripoporotetradites triporatus. activity. The palynoflora is observed to be most Stratigraphically upwards in the lake sequence prolific in the chert bands compared to the an increase in the abundance and diversity of shales and clays in the sequence. The the angiosperm pollens is observed. dominance of the chert in the sequence could Our study of the Dongargoan Lake be owing to volcanically induced acid rains that sediments deposited prior to the arrival of mobilised and dissolved silica from the earliest Deccan flows in the N-D basin and the provenance and deposited in the lake. Fresh Daiwal lake sediments deposited between the water gastropods (Melania), ostrocods two lowermost basaltic flows during the period (Cyprididae) and fishes (Lepidotes, Clupeids) of pause in the volcanic suggests that they are show their prominent presence in the shales deposits of the different environments. The and clays. former is deposited in a large open shallow lake (b) Palynology: The sediments yielded in semiarid to arid conditions with strong abundant and diverse spores, pollen and seasonality (wet and dry conditions), whereas dinoflagellate cysts. In addition, cuticular the latter are deposited in a closed shallow lake material, hard woody tissues as well as fungal formed over a fresh lava surface under spores are common in addition to fruit bodies sub-humid conditions. A change from the of epiphyllus fungi microthyriaceae. angiosperm-gymnosperm to Dinoflagellates (cf. Peridinium including a angiosperm-pteridophyte dominating couple of new species, manuscript under vegetation with appearance of Peridinium preparation) dominate the assemblage followed dinoflagellates is evident. The change in the by angiosperm pollen grains and pteridophytic depositional environments and vegetation spores. However, qualitatively the angiosperms scenario across the earliest volcanic flows is show more diversity than the pteridophytes and suggested to be an impact of initiation of dinocysts. Gymnosperm pollen grains are Deccan volcanism in the N-D basin.

References: Brookfield, M. and Sahni, A., 1987. Palaeoenvironments of Lameta beds (Late Cretaceous) at Jabalpur, Madhya Pradesh, India: Soils and biotas of semiarid alluvial plain. Cret. Res., v. 8, 1-14. Hansen, H.J., Mohabey, D.M. Lojen, S., Toft, P and Sarkar, A., 2005. Orbital cycles and stable Carbon isotopes of sediments associated with deccan volcanic suite, india: Implications for the stratigraphic correlation and Cretaceous/Tertiary Boundry. Gond. Geol. Magz. Spl. v. 8, 5-28. Mohabey, D. M., 1996. Depositional environment of Lameta formation (Late Cretaceous of Nand-Dongargaon inland basin, Maharashtra: the fossil and lithological evidences. Mem. Geol. Soc. India, v. 37, 363-386. Mohabey, D.M., 2001. Dinosaur eggs and dung mass (fecal mass) from Late Cretaceous of central India. Geol. Surv. india, Spl. Publ., v. 62, 605-615. Mohabey, D. M. and Samant, B., 2005. Lacustrine facies association of Maastrichtian Lake (Lameta Fm) from Deccan Volcanic terrain central India: implications to depositional history, sediment cyclicity and climates. Gond. Geol. Magz., Spl. v. 8, pp. 37-52. Mohabey, D. M., Udhoji, S. G. and Verma, K. K., 1993. Palaeontological and sedimentological observations on non-marine Lameta Formation (Upper Cretaceous) of Maharashtra, India: 163 their Palaeoecological and Palaeo-environmental significance. Palgeo. Palclim. Palecol. v. 105, 83-94. Samant B. and Mohabey, D.M., 2005. Response of flora to Deccan volcanism, a case study from Nand-Dongargaon basin of Maharashtra, implications to environment and climate. Gond. Geol. Magz. Spl. v. 8, 151-164. Sheth, H.C., Pande, K. and Bhutani, R. 2001. 40Ar-39Ar age of the national monument: the Gilbert hill basalt, Deccan Trap, Bombay. Curr. Sci. v. 80, pp. 1437-1440. Sheth, H. and Pande, K. 2014. Geological and 40Ar/39Ar age constraints on late-stage Deccan rhyolitic volcanism, inter-volcanic sedimentation, and the Panvel flexure from the Dongri area, Mumbai. Asi. Jour. Ear. Sci., 84, 167-175. Tandon, S.K. 2005. Sedimentary environments of Late Cretaceous sequences of Central India: Influence of Deccan Volcanism. Gond. Geol. Magz., Spl. v. 8, 1-4. Tandon S.K., Sood, A., Andrews J.E. and Dennis P.F., 1995. Paleoenvirnments of dinosur bearing Lameta beds (Mastrichtian), Narmada valley, Central India. Palaeogeo., Palaeoclim. Palaeoecol., v. 117, 489-491.

164 P19: Records of fauna and flora from Pakistan: Evolution of Indo-Pakistan Peninsula

Malkani, M. S.

Paleontol. Stratig. Bran., Geol. Surv. Pakistan, Sariab Road, Quetta, 87300, Pakistan. [email protected]

The Pakistan yielded many flora, Scaphopoda, Bryozoa, Brachiopoda invertebrates, titanosaurian sauropod and (Productus, fusilinids, etc), Echinodermata abelisaurian and noasaurian theropod (Crinoids, etc), Conodonts, Mollusca, dinosaurs, pterosaur and mesoeucrocodiles. Cephalopoda (Ammonites and belemnites Indo-Pakistan subcontinent was separated became extinct at Cretaceous-Tertiary from Madagascar during Late Jurassic. It boundary while nautiloids survived during started northward journey at end extinction), Gastropoda, Pelecypoda/Bivalves Jurassic/Earliest Cretaceous. Most of the and Arthropoda (many insect, etc, Cretaceous passes as journey and isolation. Its Trilobites-Proetus chitralensis-Early Devonian northwestern part first time collided with of Chitral-Extinct) have been reported from Afghan block of Asia at Latest Cretaceous. Its Pakistan so far. The Pakiring kharzani (the northern part collided with Asia at end bivalve/pelecypod Mollusca) tentatively Eocene/Earliest Oligocene. This collision named after Pakistan and its town Kharzan, is resulted in the form of Himalaya and found from the Cretaceous Tertiary (K-T) Indo-Pakistan Peninsula (South Asia). boundary laterite/thin rust (3km north of Records of fauna and flora from the Latest Kharzan town) on the last bed of Pab Cretaceous of Pakistan sandstone in the Kharzan area of Khuzdar The flora like algae, pollen, spores district, Balochistan, Pakistan. It is sub ring and wood fossils from Paleozoic to Cainozoic type and rough surface ornamented bivalve era of Pakistan have been reported. Dinosaurs with many rope like rises alternated by falls eat tall conifers which may be the reason of (Fig.1). Two pectin type other bivalves, 3 neck elongation. A wood log of large conifer gastropods and 1 coral like fossils are figured tentatively named as Baradarakht goeswangai and found from Shaheed Ghat Formation of (after Bara means big and long, Darakht mean Kharzan area, Mula-Zahri range, Khuzdar tree, host Goeswanga Pass area), is found from district. The Pakiwheel vitakri-the stocky type the Latest Cretaceous (Maestrichtian) Pab nautiloids named after Pakistan and its town Formation (sandstone with negligible shale) of Vitakri, is found just after the K-T boundary in Goeswanga Pass area of Dhaola Range, Sangiali Formation close to east of Vitakri Barkhan District, Balochistan, Pakistan. It is a town, Barkhan District, Balochistan, Pakistan cross section (20cm in diameter) is fibrous and and Pakiwheel karkhi-the slender type belongs to main trunk of tall tree (Fig.1). nautiloids named after Pakistan and its town Further the Kingri coal of Vitakri Formation Karkh, is found in the green mudstone may be may be formed from ferns, angiosperms, of volcanic origin of Early Paleocene gymnosperm, etc. Khadro/Sangiali Formation 5km east of Karkh The invertebrates like Protozoa, town, Khuzdar District (Fig.1). The Mulastar Foraminifera (started from Cretaceous-Goru zahri-a star fish named after Mula River and Formation like Globigerina, Rotaliapora, Zahri range and tribe, is found from the Late Globotruncana, and onward Paleocene-Early Eocene Shaheed Ghat Cainozoic-Nummulites, Alveolina, Assilina, Formation, Kharzan area of Khuzdar district, etc), Coelenterata (Anthozoa-corals, sea Balochistan, Pakistan (Fig.1). anemones, stony and horny corals; Pakistan has a unique blend of Hydrozoa-Jellyfish); Stromatoporoidea, Mesozoic vertebrates of Gondwana affinity 165 like sauropods, theropods and Kamardin Karez, Zhob district, Balochistan), mesoeucrocodiles while Cenozoic mammals of and Buzdartherium gulkirao from Oligocene Asian affinity like rhinocerotoids and Chitarwata Formation of Taunsa area, D.G. antharacotherids with few proboscideans, Khan (Punjab), and Basilosauridae, the king of carnivores, chalicotheres, deinotheres, bovids, basal whale like Sulaimanitherium dhanotri suids, Creodonta, ruminantia, amynodontiae, from Early Eocene strata of Sulaiman basin and crocodilians. The Gomphotherium (Zamri area, Musakhel district, Balochistan) buzdari-a big proboscidean (Mammalia) have been reported. remains are collected from Miocene Litra Evolution of Indo-Pakistan Peninsula (South Formation of Vihowa group in the eastern Asia) limb of Zinda Pir anticline. The proximal and During Late Triassic (220 Million distal femur and proximal tibia are its years old; Ma) the lands united as Pangea. The holotypic materials found from the Miocene breakup of Pangaea started in Middle Jurassic Litra Formation in Salari area, east of Zin in (170 Ma) while the breakup of Gondwana the northeastern part of Zinda Pir anticline, started in Late Jurassic (160 Ma). Madagascar Taunsa area, Dera Ghazi Khan. The femur is separated from Africa and also Indo-Pakistan head is circular and directed mostly upward. subcontinent during Late Jurassic (Fig.1b). Its tip is slightly more wide then its neck. The Indo-Pakistan started northward journey at head is raised more than its greater trochanter. Jurassic-Cretaceous boundary (136Ma) or There is a depression/notch between trochanter atleast Earliest Cretaceous. In the Sulaiman and and head. The trochanter raises more than Kirthar foldbelt the marine environment was notch and also more thick than adjoining notch. dominant during Triassic and Middle Jurassic There is a large fossa or shallow depression in while the Jurassic-Cretaceous boundary is the anterior part of proximal femur. There is a represented by Dilband formation (laterite; sea small rise in the posterior of proximal femur regressed) which shows uplift and first main (close to laterally transverse mid). The distal tectonic episode for starting northward journey. part of femur is massive, thick and forms its The Early Cretaceous was again marine two condyles, one for tibia and other for fibula. (transgressed). During Late Cretaceous the Fort The tibia is slender and proximal part is Munro group (sandstone, shale, marl, elongated. There is a depression on one corner limestone) deposited showing uplift and of proximal view, to be set for tibial condyle regression of sea. At latest Cretaceous (70-67 of femur. The fibular fossa on one side and Ma) the sea regressed and land uplifted resulted ridge on another side can be observed. There is in the deposition of continental Vitakri a thin oval hole in centre of bone’s cross Formation’s laterite, red muds alternated two section observed at its preserved end (Fig.1). sandstone horizons. The northwestern corner of The Quettacyonidae tentatively named as Indo-Pakistan collided first time with Afghan Bolanicyon Shahani (after Bolan river and block of Asia at Latest Cretaceous about district and coal miner Shahani) is found in the 70-67Ma. This corner may act as a pivot point Early Eocene Toi Formation of southwestern for counterclockwise rotation. This collision Mach (Gishtari) area (Fig.1). Its 1 incisor, 1 created the land bridge from canine, 4 premolar and 3 molar teeth are Afghanistan/Hindu preserved. The possible bony fishes-the Kush-Kurram-Waziristan-Zhob (Western Indus Teleostei or holostei fish or ichthyosaur Suture and adjoining Afghan land)-Ziarat-Fort tentatively named as Karkhimachli sangiali, Munro (D.G.Khan) areas. This bridge allowed the name derived after Karkh area of Khuzdar the migration of latest Cretaceous fauna from district and its host Paleocene Sangiali group Asia to Indo-Pakistan and vice versa. During (including marine Sangiali, Rakhi Gaj and Paleocene the sea transgressed on this land Dungan formations). Its preserved portion bridge and other vicinity areas and deposited mostly belongs to body cross section having the marine Sangiali Group (Sangiali, Rakhi Gaj herring bone type structure. It is small sized and Dungan formations) in the Sulaiman basin fish/ichthyosaur. The other cross section is and Nisai group in the Balochistan basin also referred to it (Fig.1). The baluchithere like (Fig.1e). During Late Paleocene the sea Pakitherium shagalai from Early Eocene strata regressed from the western Sulaiman basin and of Kakar Khorasan basin (Shagala area of northern Balochistan basin due to further uplift 166 and collision. Consequently Western Indus and also eastward. As a result the transition Suture, close to Zhob-Waziristan-Kurram and period of this transgression is represented by its adjoining western areas of Afghan block the deposition of upper Ghazij group (Drug began to rise. This uplift provided the lands for limestone and Baska evaporitic gypsum, and the migration of Eocene vertebrates like shale show rhythmic off and on sea water) and baluchithere-the largest rhinoceros from Asia major transgression is represented by the to Indo-Pakistan subcontinent or vice versa. deposition of Kahan group (Habib Rahi This rising ended the Paleo Vitakri River limestone, Domanda shale Pirkoh limestone systems of Sulaiman foldbelt flowing from east and Drazinda shale) in the Sulaiman basin of to west (Indo-Pakistan shield toward Pakistan while the Kakar Khorasan basin was Neotethys; Fig.1c) and started the birth of under erosion. The Tethys Sea was Paleo Indus River systems flowing from permanently closed by the latest Eocene northwest to southeast and north to south tectonic episode which is responsible for the (Fig.1d). It deposited the deltaic and terrestrial birth of Himalaya. The Late Eocene tectonic molasse Late Paleocene-Early Eocene episode and collision of northern Indo-Pakistan Chamalang (Ghazij) Group (Shaheed Ghat, Toi with Asia created the Himalaya. This collision and Kingri formations) in the Sulaiman basin, started the terrestrial/continental fluvial facies and Shagala Group of northern Balochistan and Neotethys permanently closed from Kohat basin (Murgha Faqirzai~2000m thick which is and Potwar and Sulaiman basins. This equivalent to Late Paleocene Shaheed Ghat increases the gradient of Indus river and also Formation of Sulaiman basin, Early Eocene created the birth of Ganges River systems Mina Formation type locality Mina Killi 310 flowing from west to east and northwest to 11.6’; 690 07.6’; 60km southwest of Zhob and southeast. This uplift is responsible for the on east of Zhob-Shagala road~3000m thick molase deposition of Siwalik, Potwar and alternated deltaic green shale unit and Vihowa groups in Indo-Pakistan Subcontinent. sandstone unit correlated with Toi Formation of Consequently the Neotethys closed from the Sulaiman basin, and Early Eocene area presently called Himalaya. The Neotethys Shagala/Shagalu Formation~3000m thick remained in the east and mostly in the west of alternated terrestrial red and brown shale unit Indo-Pakistan subcontinent but now named as and sandstone unit correlated with Kingri Indian Ocean. Due to this closure of Neotethys Formation of Sulaiman basin; Fig.1). This from north, northwest and some part of west of molasse shows the beginning of Neotethys Indo-Pakistan subcontinent, shaped it as closure from NW of Indo-Pakistan Peninsula. Due to contact and collision of subcontinent. The middle Eocene is represented Indo-Pakistan subcontinent with the southern by a major transgression of sea in the westward part of Asia it is being called as South Asia.

