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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Short Papers

Novosibirsk 2016 Russian Academy of Science Siberian Branch Trofimuk Institute of Petroleum Geology and Geophysics

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Short papers for the Fourth International Symposium of International Geoscience Programme IGCP Project 608

August 15–20, 2016 Novosibirsk, Russia

Edited by O.S. Dzyuba, E.B. Pestchevitskaya and B.N. Shurygin

Novosibirsk IPGG SB RAS 2016 УДК 551.763+551.863 ББК 26.323 М47

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific: Short papers for the Fourth International Symposium of IGCP Project 608, Novosibirsk, August 15–20, 2016 / Dzyuba, O.S., Pestchevitskaya, E.B., and Shurygin, B.N., Eds. – Novosibirsk, IPGG SB RAS, 2016. – 134 p.

The book contains materials of the reports submitted to the Fourth International Symposium of International Geoscience Programme (IGCP) Project 608. Theoretical, methodical and practical questions of Cretaceous paleogeography, paleontological characteristics and stratigraphy of different regions of Asia and the Western Pacific are discussed. The significant attention is given to the Cretaceous climate and environmental changes, biogeography, biodiversity of terrestrial and marine ecosystems, and vertebrates of Asia and Western Pacific. This book will be of interest to a wide range of geoscientists who study the Cretaceous Period.

The organization and carrying out of the Symposium are supported by the UNESCO-IUGS-IGCP Committee (IGCP Project 608) and the Russian Foundation for Basic Researches (RFBR Project 16-05-20508).

Cover illustration: Psittacosaurus sibiricus. Painting by Andrey A. Atuchin

ISBN 978-5-4262-0073-9 © IPGG SB RAS, 2016 © The authors, 2016

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 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

Regional Coordinators Prof. Guobiao Li Department of Geosciences and Sources, China University of Geosciences, China Prof. Guntupalli V. R. Prasad Department of Geology, University of Delhi, India Dr. Djadajang Sukarna New & Renewable Energy Conservation, Ministry of Energy and Minerals, Indonesia Prof. Takashi Hasegawa Department of Earth Science, Kawazawa University, Japan Prof. In Sung Paik Department of Environmental Geosciences, Pukyong National University, Korea Dr. Niiden Ichinnorov Paleontology Centre, Mongolian Academy of Sciences, Mongolia Mr. M. Sadig Malkani Paleontology & Stratigraphy branch, Geological Survey of Pakistan, Pakistan Dr. Carla Dimalanta National Institute of Geological Sciences, University of Philippines, Philippines Dr. Galina L. Kirillova Institute of Tectonics and Geophysics FEB RAS, Russia Prof. Boris N. Shurygin Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Russia Mr. Naramase Teerarungsigul Department of Mineral Resources, Thailand Prof. Nguyen Xuan Khien Vietnam Institute of Geosciences and Mineral Resources, Vietnam Organizing Committee of the Fourth International Symposium of IGCP608 RAS Academician, Prof. Alexey E. Kontorovich (Honorary Chairman) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Novosibirsk State University RAS Corresponding Member Vladimir I. Klishin (Honorary Chairman) Coal Institute of the Federal Coal and Coal Chemistry Research Center SB RAS RAS Corresponding Member, Prof. Valeriy A. Vernikovsky (Honorary Chairman) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Novosibirsk State University RAS Corresponding Member, Prof. Boris N. Shurygin (Co-chairman) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Novosibirsk State University Dr. Galina L. Kirillova (Co-chairman) Kosygin Institute of Tectonics and Geophysics FEB RAS Dr. Oksana S. Dzyuba (Vice-chairman) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS Dr. Natalya K. Lebedeva (Vice-chairman) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Novosibirsk State University Dr. Ekaterina B. Pestchevitskaya (Vice-chairman) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS Olga A. Feofanova (Vice-chairman) Director of the SCI “Kemerovo Regional Museum of Local Lore” Igor N. Kosenko (Symposium Secretary) Trofimuk Institute of Petroleum Geology and Geophysics SB RAS, Novosibirsk State University Dr. Alexandr S. Alifirov, IPGG SB RAS, NSU Dr. Alexander L. Beisel, IPGG SB RAS Dr. Larisa A. Glinskikh, IPGG SB RAS Dr. Anna A. Goryacheva, IPGG SB RAS Dr. Irina V. Khazina, IPGG SB RAS Dr. Olga B. Kuzmina, IPGG SB RAS Dr. Boris L. Nikitenko, IPGG SB RAS Dr. Petr A. Yan, IPGG SB RAS Clémentine Colpaert, NSU Natalya V. Demidenko, SCI “Kemerovo Regional Museum of Local Lore” Alexander E. Igolnikov, IPGG SB RAS, NSU Svetlana N. Khafaeva, IPGG SB RAS Anna N. Trubicyna, IPGG SB RAS Olga S. Urman, IPGG SB RAS

Co-Organizing Agency Trofimuk Institute of Petroleum Geology and Geophysics SB RAS Novosibirsk State University State Cultural Institution “Kemerovo Regional Museum of Local Lore” Coal Institute of the Federal Coal and Coal Chemistry Research Center SB RAS Cretaceous Commission of the Interdepartmental Stratigraphic Committee of Russia Russian National Committee for International Geoscience Programme

Sponsors UNESCO-IUGS-IGCP (IGCP Project 608) Russian Foundation for Basic Researches (RFBR Project 16-05-20508) INPEX Corporation Co., Ltd. (Japan) Japan Petroleum Exploration Co., Ltd. (Japan) JX Nippon Oil and Energy Corporation Co., Ltd. (Japan) Mitsui Oil Exploration Co., Ltd. (Japan) Mitsubishi Corporation Exploration Co., Ltd. (Japan) Oyo Corporation Co., Ltd. (Japan) DIA Consultants Co., Ltd. (Japan) Chuo Kaihatsu Co., Ltd. (Japan) Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific Contents

Preface ...... 9

Zakharov, V.A., and Shurygin, B.N. Vladimir N. Saks: geologist and paleontologist, and the founding father of the Mesozoic paleontology and stratigraphy Research Group in Novosibirsk Academy Town (to the 105th anniversary of the birth of V.N. Saks) ...... 10

Session 1: Biodiversity of terrestrial and marine ecosystems. Cretaceous fauna and flora of Asia and the Western Pacific

Afonin, M.A. Fossil woods from the Bykov Formation (Late Cenomanian–Early Campanian) of Sakhalin Island, Russian Far East ...... 13

Bugdaeva, E.V., and Markevich, V.S. The change of the Early Cretaceous ecosystems of Gusinoozerskiy Basin (the Buryat Republic) ...... 16

Golovneva, L.B., and Alekseev, P.I. Taxonomy and morphological diversity of infructescences co-occurred with Trochodendroides leaves ...... 19

Herman, A.B., and Spicer, R.A. The composition and dynamics of the Late Cretaceous and Paleocene Arctic plant communities ...... 22

Kosenko, I.N. Late Jurassic to Early Cretaceous oysters (Bivalvia, Ostreoidea) from Siberia: Taxonomy, palaeoecology, distribution and variations of carbon and oxygen isotopes ...... 24

Makarkin, V.N. The neuropteran assemblage (Insecta) of the mid-Cretaceous Burmese amber confirms transitional character of its biota ...... 27

Markevich, V.S., Bugdaeva, E.V., Kovaleva, T.A., Volynets, E.B., and Afonin, M.A. The mid-Cretaceous swamp plant communities of northeastern Asia ...... 30

Smokotina, I.V. Upper Cretaceous palynology (spores, pollen and dinoflagellate cysts) of the Yakovlevskaya-2 borehole, Ust-Yenisei region ...... 33

Sun, B.N., Xu, X.H., Yan, D.F., and Jin, P.H. Conifer fossils from the Lower Cretaceous of Inner Mongolia, North China and their geologic significance ...... 37

Volynets, E.B., Bugdaeva, E.V., Markevich, V.S., and Kovaleva, T.A. First flowering plants in Primorye region (Russia) ...... 39 5

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Session 2: Cretaceous paleogeography and paleobiogeography

Bajpai, S. Late Cretaceous paleobiogeography of peninsular India: An overview of constraints from fossil tetrapods ...... 42

Jafar, S.A. Terminal Maastrichtian–Danian marine incursion in Central India: Myth or Reality? ...... 43

Li, G.B., Han, Z.C., Li, X.F., Niu, X.L., Wang, T.Y., Han, Y., Yao, Y.J., Lv, B.B., and Zhang, W.Y. The discovery of the CORB in the Southern Tethyan Himalaya and its paleogeographic implication ...... 46

Sha, J.G., and Cestari, R. Palaeobiogeographic implications of the Late Aptian–Albian polyconitid rudist fauna ...... 48

Session 3: Cretaceous climate and environmental changes

Kirillova, G.L., and Medvedeva, S.A. Cretaceous paleoenvironments of the Russian Southeast ...... 51

Lebedeva, N.K. Palynomorphs and biofacies in the Upper Cretaceous sediments of northern Siberia ...... 55

Malkani, M.S. Pakistan paleoclimate under greenhouse conditions; Closure of Tethys from Pakistan; Geobiological evolution of South Asia (Indo-Pak subcontinent) ...... 59

Mohabey, D.M., and Samant, B. Assessing effects of Deccan volcanism on biota and environments of non-marine Maastrichtian– Palaeogene sediments of Central India ...... 62

Pestchevitskaya, E.B. Environmental changes in Early Cretaceous palaeobasin of Western Siberia based on marine and terrestrial palynomorphs ...... 64

Pestchevitskaya, E.B., Nikolenko, O.D., Vakulenko, L.G., Ershov, S.V., and Yan, P.A. Palaeoenvironmental changes in the Early Cretaceous of Gydan region (NW Siberia)...... 67

Samant, B., Yadav, D., and Mohabey, D.M. Palynological study of intertrappean sediments in the central and eastern parts of Deccan volcanic province of India to understand age and depositional environment ...... 70

Uranbileg, L., Ichinnorov, N., and Eviikhuu, A. The Cretaceous flora of Mongolia and its paleoenvironment ...... 72

Zorina, S.O., and Pavlova, O.V. Discontinuous euxinia during the early Aptian oceanic anoxic event (OAE 1a): A case study from the Russian Platform ...... 74

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Session 4: Cretaceous stratigraphy and sedimentology

Ando, H., Hasegawa, H., Ichinnorov, N., Hasebe, N., Ohta, T., Hasegawa, T., Yamamoto, M., Li, G.B., Erdenetsogt, B., and Heimhofer, U. Chronostratigraphy of the Jurassic–Cretaceous lacustrine deposits in southeast Mongolia: Brief results of Japan-Mongolia Joint research project ...... 77

Beisel, A.L. Supersequenses in the Upper Jurassic and Lower Cretaceous of Western Siberia ...... 79

Dzyuba, O.S., and Shurygin, B.N. The Jurassic–Cretaceous boundary in the Asian part of Russia ...... 82

Ichinnorov, N., Hofmann, Ch.-Ch., Hasegawa, H., and Uranbileg, L. Lower Cretaceous formations and palynology of the Matad area (Tamsag Basin), southeastern Mongolia ...... 86

Igolnikov, A.E., Rogov, M.A., and Alifirov, A.S. Ryazanian (Boreal Berriasian) ammonite succession of the Nordvik section (Russian Arctic): Revision and new data ...... 89

Li, G.B. The closing age of Himalayan Tethys: New evidence from planktic foraminifera ...... 93

Malkani, M.S. Revised stratigraphy of Indus Basin (Pakistan): Sea level changes ...... 96

Teerarungsigul, N. Stratigraphy of Jurassic–Cretaceous rocks of Thung Yai–Khlong Thom area, peninsular Thailand ...... 100

Thakre, D., Samant, B., and Mohabey, D.M. Palynology and magnetostratigraphy of Deccan volcanic associated sedimentary sequence of Amarkantak Group in Central India: Age and paleoenvironment...... 101

Urman, O.S., Dzyuba, O.S., Shurygin, B.N., and Kirillova, G.L. Bio- and lithostratigraphy of the Jurassic–Cretaceous boundary deposits in the Komsomolsk section (Russian Far East) ...... 103

Zlobina, O.N. Environments of conservation of the dinosaurs in the Mesozoic deposits of south-eastern West Siberia (Shestakovskii Yar section) ...... 106

Session 5: Cretaceous vertebrates of Asia and the Western Pacific

Amiot, R., Lazzerini, N., Lécuyer, Ch., and Fourel, F. Stable isotope composition of modern and fossil archosaur eggshells as a tracer of animal ecology, living environment and reproductive strategy ...... 109

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Bhadran, A. Late Cretaceous (Maastrichtian) vertebrate fossils from inland basins of Indian peninsula – their palaeogeographic significance ...... 111

Demidenko, N.V., and Maschenko, E.N. Results of paleontological excavations 2014–2015 held by the Kemerovo Regional Museum at the Early Cretaceous Shestakovo vertebrate localities...... 114

Feofanova, O.A. Historical stages of natural science collection formation in the Kemerovo Regional Museum ...... 117

Hirayama, R., Takisawa, T., Sasaki, K., Sonoda, T., Yoshida, M., Takekawa, A., Mitsuzuka, Sh., Kobayashi, Y., Tsuihiji, T., Matsumoto, R., Kurosu, M., Takakuwa, Y., Miyata, S., and Tsutsumi, Y. Fossil vertebrates from the Late Cretaceous Tamagawa Formation (Turonian) of Kuji City, Iwate Prefecture, northeastern Japan ...... 120

Ivantsov, S.V., Fayngerts, A.V., Leshchinskiy, S.V., Rezviy, A.S., Skutschas, P.P., and Averianov, A.O. The Lower Cretaceous continental vertebrate fauna from the Shestakovo locality (West Siberia): Results of 20-year research ...... 121

Kostyunin, A.E. The history of discovery and research of the Shestakovo locality of Early Cretaceous vertebrates ...... 124

Kusuhashi, N., Wang, Y.-Q., and Li, C.-K. Reinvestigation of an Early Cretaceous eutherian mammal Endotherium niinomii ...... 127

Malkani, M.S. Vitakri Dome of Pakistan – a richest graveyard of titanosaurian sauropod dinosaurs and mesoeucrocodiles in Asia ...... 129

Sonkusare, H., Samant, B., and Mohabey, D.M. Lithostratigraphy and biota of the Late Cretaceous dinosaur bearing Lameta and Intertrappean sediments along Salbardi fault in Betul and Amravati districts of Central India ...... 133

Summart, O.-U., Wongko, K., and Chantasit, Ph. Early Cretaceous fossil sites in Kalasin Province, Thailand ...... 134

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Preface

The mechanisms underlying the evolution of the Asia-Pacific Cretaceous ecosystems are far from being fully understood. The IGCP608 project lead by Prof. Hisao Ando (Ibaraki Universi- ty, Japan) is aimed to reconstruct the Cretaceous ecosystems and the history of their responses to paleoenvironmental changes in Asia and the Western Pacific. The 4th International Symposium of the IGCP608 is a follow-up of very successful previous meetings in Lucknow (India), Tokyo (Japan) and Shenyang (China). The Trofimuk Institute of Petroleum Geology and Geophysics of Siberian Branch of Russian Academy of Sciences in No- vosibirsk (Russia) was elected as a host for international meeting of the project workers in 2016. IGCP608 symposiums became an effective platform for participants to share their views on the paleoenvironmental changes impacts both on terrestrial and marine ecosystems. The scien- tific programme of the 4th International Symposium of the IGCP608 in Novosibirsk covers a wide range of topics including paleoclimate, paleogeography, paleontology, stratigraphy, tec- tonics, and petroleum geology. This symposium is an opportunity for discussion of the latest advances in studies of Asia-Pacific Cretaceous ecosystems. In addition to scientific sessions, the post-symposium field excursion will be organized in Kemerovo Oblast to examine the non- marine Cretaceous deposits yielding dinosaurs and other vertebrates. The Symposium is dedicated to the 105th anniversary of the birth of Corresponding Mem- ber of the USSR Academy of Sciences, Professor Vladimir N. Saks (1911–1979), Soviet geologist and paleontologist, and the founding father of the Mesozoic paleontology and stratigraphy Re- search Group in Novosibirsk Academy Town. This special issue is a contribution to UNESCO IUGS International Geoscience Programme (IGCP project 608). We express our sincere thanks to all of the authors who contributed to this issue.

IGCP608 Project Leaders Organizing Committee of the Fourth International Symposium of IGCP608

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Vladimir N. Saks: geologist and paleontologist, and the founding father of the Mesozoic paleontology and stratigraphy Research Group in Novosibirsk Academy Town (to the 105th anniversary of the birth of V.N. Saks)

V.A. Zakharov1 and B.N. Shurygin2,3

1Geological Institute of the RAS, Pyzhevskii per. 7, Moscow 119017, Russia; e-mail: [email protected] 2Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: [email protected] 3Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia

Vladimir Nikolaevich Saks, the founder and Quaternary and Mesozoic geology – have the first head of the Laboratory of the Mesozoic gained recognition among the experts in Russia and Cenozoic Paleontology and Stratigraphy and many countries of the Northern Hemi- (Institute of Geology and Geophysics SB AS sphere. The intact by time persistent interest in USSR, currently – Trofimuk Institute of Petrole- his works is largely attributed to the profound um Geology and Geophysics SB RAS) would knowledge, deep intuition and wisdom this re- have turned 105 years old on April 22, 2016. markable geologist and paleontologist. The school of scientific thought initiated by Vladimir Saks was known for an amazing Vladimir Saks is justifiably considered the great- diversity of his scientific interests, but his prima- est and the most important achievement of his ry academic and professional interest was given scientific career and, ultimately, his whole life. A to stratigraphy. The key idea governing the de- school of thought implies a community of scien- velopment of the detailed Mesozoic stratigraphy tists like-minded spiritually connected, united of Siberia was V.N. Saks’ pioneering conjecture by common goals and objectives, as long as the that the succession of Jurassic stages traditional- staple idea of the school founder is handed on ly assigned to the West European, including and developed further by generations of re- British stratigraphic columns is equally applica- searchers. V.N. Saks was the mastermind and ble to Siberia (Saks, 1962). It was revealed that in inspiration in such teams organized by him first the Mesozoic, the Arctic marine fauna was es- in Leningrad and later in Novosibirsk. sentially poorer versus faunas from the paleo- He always had his hand in planning the re- basins situated further south. However, in strat- search activities on stratigraphy and assisted in igraphic columns of Western Europe and Siberia organizing the work of interdepartmental a whole series of common genera and species, groups for creating the regional stratigraphic primarily ammonoids, was established, which schemes for the Mesozoic–Cenozoic deposits of form the basis for subdivisions of all Mesozoic the Boreal type. He would act as a chief scientific systems. arbiter for all regional stratigraphic schemes, re- When suggesting the possibility of using of garded as an integrated part of the geological in- the International Stratigraphic Chart for Siberia, formation on most of Siberian regions. Back in it was highlighted that the stages were to be the 1960s–70s, the Regional Stratigraphic meet- ings on approval of the Mesozoic and Cenozoic filled with zones from Siberian sections, given charts with regional columns were held under that the differences between Siberian and Euro- his scientific leadership in the cities of Novosi- pean faunas in certain stratigraphic levels birsk, Tyumen, Magadan, Khabarovsk, Vladi- proved fairly essential. That was why Vladimir vostok, including those for the European plat- Saks believed that comparison of the Western form and the Urals. Siberian ammonite scale should be based not on- As an Earth scientist, Vladimir Saks really ly on the groups of master stratigraphic col- had two careers and was equally known as a ge- umns, but rather defined by homotaxis (similar ologist and geographer. His expertise and re- positions within similar stratigraphic sequenc- search results and findings in these two relative- es). This approach bridges the major gaps in de- ly remote areas of geological knowledge – terminations of geological ages of rocks.

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

The most outstanding achievement made by Vladimir Saks, his students and fellows in the study of the Mesozoic of the Arctic region was the zonal stratigraphic scale, comprising 140 ammonite zones (Saks et al., 1980). In Western Europe, it took 125 years to develop the Jurassic and Cretaceous zonal scale, while modern paral- lel zonal scales for the Siberian Jurassic were completed within a 20 years’ time span (Zakha- rov et al., 1997; Shurygin et al., 2000). All the Triassic, Jurassic and Cretaceous zones estab- lished in Siberia are widely traceable – in North of USA, Canada, the Arctic Islands. During V.N. Saks’ scientific career, apart from dealing primarily with the ammonite- based stratigraphy, he was involved in the pio- neering attempts of developing biostratigraphic scale for other groups of invertebrates – the bel- emnites, bivalves, brachiopods, etc. Already af- ter his passing away, this work was successfully completed by his disciples. At present, the Mes- ozoic biostratigraphy of Siberia has at its dispos- al a series of intercorrelated scales based on dif- ferent groups of fossils. The second in order but not minor in signifi- Vladimir N. Saks cance, direction of his scientific activity was con- cerned with paleobiogeography of the Panboreal In his study of past climates, V.N. Saks pro- Superrealm, which was geographically equaled ceeded from the best studied later periods (like with Boreal climatic Belt by V.N. Saks. Analysis Pleistocene) to earlier (Jurassic and Cretaceous). of the area extent of several groups of Jurassic It was on his initiative and with his immediate and Early Cretaceous marine organisms – am- participation that hundreds of definitions of monites, belemnites, bivalves, brachiopods, for- paleotemperatures were obtained for the Arctic aminifers – resulted in the division of area occu- territory based on the oxygen isotopic data and pied by this superrealm beyond 50°N into three the Ca/Mg ratios from belemnite rostra. A paleobiogeographic realms: Boreal-Atlantic, Arc- wealth of scientific evidence was obtained stat- tic, and Boreal Pacific, with the provinces allocat- ing that during the Mesozoic Era (about 70– ed by the area extent of specific taxa in each of 200 Ma BP) the Arctic climate was moderately them (Saks et al., 1971). The proposed division warm, however subjected to significant changes has thus far existed in the literature. over the time. The mean annual surface water V.N. Saks in collaboration with I.S. Gramberg temperatures ranged from 11 to 24°C, and the and Z.Z. Ronkina offered one of the first paleo- Arctic water temperatures were gradually de- geographic reconstructions for the Mesozoic of creased during the Jurassic and Early Creta- the Soviet Arctic (Saks and Ronkina, 1958; Saks ceous. et al., 1959; Saks, 1961). During the ‘Siberian pe- During his research into geological history riod’ of V.N. Saks’ life, a significant part of his of the Arctic region in the Mesozoic, Vladimir work was dedicated to the research into the Saks’ interests often extended beyond the scope Mesozoic Arctic paleogeography. His theory on of terrestrial geology. This is heavily evidenced the integrity of the Arctic paleobasin and on its by the paleogeographic and tectonic reconstruc- evolution associated with plate tectonics during tions of the Arctic Ocean and the surrounding the Mesozoic got further development in Russia polar seas, built for individual time intervals of and abroad. the Mesozoic (e.g., Saks, 1958, 1960, 2007).

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

In the late forties–early fifties of the last cen- carbon resources of Western Siberia. Relaying on tury, when the nation was facing the need for his research in Ust-Yenisei region and on gen- searches of hydrocarbons in Siberia, V.N. Saks eral understanding of the geology of Western took an active part in the work of the Siberia, V.N. Saks expressed his firm belief that Glavsevmorput Mining and Geological Bureau Jurassic and Cretaceous deposits of this area are in Ust-Yenisei region. The results were summa- to be highly prospective for hydrocarbons. rized in a monograph describing the Mesozoic Vladimir Saks belonged to the generation of strata of the Ust-Yenisei and Khatanga basins in enthusiastic geologists whole-heartedly devoted northern Siberia (Saks and Ronkina, 1957; Saks to their chosen profession. His whole career was et al., 1959). For many years ahead, the books dedicated to the study and development of min- were extremely helpful to petroleum geologists eral resource base of the Soviet Arctic and to es- in the exploration and development of hydro- tablishing the academic science in Siberia.

References

Saks, V.N., 1958. Stratigraphy of Jurassic and Creta- Saks, V.N., Gramberg, I.S., Ronkina, Z.Z., Aplonova, ceous deposits of the middle sector of Soviet Arc- E.N., 1959. Mesozoic deposits of the Khatanga tic, in: Petroleum potential of the North of Sibe- depression. Gostoptekhizdat, Leningrad (in Rus- ria. Gostoptekhizdat, Leningrad, pp. 44–60 (in sian). Russian). Saks, V.N., Basov, V.A., Dagis, A.A., Dagis, A.S., Saks, V.N., 1960. Geological history of the Arctic Zakharov, V.A., Ivanova, E.F., Meledina, S.V., Ocean during the Mesozoic Era, in: Regional Mesezhnikov, M.S., Nalnyaeva, T.I., Shulgina, Paleogeography. Gosgeoltekhizdat, Moscow, N.I., 1971. Paleogeography of the seas of Boreal pp. 108–124 (in Russian). Belt in the Jurassic and Neocomian, in: Problems Saks, V.N., 1961. Paleogeography of the Arctic in the of general and regional geology. Nauka, Novosi- Jurassic and Cretaceous periods, in: Papers at birsk (in Russian). yearly readings in commemoration of Saks, V.N., Zakharov, V.A., Meledina, S.V., Mesezh- V.A. Obruchev. Izd-vo AN SSSR, Moscow- nikov, M.S., Nalnyaeva, T.I., Shulgina, N.I., Shurygin, B.N., 1980. Recent understanding of Leningrad, pp. 20–68 (in Russian). the development of flora and fauna and zonal Saks, V.N., 1962. On possibility of application of gen- stratigraphy of the Jurassic and Neocomian of eral stratigraphic scale for structural zoning of the Boreal Belt. Geol. Geofiz. 1, 9–25 (in Russian). Jurassic deposits of Siberia. Geol. Geofiz. 5, 62–75 Shurygin, B.N., Nikitenko, B.L., Devyatov, V.P., Il'ina, (in Russian). V.I., Meledina, S.V., Gaideburova, E.A., Dzyuba, Saks, V.N., 2007. Selected works. GEO, Novosibirsk O.S., Kazakov, A.M., Mogucheva, N.K., 2000. (Vol. 1, 641 p.; Vol. 2, 339 p.). Stratigraphy of oil and gas basins of Siberia: The Saks, V.N., Ronkina, Z.Z., 1957. Jurassic and Creta- Jurassic System. Geo, Novosibirsk (in Russian ceous deposits of the Ust’-Yenisei depression. with English summary). Gosgeolizdat, Moscow (in Russian). Zakharov, V.A., Bogomolov, Yu.I., Il'ina, V.I., Kon- Saks, V.N., Ronkina, Z.Z., 1958. Paleogeography of stantinov, A.G., Kurushin, N.I., Lebedeva, N.K., the Khatanga depression and the adjacent areas Meledina, S.V., Nikitenko, B.L., Sobolev, E.S., throughout the Jurassic and Cretaceous periods. Shurygin, B.N., 1997. Boreal zonal standard and Collection of articles on the Arctic geology 85(9), biostratigraphy of the Siberian Mesozoic. Russ. 70–89 (in Russian). Geol. Geophys. 38, 965–993.

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Session 1 Biodiversity of terrestrial and marine ecosystems. Cretaceous fauna and flora of Asia and the Western Pacific

Fossil woods from the Bykov Formation (Late Cenomanian–Early Campanian) of Sakhalin Island, Russian Far East

M.A. Afonin

Institute of Biology and Soil Science, Far Eastern Branch of RAS, pr. 100-letiya 159, Vladivostok 690022, Russia; e-mail: [email protected]

Fossil woods are common in the Upper Cre- tocupressinoxylon, Planoxylon, Podocarpoxylon, taceous deposits of Sakhalin, Russian Far East. Taxaceoxylon, Taxodioxylon, and Xenoxylon) and Numerous fossil wood remains were previously one dicotyledonous fossil wood taxon (Aptiana). described from the Upper Cretaceous of Sakha- We described coniferous (Sequoioxylon sp.) lin (Ay, Nayba and Susuya River basins) by Jap- and dicotyledonous (Paraphyllanthoxylon sp.) anese palaeobotanists M. Shimakura (1937), fossil wood taxa, all new to the Late Cretaceous H. Nishida and M. Nishida (Nishida, H. and fossil wood record of Sakhalin, from the Ceno- Nishida, M., 1986; Nishida, M. and Nishida, H., manian–Campanian of Nayba River, Southern 1986, 1995). They reported 15 coniferous fossil Sakhalin (Fig. 1). The fossil woods studied were wood taxa (Araucarioxylon, Brachyoxylon, Cedrox- collected by workers of the Far Eastern Geolog- ylon, Cupressinoxylon, Palaeopiceoxylon, Phyllo- ical Institute FEB RAS (Vladivostok) on the cladoxylon, Piceoxylon, Pinoxylon, Pinuxylon, Pro- right bank of the Nayba River, in the marine

Fig. 1. Map showing fossil wood collection site of Sakhalin Island.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

14

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific terrigenous deposits of the Bykov Formation. cells, uniseriate rays (1–60 cells high) with long The age of the Bykov Formation is Late Ceno- biseriate parts, marginal ray tracheids, taxodioid manian–Early Campanian, based on diagnostic cross-field pits and traumatic vertical resin ca- marine fossils (Zakharov et al., 1981; Poyarkova, nals (Fig. 2A–J). 1987). According to Yu.D. Zakharov et al. (1981), Paraphyllanthoxylon sp. (fossil wood sample these deposits contain ammonoinds, bivalves, no. IBSS 37/12) has diffuse-porous wood, dis- gastropods, scaphopods and plant remains (in- tinct growth rings, tyloses in vessels, simple per- cluding fossil woods). A detailed overview of foration plates, alternate intervessel pits, distinct the marine fossils from the Bykov Formation in circular vessel-ray pits, fiber-tracheids with the Nayba River Basin is given in the above- small, circular, bordered pits, apotracheal axial mentioned paper. The fossil woods studied are parenchyma, heterocellular rays width 1 to 5 hard, permineralized, grey to almost black, and cells, rarely uniseriate rays, ray cells with pris- they represent the remains of trunks or large matic crystals (Fig. 2K–T). branches. They were studied using the conven- It should be noted that Sequoioxylon fossil tional petrographic technique for preparing thin wood was described from the Cretaceous of Sa- sections of permineralized wood. khalin for the first time. The record of Pa- Sequoioxylon sp. (fossil wood samples no. raphyllanthoxylon represents the first from Rus- IBSS 37/3, 37/6, 37/7, 37/8, 37/9, 37/10) is charac- sia. Therefore, the investigation of the terized by the presence of distinct growth rings, Cretaceous woods of Sakhalin will improve our uniseriate, biseriate, triseriate, and sometimes understanding of the vegetation history during tetraseriate pits on the radial walls of tracheids, the Cretaceous in Northern Asia. crassulae between multiseriate pits on the radial The research was supported by the Grants walls of tracheids, uniseriate pits on the tangen- Council (under the President of the Russian Federa- tial walls of tracheids, abundant diffuse axial pa- tion) for state aid of Russian young scientists (project renchyma with smooth transverse end walls of no. MK-2993.2015.4).

References

Nishida, H., Nishida, M., 1986. Petrified plants from Shimakura, M., 1937. Studies on fossil woods from the Upper Cretaceous of Saghalien (2). Bot. Mag. Japan and adjacent lands (2). Sci. Rep. Tohoku Tokyo 99, 205–212. Imp. Univ. Sendai. Ser. 2 (Geology) 19(1), 1–73. Nishida, M., Nishida, H., 1986. Petrified plants from Zakharov, Yu.D., Grabovskaya, V.S., Kalishevich, the Upper Cretaceous of Saghalien (1). Bot. Mag. T.G., 1981. Succession of marine invertebrates Tokyo 99, 191–204. from the Nayba and Bykov formations of the ref- Nishida, M., Nishida, H., 1995. Pinoid woods with erence Upper Cretaceous section in Sakhalin, in: resin canals from the Upper Cretaceous of Hok- kaido and Saghalien. J. Plant Res. 108, 161–170. Naydin, D.P., Krassilov, V.A. (Eds.), Organic Poyarkova, Z.N. (Ed.), 1987. Reference section of the evolution and biostratigraphy in the middle of Cretaceous deposits in Sakhalin (Nayba section). the Cretaceous period. Vladivostok, pp. 47–85 (in Nauka Publishing House, Leningrad (in Russian). Russian).

Fig. 2. (A–J) Photomicrographs of Sequoioxylon sp. (sample no. IBSS 37/6). (A–C) Transverse sections showing distinct growth rings, transition from the early wood to the late wood, and traumatic vertical resin canals. (D–F) Radial sec- tions showing one, two and three rows of radial tracheid bordered pits. (G) Tangential section showing uniseriate ray with biseriate part. (H) Tangential section showing uniseriate rays and smooth transverse end walls of axial paren- chyma cells. (I, J) Radial sections showing taxodioid cross-field pits and smooth horizontal and end walls of ray cells. (K–T) Photomicrographs of Paraphyllanthoxylon sp. (sample no. IBSS 37/12). (K) Transverse section showing diffuse- porous wood. (L) Radial section showing simple perforation plate. (M, N) Radial sections showing alternate interves- sel pits. (O) Tangential section showing rays width 1 to 3 cells. (P–R) Radial sections showing ray cells with prismatic crystals. (S, T) Radial sections showing vessel-ray pits. 15

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

The change of the Early Cretaceous ecosystems of Gusinoozerskiy Basin (the Buryat Republic)

E.V. Bugdaeva and V.S. Markevich

Institute of Biology and Soil Science, Far Eastern Branch of RAS, pr. 100-letiya 159, Vladivostok 690022, Russia; e-mail: [email protected]

The Gusinoozerskiy Basin contains the sed- valves and ostracods have been found. The imentary strata united into the thickness of this formation is 140–250 m (Skoblo Gusinoozyorskaya Group, which is divided into et al., 2001). the Murtoy, Ubukun, Selenga and Kholboldzhin The Selenga Formation is represented by a formations (Skoblo et al., 2001). They overlay multi-step alternation of two-three-term trans- with stratigraphic unconformity the Upper Ju- gressive rhythms of deposits. Each of the lower rassic and older volcanic rocks. The Murtoy rhythms is formed by the fluvial or lacustrine Formation consists mainly of conglomerates and sandstones, and the overlying rhythm is repre- sandstones with remains of fossil vertebrates sented by thicker fine-grained psammite or silt- (theropods, sauropods, ornithopods, and cera- stone beds of floodplain or lacustrine origin with topsians), as well as the abundant remains of seams of brown coal. In total, 23 coal seams were limnetic fauna (Skoblo et al., 2001; Nessov and revealed. In the upper part of this formation, the Starkov, 1992; Averianov and Skutschas, 2009). cross-bedded sandstones become more wide- Its thickness is 250–450 m. spread. The shells of ostracods and mollusks, In the Murtoy Formation, the numerous bones of fish Lycoptera fragilis Huss. have been remains of conifers Pityophyllum ex gr. norden- found. The thickness of this formation varies skioldii (Heer) Nath. and Pityocladus sp. were from 575 to 1330 m (Skoblo et al., 2001). The found at the Atsay locality. The strobiles Scar- Selenga Formation yields abundant remains of burgia hillii Harris are common in the burial with leaves Pseudotorellia sp. and Phoenicopsis cf. krass- them. The horsetail stems, scale-leaved shoots ilovii Kiritch. The findings of Pityophyllum ex gr. Cyparissidium gracile Heer and strobiles of coni- nordenskioldii (Heer) Nath. are common, Coniop- fers are rare. According to V.A. Vachrameev teris setacea Vachr., Sphenopteris (Ruffordia) cf. (1964), the flora of this formation also includes goeppertii Dunk., Cladophlebidium dahuricum Coniopteris onychioides Vassil. et K.-M., Cladophle- Pryn., Cyparissidium gracile Heer, Podozamites bis aff. tongusorum Pryn., Sphenopteris (Ruffordia) lanceolatus (L. et H.) F. Braun, Samaropsis cf. auri- cf. goeppertii Dunk., Carpolithes sp. Palynological ta Krassil., Nilssoniopteris cf. prynadae Samyl., assemblage is dominated by Schizaeaceae Baisia cf. hirsuta Krassil., Umaltolepis sp., Ixostro- (mainly Concavissimisporites), the share of the lat- bus sp., Swedenborgia sp. are rare. Palynological ter in the pollen spectra can reach 36%. A num- assemblage is dominated by club-mosses and ber of club-mosses is high, up to 24%. The per- bryophytes, their number may reach 46%. Per- centage of cyatheaceous and dicksoniaceous centage of cyatheaceous and dicksoniaceous ferns does not exceed 15%. Among gymno- ferns increases up to 28%, schizaeaceous ferns sperms the bisaccate pollen having pinaceous af- become more diverse. Among gymnosperms finity prevails (up to 36%); it is accompanied by bisaccate pollen close to Pinaceae dominates, Ginkgocycadophytus sp. (up to 18%). Only for sometimes reaching 55%. The share of Ginkgocy- palynological assemblage of this formation the cadophytus sp. reduces (13%). The rare Classopol- pollen of unknown affinity, Pollenites sp., having lis classoides Pfl. et Jans. appears. The bulk mac- elongated shape with longitudinal folds is char- eration of coals of this formation has revealed acterized. Its amount may reach 12% (Kotova, that they are composed mainly of leaves 1964). Pseudotorellia sp. A. and fossil wood of Pinaceae. The Ubukun Formation is characterized by In the Kholboldzhin Formation, the cross- fine-grained clayey well-bedded deposits with bedded, light gray quartz-feldspathic sand- ash-gray massive mudstones having conchoidal stones widely spread. About 16–17 coal seams fracture. The numerous remains of lacustrine bi- having the thickness from 2–4 to 30 and even 16

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

53 m occur here. The thickness of this strati- inherent for them. A not large size of bodies of graphic unit is 1000–1200 m (Skoblo et al., 2001). herbivorous dinosaurs existed in this basin may The numerous leaves of Pseudotorellia sp. and indicate that vegetation of dinosaur ecosystems Ginkgo coriacea Florin were revealed in this for- was not abundant, highly productive and easily mation. Next in abundance in the burials are the restored. According to the paleobotanical data remains of Pityophyllum ex gr. nordenskioldii we can assume the existence of lighted conifer- (Heer) Nath., Pityocladus sp., Cyparissidium grac- ous-cheirolediaceous forests with abundant un- ile Heer, and Podozamites lanceolatus (L. et H.) F. dergrowth, consisting of shrubby cycadophytes, Braun. Palynological assemblage is dominated club-mosses, mosses, and various ferns (mostly by club-mosses and bryophytes (36%), as well as schizaeaceous, to a lesser cyatheaceous and by cyatheaceous and dicksoniaceous ferns (up to dicksoniaceous ferns). A recent representatives 30%). The share of osmundaceous ferns is signif- of Schizaeaceae are herbaceous or liana plants; icant (about 12%). As compared with the previ- usually they inhabit the moist biotopes. ous assemblage, the number of schizaeaceous As the Gusinoozerskiy Basin developed and ferns drastically reduced; they are rare. The broadened, the lakes and meandering rivers bisaccate pollen of Pinaceae maintains its quan- have formed. The environment and vegetation titative part (48%), the percentage of Ginkgocy- changed. The lacustrine ecosystem with abun- cadophytus sp. (20%) and Classopollis classoides (2– dant limnetic fauna begins to form. The shells of 3%) slightly increases. The palynological assem- ostracods and mollusks were buried under ash blage of this formation is characterized by the fall as a result of the some distant volcano erup- appearance of the taxodialeans (1.5%). The plant tion. Since the time of deposition of the Selenga basis of coals comprises mainly leaves Pseudoto- Formation an intensive swamping of this area rellia sp. B. and wood of Pinaceae in this for- occurred. The abundant vegetation provides a mation. massive phytomass in burial and gives rise to V.A. Vachrameev (1964) and I.Z. Kotova the coals. Swamp plant community was domi- (1964) believed that the composition of the meg- nated by conifers and ginkgoaleans (Pseudotorel- afossil flora of the formations in Gusinoozerskiy lia), lower plants, cyatheaceous and dicksonia- Basin almost does not change and they consid- ceous ferns. During the time of deposition of the ered the geological age of Gusinoozerskaya Kholboldzhin Formation, the diversity of the Group as the Early Cretaceous, while community increased by appearance of taxodi- V.M. Skoblo et al. (2001) dated this group as the aleans and ferns having affinity with Osmun- Berriasian–Aptian. Our findings of guide taxa of daceae. Lack of dinosaur burials in the deposits fossil plants, characteristic for the Barremian– of lacustrine and swamp origin can evidence of Aptian floras of Transbaikalia, Mongolia and such conditions were not favorable for the habi- north-eastern China (Bugdaeva, 1989; Bugdaeva tat of these animals. and Markevich, 2012; Krassilov, 1982; Krassilov and Bugdaeva, 1982; Prynada, 1962; Sun et al., Acknowledgements 2001), allow us to assume that the sedimentary The authors are grateful to the late sequence of this basin was formed within the V.A. Krassilov (University of Haifa, Israel, PIN, RAS, Barremian–Early Albian. Moscow) for a discussion of a wide range of paleobo- Thus, at the beginning of formation of the tanical problems, V.M. Skoblo, N.A. Lyamina, basin the conditions favorable for habitation and A.F. Rudnev (VostSibNIIGiMS, Irkutsk) for their help burial of herbivorous dinosaurs (mostly psitta- in field work and discussion on the stratigraphy of cosaurs, but also sauropods) appeared. Psittaco- Transbaikalia, A.R. Sokolov, T.N. Groznova (CNIGRI saurs had self-sharpening teeth well adapted to Museum VSEGEI, St. Petersburg) for kindly provid- ing us with the specimens of the coals, N.P. Domra browse rude fare and crush it. The diet of psitta- and N.N. Naryshkina (IBSS FEBRAS, Vladivostok) for cosaurs, like modern parrots, could consist of assistance in the processing of our material. Special seeds, fruits, branches, buds and leaves. There is thanks to leaders of IGCP608, corresponding member paleontological evidence that they used gastro- of RAS B. Shurygin and Prof. Hisao Ando for support liths (stones in the stomach) for grinding, as of our participation in the 4th International Symposi- some recent birds. The gregarious behavior was um of IGCP608.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

References

Averianov, A.O., Skutschas, P.P., 2009. Additions to Baikal area. Rev. Palaeobot. Palynol. (36), 279– the Early Cretaceous Dinosaur Fauna of Trans- 295. baikalia, Eastern Russia. Proc. Zoological Insti- Nessov, L.A., Starkov, A.I., 1992. The Cretaceous ver- tute RAS 313 (4), 363–378. tebrates from Gusinoozerskiy Basin of Trans- Bugdaeva, E.V., 1989. Correlation of the Lower Creta- baikalia and their significance for age definition ceous isolated depressions of Transbaikalia and conditions of formation of deposits. Geology based on flora, in: Stage and zonal scales of the and Geophysics (6), 10–18 (in Russian). Boreal Mesozoic of the USSR. Nauka, Moscow, Prynada, V.D., 1962. Mesozoic flora of Eastern Siberia pp. 162–168 (Proc. IGG SB AN SSSR 722) (in Rus- and Transbaikalia. Gosgeoltekhizdat, Moscow sian). (in Russian). Bugdaeva, E.V., Markevich, V.S., 2012. The age of Ly- Sun, G., Zheng, S.-L., Dilcher, D., Wang, Y.-D., Mei, coptera beds (Jehol biota) in Transbaikalia (Rus- S.-W., 2001. Early Angiosperms and their associ- sia) and correlation with Mongolia and China, in: ated Plants from Western Liaoning, China. Scien- Godefroit, P. (Ed.), Bernissart Dinosaurs and Ear- tific and Technological Education Publishing ly Cretaceous Terrestrial Ecosystems. Indiana House, Shanghai. University Press, Bloomington, pp. 452–464. Skoblo, V.M., Lyamina, N.A., Rudnev, A.F., Luzina, Kotova, I.Z., 1964. The age of the continental deposits I.V., 2001. The Continental Upper Mesozoic of of the Gusinoozerskaya depression and features the Pribaikalia and Transbaikalia (stratigraphy, of the Early Cretaceous floras of Transbaikalia. depositional environments, correlation). Publish- Izv. Akad. Nauk, Ser. Geol. (8), 84–93 (in Rus- ing House of the SB RAS, Novosibirsk (in Rus- sian). sian). Krassilov, V.A., 1982. Early Cretaceous flora of Mon- Vachrameev, V.A., 1964. The Jurassic and Early Cre- golia. Palaeontographica B 181, 1–43. taceous floras of Eurasia and paleofloristic prov- Krassilov, V.A., Bugdaeva, E.V., 1982. Achene-like inces of this time. Nauka, Moscow (Proc. Geolog- fossils from the Lower Cretaceous of the Lake ical Institute AS USSR 102, 1–263) (in Russian).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Taxonomy and morphological diversity of infructescences co-occurred with Trochodendroides leaves