167

Afghan block Zhob Subrecent and recent surf..dep. Laurasia C B Tethys Holocene Bostan Fm. mud, sst, cong Pleistocene Dada Fm.cong. mud 55 Ma Indo-Pakistan Sub Pliocene Chaudhwan Fm.mud,sst,cog Loralai Vitakri M Ziarat high I Litra Fm. Sandstone, mud Indo-Pakistan Sub. Quetta O

C Northern ENE Vihowa Fm. Sst, red mud Hemisphere

Equator Oligocene Chitarwata Fm.sst, mud

Khuzdar E Jacobabad high Shagala Formation O sandstone and red mud

Southern C E Hemisphere Zhob . E Karachi Afghan N Mina Formation Block Indo-Pakistan E sandstone and green mud Sub P Murgha Faqirzai Formation D A shale, slate, marl Indo-Pakistan Sub. L D. G.Khan Madagascar E Nisai Fm. massive lst Quetta 145 Ma O C ENE Jabrai Fm. Shale, minor marl

Jacobabad Cretaceous Akhtar Nika Fm. Lst, sh.

Figure 1. A Row 1 holotype of Gspsaurus pakistani in ventral view and Saraikimasoom vitakri in lateral and posterior views (titanosaurian sauropods); Vitakrisaurus saraiki in lateral and dorsalKhuzdar views (theropod ); Induszalim bala in posterior and lateral views and Pabwehshi pakistanensis in lateral views (mesoeucrocodiles); and holotypic and referred dentaries of Saraikisaurus minhui in lateral view (pterosaur) (location is black circle); new ichnotype (Pashtosaurus zhobi-Latest Cretaceous titanosaurian sauropods) Sor Muzghai, Zhob district, Balochistan (square): Row 2 holotype dentary MSM-1068- Western Mach (3 photo) of Bolanicyon shahani (star); holotype MSM-1038-6 of Baradarakht goeswangai (black circle); ammonite impression MSM- 1069-Malakhel; (triangle).); holotype MSM -1070-K of Mulastar zahri (star); holotype MSM-1062-K and referred specimen MSM-1063-K and MSM- 1063-K of Karkhimachli sangiali (star): Row 3 holotype of Gomphotherium buzdari (E side of black circle) like MSM-MSID-1 and MSM-MSID-2 Proximal femur in three views, MSM-MSID -3 distal femur with its partial two condyles and MSM-MSID-5 broken portion of probably distal femur in 2 views; MSM-MSID-4 proximal tibia in 2 views: Row 4 holotype MSM-1071-K of Pakiwheel karkhi (upper) (SW side of star) and Pakiwheel vitakri (lower) (black circle); holotype MSM-1073-K and referred MSM-1074-K of Pakiring kharzani-a pelecypod/bivalve found from K-T boundary laterite/rust on last bed of Pab sandstone in Kharzan area (star); 2 bivalves, 3 gastropods (lower) and 1 coral (upper); MSM-1065-K (in 2 photo) a specimen of cross section of limb of bird or a tooth of mammal found fragmentary from Eocene of Kel area of Kharzan (star), Khuzdar, and Map of Pakistan showing different biota localities mentioned in bracket after each taxon; Scale for row 3 is 26cm long while for other rows each black or white digit is 1cm. B northward flight of Indo-Pakistan subcontinent during Cretaceous. C pre-Late Paleocene source of clasts of Sulaiman basin from east (Indo-Pakistan shield), thick black line-Tethys Sea, thick dotted line-Western Indus suture, arrows-direction of river movement. D post Middle Paleocene source of Sulaiman basin clasts via Paleo Indus river system from north and northwest (western Indus Suture and adjoining high lands), arrows-movement direction, thick dots-Western Indus Suture. E Revised startigraphic sequence of Northern Balochistan/Pishin/Kakar Khorasan/Katawaz basin (location; square in map of Pakistan).

168 P20: Theropod dinosaurs and mesoeucrocodiles from the Terminal Cretaceous of

Pakistan

Malkani, M. S.

Paleontol. Stratig. Bran., Geol. Sur. Pakistan, Sariab Road, Quetta, 87300, Pakistan, [email protected]

The Latest Cretaceous Vitakri basipterygoid processes are basal tubera Formation of Pakistan yielded theropod instead). Its massive and thick braincase dinosaurs like large bodied Vitakridrinda parietal/ dorsal cover matches with abelisaurian theropod and small bodied Carnotaurus sastrei and Indosaurus matleyi, Vitakrisaurus noasaurian theropod dinosaurs its basipterygoid process is high angle while in and large bodied Pabwehshi pakistanensis, Indosuchus raptorius is low angle (Mickey Sulaimanisuchus kinwai and Induszalim bala Mortimer, personal communication in 2012) mesoeucrocodiles so far. The theropod The foramen magnum is covered by matrix in dinosaurs of Pakistan generally show affinity the posterior view (it will clear after specimen with the south Pangea (Gondwanalands) at preparation). Many fossils of theropods were abelisaurian level. The mesoeucrocodiles from found and documented (Fig.1). Pakistan do not show such degree of Vitakrisaurus saraiki resemblance with Madagascar and South Vitakrisaurus saraiki is a small sized America as it should be if connected (during carnivorous Vitakrisauridae noasaurian Late Cretaceous). This shows isolation (as big theropod. It is based on isolated pes (Fig.1) island) of Indo-Pakistan Subcontinent from collected from the terrestrial overbank red Madagascar and other Gondwanan landmasses muds of latest Cretaceous Vitakri Formation of during Cretaceous. Bor Kali Kakor locality, Vitakri area. The Theropod dinosaurs from the Latest Vitakrisaurus saraiki is more comparable to Cretaceous Vitakri Formation of Pakistan noasaurids (the small theropods) than Vitakridrinda sulaimani abelisaurids (the large theropods) based on its Vitakridrinda sulaimani is based on a size. The large ratio between phalanges II-2 pair of left and right proximal femora and and II-1 and proximally narrow metatarsal II basioccipital condyle alongwith partial (in dorsal view) also suggest noasaurids braincase. It has referred many vertebrae and affinities while phalanx II-2 is longer than limb bones. Its rostrum is assigned to new Velocisaurus (compared to phalanx II-1), this mesoeucrocodile (Induszalim bala) from varies within other species, and further Pakistan. Its braincase and basioccipital can be comparison is not possible pending better assigned to Maojandino alami (because of the description of the Vitakrisaurus and other yellow brown matrix covered on supposed noasaurid pes (Mickey Mortimer, personal braincase is same as on associated vertebrae communication in 2012). Many smaller bone and limb elements of Maojandino alami) if and phalanges are found just below the claw, character supports after specimen preparation. which may be the bones of left pes of The basioccipital condyle and posterior most Vitakrisaurus or may belong to birds or other part of braincase shows decurved and much flying reptiles like pterosaur. Some noasaurids taller paroccipital processes match with are Composuchus, Jubbulpuria, Laevisuchus, titanosaur braincase while the anterior view of Masiakasaurus, Noasaurus, Ornithomimoides, paroccipital processes and basipterygoid Velocisaurus and Vitakrisaurus. processes which is similar in rough outline to Pterosaur from the Latest Cretaceous Abelisaurus (assuming the supposed Vitakri Formation of Pakistan 169 Saraikisaurus minhui anteriorly/anterodorsally directed external So far dinosaurs and crocodiles are nares, very high/very deep and narrow rostrum, reported from the Cretaceous of Indo-Pakistan the ziphodont type laterally compressed teeth but now pterosaur-the flying reptile is being (Oval to D shape, heterodont in size), and reported first time. A dentary ramus (Fig.1) of thick rostral elements. It matches with the Saraikisaurus minhui (Pterosauria, Sebecosuchian due to their laterally Pterodactyloidea, Saraikisauridae, compressed and very thick teeth. The ventral Saraikisaurinae) has been found from the latest views of rostrum show V shape nature. The Cretaceous terrestrial (close to shore rostrum is triangle to sub triangular in cross meandering stream over bank deposits) Vitakri section. The external nares are located as Formation of Top Kinwa locality, Vitakri area, subterminal or little behind the termination of Barkhan District, Balochistan Province rostrum or little before the anterior most (Sulaiman Basin), Pakistan. The preserved extremity of the rostrum. The external nares dentary ramus shows carnivorous type are bifurcated by medial premaxillary belt. elongated skull with eight teeth. This ramus The external nares are bordered ventrally and shows internal pneumatic texture/structure. laterally with premaxilla, and dorsally by The teeth are oval to suboval, some overlapped. partial premaxilla and mostly nasal. Rostrum The total length of preserved dentary ramus is has pitted and sculptured surface or 5.8cm. The dentary is slender. After the ornamented with groves and ridges. The collision of Indo-Pakistan subcontinent, this sculptures are mostly found as pterosaur may be migrated from Asia like anteroposteriorly elongate, discontinuous, China, Korea, etc. pitted, rope like structure especially on the Carnivore mesoeucrocodiles from the maxilla and nasal. The rostrum has many small Latest Cretaceous of Pakistan and large internal pneumatic cavities Pabwehshi pakistanensis especially in the maxilla and dentary. The Pabwehshi pakistanensis is based on width and height/depth of rostrum at the rostrum and articulated partial dentary. Some available cross section is equal. The postcranial material is also referred (Fig.1). premaxilla is roughly quadrangular in left Sulaimanisuchus kinwai: Sulaimanisuchus lateral and right lateral views. It contacts with kinwai is based on anterior dentary and nasal dorsally and the maxilla posteriorly. The splenial. The first and third tooth are small in premaxilla and nasal enclose the external naris. dia while third is relatively more but the fourth The nasal forms the dorsal margin of external is maximum in dia, fourth dentary teeth is and internal naris upto the available cross large and marked heterodonty in size and section of snout. The premaxilla forms the compressed teeth (Fig.1). lateral wall of external and internal naris. Induszalim bala Laterally the suture of maxilla and premaxilla Previously the specimen is a butt joint running about MSM-155-19 is assigned to Vitakridrinda 40-700.dorsomedially toward nasal. Dorsally sulaimani (theropod dinosaur) but due to the premaxillae contact with each other at the secondary palate nature it is being established form the midline contact. The preserved as Induszalim bala -new genus and species of maxilla is quadrangular/sub rectangular. very large mesoeucrocodile (Fig.1). The Dorsally the maxilla meet with nasal forming Induszalim bala (Zalim is a Urdu and Saraiki horizontal contact nearly parallel to midline word for cruel, bala is a Saraiki word mean big but this suture dips medioventrally at about terrible animal; species name after Indus River 60-80 vertical. It forms the side wall of the and Indus Basin of Pakistan) is a terrestrial rostrum. It also forms part of secondary palate. mesoeucrocodile found from red muds of The maxilla, nasal and palatal encloses the Latest Cretaceous (about 65-66 million years internal naris. The nasal forms the dorsal old) Vitakri Formation of Alam Kali Kakor margin of internal naris upto the available locality of Vitakri area, Barkhan district, cross section of snout. The maxilla has no Balochistan, Pakistan. It was a terrestrial anterior process and does not participate in the predator and scavenger. The Induszalim bala boarder of external naris. A very large internal (Induszaliminae, Induszalimidae, coel (dorsoventrally elongated) is found in the Sebecosuchia, Mesoeucrocodylia) shows maxilla (observed on posterior view). The 170 outer surface of maxilla show some rugose, 6-7mm and thickness is 2.8mm. The small pitted and anteroposteriorly aligned tooth is 1.5cm thick and 6-7mm wide. The discontinuous lineations. The belt/strap like other 2 teeth vary in between these thicknesses nasal forms the roof of rostrum. It is mostly but widths are mostly subequal or constant. At flat/straight with rugose surface texture. The the supposed diastema on the contact of palatal shelf has saggital torus. The supposed maxilla and premaxilla, one small tooth with dentary is preserved in articulation with the 3mm width and 6-8mm thickness are found rostrum but the dentary rami and adjoining (Fig.1). In Induszalim the snout depth is equal splenial are embedded in the cavity just below to width while in Pabwehshi the depth is ¾ of the crocodilian tube/ inside of rostrum. The width. In Induszalim the maxillary ramus is right and left dentary bones have large internal relatively far away/down to palatal contact open cells/cavity found in the basal part while in Pabwehshi the maxillary ramus is just observed at the available cross section. Some close to palatal contact. In Induszalim the large other internal cells are also found. The teeth dia is relatively more than Pabwehshi supposed splenial are exposed only on the tooth diameter. In Induszalim on the lateral available section. These right and left splenial side of maxillary ramus there are pits with are contacted with each other in the centre of anteroposterior lineation while Pabwehshi has rostrum or midline. The splenial contacts the no lineation. The Induszalim shows marked medial aspect of the dentary along its height boundary/contact between palatal shelves and from the base of the jaw ramus to alveolar maxillary wall but Pabwehshi shows no margin. The splenial extends to the midline boundary/contact between palatal shelves and and participate in the symphysis. The maxillary wall. The Induszalim matches with splenial bones are mostly massive i.e. with the Pabwehshi on saggital torus on palatal open large internal cells. The teeth are highly shelves of Pabwehshi. Montefeltro et al. compressed transversely. The cross sections of (2011) mentioned that Pabwehshi has a the teeth embedded in the matrix just below saggital torus on its maxillary palatal shelves – the maxilla and premaxilla show elongate a character that is absent in baurusuchids. So oval/elliptical to D shape. The sizes of the the Pabwehshi and Induszalim may belong to teeth are also variable. The large tooth width is Induszalimidae.