L.B. Golovneva and P.I. Alekseev

Komarov Botanical Institute of the RAS, Prof. Popov str. 2, St. Petersburg 197376, Russia; e-mail: [email protected]

The remains of distinctive follicular fruits ey is known from shoots, leaves, pistillate inflo- with subparallel longitudinal ridges and trans- rescences, infructescences, winged seeds and verse striation often occur in the Late Cretaceous seedlings. Associated staminate inflorescences and Tertiary deposits in the Northern Hemi- were described later as Alasia (Golovneva, 2006). sphere. They were first detected from the Paleo- Although the name Nyssidium is now wide- cene deposits of Atanekerdluk in West Green- ly used, it should be rejected for isolated follicles land, and then named as Nyssa arctica Heer and racemes, associated with Trochodendroides (1869). leaves. In other case delimitation of this kind of Leaves associated with these follicular fruits fructification from other similar remains will be are usually assigned to the genus Trochoden- problematic. The earliest generic name original- droides, which was a common component of the ly designated for fruits of Cercidiphyllum-like Late Cretaceous and Paleogene floras from mid- plants with distinguishable morphology and dle and high latitudes. The investigation of their critical details of inner structures is Jenkinsella. cuticular features reveals the similarity of We suggested applying the name Jenkinsella to Trochodendroides leaves with those of living ge- dispersed follicular fruits or to fruits attached to nus Cercidiphyllum (Golovneva and Alekseev, the axis (raceme). 2010). In the genus Jenkinsella we recognized three Later, such fruits were assigned to a wide species: J. apocynoides Reid et Chandler, J. arctica range of extinct and extant genera: Leguminosites (Heer) Bell and J. filatovii (Samylina) Golovneva (Lesquereux, 1873, 1878), Nyssidium (Heer, 1870; et P. Alekseev. The first of these is applied to the Schmalhausen, 1890; Hollick, 1936; Iljinskaya, permineralized fruits from the London Clay 1974; Crane, 1984), Berrya (Knowlton, 1930), Jen- Formation for which many morphological and kinsella (Reid and Chandler, 1933), Trochodendro- anatomical details were revealed. Second name carpus (Kryshtofovich, 1958), Joffrea (Crane and we suggested to use as broadly defined species Stockey, 1985). Most part of these names is in- to accommodation of fruits preserved mostly as appropriate. The form genus Leguminosites was impression without anatomical details. Varia- erected by Bowerbank (1840) for fruits and seeds tions in shape and size usually do not provide of fossil Fabaceae from London Clay. The name sufficient basis for separation of morphological Berrya can not be used for this type of fructifica- species. tion, because earlier this name was established For present time several types of follicular for another plant from family Malvaceae. The racemose infructescence, attached to shoots, genus Trochodendrocarpus is also invalid, because were described: Joffrea speirsii from the Paskopoo name Jenkinsella had priority before Trochoden- Formation (Paleocene, Canada), “Trochodendro- drocarpus. Iljinskaja (1974) suggested using ge- carpus arcticus” from the Upper Tsagayan For- neric name Nyssidium Heer as the earliest ap- mation (Paleocene, Russia), “Nyssidium arcti- propriate generic name for this kind of fruits. cum” from the British Lower Tertiary and However, these fruits differ from those of Nyssa “Berrya racemosa” from the Dawson arkose arctica by smaller sizes and some other features (Paleocene, USA). The same kind of infructes- (Budantsev and Golovneva, 2009). cences were documented in detail from the Abundant specimens from the Upper Paleocene of north-east China as Nyssidium Paleocene Paskapoo Formation, the Joffre Bridge jiayinense G.P. Feng, C.S. Li, Zhilin, Y.F. Wang et locality, Alberta, Canada, allowed describing the Gabrielyan (Feng et al., 2000). N.M. Makulbekov most complete Cercidiphyllum-like plant (Crane (1988) described Trochodendrocarpus asiaticus and Stockey, 1985). Joffrea speirsii Crane et Stock- Makulbekov from the Paleocene of Mongolia. 19

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Fig. 1. Schematic reconstructions of fertile shoots of different species of Jenkinsella (a–d) and Joffrea speirsii (f): a – long shoot with alternate lateral infructescences in terminal position and vegetative shoot developing from apical bud (Jenkinsella krassilovii); b – long shoot with alternate short shoots, bearing singly infructescences in terminal position (Jenkinsella confertus and J. makulbekovii); c – long shoot with alternate lateral and one apical infructescences (Jenkinsella jiayinensis, J. knowltonii and J. vilyuensis); d – terminal short with one lateral and one apical infructescences (Jenkinsella gardnerii); f – long shoot with alternate short shoots, bearing three alternate lateral infructescences (Joffrea speirsii).

Two more types of these infructescences were kseev, J. confertus P. Alekseev et Golovneva, found recently in the Coniacian deposits of the J. makulbekovii Golovneva et P. Alekseev, and Sym Formation in Western Siberia and in the J. vilyuensis Golovneva et P. Alekseev (Fig. 1). Turonian–Coniacian deposits of the Tim- General organization of infructescences is merdyakh Formation in Eastern Siberia. similar in all species of Jenkinsella. This is a ra- ceme with numerous follicles that were borne on The general construction of racemose in- short side branches of infructescence axis. Each fructescences and fruits of all known specimens side branch bears one or two short-stalked folli- is practically identical. This similarity allows cles. There is the junction between the follicle supposing that these plants were closely related stalk and the side branch of the infructescence. and differences are not sufficient for separate The follicles or pairs of follicles are often broken generic designation. To avoid further confusion, away at this joint. This similarity indicates close we recommend to consider all known findings relationship of all species in spite of differences under one generic name and differentiate them in position of infructescences. The differences specifically. For this aim we suggest to use the between species in infructescence and follicles name Jenkinsella to accommodate also racemose features are insignificant. The infructescences infructescense of follicular fruits, attached to the were developed from lateral flower buds with- shoots. Now we include another seven species out leaves. Production of infructescences from in this genus: Jenkinsella krassilovii Golovneva et the apical bud terminates the growth of shoot. P. Alekseev, J. gardnerii (Chandler) Golovneva et Because the long shoots of Jenkinsella with in- P. Alekseev, J. knowltonii Golovneva et P. Ale- fructescences usually shed as a unit, it is possi- kseev, J. jiayinensis (G.P. Feng, C.S. Li, Zhilin, bly to suggest that most part of them had apical Y.F. Wang et Gabrielyan) Golovneva et P. Ale- infructescence. 20

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

The reproductive structures of Jenkinsella The fossil records of Jenkinsella range from confertus resemble those in Joffrea speirsii. This Early–Middle Albian to Oligocene and occur plant also exhibits long and short shoot differen- mostly in temperate and subtropical areas of the tiation. General construction of the racemose in- Siberian-Canadian paleofloristic realm. Majority fructescences in both species is also similar. of findings of this genus comes from the Paleo- However, short shoots of J. confertus bore one cene and Eocene deposits. terminal infructescence, while short shoots of The study was supported by the Russian Foun- Joffrea speirsii had at least two infructescences. dation for Basic Research (project no. 16-04-01411).

References

Bowerbank, J.S., 1840. A history of the fossil fruits and Hollick, A., 1936. The Tertiary floras of Alaska. U. S. seeds of the London Clay. John Van Voorst, Geol. Surv. Prof. Pap. 182, 1–185. London. Iljinskaja, I.A., 1974. Nyssidium Heer, in: Takhtajan, Budantsev, L.Y., Golovneva, L.B., 2009. Fossil Flora of A.L. (Ed.), Magnoliophyta Fossilia URSS. Vol. 1. Arctic II—Palaeogene Flora of Spitsbergen. Mar- Nauka, Leningrad, pp. 123–124 (in Russian). afon, Saint Petersburg. Knowlton, F.H., 1930. The flora of the Denver and Crane, P.R., 1984. A re-evaluation of Cercidiphyllum- associated formations of Colorado. U. S. Geol. like plant fossils from the British early Tertiary. Surv. Prof. Pap. 155, 1–135. Bot. J. Linn. Soc. 89, 199–230. Kryshtofovich, A.N., 1958. Fossil floras of Penjin Bay, Crane, P.R., Stockey, R.A., 1985. Growth and repro- Tastakh Lake and Rarytkin Range. Trans. Bot. ductive biology of Joffrea speirsii gen. et sp. nov., Inst., Ser. 8, 3, 74–121 (in Russian). a Cercidiphyllum-like plant from the Late Paleo- cene of Alberta, Canada. Can. J. Bot. 63(2), 340– Lesquereux, L., 1873. Enumeration and description of 364. fossil plants from the Western Tertiary Feng, G.P., Li, C.S., Zhilin, S.G., Wang, Y.F., Gabriel- formations. Description of species of fossil plants yan, I.G., 2000. Nyssidium jiayinense sp. nov. from the Cretaceous of Kansas. U. S. Geol. (Cercidiphyllaceae) of the Early Tertiary from Geogr. Surv. Terr., Ann. Rep., pp. 371–427. north-east China. Bot. J. Linn. Soc. 134, 471–484. Lesquereux, L., 1878. Contributions to the fossil flora Golovneva, L.B., 2006. Alasia, gen. nov. – male inflo- of the Western Territories. Pt. II. The Tertiary rescences, associated with Trochodendroides flora. U. S. Geol. Surv. Terr., Rep. 7, pp. 1–366. leaves (Cercidiphyllaceae). Bot. J. 91(12), 1898– Makulbekov, N.M., 1988. Paleogene flora of Southern 1906 (in Russian). Mongolia. Nauka, Moscow (in Russian). Golovneva, L.B., Alekseev, P.I., 2010. The genus Reid, E.M., Chandler, M.E., 1933. The London Clay Trochodendroides Berry in the Cretaceous floras of flora. British Museum Natural History, London. Siberia. Palaeobotany 1, 120–166 (in Russian). Schmalhausen, J., 1890. Wissenschaftliche Resultate Heer, O., 1869. Contributions to the fossil flora of der von der Kaiserlichen Akademie der North Greenland, being a description of the Wisswnschaften zur erforschung des Janalandes plants collected by Mr. Edward Whymper dur- und der Neusibirischen Inseln in der Jahren 1885 ing the summer of 1867. Philos. Trans. R. Soc. und 1886 ausgesandten Expedition. Abt. II. London 159, 445–488. Heer, O., 1870. Die Miocene Flora und Fauna Spitz- Tertiäre pflanzen der Insel Neusibirien. Mém. bergens. Kongl. Svenska Vetensk. Akad. Handl. Acad. Imp. Sci. St.-Pétersbourg. VII Sér. 37(5), 1– 8 (7), 1–98. 22.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

The composition and dynamics of the Late Cretaceous and Paleocene Arctic plant communities

A.B. Herman1 and R.A. Spicer2

1Geological Institute of the RAS, Pyzhevskii per. 7, Moscow 119017, Russia; e-mail: [email protected] 2Environment, Earth and Ecosystems, The Open University, Milton Keynes, MK7 6AA, UK

The Arctic is rich with Late Cretaceous and late (mature, 'climax') SPCs. By looking at tax- Paleocene plant fossils evidencing a thriving, on/facies relationships in successive taphofloras diverse, but now extinct polar ecosystem that through longer intervals of time we have been sequestered vast amounts of carbon (Herman, able to study the evolution of seral succession. 2013; Spicer and Herman, 2010). The polar cli- Successional plant communities (SPCs) are mate and light regime were key constraints on those aggregations of taxa that repeatedly occur floral composition and dynamics (Herman et al., in stages as a bare substrate is initially colonised 2016). By combining field and museum studies and the composition of the vegetation changes across North America and Northern Asia a pic- until a relatively stable state is attained, often, ture has emerged of a highly productive polar but not always, comprising a mature forest. In ecosystem surrounding a warm Arctic Ocean our case we divide the SPCs into three catego- and shrouded in an almost permanent cover of ries: Early, Middle and Late (Fig. 1). The bound- cloud and mist. High rainfall, warm tempera- aries between these stages are not rigid, but are tures and 24 hours of diffuse sunlight led to high transitional as the composition changes by the summer productivity (Spicer and Herman, addition or loss of individual taxa. 2010). Cool wet winters favoured the translation We recognise that (1) horsetails Equisetites of autumnal leaf fall and above ground biomass and some ferns (typically Birisia, but after the dieback into deep time storage, thus making beginning of the Maastrichtian, Onoclea) were these forests highly effective systems for seques- obligatory components of the early SPCs; (2) the tering carbon. By using collections and observa- first rare angiosperms (e.g., the dicot Vitiphyllum tions made over large numbers of field seasons multifidum) appeared in the middle SPCs of the working in different geographic areas and on Arctic in the Early–Middle Albian and occupied rocks of different ages it has been possible to disturbed near-channel habitats; (3) from Late gain insights into palaeofloral associations, and Albian times onwards angiosperms became even seral successions. abundant in the middle SPCs of the Arctic, but The sedimentologically dynamic Arctic were still rare in the earlier and later SPCs; floodplains captured a patchwork of plant (4) monocots appeared in the Maastrichtian in communities at different stages of development. early, predominantly aquatic, SPCs; (5) all Arctic Detailed examination of the distributions of Cretaceous late SPCs (and 'climax' vegetation) plant remains in time and space, and repeated were dominated by conifers; (6) Arctic SPCs associations that occur between particular plant were taxonomically more diverse under warm taxa and particular sedimentary facies, allows climate intervals than cold; (7) during the Albian the reconstruction of changes in Arctic vegeta- and Late Cretaceous, advanced (Cenophytic, tion composition and dynamics throughout the angiosperm-dominated) plant communities co- Late Cretaceous and into the Paleocene (Her- existed with those of a more relictual (Meso- man, 2013; Herman et al., 2016; Spicer and phytic, dominated by ferns and gymnosperms) Herman, 2010). Based on many thousands of leaf aspect, and plants in these communities tended and leafy shoot remains, fossil wood and repro- not to mix; (8) coal-forming environments ductive organ assemblages from Northeastern (mires) remained conifer, fern and bryophyte Russia and Northern Alaska we identify a num- dominated throughout the Late Cretaceous and ber of successional plant communities (SPCs) Paleocene with little penetration of woody angi- representing seral development from early osperm components and so are conservative (primary colonisers, pioneer), through middle to and predominantly Mesophytic in character;

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Fig. 1. Idealised successional plant communities based on three exemplar fossil floras: the Middle to Late Albian Kukpowruk Flora (Spicer and Herman, 2001), the latest Albian–Cenomanian Grebenka Flora (Spicer et al., 2002) and the Late Maastrichtian Koryak Flora (Moiseeva, 2005, 2012). Ecologically dominant taxa are shown in bold and angio- sperms are underlined.

(9) bryophytes and ferns, with some subordinate from Northeastern Russia into the more norther- conifers, make up a persistent raised mire cli- ly Northern Alaska and (11) there was no signif- max community that is most widely developed icant extinction across the K/Pg boundary. in Late Albian, Cenomanian and Campanian These observations attest to Arctic vegeta- times, with the Campanian exhibiting particu- tion displaying persistent structure and dynam- larly high levels of bryophyte diversity; ics despite a general Late Cretaceous cooling (10) general Cretaceous SPC characteristics were trend and events at the Cretaceous–Paleogene maintained into the Paleocene due to migrations transition.

References Herman, A.B., 2013. Albian–Paleocene flora of the Moiseeva, M.G., 2012. The Maastrichtian Flora of the North Pacific: Systematic composition, palaeoflo- Amaam Lagoon Area (Northeastern Russia). ristics and phytostratigraphy. Stratigr. Geol. Cor- Stratigr. Geol. Correl. 20(7), 579–679. rel. 21(7), 689–747. Spicer, R.A., Herman, A.B., 2001. The Albian– Herman, A.B., Spicer, R.A., Spicer, T.E.V., 2016. Envi- Cenomanian flora of the Kukpowruk River, ronmental constraints on terrestrial vertebrate western North Slope, Alaska: stratigraphy, palaeofloristics, and plant communities. behaviour and reproduction in the high Arctic of Cretaceous Res. 22, 1–40. the Late Cretaceous. Palaeogeogr. Palaeoclima- Spicer, R.A., Herman, A.B., 2010. The Late Cretaceous tol. Palaeoecol. 441, 317–338. environment of the Arctic: A quantitative Moiseeva, M.G., 2005. Koryak floristic assemblage of reassessment based on plant fossils. Palaeogeogr. Northeastern Russia: Systematic composition, Palaeoclimatol. Palaeoecol. 295, 423–442. ecological, taphonomical and palaeoclimatic Spicer, R.A., Ahlberg, A., Herman, A.B., Kelley, S.P., characteristics, in: Akhmetiev, M.A., Herman, Raikevich, M.I., Rees, P.M., 2002. Palaeoenvironment A.B. (Eds.), Modern problems of palaeofloristics, and ecology of the middle Cretaceous Grebenka palaeophytogeography and phytostratigraphy. flora of northeastern Asia. Palaeogeogr. GEOS, Moscow, pp. 212–223 (in Russian). Palaeoclimatol. Palaeoecol. 184, 65–105. 23

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Late Jurassic to Early Cretaceous oysters (Bivalvia, Ostreoidea) from Siberia: Taxonomy, palaeoecology, distribution and variations of carbon and oxygen isotopes

I.N. Kosenko1,2

1Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia 2Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia e-mail: [email protected]

The present contribution is an analysis of stages of oyster development, Jurassic stage and more than 300 specimens of Upper Jurassic– Cretaceous stage, are recognised in western Bo- Lower Cretaceous oysters collected by V.A. real and Subboreal domains (England, northern Zakharov during the 1960s and currently stored France and Poland). In Siberia, Jurassic and Ear- in Trofimuk Institute of Petroleum Geology and ly Cretaceous oysters formed a unique complex. Geophysics, Siberian Branch of RAS (Novosi- This may be explained by the absence of good birsk, Russia). They were sampled in the north- communications between west European and western margin of Western Siberia (Yatriya, Polish basins and Siberian basins during the ear- Maurynya, Tol’ya, and Lopsiya rivers) and the liest Cretaceous. north of Eastern Siberia (Boyarka, Bol’shaya Based on carbonate material of oyster shells Romanikha, and Dyabaka-Tari rivers) (Zakha- the stable isotope analyses were performed, and rov, 1966; Saks, 1972; Zakharov and Mesezhni- palaeotemperatures were calculated. Seven oys- kov, 1974; Kosenko, 2014). During the last five ter shells of Pernostrea (Pernostrea) uralensis years, they were examined with taxonomic and (Zakharov) from the Jurassic–Cretaceous palaeoecological purposes. boundary interval (Upper Volgian–lowermost Taxonomic study included classical mor- Ryazanian) of Maurynya River have been used phofunctional and biometrical analyses. A large to obtain δ13C and δ18O data (Kosenko et al., number of Cretaceous oysters from Crimea as 2013). The preservation of the carbonate material well as of modern Pacific oysters, Crassostrea gi- was controlled by the following methods: ca- gas, have been involved in this study to under- thodoluminescence analyses; control of content stand the range of modification variability be- of Fe, Mn, Sr; control of absence of correlation tween different species (Kosenko, 2016). Oysters between δ13C and δ18O and content of Fe and identified previously as Liostrea are attributed Mn. The obtained δ13C and δ18O data were com- now to four genera: Praeexogyra, Helvetostrea pared with isotopic data based on belemnites (Flemingostreidae), Pernostrea (Gryphaeidae), from the same section (Dzyuba et al., 2013) and and one new genus (Gryphaeidae) including on- were used to estimate palaeotemperatures. A ly species “Liostrea” roemeri (Quenstedt). The lat- general trend towards negative δ18O values was ter genus is characterised by peculiar ethology, recognised in the Maurynya section, from the being attached to floating ammonites, and mor- lower part of the Upper Volgian to the middle phology outlined by a beak-shaped umbo on the part of the Ryazanian Chetaites sibiricus ammo- right (!) valve. Endemic Siberian species from nite Zone. The same trend was also established the genus Pernostrea have recently been included in the Nordvik section (Dzyuba et al., 2013). The into the subgenus Boreiodeltoideum Kosenko, higher palaeotemperatures (2°C in average) de- 2016. Genera Pernostrea and Deltoideum have termined from oyster shells indicate that belem- been included into the new tribe (under descrip- nites likely migrated laterally and lived part of tion) from the subfamily Gryphaeinae. Model of their lives in cooler waters. phylogenetic relationships between species of this tribe has been proposed. This work is a contribution to the IGCP608 and Siberian oyster complexes are compared programs 30 and 43 of the Presidium of the RAS and with complexes from Western Europe, Poland financially supported by the Russian Foundation for and East European Platform (Table 1). Two Basic Researches (grant no. 16-35-00003).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Table 1 Comparison of Upper Jurassic and Lower Cretaceous complexes of oysters from northwestern part of Western Siberia, northern Eastern Siberia and Europe (author's names are kept)

Northern and European part of Western Europe Subpolar Urals Northern Eastern Poland Russia (Switzerland) (north-western part Siberia (Pugaczewska, 1971, 1975) (Gerasimov, 1955) (Koppka, 2015) of Western Siberia)

Alectryonia gregarea (Sow.), A. solitaria (Sow.), A. rastellaris (Münster), A. pulligera (Goldfuss), Circunula cotyleodon A. vallata (Étallon), (Cont.), A. flabelliformis (Nilsson), Nanogyra (Nanogyra) Arctostrea hastellata (Schl.), nana (Sow.), Pernostrea Liostrea delta (Smith), N. (Palaeogyra)

(Pernostrea) sp. n. 1, L. oxfordiana (Rollier), reniformis (Gold.), Helvetostrea exotica Pernostrea Ostrea plastica L. quadrangularis (Arkell), N. (P.) virgula (Kosenko), (Pernostrea) sp. n. 1, (Trautsch.), L. gryphaeata (Schl.), L. sequana (Deshayes), Gryphaea (Gryphaea) “Liostrea” roemeri Exogyra virgula (Thurm.), L. moreana (Buv.), Helvetostrea sequana curva (Ger.), (Quenstedt) (Defrance) L. monsbeliardensis (Cont.), (Thurm. et Étallon),

Kimmeridgian Nanogyra (Nanogyra) L. brasili Chavan, Praeexogyra dubiensis nana (Sow.) L. polymorpha (Münster), (Cont.), L. multiformis (Koch et Dunker), P. monsbeliardensis Gryphaea dilatata (Sow.), (Cont.), Nanogyra nana (Sow.), Actinostreon gregarium Exogyra virgula (Defrance), (Sow.) E. reniformis (Goldf.), E. welseni (Jourdi), E. intricata (Cont.)