Reference: Montefeltro,F.C., Larsson, H.C.E. & Langer, M.C. 2011.A new Baurusuchid (Crocodyliformes, Mesoeucrocodylia) from the Late Cretaceous of Brazil and the Phylogeny of Baurusuchidae. In Farke, Andrew Allen. PloS ONE 6(7); e21916.doi:10.1371/journal.pone. 0021916. PMC 3135595. PMID 21765925.

171 mc mc na na en m in mb en st pc pm m pm

d mr sp

Figure 1. Row 1, Holotypic skull (MSM-155-19) in anterior, posterior and left lateral views and top corner photo shows 3 or more teeth in muddy matrix (MSM-61-19) of Induszalim bala (a sebecosuchian mesoeucrocodile). Row 2, Holotypic rostrum articulated with dentary and referred dentary, vertebrae, limb bone and rib of Pabwehshi pakistanensis, holotypic dentary in 3 views of Sulaimanisuchus kinwai. Row 3, Holotypic dentary with teeth of Saraikisaurus minhui pterosaur, referred dentary of pterosaur or birds; holotypic pes of Vitakrisaurus saraiki noasaurian theropod. Row 4, Holotypic a pair of femora, a braincase with basioccipital condyle and referred 6 vertebrae of Vitakridrinda sulaimani abelisaurian theropod; Row 5,6/7, limb bones and axial elements of theropods. Scale; Each black or white digit is 1 cm. Abbreviations: en-external nares, in-internal nares, d-dentary, m-maxilla, na-nasal, mb-internarial bone bar, mc-midline contact, pc-palatal contact, mr-matrix, na-nasal, pm-premaxilla, t-teeth, st-saggital torus, sp-splenial.

172 P21: Preliminary study of the new juvenile dinosaur (Theropoda: Ornithomimosauria)

from the Upper Cretaceous Baynshire Formation of Khongil Tsav, eastern Mongolia

Chinzorig, Ts. and Tsogtbaatar, Kh.

Paleontol. Cent., Mongolian Acad. Sci., Chingeltei district-4, S. Danzangiyn street-1/3, Ulaanbaatar-15160, P.O.Box-46/650, Mongolia;

Summary to Upper Cretaceous sediments of Gobi Desert. A juvenile articulated postcranial By localities, Ornithomimosaurian specimens skeleton of ornithomimosaurian dinosaur with are abundantly found from Late Cretaceous age some mixed ornithomimid and of Tsagaan Khushuu, Bugin Tsav, Gurilin Tsav, non-ornithomimid characters, also presenting Altan Ula, Nemegt, and Shine Us Khudak the smallest known specimen of the group, has localities of Umnugovi and Dornogovi been preliminarily described of its provinces and Early Cretaceous age of Khuren morphological study have been analyzed in its Dukh locality. manus, pelvic parts and hind limb in this paper. General consideration Introduction 1. emegtian ornithomimosaurs Ornithomimosauria (Theropoda, The Nemegt Formation (Jerzykiewicz Ornithomimosauria) includes 14 genera et al., 1991) is widely distributed in the (Barsbold and Osmόlska, 1990; Kobayashi and Western areas of the Gobi Desert where to be Lu, 2003). Among the fifteen species of located Altan Ula, Bugin Tsav, Gurilin Tsav, fourteen genera in the infraorder, seven of these Nemegt, Tsagaan Khushuu, and Ulaan genera, namely Ornithomimus, Struthiomimus, Khushuu localities. The ornithomimid Dromiceiomimus (North America), Gallimimus, materials, for instance, Gallimimus bullatus Anserimimus (Mongolia) and Osmόlska et al., 1972; Anserimimus Archaeornithomimus, Sinornithomimus (China) planinychus Barsbold, 1988; Deinocheirus are Ornithomimidae. Non-ornithomimid mirificus Osmόlska and Roniewicz, 1970, are ornithomimosaurs include six genera, including abundantly revealed above these localities. The Garudimimus, Harpymimus (Mongolia), most of the nemegtian ornithomimids are Pelecanimimus (Spain), Shenzhousaurus, characterized by edentulous, relatively long, Beishanlong, and Qiupalong (China) are but a weak, non-raptorial manus with almost known from the Early Cretaceous except same length of the metacarpals, almost straight Garudimimus (Kobayashi and Barsbold, 2005). pubic shaft, and long hindlimbs equipped the The relationship of the one of the enigmatic arctometatarsalian condition, and first taxon Deinocheirus that includes both metatarsal is being lost by evolutionary. ornithomimid and non-ornithomimosaurian 2. Baynshirenian ornithomimosaurs characters is still contentious (Barsbold and The Baynshire Formation Osmόlska, 1990; Kobayashi and Barsbold, (Cenomanian-Turonian, Khand et al., 2000) is 2006). mostly distributed within Eastern areas of the Ostrich-like dinosaurs, Gobi Deserts and Garudimimus brevipes Ornithomimosauria, is the one of the main Barsbold, 1981; and Gallimimus mongoliensis group of meat eating dinosaurs and its sp. are described holotype representatives of specimens are dominantly preserved from the ornithomimosaurian group from this region. Cretaceous sediments of Central Asia and Whereas nemegtian aged ornithomimids are North America. The Mongolian representatives defined as a lightly built, arctometatarsalian of this group are revealed in all strata of Lower condition, with no pollex, the baynshirehnian 173 ornithomimosaurs are coined as mid-section Comparisons of the postcranial elements members of the group because are generally The differences between characterized to include both advanced and baynshirenian juvenile specimen and other basal characters. Although the baynshirehnian ornithomimosaurs in the postcranial elements ornithomimosaurs are similar to several deal with somewhat different shape of some characteristics to the nemegtian ornithomimids, bones and with the proportions of particular they can identify several unique characters bones, or portions of the limb. It is impossible from them. For instance, the length of the to compare a fore limb of baynshirenian slightly curved pubis is longer than the ilium; specimen to the both nemegtian specimen and length of the femur is nearly same as the tibia Garudimimus holotype because of these is length, non-arctometatarsalian condition. whether not preserved them. Though comparing the manus of the baynshirenian Preliminary results juvenile specimen to the Gallimimus that is The juvenile specimen has been exist a forelimb; the length of 1st metacarpal is recovered from the Khongil Tsav locality obviously shorter than others whereas it is a (Upper Cretaceous, Baynshire formation) of the nearly same level in Gallimimus structurally. Eastern Gobi Desert is one of the smallest Moreover, the structure of the manual unguals ornithomimosaurs among the group. This is differentiated as a slightly curved and the juvenile specimen, catalogued as MPC-D lateral grooves of the manual ungual are deep 100/125 in the Mongolian Paleontological as well as a distinctly narrower to the tip while Center, MAS, has several derived and shared the contrary is the case in Gallimimus; and the characters both Garudimimus brevipes and length of the phalange III-3 is longer than the Gallimimus bullatus holotypes, as well as combined length of the phalanges III-1 and another juvenile Gallimimus specimen. III-2, as in G.bullatus this length is nearly (Figure-1) same; There are several derived and shared

Figure-1: whole articulated skeleton of the baynshirenian juvenile specimen (MPC-D 100/125)

174 characters in the structure of the pelvis in although it is different genus. Unfortunately, baynshirenian juvenile specimen as compared due to the missing of skull and fore limbs of the with that of above specimens. For instance, the materials, it wasn’t possible to catch full shared characters with a holotype of information concerning the changes of the fore Garudimimus: the ilium length compared with limb to hind limb ratio. The following chart is a length of the femur of the baynshirenian showing selected anatomic ratios of growth juvenile specimen is relatively shorter; length changes in ornithomimosaurs as compared with of the pubis is longer than the ilium, but is nemegtian and baynshirenian: different in North American taxa; and the posterior process of the pubic boot is becoming Discussion a narrower at the end of the tip, as well as the The baynshirenian juvenile specimen, ventral ridge of the pubic boot is slightly described here, exhibits some features in its rounded. With compare with a holotype of postcranial skeleton which are regarded by Gallimimus, the baynshirenian juvenile Osmόlska et al., 1972 as characteristic of the specimen is contained several derived juvenile specimen of Bugin Tsav. It shows the characters as the anterior part of the pubic boot same relation in the structure of the caudal is shorter than the posterior ones; the midshaft vertebral column, and similar structure of the of the pubis is straight as in North American pes. However, it is different from the advanced taxa; and the pollex is completely nemegtian juvenile specimen in following of disappeared to evolve (different than G. the characteristics, the length of the femur is brevipes that has a first digit). shorter than the length of the ilium whereas in The structure of the hind limb in the nemegtian juvenile is nearly same in length; the baynshirenian juvenile specimen shows but posterior process of the pubic boot is becoming slightly differences in comparison with that of gradually narrower to the end in baynshirenian the nemegtian juvenile specimen. The unusual juvenile while the contrary is the case in rugosity is located in the medial of the nemegtian juvenile is more wider above proximal end of the femur. This character is mentioned part; The most concentrating feature different than the nemegtian juvenile specimen. of the baynshirenian juvenile specimen is its small size, in which it differs from the Measurements (in mm) of selected postcranium of nemegtian juvenile specimen in measurements juvenile specimens: of the selected postcranial elements. Nemegtian juvenile Baynshirenian The length of Conclusions specimen juvenile specimen ▼ 1. The baynshirenian juvenile specimen from (MPC-D (MPC-D 100/125) the Khongil Tsav (Upper Cretaceous,  100/10) Baynshire formation) is included the Radius - 83 both derived and shared characters of Ilium 196 182 the postcranial elements, namely, Pubis 197 185 manus, pelvic, and hind limb. Ischium 145 142 2. It is a highly necessary to determine in future Femur 195 200 detailed analyses to whether is Tibia 218 210 peculiarity of the juvenile stage of the growth differences or completely Metatarsal-III 162 139 different ornithomimosaurian taxon. *** - Osmόlska et al., 1972. 3. Although comparing to measure in selected anatomic elements of the Growth changes ornithomimosaurian dinosaurs, the Measurements of the postcranial baynshirenian juvenile specimen is skeletons include several individuals of mainly represented as smallest Gallimimus bullatus specimens in different ornithomimosaurian specimen ever growth stages. Also, the baynshirenian juvenile found from the Gobi Desert. specimen is additionally added in below chart

175 Specimen catalogue No. R/F R/T T/F mtt.III/F mtt.III/T Growth changes number The baynshirenian 1 0.41 L 0.39 L 1.09 L 0.69 L 0.66 L Juvenile juvenile specimen The nemegtian juvenile 2 - - 1.14 0.80 0.71 ↓ specimen 3 Z.Pal.No.Mg.D-I/94 0.40 0.33 1.13 0.80 0.71 ↓ 4 Z.Pal.No.Mg.D-I/1 - - 1.08 0.77 0.72 ↓ 5 MPC-D 100/11 0.53 0.47 1.11 0.78 0.72 Adult *** - Osmόlska et al., 1972.

Reference: Barsbold, R. and Osmόlska, H. 1990. Ornithomimosauria. The Dinosauria, Edited by D. B. Weishampel, Peter Dodson, Halszka Osmόlska, California univ. Press, Oxford, England. pp. 225-244. Jerzykiewicz, T and Russell, D. A. 1991. Late Mesozoic stratigraphy and vertebrates of the Gobi Basin. Cretaceous Res. 12: pp. 345-377. Khand, Y., Badamgarav, D., Ariunchimeg, Y. et Barsbold, R. 2000. Cretaceous System in Mongolia and its depositional environments. In Cretaceous environments of Asia. Edit by H. Okada and N. J. Mateer. Elsevier Science BV, Amsterdam, The Netherlands, pp. 49-51, 53-65, 67-79. Kobayashi, Y. and Barsbold, R. 2005. Reexamination of a primitive ornithomimosaur, Garudimimus brevipes Barsbold, 1981 (Dinosauria; Theropoda) from the Late Cretaceous of Mongolia, Can. J. Earth Sci. Vol. 42: 1501-1502. Kobayashi, Y. and Barsbold, R. 2006. Ornithomimids from the Nemegt Formation of Mongolia, J. Paleont. Soc. Korea. Vol. 22, No. 1: 195-207. Osmόlska, H., Roniewicz, E. et Barsbold, R. 1972. A New Dinosaur, Gallimimus bullatus n. gen. n. sp. (Ornithomimidae) from the Upper Cretaceous of Mongolia, Palaeont. Polonica, 27: 103-143.

176 P22: Diving behavior of mosasaurs (Squamata: Mosasauridae) inferred from optics

Yamashita, M.1, Konishi, T.2 and Sato, T.3

1Univ. of Tokyo, Bunkyo-ku, Tokyo 113-0033, Japan ([email protected]); 2Royal Tyrrell Mus. of Palaeontol., Drumheller, Alberta T0J 0Y0 Canada; 3Tokyo Gakugei Univ., Koganei City, Tokyo 184-8501, Japan

Mosasaurs (Squamata, Mosasauridae) respectively; Fig. 1) correlate with the were an ecologically and evolutionarily diameters of the lens and the eyeball, successful group of secondarily aquatic lizards respectively (Schmitz. 2004). Furthermore, that lived during the Late Cretaceous. The first there are strong correlations between the discovery of mosasaur remains goes back to diameter of a lens and that of the sclerotic ring 1766 in the Netherlands: more than two aperture, and between the posterior nodal centuries later, thousands of fossils of those distance (PND) and the diameter of an eyeball typically giant swimming lizards have been as well (Schmitz, 2004). Consequently, an recovered worldwide, encompassing a wide aperture and PND can be respectively geographic range that includes northwestern expressed by INT and EXT. An f-number, Pacific region, such as Japan. In the Western which is the ratio between PND and the Interior Basin of North America, specimens aperture (PND/aperture [= EXT/INT]), is a pertaining to three particular mosasaur genera, quantitative measure of the intensity of the Platecarpus, Tylosaurus, and Clidastes, have light of the image formed on the retina. A been collected in a large number (Russell, vertebrate eye with a lower f-number can 1967). These three types of mosasaurs are collect more light within a given time than an derived and can be referred to as hydropelvic eye with a higher f-number. This capability of mosasaurs (sensu Caldwell and Palci, 2007), an eye should apply to the diving behavior in which are characterized by possessing aquatic tetrapods generally, for an animal eye non-weight-bearing pelves, and their presence with a low f-number can see objects in is considered obligatory adaptation to aquatic darker—i.e., deeper—environments. Assuming environments (Caldwell and Palci, 2007). that squamate eyes exhibit a similar correlation Previous studies on their bone histology of the hard tissue and the soft tissue of an avian (Rothchild & Martin, 1987; Sheldon, 1997) and eye, a diving behavior in mosasaurs can be sedimentary environment (Kiernan, 2002) extrapolated from the value of EXT/INT, at suggest that habitual diving depth among these least in a relative sense. mosasaur genera varied, but there is no Comparing the values of EXT/INT of definitive consensus yet about which taxon was sclerotic rings in three specimens of the three more suited for life in deeper water. In this mosasaur genera from western North America, study, we estimated the diving behavior of the ratio in Tylosaurus (4.01) is larger than these three genera with optical performance those in Platecarpus (2.27) and Clidastes that we calculated from the ratio between the (2.08). This suggests that Platecarpus and external and internal diameters of the ring as an Clidastes were potentially better adapted to see approximation of an f-number. objects in darker environments, and that they Recently, Hall (2008) and Schmitz could have frequented a deeper water zone (2009) reported a strong correlation in the more than Tylosaurus did. Because the three shape and the size between the soft and hard genera are known from the same horizon of the tissues of an eye, including bony sclerotic rings. same area (Santonian–Campanian of the In living birds, the internal and external Western Interior Basin), their different values diameters of the sclerotic ring (INT and EXT in EXT/INT are possibly indicative of niche 177 partitioning among these genera, particularly main habitats from that of Tylosaurus would between Tylosaurus and the other two genera. also mitigate the predation pressure from the Tylosaurus is the largest-known mosasaur latter, improving the survivorship of Clidastes genus of the Western Interior Seaway until and Platecarpus. about 70 million years ago (Bullard, 2006), and Thus far, the discussion concerning the stomach contents of Tylosaurus are the diving behavior of mosasaurs has been taxonomically more diverse than those of restricted to the fauna that existed in the Platecarpus, indicating its dominance in the Western Interior Seaway. At the same time, most productive part of the sea near the surface, some 40 specimens of mosasaurs representing where the highest concentration of planktons at least three major subfamilies have been occurs. Consequently, Tylosaurus may have reported in Japan to date, confirming the driven other smaller mosasaur taxa such as presence of a high level of mosasaur diversity Clidastes and Platecarpus from the shallow, in the Western Pacific (e.g., Caldwell et al., most productive feeding zone. Under this 2008; Konishi et al., 2012; Sato et al., 2012). scenario, exploitation of resources by Clidastes Consequently, further effort to collect mosasaur and Platecarpus in deeper feeding zones than and other Late Cretaceous marine reptile fossils that of Tylosaurus would be advantageous, in Japan should contribute significantly to presumably leading to selection for deep diving understanding of the ecological interactions adaptation, Tylosaurus also constitutes the only among sympatric marine reptiles that inhabited taxon among the three that is known to have waters of Late Cretaceous Japan. consumed other mosasaurs: separating their

Figure 1. The structure of an eye A, aperture (= diameter of pupil); EXT, external diameter of sclerotic ring; INT, internal diameter of sclerotic ring; LD, lens diameter; N, anterior nodal point; N’, posterior nodal point; PND, posterior nodal distance; point; principal point.

References: Bullard TS (2006) Anatomy and systematics of North American tylosaurine mosasaurs. Unpublished M.Sc. thesis, University of Alberta, Edmonton, Alberta, 208 p. Caldwell MW, Palci A (2007) A new basal mosasauroid from the Cenomanian (U. Cretaceous) of Slovenia with a review of mosasauroid phylogeny and evolution. J Vertebr Paleontol 27:863–880. Caldwell MW, Konishi T, Obata I, Muramoto K (2008) A new species of Taniwhasaurus (Mosasauridae, Tylosaurinae) from the Upper Santonian-Lower Campanian (Upper Cretaceous) of Hokkaido, Japan. J Vertebr Paleontol 28: 339-348. Hall M (2009) The relationship between the lizard eye and associated bony features: a cautionary note for interpreting fossil activity patterns. Anat Rec 292: 798-812. Kiernan CR (2002) Stratigraphic distribution and habitat segregation of mosasaurs in the Upper Cretaceous of western and central Alabama, with an historical review of Alabama mosasaur discoveries. J Vertebr Paleontol 22: 91-103. Konishi T, Tanimoto M, Utsunomiya S, Sato M, Watanabe K (2012) A large mosasaurine (Squamata: Mosasauridae) from the latest Cretaceous of Osaka Prefecture (SW Japan). Paleontol Res 16: 79-87. Rothschild BM, Martin LD (1987) Avascular necrosis: occurrence in diving Cretaceous mosasaurs. Science 236: 75-77. 178 Russell DA (1967) Systematics and morphology of American mosasaurs. Bull Peabody Mus Nat Hist 23: 1–241. Sato T, Konishi T, Hirayama R, Caldwell MW (2012) A review of the Upper Cretaceous marine reptiles from Japan. Cretaceous Res 37: 319-340. Schmitz L (2009) Quantitative estimates of visual performance features in fossil birds. J Morphol 270: 759-773. Sheldon A (1997) Ecological implications of mosasaur bone microstructure. In: Callaway JM, Nicholls EL, editors. Ancient Marine Reptiles. San Diego: Academic Press. pp. 293-332.

179 P23: Functional morphology of unique feeding apparatus in the bothremydid turtles

Yoshida, M. 1 and Hirayama, R. 2

1Grad. Schl. Internat. Culture Comm., Waseda Univ. 169-8050,1-6-1, Nishi-waseda, Shinjuku-ku, Tokyo (mstkyoshida@,toki.waseda.jp) 2Schl. Internat. Liberal Stud., Waseda Univ., 169-8050,1-6-1, Nishi-waseda, Shinjuku-ku, Tokyo.

The feeding apparatus of modern triturating surfaces. These pits are one of the turtles (Testudines) are defined by the presence most characteristic synapomorphies in the tribe of rhamphotheca instead of marginal teeth. It is Bothremydini. Some have discussed about known that shape of rhamphotheca is partly these unique pits of Bothremydid turtles since controlled by the shape of bone elements Leidy 1865. Baur 1891 and Hay 1908 proposed existing underneath. We here discuss about the hypothesis on its functions. Gaffney et al., 2006 morphologically unique triturating surface of suggested that these pairs of pits served for marine side-necked turtles (Pleurodira : grasping hard shelled mollusks. Bothremydidae: Bothremydini). The High and developed coronoid rhamphotheca or the beak of turtles is made of processes of lower jaw suggest that keratins therefore cannot be preserved during bothremydids beard powerful bite. Considering fossilization. However, exceptional in most of the diversity of sea turtles (Cryptodira: archosaurian groups of Mesozoic era, it is still Chelonioidea) with various degrees of possible to observe diverse living turtles secondary palate coexisted in the Tethys Ocean feeding on their prey. By using extant turtle’ of Latest Cretaceous and Paleogene, unique osteological materials and records of feeding feeding apparatus of bothremydids seems habitats, we discuss functional morphology of competitive enough to hold their own feeding apparatus and possible feeding habitats ecological niche. of fossil turtles. The taxonomy and marine adaptation The bothremydid turtles show unique of bothremydid turtles (WSIL-RHg519) will be pairs of jugal and mandibular pits on its discussed in our oral presentation.

180

Figure: Triturating surfaces of WSILS-RHg 519. Left, ventral view of skull. Right, dorsal view of lower jaw. Scale-bar is 10 cm long.

References: Baur, G. 1891. Notes on some little known American fossil tortoises. Proceedings of the Academy of Natural Sciences of Philadelphia 43: 411–430. Brinkman, D., M. C. Aquillon-MartinezQ, C.A. De Leon Da´ Vila, H.Jamniczky, D. A. Eberth, and M. Colbert. (2009). Euclastes coahuilaensis sp. nov., a basal cheloniid turtle from the late Campanian Cerro del Pueblo Formation of Coahuila State, Mexico. PaleoBios, 28:76–88. Gaffney, E. S., Tong, H. and Meylan, P. A. 2006. Evolution of the side-necked turtles: the families Bothremydidae, Euraxemydidae, and Araripemydidae. Bulletin of the American Museum of Natural History 300, 1–698. Gaffney, E. S. and Zangerl, R. 1968. A revison of the chelonian genus Bothremys (Pleurodira: Pelomedusidae). Fieldiana: Geology 16, 193–239. Wood, R. C. 1976. Stupendemys geographicus, the world’s largest turtle. Breviora, 436:1–32. Hay, O.P. 1908. The fossil turtles of North America. Carnegie Institution of Washington Publication 75: 1–568. Leidy, J. 1865. Memoir on the extinct reptiles of the Cretaceous formations of the United States. Smithsonian Contributions to Knowledge 14(6): 1–135.

181 P24: Fossil turtles from the Lower Cretaceous Tetori Group in central Japan

Sonoda, T.1, Azuma, Y.1, 2, Hirayama, R.3 and Ando, H.4

1Fukui Pref. Dinosau Mus., 51-11 Terao, Muroko, Katsuyama, Fukui, 911-8601, Japan ([email protected]) 2Dinosaur Res. Cent., Fukui Pref. Univ., 4-1-1 Kenjojima, Matsuoka, Eiheiji, Fukui, 910-1195, Japan 3SILS, Waseda Univ.. 1-7-14 Nishiwaseda, Shinjuku, Tokyo, 169-0051, Japan 4Dept. Earth Sci., Ibaraki Univ., 2-1-1 Bunkyo, Mito, Ibaraki, 310-8512, Japan

A number of terrestrial vertebrate The Kuwajima Formation remains such as dinosaurs, crocodiles and An unnamed trionychoid turtle is turtles have been unearthed from several recognized from skulls, lower jaws, cervicals, localities of the Lower Cretaceous Tetori appendicular skeletons, some articulated shells, Group in central Japan. The Tetori Group and hundreds of fragmentary shell materials consists of the Gomijima, Kuwajima, Akaiwa, (e.g., Hirayama, 2000; Hirayama et al., 2000). and Kitadani formations in ascending order in Cervicals have opistocoelous structure on the the eastern part of the Hakusan district. The articular surface. The shell surface is covered Kuwajima Formation (Hauterivian to by the ornamentation of regular and fine pits Barremian?) is exposed at “the Kuwajima that is similar to Adocus and Ferganemys. Kaseki-kabe” site in the Shiramine area of However, Synapomorphies of Adocidae such Hakusan City, Ishikawa Prefecture. More as reduced proximal head of thracic rib and flat than 1200 specimens of cryptodiran turtles such ventral surface of costals are lacked. In as xinjiangchelyids, sinemyids and basal addition, this unnamed trionychoid is trionychoids have been discovered (Hirayama, considered as more primitive than the Adocidae 2000, 2005, 2010; Hirayama et al., 2000). and Nanhsiungchelyidae in having much wider The Kitadani Formation (the late Barremian to vertebrate scales. Especially the 5th vertebral Aptian) yields more than 730 specimens of scale overlaps the10th peripheral. cryptodiran turtles from a dinosaur quarry in Another trionychoid turtle is distinguished by Katsuyama City, Fukui Prefecture (Hirayama, its characteristic shell sculpture that decorated 2002). This turtle assemblage consists of by a coarse undulating or rugose structure, xinjiangchelyid, sinemyid and trionychoid sinuous scale sulci on its shell surface, and groups. About 84 % of the specimens are broader vertebral scales than those of the above assigned to the Trionychoidea such as the trionychoid (Hirayama, 2005). Adocidae, Nanhsiungchelyidae and Trionychidae. The Akaiwa Formation The Kitadani Formation embedded between the Kuwajima and Kitadani The Adocidae, an extinct semi-aquatic formations yields an intermediate trionychoid, turtle family, is the most dominant turtle from Kappachelys okurai (Hirayama et al., 2012) the Kitadani Formation. We detected two The Early Cretaceous records of trionychoids different taxa such as Adocus sp. and an adocid are generally poor, whereas they were common turtle, gen. et sp. indet. Almost entire shell in the Late Cretaceous of Asia and North morphology of Adocus sp. are recovered from America. We report turtle faunas relatively hundreds of fragmentary shell materials and the profilic in trionychoid from the Kuwajima and newly collected shell assemblage of one Kitadani formations. individual. Its carapace is estimated as about