Pernostrea Ostrea plastica (Pernostrea) sp. n. 2, (Trautsch.), P. (P.) gibberosa Gryphaea curva (Zakharov), (Ger.), P. (P.) uralensis Ostrea expansa Liostrea dubisensis (Cont.),

(Zakharov), Pernostrea (Sow.), L. unciformis (Buv.), Pernostrea? sp. n. 3, (Boreiodeltoideum) O. unciformis L. plastica (Trautsch.), no data Praeexogyra siberica praeanabarensis (Buv.), L. virguloides (Lew.),

Volgian (Zakharov), (Zakharov) O. kharashovensis Exogyra michalskii Lew., “Liostrea”roemeri (Roullier), E. decipiensis Lew. (Quenstedt), O. dibiensis Nanogyra (Nanogyra) (Cont.), thurmanni (Étallon), Exogyra nana N. (N.) nana (Sow.) (Sow.)

Pernostrea Ceratostreon tuberculiferum

(Pernostrea) uralensis (Koch et Dunker), Zakharov, Pernostrea Ostrea Rhynchostreon etalloni Praeexogyra (Boreiodeltoideum) no data limaciforme Ger. (Pictet et Campiche), lyapinensis anabarensis (Bodyl.) Ostrea sanctae crucis Ryazanian (Zakharov), (Pictet et Campiche) P. siberica (Zakharov)

Aetostreon latissimum (Lam.), A. neocomiensis (Orb.), Pernostrea Ceratostreon minos (Coq.), (Boreiodeltoideum) Rhynchostreon anabarensis (Bodyl.), tombeckianum (Orb.), Pernostrea no data no data Gryphaeostrea cf. lateralis (Nilss.), no data (Pernostrea) G. arduennensis (Orb.), cucurbita (Zakharov),

Valanginian Ostrea sanctae cricis (Pictet et Gryphaea borealis Campiche), O. germaini (Coq.), Zakharov Lopha cf. cotteaui (Coq.), L. cf. eos (Coq.)

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

References

Dzyuba, O.S., Izokh, O.P., Shurygin, B.N., 2013. Car- da v rakovinakh ustrits iz prigranichnykh ot- bon isotope excursions in Boreal Jurassic- lozhenii yury i mela reki Maurynya (Zapadnaya Cretaceous boundary sections and their correla- Sibir’), in: XX simpozium po geokhimii izotopov tion potential. Palaeogeogr. Palaeoclimatol. Pal- imeni akademika A.P. Vinogradova (12–14 noy- aeoecol. 381–382, 33–46. abrya 2013 g.): Tezisy dokladov. Akvarel’, Mos- Gerasimov, P.A., 1955. Index fossils of the Mesozoic cow, pp. 185–188 (in Russian). of the central regions of the European part of the Pugaczewska, H., 1971. Jurassic Ostreidae of Poland. USSR. Gosgeoltekhizdat, Moscow (in Russian). Acta Palaeontol. Polon. 16(3), 193–311. Koppka, J., 2015. Revision of the Bivalvia from the Up- Pugaczewska, H., 1975. Neocomian oysters from Cen- per Jurassic Reuchenette Formation, Northwest tral Poland. Acta Palaeontol. Polon. 20(1), 47–72. Switzerland – Ostreoidea. Zootaxa 3927, 1–117. Saks, V.N. (Ed.), 1972. The Jurassic–Cretaceous Kosenko, I.N., 2014. On Late Jurassic and Early Creta- boundary and the Berriasian Stage in the Boreal ceous oysters (Bivalvia, Ostreidae) from northern Belt. Nauka, Novosibirsk (in Russian). Siberia. Paleontol. J. 48(4), 380–388. Zakharov, V.A., 1966. Late Jurassic and Early Creta- Kosenko, I.N., 2016. On Late Jurassic and Early Creta- ceous bivalves (order Anisomyaria) of northern ceous oysters of the genus Deltoideum Rollier (Bi- Siberia and the conditions of their existence. valvia, Ostreoidea) from Siberia. Paleontol. J. Nauka, Moscow (in Russian). 50(4), 336–346. Zakharov, V.A., Mesezhnikov, M.S., 1974. The Vol- Kosenko, I.N., Izokh, O.P., Dzyuba, O.S., Shurygin, gian Stage in the Subpolar Urals. Nauka, Novo- B.N., 2013. Variatsii izotopov ugleroda i kisloro- sibirsk (in Russian).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

The neuropteran assemblage (Insecta) of the mid-Cretaceous Burmese amber confirms transitional character of its biota

V.N. Makarkin

Institute of Biology and Soil Science, Far Eastern Branch of RAS, pr. 100-letiya 159, Vladivostok 690022, Russia; e-mail: [email protected]

The biological inclusions of Burmese amber The Nevrorthidae is recorded from Burmese represent a sample of a tropical forest communi- amber (and the Mesozoic) for the first time, ty in equatorial southeastern Asia at ~12oN pale- based on the photograph of Xia et al. (2015, right olatitude (Grimaldi et al., 2002; Poinar et al., upper fig. on p. 101). Judging from this, this un- 2008). The volcaniclastic matrix of the amber is described species does not strongly differ from estimated as ~98.79±0.62 million years old, i.e., Baltic amber and extant taxa. near the Albian–Cenomanian (Early–Late Creta- The Coniopterygidae are relatively rare in ceous) boundary (Shi et al., 2012), but the amber Burmese amber. Two species assigned to two ex- is considered to be slightly older, Late Albian. tinct genera have been described (Engel, 2004a), Fossils of the order Neuroptera have been and there is at least one undescribed genus and found as old as the early Permian. Today, this species. One genus belongs to extant tribe Fon- order is comprised of 16 families. A preliminary tenelleini. analysis of published and unpublished materials All known adult specimens of Burmese am- reveals the presence of 18 neuropteran families ber Osmylidae belong to the extant relict sub- in Burmese amber, 13 of which are extant and 5 family Gumillinae (Myskowiak et al., 2016; pers. extinct. To date, 25 neuropteran species have obs.), whose single extant species is distributed been described from Burmese amber, and more in Brazil. Two possible larvae of Osmylidae specimens in existing collections remain un- would be very unusual for that group (Engel described. and Grimaldi, 2008, figs. 9–11; Xia et al., 2015, The vast majority of extant families are upper fig. on p. 95). found in Burmese amber. Polystoechotidae is The Berothidae are the most abundant and the only extant family known from the Creta- diverse neuropterans in Burmese amber, with ceous that is still not recorded from it. It is more than 100 known specimens and thirteen noteworthy, however, that only a few represent- species and one unnamed larva described (En- atives of some Coniopterygidae, Nevrorthidae, gel, 2004b; Engel and Grimaldi, 2008; Makarkin, Osmylidae and Dilaridae are similar to extant 2015; Shi et al., 2015). The subfamily affinities of taxa, certainly or probably (Nevrorthidae, Os- most of these are unclear (expect the Cretaceous mylidae) belonging to their crown groups. All subfamily Paraberothinae), but they probably do other extant families are represented in Burmese not belong to extant subfamilies. amber by unusual and/or distantly related su- One Burmese amber species assigned to the pergeneric taxa (extinct subfamilies and tribes) Mantispidae (Poinar and Buckley, 2011) is, how- that belong to their stem groups. ever, not conclusively a member of this family; Burmese amber has the oldest fossil records in any case, its subfamily affinity is entirely un- for the extant families Sisyridae, Dilaridae and clear. Nevrorthidae, but they are undoubtedly older, Some larvae of Chrysopidae from Burmese originating at least as far back as the Jurassic. All amber are in general similar to those of some other extant families in Burmese amber except extant taxa, in particular in bearing short lateral Nemopteridae are recorded from the Jurassic (its tubercles (processes) (e.g., Xia et al., 2015, figs. oldest known record is in the Late Aptian Crato on p. 96). They are extremely elongated on a Formation of Brazil). Unusual larvae similar to few undescribed chrysopoid trash/debris- those of Crocinae (Nemopteridae) are rather carrying larvae that are similar to Hallu- common in Burmese amber, represented by at cinochrysa Pérez-de la Fuente from the Albian least two species (e.g., Xia et al., 2015, see figs. of Spain. No adult chrysopids are known from on pp. 99, 100). Burmese amber. 27

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Stem group Hemerobiidae and Ithonidae The middle Cretaceous was a time of most are present in private collections, with at least intensive transformation of terrestrial ecosys- one undescribed species each. tems, shifting from those dominated by ancient Larval Nymphidae are common in Burmese gymnosperm groups to those dominated by an- amber, implying that they were probably arbor- giosperms, Pinaceae and polypod ferns (‘the eal. They represent several species, all of which mid-Cretaceous biocenotic crisis’ of Zherikhin, are generally similar to those of Nymphinae. 1978). In the Burmese amber forest, confident Adults of the family are scarce; one species has records of extinct gymnosperm groups (e.g., been described based on an incomplete speci- Bennettitales) are so far unknown (except for men (Engel and Grimaldi, 2008). possible pollen of Bennettitales: Peñalver et al., The larvae of a few species of Psychopsi- 2015), but angiosperms were already diverse, dae are quite common in Burmese amber, con- and all known ferns are polypods (Schneider et sistent with the arboreal habit of their modern al., 2016). At the same time, extant families dom- species. At least three adults are known, one of inate the neuropteran assemblage, and extinct which has been described (Engel and Grimaldi, families are rare. 2008). The transitional character of the Burmese All known specimens of Burmese amber amber neuropteran assemblage is most clearly Sisyridae belong to the extinct subfamily Para- seen in the coexistence of three neuropteran doxosisyrinae (Makarkin, 2016; pers. obs.). They groups with siphonate mouthparts, i.e., large Kal- are remarkable in possessing extremely long, si- ligrammatidae, moderately-sized Dilaridae, and phonate mouthparts. small Sisyridae. Most of the Mesozoic kalligram- The Dilaridae are rather common, and very matid species had a long proboscis. They are as- diverse in Burmese amber, with three species sumed to have fed on pollination drops and pol- described to date (Huang et al., 2015; Lu et al., len of extinct gymnosperms, mainly Bennettitales 2016). The majority of the species have long si- and Caytoniales (Labandeira et al., 2016), and be- phonate mouthparts, but some are similar to the came extinct along with most of their presump- extant Dilar Rambur and have the mandibute tive host plants in early Late Cretaceous. On the mouthparts that are usual for the family. other hand, species of Dilaridae and Sisyridae Of its five extinct families, Burmese amber with siphonate mouthparts probably fed on nec- has the youngest record for four, the Kalli- tar and pollen of flowers, as their proboscis was grammatidae, Araripeneuridae, Babinskaiidae, short, suitable to the shallow calyx (often less and Mesochrysopidae; the Dipteromantispidae than 1 mm) of known Burmese amber flowers. It are known in younger (Turonian) New Jersey may be assumed that these Burmese amber amber. Undescribed Kalligrammatidae and one sisyrids and dilarids were among the first special- species of Araripeneuridae were reported from ized groups of insect pollinators, which occupied Burmese amber by Huang et al. (2016), and Dip- the newly formed niche provided by flowers as a teromantispidae by Liu et al. (2016a). The Babin- source of food. However, these groups may have skaiidae are reported here for the first time also become extinct through an inability to com- based on photographs provided by Xia et al. pete as other more active and successful flower (2015, fig. on p. 94). The Mesochrysopidae are visitors appeared, mainly bees. represented in Burmese amber by one species The study is supported by the grant from the similar to the Barremian genus Allopterus Zhang Russian Foundation for Basic Researches no. 16-04- (Liu et al., 2016b). 00053.

References

Engel, M.S., 2004a. The Dustywings in Cretaceous Engel, M.S., Grimaldi, D.A., 2008. Diverse Neuropter- Burmese Amber (Insecta: Neuroptera: Coniop- ida in Cretaceous amber, with particular refer- terygidae). J. Syst. Palaeontol. 2(2), 133–136. ence to the paleofauna of Myanmar (Insecta). Engel, M.S., 2004b. Thorny lacewings (Neuroptera: Nova Suppl. Entomol. 20, 1–86. Rhachiberothidae) in Cretaceous amber from Grimaldi, D.A., Engel, M.S., Nascimbene, P.C., 2002. Myanmar. J. Syst. Palaeontol. 2(2), 137–140. Fossiliferous Cretaceous amber from Myanmar 28

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

(Burma): its rediscovery, biotic diversity, and imply nectarivory or hematophagy. Cretaceous paleontological significance. Am. Mus. Novit. Res. 65: 126–137. 3361, 1–72. Myskowiak, J., Huang, D., Azar, D., Cai, C.Y., Gar- Huang, D.Y., Azar, D., Cai, C.Y., Garrouste, R., Nel, rouste, R., Nel, A., 2016. New lacewings (Insecta, A., 2015. The first Mesozoic pleasing lacewing Neuroptera, Osmylidae, Nymphidae) from the (Neuroptera: Dilaridae). Cretaceous Res. 56, 274– Lower Cretaceous Burmese amber and Crato 277. Formation in Brazil. Cretaceous Res. 59, 214–227. Huang, D.Y., Azar, D., Engel, M.S., Garrouste, R., Cai, Peñalver, E., Arillo, A., Pérez-de la Fuente, R., Riccio, C.Y., Nel, A., 2016. The first araripeneurine antli- M.L., Delclòs, X., Barrón, E., Grimaldi, D.A., on in Burmese amber (Neuroptera: Myrmeleon- 2015. Long-proboscid flies as pollinators of Cre- tidae). Cretaceous Res. 63, 1–6. taceous gymnosperms. Current Biol. 25, 1917– Labandeira, C.C., Yang, Q., Santiago-Blay, J.A., Hot- 1923. ton, C.L., Monteiro, A., Wang, Y.J., Goreva, Y., Poinar Jr., G., Buckley, R., 2011. Doratomantispa bur- Shih, C.K., Siljeström, S., Rose, T.R., Dilche, D.L., manica n. gen., n. sp. (Neuroptera: Mantispidae), Ren, D., 2016. The evolutionary convergence of a new genus of mantidflies in Burmese amber. mid-Mesoizoic lacewings and Cenozoic butter- Hist. Biol.: Int. J. Paleobiol. 23(2/3), 169–176. flies. Proc. R. Soc. B 283: 20152893. Poinar Jr., G., Buckley, R., Brown, A.E., 2008. The se- Liu, X.Y., Lu, X.M., Zhang, W.W., 2016a. Halterioman- crets of Burmite amber. MAPS Digest 20, 20–29. tispa grimaldii gen. et sp. nov.: A new genus and Schneider, H., Schmidt, A.R., Heinrichs, J., 2016. Bur- species of the family Dipteromantispidae (Insec- mese amber fossils bridge the gap in the Creta- ta: Neuroptera) from the mid-Cretaceous amber ceous record of polypod ferns. PPEES 18, 70–78. of Myanmar. Zoological Systematics 41(2), 165– Shi, G.H., Grimaldi, D.A., Harlow, G.E., Wang, J., 172. Wang, J., Yang, M.C., Lei, W.Y., Li, Q.L., Li, X.H., Liu, X.Y., Zhang, W.W., Winterton, S.L., Breitkreuz, 2012. Age constraint on Burmese amber based on L.C.V., Engel, M.S., 2016b. Early morphological specialization for insect-spider associations in U–Pb dating of zircons. Cretaceous Res. 37, 155– Mesozoic lacewings. Current Biol. (in press). 163. Lu, X.M., Zhang, W.W, Liu, X.Y., 2016. New long- Shi, C.F., Ohl, M., Wunderlich, J., Ren, D., 2015. A re- proboscid lacewings of the Early Cretaceous markable new genus of Mantispidae (Insecta, provide insights into ancient plant-pollinator in- Neuroptera) from Cretaceous amber of Myan- teractions. Sci. Rep. 6: 25382. mar and its implications on raptorial foreleg evo- doi:10.1038/srep25382 lution in Mantispidae. Cretaceous Res. 52, 416– Makarkin, V.N., 2015. A new genus of the mantispid- 422. like Paraberothinae (Neuroptera: Berothidae) Xia, F.Y., Yang, G.D., Zhang, Q.Q., Shi, G.L., Wang, B., from Burmese amber, with special consideration 2015. Amber: Lives through time and space. Sci- of its probasitarsus spine-like setation. Zootaxa ence Press, Beijing (in Chinese). 4007(3), 327–342. Zherikhin, V.V., 1978. Development and changes in Makarkin, V.N., 2016. Enormously long, siphonate Cretaceous and Cenozoic faunistic complexes mouthparts of a new, oldest known spongillafly (tracheates and chelicerates). Nauka, Moscow (in (Neuroptera: Sisyridae) from Burmese amber Russian).

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

The mid-Cretaceous swamp plant communities of northeastern Asia

V.S. Markevich1, E.V. Bugdaeva1, T.A. Kovaleva1,2,3, E.B. Volynets1 and M.A. Afonin1

1Institute of Biology and Soil Science, Far Eastern Branch of RAS, pr. 100-letiya 159, Vladivostok 690022, Russia; e-mail: [email protected] 2Research Center of Paleontology & Stratigraphy, Jilin University, Changchun 130026, China 3Key Lab of Past Life & Environment in NE Asia, MOE, Changchun 130026, China

In eastern Russia, the coal-bearing deposits bryophytes, ferns, bennettites, ginkgoaleans, that were formed during the Barremian–Albian czekanowskialeans and conifers (Pinaceae, Chei- in the high and mid-latitudes are widespread. rolepidiaceae, Podozamitaceae, and Taxodiace- The former developed in the region of Yakutia ae). and Chukotka, the latter – in the Amur region Both floras have depleted and rather unvar- and Primorye. We studied the fossil floras of the ied taxonomic composition. During the Aptian, Ainakhkurgen (Aptian) and Chimchememel the plant communities were dominated by cy- (Early Albian) formations of the Ainakhkurgen atheaceous, dicksoniaceous and osmundaceous Basin located in the middle reaches of the Anuy ferns. Tree and shrub vegetation was represent- River (Chukotka). The lower part of the se- ed by pinaceous, podocarpaceous, taxodiaceous quence formed in a marine environment, the and podozamitaceous conifers, ginkgoaleans, upper part – in brackish and continental envi- czekanowskialeans, cycadaleans, and bennettita- ronments. leans. During the Albian, the ferns lose their The palynological assemblage of the Aina- significance (by reducing of the Osmundaceae), khkurgen Formation is dominated by ferns hav- trees and shrubs become more diverse (a new ing affinity with Cyatheaceae, Dicksoniaceae species of pinaceous and cheirolepidiaceous co- and Osmundaceae. They are accompanied by nifers, as well as rare gleicheniaceous ferns and ferns close to Polypodiaceae. Spores of Glei- angiosperms appear). cheniaceae are rare and sporadic, while spores The flora of the more southern coal-bearing of Schizaeaceae occur somewhat more common. basins of the Amur River region (Bureya Basin) Among gymnosperms the conifers (Pinaceae and Primorye region (Partizansk and Razdolna- and Podocarpaceae) and Ginkgocycadophytus sp. ya River basins) was studied. dominate. They are accompanied by taxa close The Bureya Basin is located in the upper to Taxodiaceae and Podozamitaceae. reaches of the Bureya River, a tributary of the The fossil plants of the Ainakhkurgen For- Amur River. The Barremian–Aptian coal- mation (Filippova, 1975) are represented by bearing deposits of this basin were divided into ferns, cycadaleans, bennettitaleans, ginkgoale- the Chagdamyn and Chemchukin formations. ans, czekanowskialeans, and conifers (Pinaceae The palynological assemblage of the Chagda- and Podozamitaceae). myn Formation (Barremian) is characterised by The palynological assemblage of the Chim- high diversity and abundance of cyatheaceous, chememel Formation is dominated by the gym- gleicheniaceous and osmundaceous ferns; nosperms. Among them Ginkgocycadophytus sp., among gymnosperms the pinaceous and taxodi- Pinaceae, Podocarpaceae and Taxodiaceae pre- aceous conifers dominate, the share of Ginkgocy- vail. The percentage of pollen of cadophytus in palynospectra remains rather high Podozamitaceae decreases and pollen of Cheiro- (Markevich and Bugdaeva 2014). The diversity lepidiaceae increases. The taxonomic composi- of ferns and cycadophytes is low in the mega- tion of spores is depleted. They are mainly rep- fossil flora of the Chagdamyn Formation. The resented by taxa close to Cyatheaceae and horsetails, bryophytes, czekanowskialeans and Dicksoniaceae, the share of Osmundaceae sharp- some ginkgoaleans (Sphenobaiera) disappear. The ly reduces. The representatives of Gleicheni- ginkgoaleans Eretmophyllum glandulosum aceae and Schizaeaceae are rare. (Samyl.) Krassil. and Ginkgoites longipilosus The fossil plants of the Chimchememel Krassil. dominate in the burials (Krassilov, 1972, Formation (Filippova, 1975) include horsetails, 1973).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