182 35 cm long in maximum size. The shell common derived character in the genus morphology is most similar to A.beatus from Basilemys from the Upper Cretaceous of North the Upper Cretaceous of North Ameica (Hay, America. A soft-shelled turtle have the 1908) except for its smaller shell size and following synapomorphies as the Trionychidae; thickend medial part of hypoplastron. vermiculated shell sculpturing, loss of scale Another adocid turtle, gen. et sp. indet., is sulci, lack of peripheral series, reduction of newly recognized on the basis of costals, plastron, and no osseous bridge between peripherals and hypoplastron materials. This carapace and plastron. It indicates that this adocid has the following synapomorphies: shell trionychid turtle could have already obtained a sculpturing with fine and regular pits, reduced quite similar morphology to extant soft-shelled proximal head of thracic rib, flat ventral suface turtles. Due to poor preservation of materials, of costal and large semicircular facet for its genus and species are not enough to be ischium on the dorsal surface of xiphiplastron. identified. It is distinguished from Adocus by the The morphological and possession of the marginal scales limited within paleoecological diversification among peripherals, and the femoral scale extending trionychoid turtles already began in the early onto the dorsal margin of hypoplastron. Early Cretaceous of East Asia. Some These features are also observed in morphological characters of trionychid, adocids Ferganemys, another adocid genus from the and nanhsiungchelyid from the Kitadani Albian of Kyrgystan and the Cenomanian of Formation suggest that they became specialized Uzbekistan (Syromyatnikova, 2011). for aquatic, semi-aquatic and terrestrial Several carapace elements are idetifiable as the environments, respectively. Although further Nanhsiungchelyidae, an extinct terrestrial new materials are desired, the fossil turtles tortoise, by shell sculpturing with course and from the Tetori Group could shed light on the irregular pits and grooves, and wide and deep morphology, diversification and phylogenetic scale sulci. The marginal scale covering the relationships of the Early Cretaceous only distal half part of the peripheral is a trionychoids.

References: Hay, O. P. 1908. The fossil turtles of North America. Carnegie Inst. Washington Publ., 75: 568 p. Hirayama, R. 2000. Fossil turtles. In, Matsuoka, H. (ed.), Fossils of Kuwajima "Kaseki-kabe" (Fossil-bluff): Scientific report on a Neocomian (Early Cretaceous) fossil assemblage from the Kuwajima Formation, Teori Group, Shiramine, Ishikawa, Japan, pp.75-92, pls.28-37. Shiramine Village Board of Edu., Ishikawa Pref., Japan. (in Japanese with English abstract) Hirayama, R. 2002. Preliminary report of the fossil turtles from the Kitadani Formation (Early Cretaceous) of the Tetori Group of Katsuyama, Fukui Prefecture, Central Japan. Mem. Fukui Pref. Dinosaur Mus., 1: 29-40. (in Japanese with English abstract). Hirayama, R. 2005. New materials of non-marine turtles from the Early Cretaceous Tetori Group of former Shiramine-mura of Hakusan City, Ishikawa Prefecture, Central Japan. In, [Scientific report on fossil animals of Kuwajima "Kaseki-kabe" (Fossil-bluff) from the Kuwajima Formation, Tetori Group, Hakusan, Ishikawa, Japan, pp.12-20, 2 figs., 3 pls. Shiramine Village Board of Edu., Ishikawa Pref., Japan. (in Japanese) Hirayama, R. 2010. Non-marine turtles from the Early Cretaceous Tetori Group of Kasekikabe of Hakusan City, Ishikawa Prefecture, Central Japan. In, [Scientific report on fossils from the Kuwajima Formation, Tetori Group, of Kuwajima "Kaseki-kabe", Hakusan City, Ishikawa, Japan], pp.19-24, 2 figs. Hakusan City Board of Edu., Ishikawa Pref., Japan. (in Japanese) Hirayama, R., Brinkman, D.B. and Danilov, I.G. 2000. Distribution and biogeography of non-marine Cretaceous turtles. Russian J. Herpetology, 7:181-198. Hirayama, R., Isaji, S. and Hibino, T. 2012. Kappachelys okurai gen. et sp. nov., a new stem soft-shelled turtle from the Early Cretaceous of Japan. In: Brinkman, D.B., P. A. Holroyd, and J. D. Gardner (eds.), “Morphology and Evolution of Turtles: Origin and Early Diversification.”, pp. 179-185. Springer, Dordrecht.

183 Syromyatnikova, E. V. 2011. Turtles of the genus Freganemys Nessov et Khosatzky, 1977 (Adocidae): shell morphology and Phylogenetic position. Proc. Zool. Inst. RAS, 315: 38–52.

184 P25: A second specimen of the crossognathiform fish Apsopelix miyazakii from the

Cretaceous Yezo Group of central Hokkaido, Japan

1Miyata, S., 2Yabumoto, Y., 3Nakajima, Y., 4Ito, Y., Sasaki, T., Hirano, H.

1Res. Inst. Sci. Eng., Waseda Univ., 1-6-1, Nishiwaseda, Shinjuku-ku, Tokyo, 169-8050, Japan ([email protected]). 2Kitakyushu Mus. Nat. Hist. Human Hist., 2-4-1, Higashida, Yahatahigashi-ku, Kitakyushu, 805-0071, Japan. 3Steinmann Inst. Geol., Mineral. Paleont., University of Bonn, Nussallee 8, 53115 Bonn, Germany 4The Univ. Mus., The Univ. of Tokyo, 113-0033, 7-3-1 Hongo, Bunkyo-ku, Tokyo, Japan. 5Fac. Edu. Integ. Arts Sci., Waseda Univ., 1-6-1, Nishiwaseda, Shinjuku, Tokyo, 169-8050, Japan.

Crossognathiforms are marine tenuistriatus and I. teshioensis, and these teleostian fishes known from the Oxfordian inoceramid bivalves indicate the Upper extending to the middle Eocene (Arratia, 2008; Turonian (e.g. Matsumoto, 1965). Arratia and Tischlinger, 2010; Nelson, 2006). In the fish fossil, the anterior part of The order Crossognathiformes consists of at the body from the snout to the pelvic insertion least five families, namely Chongichthyidae, is preserved, the dorsal fin is missing, and the Crossognathidae, Notelopidae, most of the skull bones are articulated. The Pachyrhizodontidae, and Varasichthyidae. specimen is identified as Apsopelix miyazakii, Recently, Apsopelix miyazakii, the first record by the following characters; scales are large; of the Northwestern Pacific crossognathid fish the opercle is narrow (it is not preserved in the was described from a loose gravel of the Upper holotype); the preopercle is covered by the Turonian of Nakagawa area in the northern infraorbitals (it is obscure in the holotype); the Hokkaido, Japan by Yabumoto et al. (2012). large antorbital has a groove; there is a median After that, we re-discovered a fossil fish convexity close to the posterior end of the specimen from the collection of the University frontals; and the articulation of the lower jaw is Museum, The University of Tokyo. The label behind under anterior one-third of the orbit. In information indicates that this specimen was addition, the Ponbetsu specimen shows collected from the Upper Cretaceous of Mikasa following four characters; the second area, central Hokkaido in 1955. This specimen infraorbital bone is long, and its sensory canal is well-preserved, and identified as Apsopelix runs at the middle part and branched; the fourth miyazakii, which had been known from a single infraorbital bone is observed; the specimen. Here, we describe it in detail and supracleithrum is wide and large; and the make comments on the morphological posttemporal is squamous. These characters are characters. not preserved on the holotype, and the fourth The fish fossil reported here was infraorbital bone had not been recognized in collected from the IK2013g1 site of Matsumoto the crossognathid fishes. (1965) along the Ponbetsu river by Dr. T. Among of the crossognathid fishes, Matsumoto and Mr. T. Omori, and contained in only the genus Apsopelix had been distributed the calcareous concretion from the bioturbated in Western Interior and European region at the sandy silt stone of the Ⅲa’ Formation of Late Turonian time (e.g. Taverne, 1989; Matsumoto (1965) (= the part of the Teller-Marshall and Bardack, 1978; Patterson Haborogawa Formation of Takashima et al., and Rosen, 1977). The second specimen of 2004). The Ⅲa’ Formation contains Inoceramus Apsopelix miyazakii demonstrates the 185 morphological characters and validate that distributed in the northern hemisphere at the crossognathid fishes had been widely Late Turonian time

References: Arratia, 2008, In Fishes and the break-up of Pangaea, Ed. by, Forey et al., 71–92. Arratia and Tischlinger, 2010, Fossil Record, 13, 317–341. Nelson, 2006, Fishes of the world, 601 p. Matsumoto, 1965, Memoirs of the Faculty of Science, Kyushu University, Series D, 16, 1 – 80, pls,1 – 18． Patterson and Rosen, 1977, Bulletin of the American Museum of Natural History, 158, 81–172. Takashima et al., 2004, Cretaceous Research, 25, 365 – 390. Taverne, 1989, Palaeontographica Abteilung A, 207, 79–105. Teller-Marshall and Bardack, 1987, Fieldiana Geology, 41, 1–35. Yabumoto et al., 2012, Paleontological Research, 16, 37–46.

186 P26: A mammal jaw from the Upper Cretaceous Ashizawa Formation (Futaba Group),

Fukushima, northeastern Japan

Kusuhashi, N.1, Suzuki, T.2, Terui, K.3, Sato, A.4 and Amiot, R.5

1Grad. Schl. Sci. Eng., Ehime Univ., Matsuyama, Ehime 790-8577, Japan ([email protected]). 2Iwaki Edu. and Cult. Corp., Iwaki, Fukushima 972-8326, Japan. 3Shiwa, Iwate 028-3301, Japan 4Iwaki, Fukushima 979-0201, Japan 5CNRS UMR 5276, Université Claude Bernard Lyon 1 and Ecole Normale Supérieure de Lyon, 2, Rue Raphaël Dubois, 69622 Villeurbanne Cedex, France.

We report the first discovery of a five alveoli for three teeth; the posterior four Mesozoic mammal from northeastern Japan. To are alveoli for two double-rooted teeth and the date, at least four fossil localities of Mesozoic anteriormost one is a damaged alveolus for mammals are known in central to southwestern another tooth; the posterior four contain roots Japan: from old to young, the Lower of the teeth. The anterior two roots have Cretaceous Kuwajima Formation (Tetori rounded cross section in occlusal view, Group), Hakusan, Ishikawa Prefecture (Rougier whereas the posterior two roots are oval, being et al., 2007; Kusuhashi, 2008); the Lower expanded labiolingually. Judged from the Cretaceous Kitadani Formation (Tetori Group), anteriormost alveolus, the root of this tooth was Katsuyama, Fukui Prefecture (Tsubamoto et al., probably sub-equal sized with and 2004; Miyata et al., 2013); the Lower morphologically similar with those of Cretaceous Sasayama Group, Sasayama, subsequent tooth. There is a mental foramen Hyogo Prefecture (Kusuhashi et al., 2013); and below the posterior root of the middle tooth. the Upper Cretaceous Mifune Group, Mifune, On the basis of the morphology of the Kumamoto Prefecture (Setoguchi et al., 1999; preserved dentary without the dentary Kusuhashi et al., 2008). symphysis, the size and position of the mental The fossil specimen reported here was foramen, and morphologies of the roots and discovered from the Asamigawa Member of the alveoli, the three teeth are considered to be Ashizawa Formation (Futaba Group), at Hirono postcanines. The distalmost tooth with Town, Futaba, Fukushima Prefecture, transversely expanded roots is interpreted to be northeastern Japan. The member composes the a molar or a molariform premolar with basal part of the Futaba Group, and consists labiolingually wide crown. mainly of non-marine sediments (Ando et al., The presence of transversely expanded 1995); the depositional age of the member is roots suggests that the present specimen is thought to be the early Coniacian (e.g., Kubo et highly probably not a dentary of a “triconodont” al., 2002). mammal, because “triconodont” lower The specimen is a fragment of the molariforms are usually mesiodistally longer horizontal ramus of the left dentary, which is than wide with rounded or slightly not slender. On the preserved portion of the mesiodistally elongated roots. Spalacotheriid dentary, there is no sign of the dentary dentaries are usually slender, and thus the symphysis. Unfortunately, no tooth crown is present specimen is unlikely to belong to them. preserved on the dentary, but there are at least Most mammalian fossil records from Asian

187 Upper Cretaceous belong to multituberculates, Acknowledgement metatherians, or eutherians (e.g., We thank C. Sakata (National Kielan-Jaworowska et al., 2004). The present Museum of Nature and Science, Japan), Y.-Q. specimen is, therefore, probably attributed to Wang (Institute of Vertebrate Paleontology & one of these groups, but the dentary is clearly Paleoanthropology, Chinese Academy of different morphologically from those of Sciences, China), and others for their help with multituberculates. Although it is currently computed tomography scanning of the difficult to assert whether it belongs to a specimen. This work is partly supported by a eutherian or a metatherian mammal, the first Grant-in-Aid for Young Scientists (B) (no. discovery of mammalian fossil from 24740349) from JSPS to N.K., and Projet northeastern Japan demonstrates that the International de Coopération Scientifique Futaba Group or neighboring strata have (DINASIA) from Centre National de la potential for yielding additional mammalian Recherche Scientifique, France, to N.K. and R. fossils, which will be significant to disclose the A. mammalian faunal evolution in East Asia during the Late Cretaceous.