The palynological assemblage of the Chem- remain as ground cover beneath a canopy of chukin Formation (Aptian) is dominated by taxodiaceous trees. The Cyatheaceae lost its spores Cyathidites and Gleicheniidites, pollen of leading role in lowland plant communities; it taxa close to Taxodiaceae and Pinaceae, locally appears that these ferns shifted to the periphery Ginkgocycadophytus. The megafossil flora of the of swamps. Chemchukin Formation is characterised by an Coeval floras of Partizansk and Razdolnaya increase in taxonomic diversity (Vachrameev River basins of Southern Primorye formed un- and Doludenko, 1961; Krassilov, 1972, 1973). The der different conditions: the former existed in ferns and ginkgoaleans hold a role of domi- environments of the coastal lowlands and influ- nants. The bryophytes, cycadophytes, ence of the sea, the latter – mainly in environ- czekanowskialeans, conifers Elatides sp. and ments of intracontinental basin. Athrotaxopsis expansa Font. are locally abundant The Barremian megafossil flora of Parti- (Krassilov, 1973). zansk Basin is dominated by Taxodiaceae and The significant floristic events took place Schizaeaceae. The Polypodiaceae and cycads during the Barremian in the Bureya Basin: the played an important role in plant communities diversity of ferns abruptly reduced, Gleicheni- (Krassilov, 1967). The Aptian plant communities aceae began to play a dominant role in plant here were dominated by Taxodiaceae and Glei- communities, Czekanowskiales and cycado- cheniaceae, while Pinaceae, Miroviaceae, Gink- phytes disappeared, among Ginkgoales Er- goales and bennettites appeared as minor etmophyllum glandulosum and Ginkgoites longi- ground cover components. During the Albian, pilosus replaced extinct Baiera and Sphenobaiera Taxodiaceae retains its dominating status in the (Krassilov, 1973). The swamp plant communities plant communities, polypodiaceous ferns re- were represented by mainly gleicheniaceous turned to the status of dominant. The vegetation ferns, mosses, and lycopsids, and to a lesser ex- becomes more diverse (new species of ferns and tent by Pinaceae, Ginkgoales, and Cyatheaceae. conifers, as well as the first angiosperms have The megafossil flora of the Chemchukin appeared). Formation is characterised by an increase in tax- The Barremian flora of Razdolnaya River onomic diversity while ginkgoaleans remain as Basin is characterised by an increase in fern di- dominant components. The czekanowskialeans versity and dominance of Schizaeaceae. The Cy- Hartzia angusta Krassil. and Phoenicopsis sp. ap- atheaceae and Pteridaceae played a great role in pear. This flora has ever-increasing abundance plant communities. Among gymnosperms the of cycadophytes suggesting a thermophilic fea- Pinaceae, Miroviaceae and cycadophytes domi- ture of vegetation (Krassilov, 1973). In the nate. The Aptian plant communities are very di- Chemchukin megaflora, Athrotaxopsis expansa verse. On the foothills or near the watershed, (Taxodiaceae) appears. This plant is a typical taxon of the Barremian–Albian floras of South- they were dominated by pinaceous and podo- ern Primorye. The introduction of this repre- carpaceous, and to a lesser extent by taxodia- sentative of the more southern floras in the plant ceous conifers. Cyatheaceous, dicksoniaceous communities of Bureya Basin may indicate and gleicheniaceous ferns are abundant. The warming, as well as the creation of conditions lowland plant communities located in the cen- for the floristic exchanges between these regions. tral part of this basin were dominated by glei- The predominance of Gleicheniaceae in palyno- cheniaceous and cyatheaceous ferns; followed logical spectra may also indicate a climatic op- by dicksoniaceous ferns and plants produced timum. pollen Ginkgocycadophytus. Minor components of The composition of swamp communities these communities were Taxodiaceae, Bryo- during the time of deposition of the Chem- phyta, Lycophyta, other groups of ferns, Arau- chukin Formation has changed drastically. They cariaceae, Cheirolepidiaceae, and Erdtmanithe- were dominated by Gleicheniaceae along with caceae. The bisaccate pollen which was Cyatheaceae, followed by Taxodiaceae and produced by Pinaceae, Podocarpaceae and Cay- plants produced Ginkgocycadophytus pollen. In toniaceae is absent in the spectra. Angiosperms moister environments, ferns and cycadophytes appear in this flora.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

During the mid-Cretaceous, the wetland Barremian–Aptian–Early Albian, the time of ecosystems with their specific vegetation wide- climatic optimum and the Oceanic Anoxic Event 1 spread on the eastern margin of the Asian conti- (OAE 1). Obviously, these events were closely nent. Living in similar habitats, swamp vegeta- linked: transgression of the sea, flooding and tion had similar features, such as the dominance waterlogging of vast areas, the emission of large of ferns, conifers and plants produced Ginkgocy- amounts of greenhouse gases (mainly water va- cadophytus (Ginkgoales, Czekanowskiales, Cyc- pour, methane and carbon dioxide; the release of adales, and Bennettitales). However, there are the latter could be result of the volcanic erup- differences. The taxonomical composition of tions what the occurrences of tuffaceous inter- plant communities existed at high latitudes was layers in the coal-bearing deposits testify) con- depleted, whereas more southern swamp vege- tributed to warming of climate, an increase of tation was characterised by ever-increasing biodiversity and ecosystem productivity. The plant diversity. Among ferns the role of Glei- Barremian–Early Albian peat-formation with the cheniaceae increased to the south; it is possible peak in the Aptian was widely manifested in that this was due to the nature of these light- other parts of Asia and North America (Krassi- loving ferns. Cycadophytes have similar distri- lov, 1985). bution, though perhaps it was related to the temperature factor. Near-polar environments Acknowledgements formed under conditions of the mid-Cretaceous Our research was supported by the Russian pronounced global warmth and the absence of Foundation for Basic Research (grant no. 16-04-01411) cold winters. Winter dormancy plants lasted for and the grant of the President of the Russian Federa- tion for state support of young Russian candidates of no more than four and a half months and were sciences (project no. MK-2993.2015.4). The authors are largely controlled by light rather than tempera- grateful to the late Prof. V. Krassilov, V. Podolyan, ture (Spicer et al., 2002). On the contrary, V. Golozubov, V. Nechaev, E. Korochkin, K. Gavrilov, Czekanowskiales and Podozamitaceae typical of E. Zubkov, T. and V. Shishikin, N. Domra and seasonal climate disappeared in the plant com- S. Alexeev for fruitful discussions, advices and help. munities from north to south. We are indebted to corresponding member of RAS Thus, the maximum spread of the marshes B. Shurygin and Prof. Hisao Ando for support of our and the peak of a peat-accumulation in them on participation in the 4th International Symposium of the eastern margin of Asia occurred in IGCP608.

References

Filippova, G.G., 1975. Flora of the Lower Cretaceous Krassilov, V.A., 1985. The Cretaceous Period: Evolu- deposits of the Umkuveem and Ainakhkurgen tion of the Earth’s Crust and Biosphere. Nauka, Depressions, in: Materials on Geology and Min- Moscow (in Russian). eral Resources of the North-East USSR 22. Markevich, V.S., Bugdaeva, E.V., 2014. Late Jurassic– Magadanskoe knizhnoe izdatelstvo, Magadan, Early Cretaceous coal-forming plants of the Bu- pp. 23–35 (in Russian). reya Basin, Russian Far East. Stratigr. Geol. Cor- Krassilov, V.A., 1967. Early Cretaceous flora of South- rel. 22 (3), 239–255. ern Primorye and its stratigraphic significance. Spicer, R.A., Ahlberg, A., Herman, A.B., Kelley, S.P., Nauka, Moscow (in Russian). Raikevich, M.I., Rees, P.M., 2002. Palaeoenvi- Krassilov, V.A., 1972. Mesozoic flora of the Bureya River (Ginkgoales and Czekanowskiales). Nau- ronment and ecology of the middle Cretaceous ka, Moscow (in Russian). Grebenka flora of northeastern Asia. Palaeoge- Krassilov, V.A., 1973. Materials on stratigraphy and ogr. Palaeoclimatol. Palaeoecol. 184, 65–105. palaeofloristics of coal-bearing deposits in the Bu- Vachrameev, V.A., Doludenko, M.P., 1961. The Late reya Basin, in: Krassilov, V.A. (Ed.), Fossil floras Jurassic and Early Cretaceous flora of the Bureya and phytostratigraphy in the Far East. DVNTs AN Basin and its stratigraphic significance. AN SSSR, Vladivostok, pp. 28–51 (in Russian). SSSR, Moscow (in Russian).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Upper Cretaceous palynology (spores, pollen and dinoflagellate cysts) of the Yakovlevskaya-2 borehole, Ust-Yenisei region

I.V. Smokotina

JSC “SIBIRSKOE PGO”, Berezin str. 3D, Krasnoyarsk 660020, Russia; e-mail: [email protected]

Palynological studies of the Upper Creta- Densoisporites microrugulatus Brenner., D. velatus ceous sediments in the section of Ya- Weyl. et Krieg., Kuylisporites lunaris Cook. et kovlevskaya-2 borehole located in the Yakovlev Dett., Aequatriradites verrucosus Cook. et Dett., River Basin in the north of Ust-Yenisei region of Camptotriletes ambigens Fradk., Osmundacidites northern Siberia (Fig. 1) permit the biostrati- spp., Selaginella spр., Gleicheniidites senonicus graphic subdivision of the sediments for defini- Ross., Appendicisporites spp. (A. tricostatus Bolch., tion of age, boundaries of formations and for re- A. exilioides (Mal.) Bolch., etc.), Cicatricosisporites construction of paleogeography. The present dorogensis R. Pot. et Gell., Lygodiumsporites sub- report is based on a study of core materials con- simplex Bolch., L. asper Bolch., Trilobosporites mi- taining a varied and highly rich coastal and ma- rabilis Bolch., Klukisporites pseudoreticulatus rine microflora. Spores, pollen and dinoflagel- Coup., Leptolepidites major Coup., Foramini- lates have been identified. The diverse sporites asymmetricus (Cook. et Det.) Det., taxonomic composition and stratigraphic distri- Rouseisporites reticulatus Poc., Cycadopites dilu- bution of microphytofossils are analyzed. Five cidus (Bolch.) Il., Araucariacites pexus Sach. et palynological assemblages are revealed here in Kosenk., Podocarpidites sрp., Pseudopicea sp., the Upper Cretaceous on the basis of their com- Picea complanatiformis Bolch., Piceapollenites varia- parison with standard assemblages characteriz- biliformis (Bolch.) Petr., Sciadopityspollenites mul- ing a zonal palynostratigraphic scale of northern tiverrucosus Sach. et Il., Classopollis, Alisporites Siberia (Bochkarev, 1981; Bondarenko, 2001; Gu- sp., A. similis (Balme) Dett., Phyllocladidites spp., rari, 2004; Nikitenko et al., 2013). By means of typical Pteris cretacea Chlon., Ruminatisporites sp. the cores a very rich microflora (spores of ferns (0.3%), Taurocusporites reduncus (Bolch.) Stov., and mosses, pollen of gymnosperms and angio- and Pinus aralica Bolch., dinocysts Chlamidopho- sperms, and algae) could be collected from vari- rella nеyei Cook. et Eis., Chlonoviella agapica Leb., ous stratigraphic levels. Studied palynological Chatangiella spр., Amphydiadema sp., and Oli- assemblages indicate the following stratigraphic gospheridium sp., prasinophyte Leiospheridia spp., units: Cenomanian (820.0–890.0 m depth), Up- and algae Ovoidites sp. per Turonian–Coniacian (270.0–280.0 m depth), Santonian–Campanian (190.0–270.0 m depth), Upper Campanian–Maastrichtian (150.0–190.0 m depth), and Upper Maastrichtian (70.0–130.0 m depth) (Fig. 2). Cenomanian. Abundant spores (up to 59.2%); the subdominant: dinoflagellates (up to 16.6%), Cyathidites spp. (up to 12.9%), Ginkgocy- cadophytus (10.0%), Leiotriletes spp. (up to 19.5%), and Disaccites (up to 10.8%); many Polypodis- porites sp. (6.7%). Related: Foveosporites cenoman- icus (Chl.) Schvez., Stenozonotriletes sp., Lycopo- diumsporites marginatus Singh., Sphagnum spp. (up to 4.7%), Appendicisporites macrohysus (Bolch.) Pot., Balmeisporites glenelgensis Cook. et Dett., pollen Taxodiaceae, Cedrus spp., Pinuspol- lenites minimus (Coup.) Kemp., Tetraporina sp., single Lycopodiumsporites spp., Dicksoniaceae, Fig. 1. The location of the Yakovlevskaya-2 borehole Marattisporites sp., Auritulina sp., Salviniaceae, in Ust-Yenisei region.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Upper Turonian–Coniacian. Abundant yspollenites multiverrucosus, Classopollis, spores (46.1%); the subdominant: dinoflagellates Alisporites sp., Eucommiidites troedssonii Erdtm., (16%). Related: Pilasporites marcidus Balme, Poly- Callialasporites sp., and Vitreisporites spp. Typical podisporites sp., Sphagnum spp., Lycopodi- angiosperms: Triprojectus sp., Gnetaceapollenites umsporites spp., Leiotriletes spp., Cyathidites spp., sp., Ilexs sp., Pterocarya sp., Platanus sp., Myrica Foveosporites cenomanicus, Pteridaceae, Dictyo- sp., Corylopsis sp., Ericaceae, Gothanipollis sp., phyllidites sp., Clathropteris obovata, Densoisporites Tricolpites sp., Hamamelidaceae, Rhamnus glabra spp., Pteris cretacea, Kuylisporites lunaris, Bolch., and Inaperturepollenites sp.; dinocysts: Aequatriradites spinulosus Cook. et Dett., Os- Chatangiella granulifera (Manum) Len. et Wil., mundacidites spp., Gleicheniidites spp., Appen- C. victoriens (Cook. et Man.) Len. et Wil., dicisporites spp., Cicatricosisporites spp., Lygodi- C. bondarenkoi (Voz.) Len. et Wil., C. niiga Voz., umsporites spp., Klukisporites variegates Coup., C. chetensis (Voz.) Len. et Wil., Isabeledinium spр., Stenozonotriletes divulgatus Chlon., Rouseisporites Spinidinium sp., Altertia sp., A. daveyi (Stover et reticulatus, Taurocusporites reduncus (Bolch.) Evitt) Lentin et Williams, ?Deflandria magna Stov., pollen Ginkgocycadophytus, Glyptostrobus Davey., and cf. Kallsphaeridium circulare (Cook- sp., Taxodiaceae, Cedrus spp., Araucariacites pex- son et Eisenack) Helby; microphytofossils: Pter- us, Podocarpidites spp., Pseudopicea sp., Piceapol- ospermella sp., cf. Veryhachius reductus, Botriocco- lenites spp., Pinus aralica, Sciadopityspollenites cus sp., Aletes striatus, and Ovoidites sp. Upper Campanian–Maastrichtian. Abun- multiverrucosus, Classopollis, Alisporites sp., and Phyllocladidites spp., typical dinocysts Chlami- dant spores (up to 54.6%), the subdominant: di- dophorella nyei Cook. et Eis., and Chatangiella nocysts (up to 16.1%); many Polypodisporites sp. spp., Angiosperms (5.7%): Proteacidites sp., Ilex (up to 9.4%), Leiotriletes sрр. (up to 7.2%), Glei- sp., Corylopsis sp., Ericaceae, Inaperturepollenites cheniidites senonicus (up to 6.5%), Phyllocladidites sp., and Gotanipollis sp. spp., Piceapollenites sp., Chatangiella spp. (6.5%), Santonian–Campanian. Abundant spores Gothanipollis sp. (up to 7.2%). Related: Pi- (up to 56.2%); the subdominant: dinocysts (up to lasporites marcidus, Sphagnum spр., Cyathidites 17.3%); many Polypodisporites sp. (up to 6.0%), spp., Foveosporites cenomanicus, Concavisporites Leiotriletes spр., Gleicheniidites laeta Bolch. (up to juriensis, Hymenozonotriletes bicycla (Mal.) Sach. 6.0%), G. senonicus Ross. (up to 6.0%), Disaccites ex Fradk., Salviniaceae, Densoisporites velatus, (up to 5.2%), Phyllocladidites spp. Related: Camptotriletes sрр., Gleicheniidites spр., Appen- Clavifera rudius Bolch., Pilasporites marcidus Bal- dicisporites sрp., Cicatricosisporites spp., Lygodi- me, Sphagnum spp., Stereisporites psilatus (Ross.) umsporites spp., Stenozonotriletes divulgatus, Pfl., S. regium Drozh., Lycopodiumsporites spp., Foraminisporites daijli, Rouseisporites reticulatus, Cyathidites spp., Ruminatisporites sp. (0.2%), Ste- Taurocusporites reduncus, pollen Ginkgocycadophy- nozonotriletes radiatus Chlon., Foveosporites ceno- tus, Glyptostrobus, Taxodiaceae, Sequoia sp., manicus, Pteridaceae, Dictyophyllidites sp., Dip- Cedrus spр., Podocarpidites spр., Piceapollenites teridaceae, Clathropteris obovate var. magna Tur.- spp., Abies sp., Pinuspollenites spр., Sciadopit- Ket., Obtusisporites junctus (K.-M.) Pocock., Tri- yspollenites multiverrucosus, Classopollis, partina variabilis Mal., Concavisporites juriensis Alisporites sрp., Eucommiidites troedssonii, Piceites Balme, Densoisporites velatus, Camptotriletes ambi- sp., Vitreisporites pallidus (Reis.) Nils., and Disac- gens, Osmundacidites spp., Appendicisporites spp., Cicatricosisporites spp., Lygodiumsporites spp., cites. Typical angiosperms: Gnetaceapollenites sp., Stenozonotriletes divulgatus, Leptolepidites spp., Ilex sp., Quercus sp., Myrica sp., Ericaceae, Tricol- Foraminisporites daijli, F. asymmetricus, pites sp., Aquilapollenites sp., and Tetraporina sp.; Rouseisporites reticulatus Poc., Ginkgocycadophy- dinocysts: Chlonoviella agapica, Isabilidinium spp., tus, Cycadopites dilucidus, Glyptostrobus, Taxodi- Spinidinium echinoideum (Cook.et Eis.) Lentin et aceae, Cedrus spp. (4.2%), Araucariacites pexus, Wil., Alterbidinium acutulum (Wilson) Lentin, De- Podocarpidites spp., Quadraecullina limbata Mal., conodinium sрp., ?Deflandria magna, and Framea Pinuspollenites spp., P. aralica Bolch., Sciadopit- sp.; prasinophyte Pterospermella sp.

Fig. 2. The subdivision of the Cretaceous deposits in the Yakovlevskaya-2 borehole based on palynological data.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Upper Maastrichtian. Abundant spores (up sрp., Vitreisporites pallidus, and Disaccites. Typi- to 55.5%); the subdominant: dinocysts (up to cal angiosperms: Aquilapollenites sp., Triprojectus 15,8%); many Laevigataesporites ovatus (up to sp., Platanus sp., Ericaceae, Gothanipollis sp., 9.4%), Leiotriletes spр., Gleicheniidites senonicus, Hamamelidaceae, Kryshtofoviana jacutense Piceapollenites sp., Phyllocladidites spp. Related: Samoil., and Tetraporina sp.; dinocysts: Mem- Sphagnum sрp., Lycopodiumsporites sрp., Cy- branosphaerama astrichtica Samoil., Chatangiella athidites sрp., Foveosporites cenomanicus, Pterida- sрp., Amphydiadema sp., Spinidinium ornatum ceae, Auritulina sp., Camptotriletes ambigens, Os- (May) Lentin et Williams, Alterbidinium acutu- mundacidites sp., Selaginella sрp., Gleicheniidites lum, and Laciniadinium arcticum (Manum) Lentin spр., Appendicisporites sp., Cicatricosisporites sp., et Williams; green algae Palambages sp. Lygodiumsporites spр., Rouseisporites reticulatus, Analysis of abundant palyonological data Ginkgocycadophytus, Taxodiaceae, Cedrus sрp., revealed a high share of various species of dino- Araucariacites pexus, Podocarpidites sрp., Abies sp., cysts that indicates a marine condition of accu- Sciadopityspollenites multiverrucosus, Alisporites mulation of the Late Cretaceous sediments.

References

Bochkarev, V.S. (Ed.), 1981. Regional stratigraphic scales of the Mesozoic deposits of West Siberia. charts of the Mesozoic and Cenozoic sediments SNIIGGiMS, Novosibirsk (in Russian). of the West Siberian Plain. ZapSibNIGNI, Tyu- Ilyina, V.I., Kul’kova, I.A., Lebedeva, N.K., 1994. Mi- men’ (in Russian). crophytofossils and detail stratigraphy of marine Bondarenko, N.M., 2001. Early Cretaceous spores of Mesozoic and Cenozoic of Siberia. UIGGM SB Schizeaceae ferns in the core of Yakovlevskaya 1- RAS, Novosibirsk (in Russian). P borehole (the north part of Ust-Yenisei region), Nikitenko, B.L., Shurygin, B.N., Knyazev, V.G., in: Biostratigraphy of Mesozoic and Cenozoic in Meledina, S.V., Dzyuba, O.S., Lebedeva, N.K., some regions of the Arctic and the oceans. VNII- Peshchevitskaya, E.B., Glinskikh, L.A., Oceangeologia, St. Petersburg, pp. 34–52 (in Rus- Goryacheva, A.A., Khafaeva, S.N., 2013. Jurassic sian). and Cretaceous stratigraphy of the Anabar area Gurari, F.G. (Ed.), 2004. A decision of the 6th Interde- (Arctic Siberia, Laptev Sea coast) and the Boreal partmental stratigraphic meeting on considera- zonal standard. Russian Geology and Geophys- tion and arrival of the improved stratigraphic ics 54, 808–837.

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Conifer fossils from the Lower Cretaceous of Inner Mongolia, North China and their geologic significance

B.N. Sun, X.H. Xu, D.F. Yan and P.H. Jin

School of Earth Sciences, Lanzhou University, South Tianshui Road 222, Lanzhou 730000, China; e-mail: [email protected]

Some conifer fossils collected from the Basin, Inner Mongolia, northern China, based on Lower Cretaceous of the Huolinhe and Guyang an excellently preserved leafy branch with at- Basins (Inner Mongolia, North China) are de- tached leaves and seed-bearing structures. Three scribed. These fossils are three Schizolepis spe- ovules can be found on the leafy branch. It is the cies, S. longipetiolus Xu X.H. et Sun B.N., S. cf. first fossil record of Taxus in Guyang Basin, Chi- heilongjiangensis Zheng et Zhang and na. The species has been compared with living S. neimengensis Deng, and one Taxus species, and other previously published fossil species of T. guyangensis Xu X.H et Sun B.N. Taxus. The present fossil evidence also appears Schizolepis longipetiolus is a well-preserved to suggest that the multi-ovulate shoots of extant female cone, slender and cylindrical in shape. Taxus are probably not the result of plant evolu- The seed-scale complexes have long petioles and tion or the gene mutation. Otherwise, a warm are arranged on the cone axis loosely and heli- and humid climate is indicated in the Guyang cally. The seed scales are divided into two lobes Basin during the late Early Cretaceous on the from the base. The seed is borne on the adaxial basis of the fossil remains and lithology. Fur- surface at the base or middle of each lobe. thermore, majority living Taxus species are dis- Schizolepis was established in 1847. Although tributed in tropical-subtropical regions of the more than twenty species have been discovered Northern Hemisphere, and the leaf cuticle of and reported, its phylogenetic position is con- T. guyangensis is too thin to separate that maybe troversial because of the imperfection of fossils. suggest a moist environment. The present result indicates that the genus prob- ably has a distant evolutionary relationship with Acknowledgments extant Pinaceae. In the Early Cretaceous most This research is supported by the National species existed in China’s three northeastern Basic Research Program of China (973 Program) provinces and the Inner Mongolia Autonomous (no. 2012CB822003), the Specialized Research Fund Region and adjacent areas. Combining the for the Doctoral Program of Higher Education paleogeographic distribution of the genus with (no. 20120211110022), the National Natural Science ancient climatic factors, authors deduced that Foundation of China (no. 41172022) and the Funda- Schizolepis began to decline and became extinct mental Research Funds for the Central Universities in the Early Cretaceous, and the reason for its (no. lzujbky-2015-201). extinction is closely related to the icehouse cli- mate during the Early Cretaceous. Keywords Taxus guyangensis Xu X.H et Sun B.N is de- Schizolepis, Taxus, Early Cretaceous, paleoclimat- scribed from the Lower Cretaceous of Guyang ic significance, China.

References

Bobrov, A.V.F.Ch., Melkian, A.P., Mikhail, S., Roma- Deforce, K., Bastiaens, J., 2007. The Holocene history nov, S., Sorokin, A.N., 2004. Seed morphology of Taxus baccata (Yew) in Belgium and neigh- and anatomy of Austrotaxus spicata (Taxaceae) bouring regions. Belg. J. Bot. 140 (2), 222–237. and its systematic position. Bot. J. Linn. Soc. 145, Hao, D.C., Xiao, P.G., Huang, B.L., Ge, G.B., Yang, L., 437–443. 2008a. Interspecific relationships and origins of Chang, S.C., Zhang, H.C., Renne, P.R., Fang, Y., 2009. Taxaceae and Cephalotaxaceae revealed by parti- High-precision 40Ar/39Ar age for the Jehol biota. tioned Bayesian analyses of chloroplast and nu- Palaeogeogr. Palaeoclimatol. Palaeoecol. 280, 90– clear DNA sequences. Plant Syst. Evol. 276, 89– 104. 104.

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Hao, D.C., Huang, B.L., Yang, L., 2008b. Phylogenetic berculata; Mammalia) genera from the Lower relationships of the genus Taxus inferred from Cretaceous Shahai and Fuxin formations, chloroplast intergenic spacer and nuclear coding northeastern China. J. Vert. Paleontol. 29, 1264– DNA. Biol. Pharm. Bull. 31(2), 260–265. 1288. Kusuhashi, N., Hu, Y.M., Wang, Y.Q., Hirasawa, S., Zhang, J., D'Rozario, A., Yao, J., Wu, Z., Wang L., 2011. Matsuoka, H., 2009a. New triconodontids A new species of the extinct genus Schizolepis (Mammalia) from the Lower Cretaceous Shahai from the Jurassic Daohugou Flora, Innner Men- and Fuxin formations, northeastern China. Geo- bios 42, 765–781. golia, China with special reference to the fossil Kusuhashi, N., Hu, Y.M., Wang, Y.Q., Setoguchi, T., diversity and evolutionary implications. Acta Matsuoka, H., 2009b. Two eobaatarid (Multitu- Geol. Sin., Engl. Ed. 85(2), 471–481.

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

First flowering plants in Primorye region (Russia)

E.B. Volynets1, E.V. Bugdaeva1, V.S. Markevich1 and T.A. Kovaleva1,2,3

1Institute of Biology and Soil Science, Far Eastern Branch of RAS, pr. 100-letiya 159, Vladivostok 690022, Russia; e-mail: [email protected] 2Research Center of Paleontology & Stratigraphy, Jilin University, Changchun 130026, China 3Key Lab of Past Life & Environment in NE Asia, MOE, Changchun 130026, China

The interaction between biotic and abiotic Albian flora was taxonomically most diverse in- processes during the Cretaceous was best pro- cluding subtropical elements. At the Early–Late nounced in Primorye region located at the Cretaceous boundary, the significant geological boundary of temperate and subtropical zones. events (a lull in volcanic activity of the Sikhote- The mid-Cretaceous deposits here are widely Alin volcanic belt, a change in nature of sedi- distributed in the Alchan River, Partizansk and mentation) and climatic changes (climate be- Razdolnaya River basins. Their sedimentary se- came warmer and more humid) occurred. quences were formed under different condi- The events that occurred in both marine tions. In the eastern part of this area, since the and continental ecosystems are believed to be Aptian time the largest sea transgression began. synchronous and are considered as reflecting Marine biota was of the Tethyan type. In North- climatic evolution and tectogenesis. West Pacific region, the first Ocean Anoxic Flowering plants in the geological record of Event (OAE1), which was recorded both in the Primorye region first appeared in the Aptian of ocean and epicontinental basins, occurred in the the Razdolnaya River Basin. The angiosperm Aptian–Albian time. The beginning of the Albi- remains are almost entirely restricted to sand- an was marked by maximum transgression. The stone or sandy beds with cross-bedding or cross- lamination, or light-gray mudstone beds repre- predominant biota of epicontinental basins was senting weathered volcanic ash. In contrast, only represented by bivalves (Aucella and Inoceramus) conifer, cycadophyte and fern remains are found and ammonites typical of North-Pacific Prov- in equivalent finer-grained, parallel-bedded ince. The sediments of Alchan River, Partizansk units. It is possible to recover their remains from and southern part of Razdolnaya River basins tuffaceous mudstone, because that ash fall cov- accumulated under influence of sea; the north- ered all area of basin. The environmental inter- ern part of the latter was developed as intracon- pretation of these deposits can evidence about tinental basin. the early angiosperm ecology. These plants ap- Any variation in deposition and climatic parently colonized disturbed surfaces of the conditions resulted in abrupt changes in the tax- land such as riparian settings or place of accu- onomic composition of fossil floras. The Aptian mulations of fallen volcanic ash. fossil flora of the Primorye region was character- Most recently, we have found new remains ized by high diversity, considerable share of of the flowering plants in the Late Aptian (prob- thermophilic elements, and maximum values of ably, Late Aptian–Early Albian) deposits in the cycadophyte index suggesting obvious trend to Razdolnaya River Basin, belonging to the Lipov- increase in temperature. Since the Early Albian a tsy Formation (Bugdaeva et al., 2014; Kovaleva volcanic activity within this region gradually in- et al., 2016). The earliest angiosperms of Pri- creased, being maximum in the mid-early Late morye region are represented by leaves of Dicot- Albian. At this time, the sea regression and ex- ylophyllum sp. (Podgorodnenka coal field – Sokol pansion of continental environments were rec- Bay, nearly Vladivostok City) and by dispersed orded. The vegetation typical of humid climate cuticle of indeterminable platanoids (Porechye deteriorated. The diversity of terrestrial floras coal mine and nearly Dongning City, China). decreased; the number of thermophilic elements The extremely rare Aptian angiosperm leaves dropped, and values of cycadophyte index re- are generally small, have disorganized venation, duced. Intensification in a volcanic activity and are largely restricted to sandy and coaly caused the formation of specific floras. The Late stream margin lithofacies.

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Throughout the Aptian and probably Lower Platanifolia were added to them in the Albian. Albian corresponding to the Lipovtsy Formation, Morphotype Nymphaefolia appears in the palynoflora consists almost entirely of pterido- Cenomanian, the importance of Platanifolia in- phyte spores and gymnosperm pollen. In other creases (Volynets, 2005). localities of the Lipovtsy Formation, such as There is an opinion that the early flowering Porechye mine and outcrop nearly Dongning plants were “weeds”. This fact was supported City, the Dongning Formation, the Chinese part by findings of angiosperms in the Partizansk of the Razdolnaya River Basin, the upper part of (Krassilov and Volynets, 2008) and Alchan River the Staryi Sutschan Formation of the Partizansk (Bugdaeva et al., 2006; Volynets, 2005) basins. Coal Basin, tricolpate, tricolporoidate, and mono- V.A. Krassilov and E.B. Volynets (2008) de- sulcate pollen grains of recognizably angiosper- scribed a new plants Achaenocarpites capitellatus mous affinities occur. The earliest angiosperm and Ternaricarpites floribundus (morphotype Ra- pollen is represented by Clavatipollenites hughesii nunculifolia) from the Late Albian of Primorye. Coup., Tricolpites micromunus (Groot. et Penny) These plants composed the pioneer communities Singh, T. vulgaris (Pierce) Sriv., T. variabilis Burg., colonizing a surface of volcanic ash. Tricolpites spp., Quercites sparsus (Mart.) Samoil., An important aspect of our study has been Retitricolpites vulgaris Pierce, R. georgiensis Brenn., an attempt to draw inferences on the paleoecol- and Fraxiniopollenites variabilis Stanl. in Razdolna- ogy of early angiosperms from the types of sed- ya River Basin. Asteropollis asteroides Hedl et Nor- iment in which their remains are preserved. ris and Cyclusphaera psilata Volkh. et Sepul. were Depositional settings for sedimentary sequences found in Partizansk Coal Basin. containing the first flowering plants included It may be noted that there is co-occurrence river valleys and area after volcanic ash falls. of the above-mentioned morphotypes, although The appearance, invasion and wide spread of in the Potomac Group of North America mono- these plants in the plant communities took place sulcates appear earlier and were described as during the deterioration of climatic and envi- older pollen types (Hickey and Doyle, 1977). ronmental conditions. They include small, finely columellar grains Morphological, stratigraphic, and sedimen- with granular sulcus membranes (Clavatipol- tological analyses of the Early Cretaceous pollen lenites hughesii). and leaf sequences from Alchan River, Parti- We did not reveal megafossils of flowering zansk and Razdolnaya River basins of Primorye plants in the Aptian of the Alchan River and region show an approximate scheme of the Partizansk basins. The sediments of this age ac- adaptive radiation of the early angiosperms and cumulated in environments of seaside plains suggest the ways of their initial ecological and under marine influence. systematic diversification. During the Albian, the thermophilic bennet- titaleans lose their importance and vacate eco- Acknowledgements logical niches in the brushwood and under a This work was partly supported by the grant of canopy of coniferous forests; these niches were the President of the Russian Federation for state sup- actively colonized by angiosperms. The Albian port of young Russian candidates of sciences (project palynofloras in the Alchan and Partizansk River no. MK-2993.2015.4), the Russian Foundation for basins contain rapidly diversifying tricolpate Basic Research (grant no. 16-04-01411), the Project 111 pollen and several new assemblages of locally of China and the Project 2015FY310100-15 of the MST, abundant angiosperm leaves. China. The authors are grateful to the late In the Cenomanian the flowering plants V.A. Krassilov (Haifa University, Israel), N.P. Domra dominate in the plant communities of and N.N. Naryshkina (Institute of Biology and Soil Science, Far East Branch, Russian Academy of Scienc- Razdolnaya River, Alchan River, and Partizansk es), V.V. Golozubov, V.P. Nechaev (Far East Geologi- River basins. Aquatic plants Potamogeton, cal Institute, Far East Branch, Russian Academy of Quereuxia, and Cobbania appeared in the Alchan Sciences). Special thanks to Chinese colleagues Prof. River Basin. G. Sun, F. Liang, C.T. Li, F. Chen, P. Yu, Y.G. Yang The first morphotypes of dicot leaves were and Y. Xu from Jilin and Shenyang Normal Universi- Laurifolia and Rosifolia. Ranunculifolia and ties, and S.L. Hai (Geological Museum of Hei-

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific longjiang, China) who helped to collect paleobotani- B. Shurygin and Prof. Hisao Ando for support of our cal material nearly Dongning City. The authors thank participation in the 4th International Symposium of leaders of IGCP608, corresponding member of RAS IGCP608.

References

Bugdaeva, E.V., Markevich, V.S., Volynets, E.B., Ko- Hickey, L.J., Doyle, J.A., 1977. Early Cretaceous fossil valeva, T.A., Nechaev, V.P., 2014. The Early Creta- evidence for angiosperm evolution. Bot. Rev. ceous coal-forming plants from the Razdolnaya 43(1), 3–104. Basin (Southern Primorye), in: Baraboshkin, E.Yu., Kovaleva, T.A., Markevich, V.S., Bugdaeva, E.V., Vol- et al. (Eds.), Cretaceous System of Russia and the ynets, E.B., Afonin, M.A., 2016. New data on near abroad: problems of stratigraphy and paleo- palynostratigraphy of the Lipovtsy Formation in geography. Proc. Seventh Russian scientific con- the Razdol’naya Coal Basin (Southern Primorye). ference with international participation. Dalnau- Russ. J. Pac. Geol. 10(1), 50–62. ka, Vladivostok, pp. 70–71 (in Russian). Krassilov, V.A., Volynets, E.B., 2008. Weedy Albian Bugdaeva, E.V., Volynets, E.B., Golozubov, V.V., angiosperms. Acta Palaeobotanica 48(2), 151–169. Markevich, V.S., Amelchenko, G.L., 2006. Flora Volynets, E.B., 2005. The Aptian–Cenomanian Flora of and geological events of the mid-Cretaceous time (Alchan River Basin, Primorye). Dalnauka, Primorye, Part 1: Floral Assemblages. Stratigr. Vladivostok. Geol. Correl. 13(5), 613–631.

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Session 2 Cretaceous paleogeography and paleobiogeography

Late Cretaceous paleobiogeography of peninsular India: An overview of constraints from fossil tetrapods

S. Bajpai

Birbal Sahni Institute of Palaeosciences, Lucknow 226007, India; e-mail: [email protected]

A Late Cretaceous phase of the geodynamic (Maastrichtian) has opened up several hotly de- history of the peninsular India is marked by two bated paleobiogeographic issues. Possible ex- major tectonic events, the break-up of India- planations involving filter bridges connecting Seychelles block from Madagascar at ~88 Ma Africa, Antarctica, Indo-Madagascar, South and the Deccan flood basalt volcanism and sepa- America at different times (Chatterjee et al., ration of India from Seychelles around 65 Ma. 2013) need to be reconciled with the geological Both dispersal and vicariance shaped the paleo- and geophysical evidence. biogeographic patterns in time and space during A number of hypothesized ephemeral biotic India’s rapid northward drift in the Late Creta- filter bridges connecting India with other ceous. As the Indian plate separated from Mad- Gondwana landmasses need a serious consider- agascar, it became a continental island initially, ation: i) the Kohistan-Ladakh–Oman Arc that al- resulting in increased opportunities for allopat- lowed faunal interchanges between India and ric speciation and biodiversity peaks. northern Africa during the Late Cretaceous, The tetrapod record, including dinosaurs ii) the Laxmi Ridge–Seychelles Island that and mammals, from horizons postdating Indo- bridged the gap between India and Madagascar, Madagascar rifting is yet to be discovered in In- and iii) the emergent Ninetyeast Ridge– dia. However, the common presence of several Kerguelen Plateau–Antarctica that formed a cir- family-level taxa in India, Madagascar and cumpolar biotic filter bridge between India and South America during the latest Cretaceous South America.

References

Chatterjee, S., Goswami, A., Scotese, C.R., 2013. The northward flight from Gondwana to Asia. longest voyage: tectonic, magmatic, and paleo- Gondwana Res. 23, 238–267. climatic evolution of the Indian plate during its

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Terminal Maastrichtian–Danian marine incursion in Central India: Myth or Reality?

S.A. Jafar1,2

1National Centre for Antarctic and Ocean Research, Headland Sada, Vasco-da-Gama, Goa 403804, India 2Flat 5-B, Whispering Meadows, Haralur Road, Bangalore 560102, India e-mail: [email protected]

Wisdom and intellectual integrity is the Late Cretaceous as the sea level rose up to 200 m backbone of reliable knowledge built on a varie- higher than today, but surprisingly, none of the ty of meticulously collected empirical and testa- lineaments on the east and west of India re- ble data (Mario, 2013). It is instructive to be ceived any deep incursion of sea, with notable aware of distinct rifting events which carved the and unique exception of Narmada Valley. Crea- outline of India out of the supercontinent Pan- tion of new rifts, record speed with which India gaea for understanding the possible nature of approached Eurasian continent coupled with lo- exceptionally deep incursion of sea during the cal Large Igneous Province episodes led to the Maastrichtian–Danian. deep flooding of continents by warm marine Extensive volcanism in East Africa, Antarc- waters. Réunion hotspot induced eruption of tica and Madagascar coupled with rifting of massive Deccan Flood Basalt sub-aerial Large Madagascar–Seychelles–India–Australia–New Igneous Province (LIP at ca. 66 Ma) during the Zealand–Antarctica combined continent from terminal Cretaceous covering over 500.000 sq. continents of Africa–South America led to the km area of India and attracted world attention creation of Proto-Indian Ocean during the Early for exceptionally well preserved fossil fauna and Jurassic (ca. 185 Ma). Significant Early Creta- flora in intertrappean lacustrine sediments ceous (ca. 145 Ma) rifting and subsequent straddling Cretaceous–Palaeogene boundary. Rajmahal volcanism carved Eastern Indian No concrete evidence of deep sea incursion is Ocean with prominent aulacogens and triple forthcoming during this time slice either via junctions at marginal basins of Cauvery, Palar, Narmada valley or Krishna-Godavari lineament, Krishna-Godavari and Mahanadi. India overly- except in the northern collision facing East-West ing solid marine crustal support, tilted eastward trending Subathu-Dogadda lineament now des- causing easterly flow of rivers except Narmada ignated as Lesser Himalaya (Jafar and Singh, and Tapti which continue to flow today west- 1992). After colliding with Eurasian continent ward. It is noteworthy that during this time (ca. 50 Ma) the northern portion of India (Great- Madagascar reached current position relative to er India) started subducting giving rise to raised Africa and India–Madagascar separated from Tibetan Plateau (Fig. 1). Antarctica–Australia–New Zealand and none of The Tethys finally closed after displaying the lineaments permitted any deep incursion of last signs of marine waters in Lesser Himalaya the sea. in the Early Miocene. As juvenile Indian Ocean continued to grow, rifting separated Australia–New Zealand Deep incursion of sea along Narmada Valley from Antarctica (ca. 105 Ma). One of the most Contrary to the earlier assumption of some dramatic plate tectonic event was the rifting workers (Keller et al., 2009; Keller, 2014), it is causing separation of India–Seychelles from noteworthy that during K/T transition time there Madagascar, episode of sub-aerial Large Igne- was absolutely no marine incursion as evi- ous Province (LIP at ca. 92 Ma), the Mahajanga denced by the following observations: (1) K/T Flood Basalt of Madagascar possibly inducing transition marine sediments are missing from concomitant Late Turonian deep incursion of sea the western margin of India; (2) critical evalua- (>800 Km) along Narmada Valley into central tion of various fossil records suggests an age not India (Jafar, 2015). Shallow seas generally inun- older or younger than Late Turonian for ma- dated most continents of the world during the rine/estuarine sediment package in the Lower

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Fig. 1. K/T boundary palaeogeographic map showing rapid northward and anticlockwise movement of Indian block which received significant deep marine incursion from the East along Subathu-Dogadda lineament before colliding with Eurasian continent in the Late Ypresian (ca. 50 Ma).

Narmada Valley, comprising of Nimar Sandstone recently reported from the Kakra section (dinosaur bearing, fully marine) – Bagh Beds – (Thakur et al., 2013), but Maastrichtian–Danian Nodular Limestone – Coralline Limestone, in as- global calcareous nannofossils were detected as cending order. In Upper Narmada Valley, well tectonically sandwiched within Precambrian known Lameta beds of Maastrichtian age (dino- Krols and frequently detected as reworked in saur bearing) signify predominant deposition the Early Eocene Subathu Formation (Jafar, under sub-aerial conditions, despite several spu- 2013), signifying unroofing and collision event rious counter claims of marine origin. of India against Eurasia (Late Ypresian ca. 50 Ma). Noteworthy is the complete absence of Deep incursion of sea along Krishna-Godavari marine siliceous plankton and extremely scarce Valley Cretaceous megafossils. K/T transition marine sediments are devel- oped all along eastern margin of India but nota- So, what is the most plausible postulate? bly with intertrappean beds of Rajahmundry ar- Envisage a large ephemeral Athalassic sa- ea. Based on the presence of certain fossil line Lake (Deckker, 1981) which had all geo- mangrove / coastal elements like Nypa, Cocos morphic features of a miniature sea and in con- and Acrostichum etc. in several intertrappean trast with “brackish” waters, was not sections, it was postulated some 150 years ago contiguous with sea water. It would not be en- that deep sea incursion could have occurred via tirely misleading to assume that some kind of Krishna-Godavari Valley. More recently, dis- seeding mechanism including contamination by covery of a thin horizon (ca. 60 cm) yielding di- wind and birds (Palaeocene records of birds are minutive sized planktonic foraminifera of Dani- known from major continents except India) pre- an age in Jhilmili intertrappean area also led to vailed and coastal / mangrove elements includ- rather strange speculation of the deep entry of ing ostracods and planktonic foraminifera could short lived sea via Narmada or Krishna- be transported to “adapt” and flourish for a Godavari valley (Keller, 2014). short spell. Similar occurrence of varied marine elements (Xi et al., 2011; Boonstra et al., 2015) Deep incursion of sea along Subathu-Dogadda deep into the heart of continents is reported Lineament from several regions but has not been interpret- Autochthonous Late Maastrichtian–?Danian ed without a flaw. We need a complete biotope marine sediments based on dinoflagellates are and sedimentary facies link up to strongly sup-

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific port full-fledged deep sea incursion like the one strophic events like Deccan volcanism or Chicx- seen along Narmada Valley during the Late Tu- ulub Impact had anything to do with mass ex- ronian. Also, it is absurd to assume that cata- tinction at the K/T boundary (Jafar, 2014).