References: Ando, H., Seishi, M., Oshima, M., and Matsumaru, T. 1995. Journal of Geography 104:284–303. Kielan-Jaworowska, Z., Cifelli, R. L., and Luo, Z.-X. 2004. Mammals from the Age of Dinosaurs: Origins, Evolution, and Structure. Kubo, K., Yanagisawa, Y., Toshimitsu, S., Banno, Y., Kaneko, N., Yoshioka, T., and Takagi, T. 2002. Geology of the Kawamae and Ide District. Quadrangle Series, 1:50,000. Kusuhashi, N. 2008. Acta Palaeontologica Polonica 53:379–390. Kusuhashi, N., Ikegami, N., and Matsuoka, H. 2008. Paleontological Research 12:199–203. Kusuhashi, N., Tsutsumi, Y., Saegusa, H., Horie, K, Ikeda, T., Yokoyama, K., and Shiraishi, K. 2013. Proceedings of the Royal Society B 280:20130142. Miyata, K., Shibata, M., and Azuma, Y. 2013. Abstracts with Programs, the 2013 Annual Meeting, the Palaeontological Society of Japan:33. Rougier, G.W., Isaji, S., Manabe, M. 2007. Annals of Carnegie Museum 76:73–115. Setoguchi, T., Tsubamoto, T., Hanamura, H. and Hachiya, K. 1999. Paleontological Research 3:18–28. Tsubamoto, T., Rougier, G.W., Isaji, S., Manabe, M., Forasiepi, A.M. 2004. Acta Palaeontologica Polonica 49:329–346.

188 P27: Dinosaur remains from the mid-Cretaceous shallow marine sediments of

the Futaba Group, Japan

Ohashi, T.1, Hasegawa, Y.2, and Suzuki, C.3

1Kitakyushu Mus. Nat. Hist. and Human Hist., 805-0071, Kitakyushu, Japan ([email protected]) 2Gunma Mus. Nat. Hist., 370-2345, Takaoka, Japan 3Iwaki City, Fukushima, Japan

The Futaba Group—which is the Ashizawa Formation. The base of the tooth distributed in Hirono Town and Iwaki City, specimen’s crown is preserved. The cingulum Fukushima Prefecture, Japan—consists of is not prominent on the crown base. A fluvial to shallow marine sediments (Coniacian prominent primary ridge is present at the to Santonian). This Group is known for midline of the crown, whereas secondary ridges yielding marine invertebrate and vertebrate are absent. Fine vertical wrinkle-like structures fossils, and is divided into the following three cover the crown surface. The cross-sectional formations in the ascending order: Ashizawa shape is pentagonal. No wear facet is observed Formation, Kasamatsu Formation, and because of the preserved condition. The Asamigawa Formation. Dinosaur remains have external surface of the right sternal bone can be been recovered from the Ashizawa and obsereved. The bone is about 120 mm long. Kasamatsu Formations. The caudolateral process is as long as the craniomedial plate, whose middle part is Sauropod dinosaur broken. The medial ridge of the surface is An isolated tooth is found in the slightly convex. The size of this sternal bone is Kasamatsu Formation. It is cylindrical, with a small as compared with the sternal bone of crown length of about 34 mm. No wear facet is other hadrosaurid dinosaurs. observed, although one side of the crown’s top Sauropod and Hadrosaurid dinosaurs is broken. The crown shape does not resemble have been reported from the Futaba Group in that of the previously reported sauropod teeth previous studies; however, the specimens found in the Futaba Group. reported here differ from the previously reported ones in shape. These findings facilitate Hadrosaurid dinosaur a better understanding of the dinosaurian fauna An incompletely isolated tooth and of the Futaba Group. almost complete right sternal bone are found in

189 P28: Record of Seribiscutum primitivum, a high latitude, bipolar nannofossil taxa from

Jaisalmer Basin: Implications on palaeogeographic distribution

Singh,A. and Rai, J.

Birbal Sahni Inst. Palaeobot., 53, University Road, Lucknow, Uttar Pradesh, India-226007

([email protected]; [email protected])

Seribiscutum primitivum, a restricted distribution between 40º to 50º N and representative of cold water masses is recorded 35º to 60º S latitudes (Mutterlose, 1992; from Albian age surface sample of Pariwar Baumgartner et al., 1992). The biogeographic Formation and Albian to Santonian age expanse of several oceanic sites containing S. subsurface samples of Tanot #1, Jaisalmer primitivum may reflect latitudinal changes in Basin, western India. temperature and or effect of ocean circulation. Global occurrences of S. primitivum The indication of warm water influx in from the high to mid latitudes of northern and the Albian nannofloral assemblage from southern hemispheres are documented by Jaisalmer Basin is evident by the occurrence of Kulhanek and Wise (2006). The previous few Nannoconus spp. both in surface and Indian record of S. primitivum is from Cauvery subsurface samples. Abundance of Nannoconus Basin lying in southern mid-latitudinal position spp.is restricted to warm surface waters and its (Kale & Phansalkar, 1989). The presence of distribution in Tethyan realm can be explained this species in Jaisalmer basin indicates by temperature control (Mutterlose, 1989; incursion of cooler water currents in western Dumoulin and Bown, 1992). Further, rarity of Rajasthan during Albian - Santonian time. Rhagodiscus asper is thought to reflect cold Jaisalmer Basin was situated ~ 35º S latitudinal water surface temperature (Erba, 1987). There position during Albian time as is evident in is progressive increase in R. asper specimens most of palaeogeographical reconstructions. from Albian to Santonian time in Jaisalmer The distribution of calcareous succession followed by occurrence of nannoplankton is mainly governed by the light Nephrolithus spp., another cold water taxa. intensity, temperature, nutrient availability, The coexistence of Nannoconus spp. salinity and water depth (Tappan, 1980). The and S. primitivum suggests mixing of degree to which these factors affect the nannoflora due to the mixing of warm and cold distribution pattern is uncertain. The bipolar water masses as the study area was transitional distribution of S. primitivum and presence of between low latitude (Tethyan) and high certain Tethyan taxa (nannoconids) in the latitude (? Austral) provinces and perhaps it present assemblage may be explained by also implies to the limit of their ecological temperature control. S. primitivum has a tolerance.

References: Baumgartner, P.O., Bown, P.; Marcoux, J., Mutterlose, J., Kaminski, M., Haig, D & McMinn,A. 1992. Early Cretaceous biogeographic and oceanographic synthesis of Leg 123 (Off northwestern Australia). Proc. of ODP, Sci. Res., 123: 739-758.

190 Dumoulin, J.A. & Bown, P.R. 1992. Depositional history, nannofossil biostratigraphy and correlation of Argo abyssal plain Sites 765 and 261. Proc. of ODP, Sci. Res., 123: 3-56. Erba, E. 1987. Mid-Cretaceous cyclic pelagic facies from the Umbrian-Marchean Basin: what do the nannofossils suggest? INA Newsletter, 9: 52-53. Kale, A.S. & phansalkar, V.G. 1992. Nannofossil biostratigraphy of the Utatur Group, Trichinopoly district, South India. Mem. di Scienze Geol., XLIII: 89-107. Kulhanek D.K. & Wise, S.W. Jr. 2006. Albian calcareous nannofossils from ODP Site 1258, Demerara Rise. Revue de Micropaléontologie, 49: 181-195. Mutterlose, J. 1989. Temperature controlled migration of calcareous nannofloras in the NW European Aptian. In: Crux, J.A. and Heck, S.E. van (eds). Nannofoosils and their applications. Ellis Horwood, Chichester: 122-142. Mutterlose, J. 1992. Biostratigraphy and palaeobiogeography of Early Cretaceous calcareous nannofossils. Cretaceous Res., 13: 167-189. Tappan, H. 1980. The Paleobiology of Plant Protists: San Francisco (W.H.Freeman).

191 P29: Aptian micro-organisms captured in amber: first records from the eastern

margin of Eurasia

Kubota, A.1, Iba, Y.1, Hikida.2, Y and Yi, K.3,

1Dept. Nat. Hist. Sci., Hokkaido Univ., 060-0810, Hokkaido, Japan ([email protected]) 2Nakagawa Mus. Nat. Hist., 098-2626, Hokkaido, Japan 3Korea Basic Sci. Inst., 363-883, Chungbuk, Korea

Introduction geological age was determined by age Micro- and soft-bodied organisms diagnostic ammonites and SHRIMP U-Pb such as insects and fungi play an important role dating of zircon in the intercalated tuff. in terrestrial ecosystems during the Earth’s Bio-inclusions of amber are observed under a history. Especially, they have promoted digital zoom microscope for systematic evolution of plants that are essential elements determinations. of terrestrial environment. Angiosperms, which arose in the Early Cretaceous and now accounts Results and Discussion for 98％ of living terrestrial plants species, Amber is highly abundant in proximal have also co-evolved with insects and fungi by turbidites, which overlies the deep-sea their pollination, decomposition and nutrient mudstone of the uppermost part of the Sorachi supply. Group. This observation implies the existence Fossil records of micro- and of an enigmatic sedimentary event at the soft-bodied organisms are mostly restricted to boundary between the Sorachi and the Yezo amber because amber protects them from Group, which transported numerous resins into pressure, decomposition or oxidization the deep sea by turbidity currents. The (Martínez-Delclòs et al., 2004; Perrichot and depositional age of amber-turbidite is about Girard, 2009). In amber, we can observe 118 Ma (late Early Aptian). Numerous three-dimensionally preserved organisms. The terrestrial bio-inclusions occur in the amber, Mid-Cretaceous represents the most important such as arthropods (e.g., Diptera, Chacidoidea, period for understanding the initial mite), fungi (unidentified mycelium, spore-like co-evolution between insects, fungi, and objects, and septum), pollens (Classopollis? angiosperms. Though Mid-Cretaceous amber and Cyatheaceae?), plant fragments (tracheids localities are rare, we recovered new amber and stellate hair). These occurrences are the containing deposits in northern Japan. first reports of bio-inclusions in the Aptian amber from the eastern margin of Eurasia. Geological Settings and Methods Tricolpate pollen, the pollen type of The Yezo Group is exposed in a belt predominant angiosperm groups at present, has roughly 1200 km long from Sakhalin Island to recently been reported from uppermost part of southern Hokkaido and consists of a thick Sorachi Group in the same area Aptian to Paleocene fore-arc siliciclastic (Barremian?-Aptian) (Tanaka and Hirano, sequence. Amber-concentrated strata are 2009). This represents the oldest record of intercalated in the lowest part of the Yezo angiosperm in Asia at all. Further studies of the Group in Nakagawa area, northern Hokkaido, Aptian amber bio-inclusions will provide Japan. To clarify depositional environments critical information about earliest and processes of ambers, sedimentary and co-evolutionary history of angiosperm and ichnofacies analyses have been done. The micro-biota.

192

References: Martínez-Delcòs, X., Briggs, D. and Peñalver, E. 2004. Taphonomy of insects in carbonates and amber. Palaeo-3, 203: 19-64. Perrichot,V. and Girard,V. 2009. A Unique Piece of Amber and the Complexity of Ancient Forest Ecosystems. Palaios, 24: 137-139. Tanaka, S. and Hirano, H. 2009. First Appearance of Angiosperm pollen in the Japanese Cretaceous: Pollen Fossils from the Lower Cretaceous of the Teshionakagawa area of Hokkaido. Palynol. Soc. Japan, 55: 67-75.