References

Boonstra, M., Ramos, M.I.F., Lammertsma, E.I., An- Subathu Formation, Shimla Himalaya, India. toine, P.-O., Hoorn, C., 2015. Marine connections Curr. Sci. 62(5), 409–413. of Amazonia: Evidence from foraminifera and Keller, G., 2014. Deccan volcanism, the Chicxulub im- dinoflagellate cysts (early to middle Miocene, pact, and the end-Cretaceous mass extinction: Colombia/Peru). Palaeogeogr. Palaeoclimatol. Coincidence? Cause and effect? Geol. Soc. Am. Palaeoecol. 417, 176–194. Spec. Pap. 505, 57–89. Deckker, P.D., 1981. Ostracods of athalassic saline Keller, G., Adatte, T., Bajpai, S., Mohabey, D.M., lakes. Hydrobiol. 81, 131–144. Widdowson, M., Khosla, A., Sharma, R., Khosla, Jafar, S.A., 2013. Unfinished Symphony in Lesser S.C., Gertsch, B., Fleitmann, D., Sahni, A., 2009. Himalaya: Calcareous nannofossils strive to fill the gaps, in: XXIV Indian Colloq. Micropal. K–T transition in Deccan Traps of central India Stratigr. Dehradun, India. Dehradun, pp. 39–41. marks major marine Seaway across India. Earth Jafar, S.A., 2014. Dynamics of Terminal Cretaceous Planet. Sci. Lett. 282, 10–23. global biotic turnover, in: 2nd Int. Symp. IGCP608 Mario, L., 2013. Brilliant Blunders. Simon and Schus- “Land-Ocean Linkages and Biotic Evolution dur- ter, New York. ing the Cretaceous: Contribution from Asia and Thakur, O.P., Sarkar, S., Dogra, N.N., 2013. A Late Western Pacific”, Waseda, Japan: Abstract vol- Maastrichtian palynofloral assemblage from Na- ume. Tokyo, pp. 87–90. han area of the Himachal Pradesh, India: Palaeo- Jafar, S.A., 2015. Episodes of subaerial Large Igneous environmental and age implications. Himalayan Provinces (LIPs) linked to late Turonian/Late Geol. 34(2), 148–157. Maastrichtian deep incursions of Sea on Indian Xi, D.P., Wan, X.Q., Feng, Z.Q., Li, S., Feng, Z.H., Jia, continental block, in: Zhang, Y., Wu, S.Z., Sun, G. (Eds.), Abstracts of the 12th Symposium on Mes- J.Z., Jing, X., Si, W.M., 2011. Discovery of Late ozoic Terrestrial Ecosystems, Shenyang, China. Cretaceous foraminifera in the Songliao Basin: Shenyang, pp. 37–39. Evidence from SK-1 and implications for identi- Jafar, S.A., Singh, O.P., 1992. K/T boundary species fying seawater incursions. Chinese Sci. Bull. with early Eocene nannofossils discovered from 56(3), 253–256.

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The discovery of the CORB in the Southern Tethyan Himalaya and its paleogeographic implication

G.B. Li1, Z.C. Han1,2, X.F. Li1, X.L. Niu1, T.Y. Wang1, Y. Han1, Y.J. Yao1, B.B. Lv1 and W.Y. Zhang1

1China University of Geosciences, Beijing 100083, China; e-mail: [email protected] 2Shandong Geological Engineering Group Co., Ltd., Shandong Ji'nan 250200, China

The Cretaceous oceanic red beds (CORB) ⑤ Radotruncana calcarata Zone (Kj109–129), and are widespread in the Northern Tethyan Hima- ⑥ Globotruncanella havanensis Zone (Kj130–134). laya (NTH) but never reported in the Southern The planktic foraminiferal assemblage provides Tethyan Himalaya (STH). In this study, red beds a Late Cretaceous age for the Gambacunkou and (CORB, composed of 5 m thick cherry-red thin- Zongshan formations and an early Late Campa- bedded marl) are firstly discovery from the Up- nian age for the CORB (corresponding to the per Cretaceous of the Jinshansibei section, Tüna, upper R. calcarata Zone) in the Jinsangsibei sec- Yadong, STH. The litho- and biostratigraphy of tion. upper Gambacunkou Formation and lower In contrast to those in NTH, the CORB in Zongshan Formation (containing the CORB) of STH is characterized by monotonous cherry-red the Jinsangsibei section were investigated. Mi- marl with smaller thickness and shorter age. The cropaleontologic study of the strata led to the discovery of the CORB in STH challenges the discovery of abundant planktic foraminifers in previous view that the CORB in the Tethyan marl, limestone and shale. The foraminifer Himalaya should be restricted to the NTH (slope preservation is mostly satisfactory, and sixty- to basin) and entirely miss in STH (shelf). This seven species from 22 genera were identified. discovery contributes to the paleogeographic in- These allow recognition of six planktic forami- terpretation of the CORBs in southern Tibet and niferal zones: ① Dicarinella concavata Zone (Kj1– the Tethyan Himalaya. 6), ② Dicarinella asymetrica Zone (Kj7–44), Keywords ③ Globotruncanita elevata Zone (Kj45–60), CORB, planktic foraminifera, palaeogeography, ④ Globotruncana ventricosa Zone (Kj61–108), Late Cretaceous, Southern Tethyan Himalaya.

References Li, G.B., Jiang, G.Q., Hu, X.M., Wan, X.Q., 2009a. New its paleogeographic implication. Palaeogeogr. biostratigraphic data from the Cretaceous Palaeoclimatol. Palaeoecol. 312(1–2), 127–137. Bolinxiala Formationin Zanda, southwestern Ti- Li, G.B., Jiang, G.Q., Wan, X.Q., 2011b. The age of the bet of China, and their paleogeographic and Chuangde Formation in Kangmar, southern Ti- paleoceanographic implications. Cretaceous Res. bet of China: Implications for the origin of Creta- 30(4), 1005–1018. ceous oceanic red beds (CORBs) in the northern Li, G.B., Xie, D., Wan, X.Q., Han, H.D., Chen, P.L., Tethyan Himalaya. Sediment. Geol. 235(1–2), 2009b. Discovery of Radiolaria from the 111–121. Zongzhuo Formation in Tianba, Kangmar and its age implication. Acta Geol. Sin. 83(5), 853–859. Li, G.B., Wan, X.Q., Pan, M., 2011c. Planktic forami- Li, G.B., Jansa, L., Wan, X.Q., Pan, M., Xiu, D., Xie, D., niferal biostratigraphy of the Cretaceous oceanic 2011a. Discovery of radiolaria from Upper Creta- red beds in Kangmar, Southern Tibet, China. Ac- ceous Oceanic Red Beds in Daba, Kangmar and ta Geol. Sin. 85(6), 1238–1253.

Fig. 1. Correlation of the Gambacunkou and Zongshan formations at Jiansangsibei, Yadong (14) to late Early–Late Cretaceous successions in (1) Itchu La, northern Zanskar (Fuchs, 1982); (3) Chikkim, Spiti (Bertle and Suttner, 2005); (4) Bolin, Zanda (Li et al., 2009a); (11) Tianba, Kangmar (Li et al., 2009a,b, 2011a,b,c); (12) Zongshan, Gamba (Wan, 1985; Wan et al., 2000; Zhao and Wan, 2003; Li et al., 2003); and (10) Jiabula, Gyangze (Zhao and Wan, 2003). Stages and biozones: Al – Albian, Ce – Cenomanian, Tu – Turonian, Co – Coniacian, Sa – Santonian, Ca – Campanian, Ma – Maastrichtian, Tic – Ticinensis Zone, App – Appenninica Zone, Bro – Brotzeni Zone, Rei – Reicheli Zone, Cus – Cushmani Zone, Arc – Archaeocretacea Zone, Hel – Helvetica Zone, Con – Concavata Zone, Asy – Asymetrica Zone, Ele – Elevata Zone, Ven – Ventricosa Zone, Cal – Calcarata Zone, Hav – Havanensis Zone, Aeg – Aegyptiaca Zone, Gan – Gansseri Zone, May – Mayaroensis Zone. 46

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Palaeobiogeographic implications of the late Aptian–Albian polyconitid rudist fauna

J.G. Sha1 and R. Cestari2

1State Key Laboratory of Palaeobiology and Stratigraphy, Nanjing Institute of Geology and Palaeontology, Chinese Academy of Sciences, 39 East Beijing Road, Nanjing 210008, China; e-mail: [email protected] 2STRATA Georesearch, c/o INGEO Dept., G. d'Annunzio University, Via dei Vestini 31, Chieti Scalo 66013, Italy

Rudists are a group of thermophilic shallow Tethys). Assemblages are marked by the pres- water benthic bivalves ranging from the Late Ju- ence of Horiopleura in the Asian north Tethyan rassic to the end of the Maastrichtian and span- margin (northeastern margin of Tethys) (e.g., the ning tropical and subtropical latitudes during Mega-Lhasa intra-oceanic platform) and in the the “Greenhouse” Aptian–Albian interval. They Kohistan–Ladakh (Kohistan-Dras) intra-oceanic were organic builders and sediment constituents volcanic arc. Such different assemblages have of neritic carbonates, and thus they are signifi- indicated two distinct bioprovinces: Mediterra- cant indicators of stratigraphy, palaeogeography nean Province yielding Horiopleura and Poly- and palaeoenvironmental indicators. conites assemblages and South West Asian Prov- The late Aptian–Albian polyconitid rudist ince remarked by the presence of Horiopleura fauna is remarked by Horiopleura (including assemblage (or “Yasin-type” Horiopleura haydeni H. haydeni Douvillé, H. lamberti Hébert, and fauna), without the Polyconites one. H. almerae Paquier) and Polyconites (including Such rudists could have had a very high P. verneuili Coquand, P. hadriani Skelton et al., larval productivity and thus were able to mi- and P. africanus Tavani) that give rise to diverse grate along the continental margins and islands, assemblages with radiolitid rudists, nerineid and drift or passively swim with the ocean cur- gastropods, corals and benthic orbitolinid rents, like the other sessile bivalves, particularly forams. The general external morphology of the cemented thermophilous bivalves including these two taxa is marked by a low cupuloid up- ostreids (Sha, 2003; Sha et al., 2014). The distri- per valve and an umbo projected towards the bution pattern of polyconitid rudist fauna external side in Horiopleura, while in Polyconites (Fig. 2) has implied that larvae dispersal of the the upper valve is flat. The inner features are Late Aptian–Albian rudists were mainly con- marked by the different development of the ec- trolled by the westward Tethys Circumglobal tomyophoral cavity between the two valves and Current (Bush et al., 1997) and by recirculation the arrangement of the cardinal apparatus that is gyres in epicontinental seas such as in the Ban- more developed in Horiopleura (Fig. 1). gong–Nujiang. The influx of cooler boreal wa- This fauna was globally distributed along ters from the Russian engulfment (Fig. 2) were probably a major factor, like a thermal barrier, the margins of Tethys: in the Lhasa terranes, in- separating the European North Tethyan margin cluding Lameila Mt., Ngari area, Nyer Lake, from the Asiatic North Tethyan margin, forming Zabuye Lake, Duba region, east of Xigaze (Tibet, different bioprovinces. The microplates forming China); Kohistan-Ladakh (K-L) volcanic arc, in- the Kohistan–Ladakh or Oman-Kohistan-Dras cluding Yasin (Northern Pakistan), Shukur and arc had separated from Indian Plate and drift in- Khalsi (Northern India); Pontides platform to the tropic (Gibbons et al., 2015) area during (Northern Turkey); Iberia; Ouenza platform the late Aptian–Albian as they are documented (Northern Africa); Apulia; Southeast Arabia by the late Aptian–Albian neritic carbonates (Fig. 2); and even it extended eastwards to the with rudists. Pacific area from the Iberia region via the Hima- layas (Sha and Cestari, 2016). Acknowledgements This work was supported by the “Strategic Prior- However, fossil assemblages with both Ho- ity Research Program (B)” of the Chinese Academy of riopleura and Polyconites were widely distributed Sciences (XDB03010101), and it is a contribution to in the south Tethyan margin, from southern Ibe- UNESCO-IUGS IGCP Project 632. ria to southeast Arabia, and in the European Keywords north Tethyan margin (northwestern margin of Rudists, Early Cretaceous, palaeobiogeography. 48

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Fig. 1. General shell shape and features of Horiopleura and Polyconites rudists: (a) drawing of the transverse section showing the main features of the two valves (modified from Fig. 1 of Skelton et al., 2010); (b) Polyconites hadriani seen from the ventral side (after Skelton et al., 2010: Fig. 5a); (c) P. hadriani postero-ventral view (after Skelton et al., 2010: Fig. 6i); (d) P. hadriani antero-posterior section of the valves (after Skelton et al., 2010: Fig. 5d); (e) Horiopleura haydeni seen from the dorsal side (type no. MPUM 11381 of H. desioi emended to be H. haydeni in Sha and Cestari, 2016); (f) lower valve of H. haydeni cut near the commissure, showing the inner features; (g) transverse section of the upper valve (L ‒ ligamentary ridge, ec ‒ ectomyophoral cavity, pm ‒ posterior myophore, am ‒ anterior myophore); (h) same specimens, upper valve seen from above (after Sha and Cestari, 2016: Fig. 5f‒h). Scale bar equals 2 cm.

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Fig. 2. Configuration of the Tethys Ocean during Indian plate drifting (arrow). The Horiopleura assemblage is com- mon on the northern shore of Tethys while the Polyconites and Horiopleura assemblages are common on the southern shore. The Russian engulfment could act as a thermal barrier. 1 ‒ Lhasa terranes, including Lameila Mt., Ngari area, Nyer Lake, Zabuye Lake, Duba region, east of Xigaze (Tibet, China); 2 ‒ Kohistan–Ladakh (K–L) volcanic arc, includ- ing Yasin (Northern Pakistan), Shukur and Khalsi (Northern India); 3 ‒ Pontides platform; 4 ‒ Iberia; 5 ‒ Ouenza plat- form, Northern Africa; 6 ‒ Apulia; 7 ‒ South-east Arabia. KP ‒ Kerguelen Plateau; B–N ‒ Bangong-Nujiang sea (modi- fied from Aptian base map 120 Ma, Blakey, 2010; © Ron Blakey, Colorado Plateau Geosystems) (after Sha and Cestari, 2016: Fig. 10).

References

Blakey, R.C., 2010. Paleogeographic Maps. Colorado Sha, J., Cestari, R., 2016. Late Aptian–Albian Yasin- Plateau Geosystems. AZ, Phoenix. URL: type rudist assemblage in the Himalayas: pal- http://cpgeosystems.com aeobiogeographic implications. Cretaceous Res. Bush, A.B., George, S., Philander, H., 1997. The late 65, 34–47. Cretaceous: simulation with a coupled atmos- Sha, J.G., Rao, X., Cai, H.W., Pan, Y.H., Wang, Y.Q., phere-ocean general circulation model. 2014. Pan-tropical distribution of the Jurassic os- Paleoceanogr. 12, 495–516. treid bivalves. Palaeoworld 23, 155−161. Gibbons, A.D., Zahirovic, S., Müller, R.D., Whittaker, Skelton, P.W., Gili, E., Bover-Arnal, T., Salas, R., J.M., Yatheesh, V., 2015. A tectonic model recon- Moreno-Bedmar, J.A., 2010. A new species of ciling evidence for the collisions between India, Polyconites from the lower Aptian of Iberia and Eurasia and intra-oceanic arcs of the central- the early evolution of polyconitid rudists. Turk- eastern Tethys. Gondwana Res. 28, 451–492. ish J. Earth Sci. 19, 557‒572. Sha, J., 2003. Plankton and pseudoplankton of the ma- rine Mesozoic bivalves. Acta Palaeontol. Sin. 42, 408–416 (in Chinese with English abstract).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Session 3 Cretaceous climate and environmental changes

Cretaceous paleoenvironments of the Russian Southeast

G.L. Kirillova and S.A. Medvedeva

Kosygin Institute of Tectonics and Geophysics, Far Eastern Branch of RAS, Kim Yu Chen str. 65, Khabarovsk 680000, Russia; e-mail: [email protected]

Attention to the study of the Cretaceous represented by epicontinental seas with rich System does not become weaker both on global benthos where diversified terrigenous material, and regional scales, since the most important generally containing products of terrestrial vol- geological events in the Earth’s history as well as canism, accumulated during the Berriasian to valuable mineral resources are associated with Early Hauterivian. Here epochs of intensive this system. International and All-Russian meet- downwarping repeatedly alternated with uplift- ings are held regularly (Baraboshkin et al., 2014). ing and erosion and continental sedimentation New data on the southeastern Russia and adja- with coal formation. The thickness of the depos- cent territories of China, where Cretaceous rocks its varies from 2000 to 4000 m. of different types are widespread (Fig. 1) are be- Intracontinental rift and postcollisional ba- ing published systematically (Decisions…, 1994; sins, in which continental coal-bearing 1000-m- Likht, 1997; Liu et al., 1997; Markevich et al., thick sediments were deposited during the Ber- 1997; Yarmolyuk et al., 2000; Zhang et al., 2008; riasian–Hauterivian interval (Cao et al., 2013), Cao et al., 2013; Didenko et al., 2014; Kirillova et are related to the third basin type. They are sep- al., 2015; Khanchuk et al., 2015). arated by low mountains (Amur-Zeya and Pre- The development of the Far Eastern region Dzhugdzhur basins). during the Early Cretaceous closely follows that According to geodynamic reconstructions, of the Late Jurassic (Kirillova et al., 2000). Three the Khingan-Okhotsk active continental margin, types of basins existed there in the Early Creta- bounded by the Amur suture from the east, ex- ceous. The Lower Amur and Sikhote-Alin ba- isted in the Early Cretaceous. This margin com- sins, located eastward, are considered the first prised a magmatic arc marked by a chain of vol- type and appear to be rather deep seas, in which canic areas extending from the Lesser Khingan mostly Berrisasin–Valanginian turbidites, about as far as the Sea of Okhotsk, along with an accre- 6000 m thick, with a subordinate amount of tionary complex made up mainly of turbidites. cherty-volcanic rocks and limestones accumu- Olistostrome horizons discovered at different lated in the conditions of stable downwarping Early Cretaceous stratigraphic levels are con- environment. Horizons with olistostromes con- taining diversified Paleozoic and Mesozoic clas- fined to zones of the largest bed-by-bed disinte- tics are often observed near the continental gration. As a result of the oblique subduction of boundary. Some researchers suggest the exist- the Izanagi Plate, the sinistral margin-slip ence of an early Cretaceous oceanic basin, the movements have been initiated in the Val- deposits of which (jasper, cherts, mudstones) are anginian on the East Asian margin and the associated with alkaline basalts described in the transform continental margin started its for- Kiselevka–Manoma terrane. mation. These movements accompanied by local Basins located along the margin of the pre- collision events became more intensive in the Jurassic continental structures (Torom, Uda, Bu- Hauterivian, causing elevation of large tectonic reya, Okrainy and South Primorye) belong to blocks, hiatuses in sedimentation and consider- the second type (Kirillova et al., 2015). They are able changes in the coastline. 51

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Fig. 1. The types of Cretaceous rocks in the southeastern Russia.

Marine Hauterivian deposits are reported Barremian. Since the beginning of the Aptian, a only from the southeastern Primorye, where a volcanic material is observed in the turbidites, continuous Berriasian–Albian section has been and the rate of sedimentation increased sharply. described, and no marine deposits of this age are Since that time, it was a forearc basin where sed- observed in the rest of the area. imentation continued until the mid-Albian. The For the time interval from the Barremian to thickness of the deposits is about 9000 m. the mid-Albian, four sedimentation areas can be The marginal-continental basin area cov- distinguished: West Sikhote-Alin basin area, ered the Uda, Torom, Bureya, Razdolny and East Sikhote-Alin basin area, marginal- Partizansk basins. Terrigenous continental de- continental basin area, and intracontinental ba- posits about 1500 m thick are among the depos- sin area. its predominant. The deposits of the first two The West Sikhote-Alin basin is viewed as a basins are represented mostly by conglomerates pull-apart sea basin filled with Late Hauterivian and diversified sandstones (about 600 m) which and Barremian turbidites. In the Aptian–Early contain volcanic material, evidencing about the Albian the Samarga and Udyl island arcs were proximity to the volcanic arcs. In the Late Apti- generated in the eastern part of the basin; and an to mid-Albian, the Okhotsk-Chukchi volcanic the basin assumed the features of a back-arc ba- belt and its fragments began to form along the sin. Volcanogenic sandstones, tuffs and tuffa- basin margins. Rhyolites and dacites were the ceous siltstones are among the terrigenous mate- first volcanics to appear. The Bureya, Razdolny rial predominant. The rate of sedimentation and Partizansk basins were coastal-marine sharply increased after the Aptian time, when is- marsh plains during the Hauterivian to mid- land arcs were becoming larger. The thickness of Albian. A cyclic terrigenous coal formation the Late Hauterivian–Middle Albian deposits about 1500 m thick accumulated there. The reaches 5500 m. Razdolny and Partizansk basins can be consid- The East Sikhote-Alin basin is also inter- ered as pull-apart basins because their formation preted as a pull-apart basin being filled with ter- during the Hauterivian was associated with the rigenous turbidites during the Hauterivian and intensive left-lateral strike-slip faults. During the

52

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Fig. 2. Diagram showing CI, CIA and CIW values obtained for the Upper Jurassic–Lower Cretaceous of southeastern Russia. Formations: J3tl – Talyndzhan, J3db – Dublican, K1sn – Soloni, K1čg – Chagdamyn, K1čm – Chemchuki.

mid-Albian transgression, the sea penetrated We have determined standard lithochemi- briefly the Bureya and Partizansk basins, as con- cal indices: firmed by the beds with marine Trigonia and CIA = Al2O3 / (Al2O3+CaO*+Na2O+K2O) x 100 foraminifers. Since the Late Albian, however, the (chemical index of alteration) type of sedimentation in the Partizansk and CIW = Al2O3 / (Al2O3+CaO+Na2O) x100 Razdolny basins sharply changed: after short (a new chemical index of weathering) pause the continental coarse clastic, variegated The boundary between cold and warm cli- volcanogenic-terrigenous sediments about 3500 mates is defined by CIA value of 70 or CIW val- m thick were deposited. ue of 80 in the clay shales (aleuropelites) and by The Amur-Zeya basin is related to the in- the lower values in the psammites. The average tracontinental basin areas that expanded sub- CIA and CIW values of the studied Late Jurassic stantially during the Hauterivian to early Albi- psammites are 58.3 and 73.3, respectively, and an, thus marking a post-rift subsidence stage of those of the Early Cretaceous psammites are the development. During this time 1200 m of lower (57 and 67). The average CIA and CIW terrigenous deposits accumulated and acid vol- values of the Late Jurassic aleuropelites are 75.2 canics erupted. and 87.2. Based on these parameters, it should Early Cretaceous paleoclimates can be in- be concluded that climate in the Tithonian was ferred from lithological, paleobotanic and litho- warm while during the other studied time inter- chemical data obtained in the most studied Bu- vals the climate was warm-temperate (Fig. 2). reya Basin. The formation of the Late Jurassic– An increase in CI values indicates a warming Early Cretaceous coal beds occurred in a warm process. humid climate. The formation of the extended Okhotsk- From K. Raunkier cycadophyte index Chukchi magmatic arc (or volcanic belt) was b b ( CI  1  100) of the floral remains V.A. commenced in the mid-Albian and was the most а1 а remarkable event at the Early–Late Cretaceous Krassilov established that a warming event oc- transition. The East Sikhote-Alin belt, which also curred in the Tithonian (Dublican Formation). began to form at the same time, was a southern This warm period was followed by a cooling in continuation of the Okhotsk-Chukchi belt. the Berriasian–Early Hauterivian (Urgal and In the Late Cretaceous the Far Eastern re- Chagdamyn formations) and then by some gion included eastern and western depositional warming in the Late Hauterivian–Aptian areas. The western continental area was charac- (Chemchuki Formation) (Krassilov, 1973). terized by the eruption of acid to intermediate 53

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 volcanics during the Cenomanian–Turonian; sedimentary regimes. Within the back arcs, however, a hiatus in sedimentation is observed Cenomanian–Turonian continental variegated in the Amur-Zeya basin. During the Turonian to volcanogenic-sedimentary deposits (about Senonian, extensive 300 m thick lacustrine sand- 3000 m) were generated suggesting an initial stones and clays with rich fauna were deposited. high rate of volcanic arc denudation while Along the basin margins, conglomerates occur troughs were being formed. with deposits reaching 800 m in thickness. During the Late Cretaceous, most of the Far Maastrichtian–Danian cyclic sandstones, gravels Eastern region was a land. A marine embayment and claystones up to 450 m thick are wide- persisted only in the northeastern part, along the spread. Dinosaur remains were found in the present-day Amur River valley. It represented a mid-Maastrichtian beds. back-arc basin, in which about 4000 m of coarse In the eastern area, the Late Cretaceous East sandstones, siltstones and mudstones mixed Sikhote-Alin volcanic belt was formed in the with tuffaceous material were deposited during coastal part of the continent. An alternating se- the Cenomanian–Turonian. Basal conglomerates ries of lavas and intermediate to acid tuff of mark the base of the sequence. At the end of the about 1500 m in total thickness have been formed. During the Late Cretaceous, the West Turonian, the sea retreated from the region Sikhote-Alin belt continued to form, generating completely, and since that time until the latest 1800 m thick series of alternating lavas and in- Cretaceous, andesite and rhyolite volcanic rocks termediate to acid tuff. Volcanic arcs represent- up to 1000 m thick were formed. The sea retreat- ed topographic highs that probably had an im- ed to the eastern margin of the East Sikhote-Alin pact on local climatic conditions and thus belt.