193 P30: The tentative new Cretaceous non-marine ostracods from the southern coast of

Korean peninsula

Choi B.-D.1, Jugdernamjil, M. 2 and Huh, M.1

1Dept. Earth Sys. Env. Sci. & Korea Dinosaur Res. Center, Chonnam Nat. Univ., Gwangju 500-757, Republic of Korea ([email protected]) 2Paleont. Center, Mongolian Acad. of Sci., Enkhtaivan Avenue, 63 Ulaanbataar, Mongolia

We have many Cretaceous terrestrial principalis, Mongolocypris hampyeongensis sp. basins in Korea. Especially various kinds of nov., and Mongolocypris huhi sp. nov.. 2) Jinju fossils including vertebrates, invertebrate and Formation: Cypridea sp. 1, C. sp. 2, C. sp. 3, C. plant fossils are found from the Cretaceous sp. 4, C. sp. 5, Mongolocypris sp. 1, M. sp. 2., sedimentary deposits. Among them, the Scabriculocypris jinjuria, Lycopterocypris sp., Hampyeong Basin (Aptian? – Albian?) and the Candona sp., Limnocypridea? sp., Djungarica Jinju Formation (Albian; the lower part of sp. and Darwinula sp.. Among the ostracods, Gyeongsang Basin) are the most Mongolocypris hampyeongensis, well-preserved ostracod fossil deposits in South Mongolocypris huhi, Mongolocypris sp. 1 and Korea. In this study, we collected 11 species of Mongolocypris sp. 2 are considered as new 6 genera from the Black shale of the species, and former Cypridea Hampyeong Basin in Hampyeong County, and (Pseudocypridina) jinjuria Choi, 1990 revised also 13 species of 7 genera were identified as a species of genus Scabriculocypris. These from the Black shale of the Jinju Formation in four species of genus Mongolocypris and Jinju City. All ostracods species are divided by revised species of Scabriculocypris are to be biostratigraphic units as follows: 1) described further. The results of this study are Hampyeong Basin: Cypridea subprognata, C. expected to provide more information for cf. changluensis, C. sp., Darwinula aff. paleoecological and paleoenvironmental Leguminella, Candona cf. arcinaeformis, C. sp., reconstruction of Cretaceous strata in East Asia. Lycopterocypris cf. profunda, Timiriasevia

194 P31: Cheilostome bryozoans from the Upper Cretaceous Himenoura Group, Kyushu,

Japan

Sakamoto, C.1, Dick, M. H.2, Komatsu, T.1, and Miyake, Y.1

1Grad. Schl. Sci. Tech., Kumamoto Univ., 2-39-1 Kurokami, Chuo-ku Kumamoto 860-8555, Japan ([email protected]) 2Dept. Nat. Hist. Sci., Fac. Sci., Hokkaido Univ., N10 W8, Sapporo 060-0810, Japan ([email protected])

Cheilostomes (Phylum Bryozoa, Class part of the section at Loc. 01b, and in the upper Gymnolaemata, Order Cheilostomata), the part at Loc. 02. Bryozoan colonies, corals, and dominant modern bryozoan group, originated calcareous serpulid tubes commonly encrust in the late Jurassic. Starting in the large inoceramid and ammonoid shells. mid-Cretaceous (late Albian to early From approximately 50 bryozoan Cenomanian), they began an explosive specimens collected at Locs. 01b and 02, we radiation that has continued to the present. detected 5 cheilostome species, 4 of them Prior to our study, there were few records of forming multiserial encrusting colonies and any Cretaceous cheilostome from eastern Asia. another forming an erect, branching colony. Upper Cretaceous (Santonian- We have preliminarily identified the encrusting Maastrichtian?) strata in the Himenoura Group species as Conopeum sp. nov., Marginaria sp. are widely distributed on the Amakusa and nov., Charixa sp., and ?Antropora sp. The Koshikijima Islands, southwestern Kyushu, generic assignment of the erect species is Japan. Lower to Middle Campanian strata in unclear. Species of Conopeum and Antropora this group consist of non-marine and shallow have previously been reported from Cretaceous marine siliciclastics, and crop out in the shelf sediments in the USA and England, and Kashima area, northern Shimokoshikijima both genera persist today. Charixa has been Island. In western Nakayama in the central part reported from Early Cretaceous shallow marine of the Kashima area, Lower to Middle deposits in England, South Africa, and Japan. Campanian outer-shelf mudstone is exposed In the USA and Europe, Upper (Locs. 01a-g) and yields abundant bivalves, Cretaceous bryozoan assemblages are gastropods, ammonoids, echinoids, bryozoans, characterized by a high diversity of and radiolarians (Komatsu et al., 2014). At cheilostomes. For example, Taylor and Locs. 01a-g and 02, a section of mudstone McKinney (2006) reported 94 cheilostome about 20 m thick, intercalated with thin species from Campanian-Maastrichtian laminated sandstone beds and layers, is siliciclastic and chalky sediments on the subdivided into lower and upper parts. The Atlantic and Gulf Plains of the USA. In lower part yields the Santonian to Lower contrast, the bryozoan assemblage in the Campanian ammonoid Eupachydiscus haradai Campanian Himenoura Group is low in and Santonian to Campanian Inoceramus diversity (both of cheilostome and cyclostome assemblages consisting mainly of Inoceramus bryozoans). In this study, we will focus on ezoensis and Inoceramus toyajoanus. The comparing the composition of Campanian upper part is characterized by the Middle cheilostome assemblages in the Himenoura Campanian bivalve Sphenoceramus schmidti. Group with coeval Tethyan assemblages. Abundant bryozoan fossils occur in the lower

195

Fig. 1 Scanning electron microcope (SEM) images of silicone casts of bryozoan colonies. A, B, Conopeum sp. nov. A, Autozooids, with paired, triangular kenozooids at corners of proximal gymnocyst. B, Enlargement showing buttressed pore chambers. C, Marginaria sp. nov. Part of colony, showing autozooids, ovicells, and avicularia. D, Charixa sp. E, ?Antropora sp. F, Part of an erect, branched cheilostome colony. Scale bars: (A) 0.2 mm; (B) 0.05 mm; (C, D, E) 0.5 mm; (F) 1 mm.

References: Taylor and McKinny, 2006. Cretaceous Bryozoa from the Campanian and Maastrichtian of the Atlantic and Gulf coastal plains, United States. Scripta Geologica, 132, 1–346. Komatsu et al, 2014. Stratigraphy, fossils and depositional environments of the Upper Cretaceous Himenoura Group on the Koshikijima Islands. Excursion Guidebook, Journal of the Geological Society of Japan, Supplement. (In press)

196 P32: Characteristics and modes of construction of rudist-bearing reefs unique to the Yura

area, Wakayama Prefecture, southwest Japan

Hirata, Y.1, Minami, S.2, 3, Adachi, N.1, and Ezaki, Y.2

1Dept. Geosci., Naruto Univ. of Edu., Naruto, Tokushima 772-8502, Japan ([email protected]) 2Dept. Geosci., Osaka City Univ., Sugimoto, Sumiyoshi-ku, Osaka 558-8585, Japan 3JA Coop., Koraibashi, Chuo-ku, Osaka 541-0043, Japan (Present address)

Introduction the field and on polished slabs and thin sections. Rudists, which were sessile gregarious We then discuss the modes of construction of bivalves that appeared in the Late Jurassic and the rudist-bearing reefs in light of mutual disappeared at the end of the Cretaceous, relationships between the rudists and formed dense usually monospecific microencrusters. aggregations on carbonate platforms during the Cretaceous (Hernández, 2011). However, Characteristics of rudist-bearing reefs occurrences of Late Jurassic–earliest A lenticular fossiliferous limestone Cretaceous rudists in reef environments have body (37 m in thickness) was examined in the not been fully documented. A well-developed Yura area, Wakayama Prefecture. The Upper Jurassic–Lower Cretaceous limestone rudist-bearing reefs, which take the form of mass in southwest Japan (the so-called small-scale domes (0.5–2.5 m in height), are Torinosu Limestone) contains abundant prominently developed at intervals of 6 to 15 m. reef-building organisms such as corals, The reefs are constructed on oolitic and stromatoporoids, and microencrusters (e.g., peloidal limestones, and show lateral Shiraishi and Kano, 2004; Ohga et al., 2013). transitions to bioclastic limestone in which Rudists have been recently reported from the domal and tabular stromatoporoids or Torinosu Limestone at several localities (e.g., branching corals are preserved in places. The Sano et al., 2008; Sano and Skelton, 2010; rudists occupy up to 40%–45% of the volume Kakizaki et al., 2011). Kakizaki et al. (2011) of the reefs. They show remarkably asymmetric reported that some rudists and associated growth forms (~2.0 cm in diameter) consisting microencrusters produced small framestones. of a much larger conical (right) valve and a However, no previous study has documented smaller opercular (left) valve. The valves of the relationship of these Late Jurassic–earliest most of the preserved rudists are articulated, Cretaceous rudists to reef construction. Here, and little damage to the shells was observed. we report on a primitive group of rudists The conical right valves are attached directly to (Diceratidae, Valletia) that, along with a variety the substrate, which is comprised of microbial of microencrusters, constructed reefs which are micrite. The aggregated rudists tend to grow in preserved in the Yura Formation in the Yura the same direction. The surfaces of the rudists area, Wakayama Prefecture, Japan. The Yura are directly encrusted by various Formation, which belongs to the Chuki microencrusters, including Lithocodium, Complex of the Southern Chichibu Terrane Ortonella, and Girvanella, and Bacinella fills (e.g., Yao, 2012), includes late Kimmeridgian the remaining spaces. Bacinella is the most ammonites (Zeiss et al., 2003) and Late abundant microencruster, with subordinate Jurassic radiolarians (Yao, 1985). First, we Lithocodium, Ortonella, and Girvanella. describe the characteristics of the Well-sorted ooids, peloids, and bioclasts rudist-bearing reefs based on observations in (including foraminifers and thin-shelled 197 bivalves) are found within the interiors of frameworks. Thus, although different in scale, individual rudists, as well as within the rudist-bearing structures in both areas may inter-framework spaces. have been produced through similar processes; i.e., by the combined activities of rudists and Modes of construction of rudist-bearing microencrusters. reefs The evidence described above In most cases, the rudists observed in suggests that reefs in the Yura area were the Yura area possess articulated valves, are constructed through mutual interactions preferentially oriented, and are well preserved. between rudists and microencrusters, according The available evidence suggests that the rudists to the following succession. (1) Microbes first were preserved in a growth position. Whether became established on the bioclastic or oolitic or not they formed rigid reef frameworks or sediments and stabilized the underlying were merely bafflers forming bafflestones is a sediments. (2) Rudists colonized the stabilized matter of debate (e.g., Gili et al., 1995; Flügel, sediments. (3) Lithocodium, Ortonella, and 2004). The rigid frameworks in the Yura area Girvanella directly encrusted the surfaces of were not constructed by rudists alone. Rather, the rudists, and were then substrates for further abundant microencrusters played a pivotal role encrustation. Bacinella filled the in consolidating the rudist frameworks, by inter-framework spaces in the encrusting their surfaces and filling inter-rudist rudist-microencruster frameworks. Bacinella, spaces. Thus, the rudists constructed the reefs which was the most abundant microencruster, with rigid frameworks, with the aid of various was important as an encruster, binder, and microbial organisms that stabilized, encrusted, consolidator of reef frameworks. (4) filled, and consolidated the reef framework. Gregarious rudists further colonized the Although not reported as reef structures, framework and grew upwards in association small-scale (~1–2 m) rudist and microencruster with the activities of microencrusters. Thus, a framestones were recently reported from the series of reef-building processes led to the Torinosu Limestone in the Shirokawa area, construction of the rudist-microbial reefs. Ehime Prefecture, Japan (Kakizaki et al., The modes of reef construction provide us 2011); however, the rudist-bearing structures in with invaluable information on the early this area differ from those in our study, which evolution and palaeoecology of rudists, on are much larger in scale and exhibit a greater transitions involving the compositions and diversity of microencrusters. However, the structures of reefs during the Late Jurassic and rudist-bearing structures in both the Yura and Cretaceous, and on marine palaeoenvironments Shirokawa areas include abundant which were suitable for colonization by microencrusters (e.g., Bacinella) which rudist-microencruster communities. contributed greatly to the construction of the

References: Flügel, E. 2004. Microfacies of carbonate rocks: analysis, interpretation and application. Springer-Verlag, Berlin Heidelberg. Gili, E., Masse, J.P., and Skelton, P.W. 1995. Rudists as gregarious sediment-dwellers, not reef-builders, on Cretaceous carbonate platforms. Palaeo-3 118: 245-267. Hernández, O.J. 2011. Fossils Explained: Rudists. Geology Today 27: 74-77. Kakizaki, Y., Sano, S., and Kano, A. 2011. Autochthonous occurrence of rudist and microencrusters from the Late Jurassic Torinosu-type Limestone in Nakatsugawa in the Shirokawa area, western Shikoku, Southwest Japan. Mem. Fukui Pref. Dinosaur Mus. 10: 113-20 (in Japanese with English abstract) Ohga, H., Kolodziej, B., Noze, M., Schmid, D.U., Takayanagi, H., and Iryu, Y. 2013. Sedimentary facies and biofacies of the Torinosu Limestone in the Torinosu area, Kochi prefecture, Japan. Island Arc 22: 150-169. Sano, S., Morino, Y., Skelton, P.W., Mimoto, K., Nose, K., and Hirota, T. 2008. Late Jurassic-earliest Cretaceous rudists from the Torinosu-type limestones in Southwest Japan-preliminary report. Mem. Fukui Pref. Dinosaur Mus. 7: 67-81 (in Japanese with English abstract) 198 Sano, S., and Skelton, P.W. 2010. Epidiceras (Bivalvia, Hippuritoidea) from the Tithonian-Berriasian Torinosu-type limestones of the Sakawa area, Southwest Japan. Turkish J. Earth Sci. 19: 733-743. Shiraishi, F., and Kano A. 2004. Composition and spatial distribution of microencrusters and microbial crusts in upper Jurassic-lowermost Cretaceous reef limestone (Torinosu Limestone, southwest Japan). Facies 50: 217-227. Yao, A. 1985. Geology of Yura Town. In: Ichikawa, K., Ishii, K., Yamagiwa, N., and Yao, A. (eds.) Geology of Yura Town. Record of Yura Town (Vol. Hist. Materials): 8-27. (in Japanese) Yao, A. 2012. The Chichibu and Kurosegawa terranes in the western part of the Kii Peninsula. J. Geol. Soc. Japan 118: 90-106 (in Japanese) Zeiss, A., Schwegert, G., Sato, T., and Yao, A. 2003. Late Kimmeridgian Ammonites from the Yura Formation of Kii, SW Japan. Neues Jahrbuch für Geologie und Paläontologie 2003-1: 1-10.

199 P33: Bivalves from the Upper Cretaceous Himenoura Group on Shimokoshiki-jima Island,

Kagoshima, Japan

Miyake, Y. and Komatsu, T.

Grad. Schl. Sci. Tech., Kumamoto Univ., Kumamoto 860-8555, Japan ([email protected])

The Upper Cretaceous Himenoura deposits yield abundant brackish-water Group is exposed on the northern part of bivalves Crassostrea sp. and Corbula Shimokoshiki-jima Island, Kagoshima ushibukensis. In-situ preserved Crassostrea Prefecture, Kyushu, Japan. The group colonies are commonly found in the tidal composed mainly of non-marine to marine deposits characterized by tidal bundles and fossiliferous siliciclastic deposits. The bioturbated sandstones. In-situ preserved successions of this group are important for Yaadia koshikiana and Yaadia japonica are understanding regional correlations, coastal common in the lower Campanian upper environments and brackish-water and shallow shoreface sandstones. The middle Campanian marine fauna during the Upper Cretaceous in upper shoreface sandstone yields only the East Asia. autochthonous Yaadia japonica. Abundant In the study area, the Himenoura shell concentrations consisting of Loxo Group is divided into three parts, the lithologic japonica and Glycymeris amakusensis are unit B4 described by Tanaka and Teraoka embedded within lower shoreface to inner shelf (1973), Nakayama and Imuta formations sandstone containing hummocky (newly defined) in ascending order. The cross-stratification. Autochthonous and Nakayama Formation composed mainly of parautochthonous L. japonica and G. shallow marine sandstone and mudstone amakusensis are found in bioturbated sandstone contains the upper Santonian to lower overlying hummocky cross-stratified sandstone. Campanian Eupachydiscus haradai Inoceramus ezoensis, I. toyajoanus, (ammonoid) and the middle Campanian Sphenoceramus naumanni, Apiotrigonia Sphenoceramus schmidti (inoceramids). The imutensis, A. postonodosa, Ezonuculana sp. Imuta Formation is characterized by and “Eriphyla” sp. are collected abundantly non-marine deposits yielding brackish-water from outer shelf mudstone. In-situ preserved bivalves (Crassostrea) and in-situ roots, and is Nanonavis sachalinensis, Acila hokkaidoensis overlain by the middle Campanian marine and G. amakusensis are common in bioturbated deposits (Aramaki et al., 2013). sandy mudstone of shelf deposits. Slope facies We collected over 30 species of bivalves from characterized by slump deposits contain the slope, shelf, shoreface, and tidal deposits in articulated Nucula sp. and Nanonavis sp. the Nakayama and Imuta formations. Tidal

References: Tanaka and Teraoka, 1973. Bulletin of the Geological Survey of Japan, 24, 157-184. Aramaki, Komatsu, Miyake, Takahashi and Tsutsumi, 2013. Journal of the Geological Society of Japan, 119, 45-50.

200 Geoparks highlighting Cretaceous

P34: Working on ‘Amakusa Goshoura Geopark’

Ugai, H.1, Hirose, K.1, Hase, Y.1, Miyake, Y.2 and Komatsu, T.2

1Goshoura Cretaceous Mus., 866-0313, Amakusa, Kumamoto, Japan 2Kumamoto Univ., 860-8555, Kumamoto, Japan

Abstract Himeura Group are exposed at various places, Goshoura area is located on the mostly in central part of Goshura Islands. At southeastern coast of Amakusa Islands in Isle of Maeshima and western coast of Kumamoto Prefecture, and is surrounded by Goshoura Island, some lower part of these calm sea. Goshoura Town consists of 18 strata contains abundant remains of ammonite, isolated islands, including 15 uninhabited large marine bivalves and rarely fish and islands, extending 7 kilometers southeast of echinoderms. On the basis of fossil zones such Amakusa Islands. Rare display of dinosaur and as Ammonite fossil zone and radiolarian mammalian fossils and experience of shell biostratigraphic zone, are found at the lower fossils hunting in this island are attracting part of the Himeura Group to late Cretaceous visitors. age (85 million years).

Geology of Goshoura area in Amakusa Working on ‘Amakusa Goshoura Geopark’ Islands The board of education of Amakusa The geology of Goshoura Islands City has a project based on a cultural consists of Cretaceous and Tertiary strata. promotion plan called “All Islands Museum” Cretaceous strata are widely exposed from which proposes a design for a network of central to eastern part of these islands, such as cultural facilities and a kind of field museum Goshoura, Makishima and Yokoura Islands. designed to promote cultural and historical They are divided into the Goshoura and heritage sites in the city. In conjunction with Himeura Groups in ascending order. Tertiary this, there is a proposed plan entitled ‘Amakusa strata are narrowly exposed in western part of Geopark.’ The plan will start at the Goshoura the Makishima, Yokoura and Takeshima area and will eventually cover all of the Islands, and they are divided into the Miroku Amakusa Islands. After that, an application and Hondo Groups. will be made to add Amakusa Geopark to the The Goshoura Group of lagoonal or Global Geopark Network. shallow marine siltstone and lacustrine There are many important geologic sandstone that are alternating with aspects including valuable fossils of dinosaurs, conglomerates and shales is mainly formed of mammals and mollusks in the Goshoura area. middle Cretaceous age (98 million years). There are over 40 educational spots for finding These strata are distributed in eastern part of fossils in the area, a fossil park, a show-house Goshoura Island. Fossil remains of dinosaurs, of ammonite and others with plates for turtles, crocodiles, fish, crustaceans, mollusks explanation, not to mention various dinosaur and plants have been found here. Fossil remains. remains of dinosaur are found at three horizons There are short trip programs giving in these strata on Eboshoi quarry, Kyodomari elementary, junior high school and high school bay and in the Hanaokayama fossil park. students hands-on experience in fossil The deep-sea clays or shakes that are identification and gathering. The programs for alternating with some thinner sandstones of the tourists, which include taking fossils, learning a 201 traditional fishing method called tontoko-ryo some neighboring city and town will apply to and a home-stay plan. have Amakusa Geopark join the Global We think that the actions and events Geoparks Network. which began in 1997 in Goshoura area, already We have some plans to encourage comply with the main theme of the geopark. volunteer service and will prepare English Amakusa City will start consultation for language geologic guide panels. We will also Amakusa Geopark in 2009 and will apply to continue to produce successive plans for the the Japanese Geopark Committee. Within three park and publish a guidebook for Japanese years from that time, Amakusa City, along with visitors.

202 P35: Selecting potential geosites in the eastern Kii Peninsula, Southwest Japan

Dorota Kapuscik

Dept. Edu., Waseda Univ., 169-8050, Shinjuku-ku Tokyo, Japan ([email protected])

The concept of geosite gives various either, therefore, proposed locations require opportunities for local economy growth and more promotion activities and should be popularization of geological knowledge. The supported by a secondary offer. eastern Kii peninsula presents various This work also focus on the lack of geological features formed by plate subduction geotouristic infrastructure that would make along trenches, such as the accretionary available all site’s advantages for educational complexes, a high-pressure metamorphic rocks and tourism purposes. An improvement of and the Median Tectonic Line (MTL). The aim existing facilities, such as JR Sangu Line to of this presentation is to describe the form a kind of ‘geo-train’ offering trips along geotouristic potential of the study area based on the MTL in the Ise City, might be significant the presence of significant rock exposures and for geotouristic activities in the region. set the basis for establishing geosites in future. Establishing a tentative geotouristic courses, A first selection of prospective sites including the location of the MTL in the Geku was made, based on study documents on the (outer) Shrine of the famous Grand Shrine and geomorphology and history of the eastern Kii the Arashima coast area, would give a Peninsula, and collecting data from surface relatively easy access to most valuable sites, exposures in analyzed areas. Geologically whereas an access to geological information important objects have been picked up together about particular site on the Internet and/or with places of unique history and culture within provided by information boards might enhance the Ise and Toba City. In fact, the potential of the attractiveness of selected objects and help this region is not properly used and most of tourists with better understanding the geology interesting geological sites are not well known of visited area.

203 P36: Hakusan Tedorigawa Geopark: activity utilizing Early Cretaceous fossils and

terrestrial sequences

Hasegawa, T.1 and Hibino, T.2

1Faculty of Natural Systems, Institute of Natural Science and Engineering, Kanazawa University, 920-1192, Kakuma-machi, Kanazawa, Ishikawa, Japan. [email protected] 2Hakusan Tedorigawa Geopark Promotion Council, 924-8688, 2-1 Kuramitsu, Hakusan, Ishikawa, Japan. [email protected]

Hakusan Tedorigawa Geopark Topography of the geopark is also full encompasses over the entire area of Hakusan of diversity: from highly elevated alpine belt City, Ishikawa Prefecture in the Hokuriku (altitude of 2,702 m), the Tedori River flow region, Japan. It is selected as a national through the upper stream of V-shaped valley, geopark (Japanese Geopark) by Japanese the midstream with river terraces, beautifully Geopark Committee in 2011 and continues its expanded fan at the mouth of the valley and activity to join Global Geopark Network as a finally reaches to the Japan Sea. A dramatic 72 member near future. km has a spectacular variety of riverine topography as a natural textbook of an ideal The main concept of the geopark is river. “Water nurtures the lives – on the way through the Mountain, River and Sea”. On the basis of These geologic and topographic the water circulation in the area of Hakusan resources are utilized for learning how strata City, we emphasize water movement on and and surface topography are evolved. Movement beneath the ground and associated erosion, of water is emphasized as “Journey of Water”, transportation and sedimentation observed in and special attention is also paid to such a compact area. transportation of debris as “Odyssey of Stones”: such romantic “tour story” is utilized Geology of the area is composed of not only for travelers but also for regional variety of elements: metamorphic rocks students and people as a part of scientific associated with collision of microplates in late education. Paleozoic, Early Cretaceous non-marine fresh water, brackish water and marine sediments, debris flow deposits derived from intensified volcanic activities during Late Cretaceous through Cenozoic, volcanics erupted in association with Japan Sea opening during Miocene, volcanics erupted during Quaternary. The Early Cretaceous Tetori Group, which is mainly non-marine fresh water sediments, is a special component of this geopark because of its variety of fossils. It is internationally well-known strata as it could give clue to understanding the evolution of the Jurassic and Cretaceous animals and plants, and their communities.

Outcrop of fossil bluff in Hakusan Tedorigawa Geopark. Many 204 scientific descriptions of Early Cretaceous animals are made from this outcrop. The journey and odyssey of water and water and stones that nurture lives through stones, the topics of this geopark are often deep ancient period until now and future. The recognized as phenomena over the surface of Tetori Group, Early Cretaceous strata is an the present ground; however, they also give a important resource for Hakusan Tedorigawa principle of strata formation and evolution of Geopark that plays a role to extend the range of the earth: it is another story to tell. The fossil geostories and entire picture of the geopark. site, “fossil bluff” of the Tetori Group is a The odyssey is on and beneath the ground geosite that plays important role for this AND trough time. geostory.

We can realize the flow regime of prehistoric river from the alternating beds of Keywords: Kuwajima Fossil Bluff, Tetori sandstone and mudstone. The fossil community Group, Journey of water, Odyssey of stones, from the outcrop gives us a specific impression Water nurtures lives –on the way through the of the environment of ancient river with mountains, rivers, and sea., Mt. Hakusan, ecosystem rich in diversified animals and Tedori River. plants. The strata, fossils and outcrop of Kuwajima fossil bluff geosite help the tourist to study the uninterrupted journey and odyssey of

205 P37: Geopark activities utilized results and materials of Cretaceous researches in the

Mikasa Geopark, Japan

Kurihara, K.1, 3 and Shimomura, K.2, 3

1Mikasa City Mus., 1-212-1 Nishiki-cho, Ikushumbetsu, Mikasa, Hokkaido 068-2111, Japan 2Reg. Develop. Geopark Prom. Div., Mikasa City Office, 2 Saiwai-cho, Mikasa, Hokkaido 068-2192, Japan 3Sec. Mikasa Geopark Prom. Coun., 2 Saiwai-cho, Mikasa, Hokkaido 068-2192, Japan

The Mikasa Geopark, admitted to the the Yezo Group. Moreover, the Cretaceous Japanese Geoparks Network (JGN) in 2013, is period was characterized by one of the warmest located in the central Hokkaido, Japan. The climates during the Phanerozoic. Knowledge of JGN is a specified non-profit organization the Cretaceous ocean-climate systems, which provides support and a networking therefore, provides important information for platform for Japanese Geoparks and aspiring our life and environments undergoing the Geoparks. effects of global warming. “Geopark” is a program supported by Now the Mikasa Geopark is promoting UNESCO with the goal of protecting and the various activities utilized results and conserving important geological and materials of Cretaceous researches. In 2013, we geomorphologic heritage, as well as utilizing hold the two courses of the geo-tour visiting the this Earth heritage in the areas of education, outcrop of Cretaceous strata, and the disaster mitigation activities and geo-tourism, experience-based programs using the all with the aim of sustainable development for Cretaceous fossils as the museum activities. local communities. About 100 persons in the geo-tour and 200 The Cretaceous Yezo Group, persons in the experience-based program took interpreted as forearc basin sediments, is place in. We carried out a questionnaire survey widely distributed in the Mikasa Geopark. This for the participants of the geo-tour. As a result, group was probably deposited at approximately most of participants were satisfied with the tour, 35–45° N along a westward subduction margin but some people pointed out the difficulty of in the northeastern Asian continent. The strata understanding fossils and geological yield abundant, well-preserved macro- and phenomena. We, therefore, need to plan the microfossils, and thus there are many better science programs for people who don’t paleontological studies using materials from have knowledge of geosciences.

206

2014 September

Organizing Committee of the 2nd International Symposium of IGCP608