References Baraboshkin, E.Yu., Markevich, V.S., Bugdaeva, E.V., Kirillova, G.L., Krapiventseva, V.V., Gresov, A.I., Afonin, M.A., Cherepanova, M.V. (Eds.), 2014. 2015. Cretaceous evolution stage of the Jiamusi– Cretaceous System of Russia and the near Bureya fragment of the continental margin as ex- abroad: problems of stratigraphy and paleogeog- emplified from the Bureya and Hegang basins. th raphy. Proceedings of the 7 Russian Scientific Rus. J. Pac. Geol. 9(2), 96–108. Conference with international participation. Krassilov, V.A., 1973. Palaeoecological correlation Dalnauka, Vladivostok. method for continental rocks. Bull. Moscow Soc. Cao, C.R., Kirillova, G.L., Sorokin, A.P., Kaplun, V.B., Nat., Geol. Ser. 48(4), 37–50. Cao, Y.Qu., Zhang, Y.J., 2013. Structural frame- Likht, F.R., 1997. Sedimentological features of the Cre- work and evolution of the Sunwu-Jiayin Basin in NE China and its relation to the structures of the taceous basins of the Western Sikhote-Alin. Zeya-Bureya Basin, the Far East of Russia. Tikhookean. Geol. 16(6), 92–101. Tikhookean. Geol. 32(6), 68–78. Liu, Zh., Kirillova, G.L., Zhang, X., Wang, S., 1997. Decisions of IV Interdepartment Regional Stratigraph- Mesozoic–Cenozoic tectono-stratigraphic com- ic Meeting on Precambrian and Phanerozoic of plexes along the Manchzhuria–Suifenhe transect the southern Far East and Eastern Transbaikalia. zone and adjoining area as a reflection of geody- A set of stratigraphic charts. Khabarovsk, 1994. namic evolution of the region. Tikhookean. Geol. Didenko, A.N., Khanchuk, A.I., Tikhomirova, A.I., 16(6), 36–45. Voinova, I.P., 2014. Eastern segment of the Markevich, P.V., Konovalov, V.P., 1997. Early Creta- Kiselevka-Manoma terrane (northern Sikhote- ceous deposits of Sikhote-Alin: certain results of Alin): Paleomagnetism and geodynamic conse- sedimentological investigations. Tikhookean. quences. Tikhookean. Geol. 33(1), 20–40. Geol. 16(6), 80–91. Khanchuk, A.I., Didenko, A.N., Popeko, L.I., Sorokin, Yarmolyuk, V.V., Kovalenko, V.I., Kuzmin, M.I., 2000. A.A., Shevchenko, B.F., 2015. Structure and evo- North Asian superplume in the Phanerozoic: lution of the Central Asian orogenic belt, in: Magmatism and deep geodynamics. Geotecton- Kroner, A. (Ed.), The Central Asian orogenic belt: Geology, evolution, tectonics and models. Born- ics 5, 3–29. traeger Sci. Publ., Stuttgart, pp. 211–234. Zhang, X., Zhang, M., Chi, X., Liu, Zh., 2008.The divi- Kirillova, G.L., Markevich, V.S., Bely, V.F., 2000. Cre- sion and evolution of Mesozoic basin groups in taceous environmental changes of East Russia, Northeastern China, in: Workshop on petroleum in: Okada, H., Mateer, N. (Eds.), Cretaceous en- geology and mineral resources in Northeastern vironments of Asia. Elsevier, pp. 1–47. Asia: Abstract volume. Changchun, pp. 38–39. 54

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Palynomorphs and biofacies in the Upper Cretaceous sediments of northern Siberia

N.K. Lebedeva1,2

1Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia 2Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia e-mail: [email protected]

The significance of microphytofossils for ed by freshwater Schizoporis, Schizocysta, and paleogeographic and paleoecological reconstruc- Tetraporina forms. tions is one of the most complex and debatable Coastal-marine (sublittoral settings with high- questions. The distribution of different palyno- energy hydrodynamics and a varying degree of morph groups, including dinoflagellate cysts, desalination) acritarchs, and unicellular green algae, through bionomic zones of sea depends on many interre- Assemblage 2a is dominated by spores and lated factors, the influence of which on the biota pollen (40–90%). Phytoplankton includes fresh- structure frequently cannot be discriminated water algae (0–10%), acritarchs (8%: Micrhystrid- when reconstructing different parameters of ium, Veryhachium, Leiofusa), and prasinophytes paleobasin (depth, salinity, hydrodynamics, iso- (0–12%: Pterospermella, Cymatiosphaera). Parale- lation degree of the basin, water chemistry and caniella: 5–45%. Dinocysts are largely represent- others). This work continues the series of papers ed by the gonyaulacoid group accompanied by dedicated to paleoecological properties of ma- chorate (0–40%), diverse cavate (Chatangiella, rine microphytofossils and their significance for Trithyrodinium, Alterbidinium, Palaeohystrichopho- reconstructing habitat conditions (Lebedeva and ra), and rare (up to 6%) holocavate (Chlamydo- Zverev, 2003; Lebedeva, 2008). Altogether they phorella, Chlonoviella) forms. The remarkable fea- present the results of the biofacies analysis of ture of the assemblage is the occurrence of palynomorphs from natural outcrops of Upper proximochorate cysts of the Cyclonephelium– Cretaceous sediments in the Ust’-Yenisei area. Circulodinium group, Fromea, and Microdinium This section was selected to serve as a standard species (locally >5%). for development of methodical approaches, Assemblage 2b is also dominated by spores since it is composed of different-facies sediments and pollen (40–90%). The composition of micro- with abundant and diverse assemblages of plant phytofossils is highly impoverished. All the microfossils and is well studied both in the groups occur in insignificant quantities except paleontological and sedimentological aspects for freshwater algae, which constitute 5–20%, (Zakharov et al., 1991, 2003; Sahagian et al., and Paralecaniella (up to 50%). Dinocysts are of 1996; Lebedeva and Zverev, 2003; Lebedeva, extremely low diversity with Fromea playing the 2006). The analysis of quantitative characteristics most notable role. of individual palynomorph groups, mor- Assemblage 3 is characterized by the domi- photypes and taxa of dinocysts, as well as nant role of the genus Paralecaniella (80–100%) changes in their taxonomical structures revealed and a highly impoverished dinocyst composi- seven palynomorph assemblages that character- tion, which are either missing or uniform lack- ize terrestrial, coastal marine, shallow-, and ing chorate forms such as Pterospermella and deep-water settings (Lebedeva, 2008). It should Schizoporis representatives. be noted that the terms “shallow-water” and Shallow-water (sublittoral settings with normal “deep-water” are conditional, since microphy- marine salinity, subjected to substantial toplankton is linked more to distance from the influence of land: dominant role of terrestrial shore than to depth of the basin. plants and others) Terrestrial Assemblage 4 is largely composed of spores Assemblage 1 is dominated by spores and and pollen (40–60%) accompanied by freshwater pollen (90–100%) accompanied by common algae (0–10%), acritarchs (0–20%), prasinophytes aqueous ferns and microphytofossils represent- (0–12%), and Paralecaniella (0–20%). Dinocysts 55

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 are dominated by the peridinioid group mainly tives of this genus may tolerate desalination, represented by cavate, proximate (Microdinium, which is evident from its mass occurrence in as- Rhyptocorys, Glyphanodinium), and chorate forms; semblages 2a and 3. May (1980) noted the con- the last group is relatively abundant (0–24%), finement of Palaeohystrichophora forms to estua- although of uniform composition. rine or coastal bay settings. The genus Assemblage 5 dominated by spores and Odontochitina is probably eurybiontic, since it pollen (40–60%) also includes freshwater algae occurs in all the defined assemblages, except for (0–5%), acritarchs (0–15%), prasinophytes (1– assemblages dominated by Paralecaniella. Many 25%), and Paralecaniella (0–40%) forms. Dino- authors (e.g., Brideaux and McIntyre, 1975; cysts are dominated by the peridinioid group Tocher and Jarvis, 1987) also emphasized the with diverse cavate and proximate forms being tolerance of this genus to changeable environ- represented in approximately equal proportions; ments. The genera Spinidinium and Isabelidinium chorate and holocavate forms are rare. prefer shallow-water and deep-water facies (as- semblages 4 and 7). The maximal Spinidinium Deepwater (sublittoral zone with normal marine content is recorded in the Seida River section. salinity, most remote from the shoreline) Proximate, proximochorate cysts (Rhypto- Assemblage 6 is dominated by marine mi- corys, Microdinium, Cribroperidinium, Apteodini- crophytoplankton (up to 70%) with freshwater um, Kallosphaeridium, Circulodinium, Laciniadini- algae, acritarchs, prasinophytes, and Paralecan- um, Dorocysta and others) include taxa with a iella present in small quantities. Dinocysts are al- wide habitat range, being most abundant in as- ternatively dominated by either gonyaulacoid semblages 2a and 6. The genera Cyclonephelium and peridinioid forms; diverse cavate and prox- and Circulodinium occur universally. They toler- imate forms occur in approximately equal pro- ate brackish-water settings, as is evident from portions, and abundance of chorate cysts their abundance in Assemblage 2a. The genera amounts to 40%. Cribroperidinium, Apteodinium, Kallosphaeridium Assemblage 7 is dominated by marine mi- and Canningia are similarly tolerant to different crophytoplankton (up to 100%) accompanied by environments, which is also confirmed by pub- rare freshwater algae, acritarchs, prasinophytes, lished data (Harris and Tocher, 2003). Develop- and Paralecaniella species, which constitute a few ment of the genera Apteodinium, Kallosphaeridium percent. Diverse dinocysts represented by all and Batiacasphaera is closely connected with pro- morphotypes are dominated by the peridinioid grading transgression: their content increases group (mostly cavate forms). seaward. The genus Microdinium is most abun- The analysis of proportions between differ- dant in coastal-marine and shallow-water set- ent taxa and morphotypes of dinocysts, acri- tings (assemblages 2a, 4, 5). The genus Rhypto- tarchs and prasinophytes in defined assemblag- corys is usually confined to shallow- and deep- es revealed certain patterns in their distribution. water sediments (assemblages 4, 6). Holocavate cysts (Chlonoviella, Chlamydo- Cavate cysts (Eurydinium, Trithyrodinium, phorella, Membranisphaera) occur in all the de- Palaeohystrichophora, Alterbidinium, Odontochitina, fined assemblages. They represent one of a few Spinidinium, Isabelidinium, Chatangiella). This tol- groups, which occur in Assemblage 3. In the erant cosmopolitan group occurs in practically Ust’-Yenisei section, the genera Chlonoviella and all the facies types of assemblages, except for as- Chlamydophorella are abundant in Assemblage 6. semblages 1 and 3, although is most abundant In sections of West Siberia, Kara Sea shelf and and diverse in assemblages 4–7 (shallow-water Polar Cis-Urals, the content of holocavate cysts and deep-water facies). The genera Chatangiella is substantially higher and they are abundant in and Trithyodinium are registered in all assem- shallow- and deep-water assemblages 5–7 as blages, being most abundant in assemblages 4–6 well as in coastal-marine Assemblage 2a. This and prevailing in sandy sediments (Lebedeva, group probably occupied remote biotopes re- 2001). The genus Palaeohystrichophora occurs as gardless of their depths. This assumption is con- single specimens in most sections, but is abun- firmed by data on other regions and stratigraph- dant only in the Seida and Leningradskaya-1 ic intervals (e.g., Lebedeva and Nikitenko, 1999; Well sections. It is conceivable that representa- Harris and Tocher, 2003; Nikitenko et al., 2008).

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Chorate cysts (Spiniferites, Achomosphaera, flecting either the initial stage of a transgression Coronifera, Oligosphaeridium, Hystrichosphaeridi- or regression. Moreover, they are more abun- um, Heterosphaeridium, Exochosphaeridium, Floren- dant in clayey and silty sediments as compared tinia, Pervosphaeridium, Membranilarnacia and with coarse-grained varieties. Acritarchs (largely others) occur in all the assemblages (except for Veryhachium representatives) are also abundant assemblages 1 and 3), although they prefer envi- in deep-water environments with slightly stag- ronments with low-energy hydrodynamics (as- nant waters. semblages 2a, 4, 6, 7). The genera and their spe- Paralecaniella representatives occur in all cies constituting this group exhibit different the assemblages in variable proportions. The ecological preferences. As previously men- largest proportion of this genus is recorded in tioned, the data on facies confinement of the ge- assemblages 2a and 3 with its dominant role in nus Spiniferites are ambiguous. Our materials the last one. The genus is generally characteristic contribute little to the solution of this problem. of rapidly changeable settings (Chaika River sec- The substantial increase in abundance and di- tion). The coastal-marine settings with normal versity of this genus is observable both in deep- salinity, high-energy hydrodynamics and suffi- water assemblages 6 and 7 and in coastal-marine cient aeration were probably most favorable for Assemblage 2a. At the same time, there are no the genus Paralecaniella. The data obtained are grounds to speak about wide-range tolerance of consistent with the results of other studies the genus Spiniferites, since in all other settings it (Brinkhuis and Schiøler, 1996; Schiøler et al., is either absent or occurs as single specimens. 1997). The genus Oligosphaeridium occurs in all the set- The comparative analysis of palynomorph tings, although the species Oligosphaeridium com- assemblages from the Cenomanian–Coniacian plex is usually confined to deep-water facies (As- sections of the Ust’-Yenisei area and other West semblage 7). Oligosphaeridium pulcherrimum is Siberian areas (Berezovskaya-23k, Yuzhno- considered to be a euryhaline species (probably, Russkaya-113, and Leningradskaya-1 wells) as well as from the Santonian–Campanian sedi- preferring lowered salinity) (Harris and Tocher, ments of the Ust’-Yenisei, Khatanga and Polar 2003). The genera Pterodinium and Dapsilidinium Cis-Urals regions demonstrates that transgres- are confined to deep-water remote settings. In sive–regressive cycles reflected in the taxonomic contrast, the genera Exochosphaeridium and Cleis- structure of assemblages are most distinct in tosphaeridium are abundant in coastal-marine coastal sections (particularly at the transition be- and shallow-water facies. tween terrestrial and marine sediments) and less Prasinophytes (Pterospermella, Cymati- distinct in the marine section. The biofacies and osphaera, Leiosphaeridia) occur in facies of two palynomorph compositions exhibit regular suc- types. They are usually confined to shallow- cession from the periphery toward central parts water and deep-water sediments (assemblages 5 of the West Siberian basin. It is established that and 6) in the Ust’-Yenisei section and coastal- facies successions in sections of the eastern and marine facies (Assemblage 2a) in sections of western areas of West Siberia during the Santo- West Siberia and Polar Cis-Urals region. The nian–Campanian differ from each other, which dual distribution patterns were also noted else- is probably explained by the influence of both where (Lebedeva, 2008). It should, however, be the West Siberian and Russian seas on sedimen- noted that no representatives of the genus Pter- tation in the last domain at that time. Some de- ospermella are found in brackish-water environ- fined patterns in the facies affinity of individual ments. The genus Leiosphaeridia occurs universal- palynomorph groups, morphotypes and taxa of ly in small quantities being usually confined to dinocysts may be used for paleogeographic in- sediments reflecting the onset of transgression terpretations. The established distribution pat- or regressive phase. terns of dinocyst and other microphytofossil Acritarchs occur in small abundance in As- morphotypes determined by transgressive– semblage 2a, where they are represented by the regressive cycles make them a useful tool for re- genera Micrhystridium and Leiofusa. Such a dis- construction of sedimentation paleosettings. tribution of acritarchs is consistent with the data This is a contribution to the IGCP608 and pro- indicating their confinement to sediments re- grams 30 and 43 of the Presidium of the RAS.

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References

Brideaux, W.W., McIntyre, D.J., 1975. Miospores and Turonian event in Northern Siberia. Rus. Geol. microplankton from Aptian-Albian rocks along Geophys. 44 (8), 769–780. Horton River, district of Mackenzie. Geol. Surv. May, F.E., 1980. Dinoflagellate cysts of the Gymnodin- Can. 252, 1–81. iaceae, Peridiniaceae and Gonyaulacaceae from Brinkhuis, H., Schiøler, P., 1996. Palynology of the the Upper Cretaceous Monmouth Group, Atlan- Geuihemmerberg Cretaceous/Tertiary boundary tic Highland, New Jersey. Palaeontographica B section (Limburg, SE Netherlands), in: Brinkhuis, 172, 10–116. H., Smith, J. (Eds.), The Geulhemmerberg Creta- Nikitenko, B.L., Pestchevitskaya, E.B., Lebedeva, ceous/Tertiary boundary section (Maastrichtian N.K., Ilyina, V.I., 2008. Micropaleontological and type area, SE Netherlands). Kluwer Academic palynological analyses across the Jurassic– Publishers, Dordrecht, pp. 193–213 (Geol. Mijnb. Cretaceous boundary on Nordvik Peninsula, 75, Spec. Iss.). Northeast Siberia. Newslett. Stratigr. 42, 181–222. Harris, A.J., Tocher, B.A., 2003. Palaeoenvironmental Sahagian, D., Pinous, O.V., Olferiev, A.G., Zakharov, analysis of Late Cretaceous dinoflagellate cyst V.A., 1996. Eustatic curve for the Middle Juras- assemblage using high-resolution sample corre- sic–Cretaceous based on Russian Platform and lation from the Western Interior Basin, USA. Siberian stratigraphy: zonal resolution. AAPG Mar. Micropaleontol. 48, 127–148. Bull. 80, 1433–1458. Lebedeva, N.K., 2001. Genus Chatangiella (dinoflagel- Schiøler, P., Brinkhuis, H., Roncaglia, L., Wilson, G.J., late cysts): stratigraphic significance and geo- 1997. Dinoflagellate biostratigraphy and se- graphic distribution. News of Paleontology and quence stratigraphy of the type Maastrichtian Stratigraphy 4, 125–133; Suppl. to journal Geol. (Upper Cretaceous), ENCI Quarry, the Nether- Geofiz. 42 (in Russian). lands. Mar. Micropaleontol. 31, 65–95. Lebedeva, N.K., 2006. Dinocyst biostratigraphy of the Tocher, B.A., Jarvis, I., 1987. Dinoflagellate cysts and Upper Cretaceous of Northern Siberia. Paleontol. stratigraphy of the Turonian (Upper Cretaceous) J. 40, 604–621. Chalk near Beer, Southeast Devon, England, in: Lebedeva, N.K., 2008. Biofacies analysis of Upper Cre- Hart, M.B. (Ed.), Micropaleontology of Car- taceous deposits in the Ust-Yenisei region: impli- bonate Environments. Ellis Horwood Ltd, pp. cations of palynomorphs. Stratigr. Geol. Correl. 138–175. 16 (2), 182–197. Zakharov, V.A., Beizel, A.L., Lebedeva, N.K., Lebedeva, N.K., Nikitenko, B.L., 1999. Dinoflagellate Khomentovsky, O.V., 1991. Evidence for eustatic cysts and microforaminifera of the Lower Creta- fluctuations of the ocean in Northern Siberia ceous Yatria River section, Subarctic Ural, NW during the Late Cretaceous. Geol. Geofiz. 8, 9–14. Siberia (Russia). Palaeogeographic and paleoen- Zakharov, V.A., Lebedeva, N.K., Marinov, V.A., 2003. vironmental discussion. Grana 38, 134–143. Biotic and abiotic events in the Arctic biogeo- Lebedeva, N.K., Zverev, K.V., 2003. Sedimentological graphic region during the Late Cretaceous. Rus. and palynological analysis of the Cenomanian– Geol. Geophys. 44, 1093–1103.

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Pakistan paleoclimate under greenhouse conditions; Closure of Tethys from Pakistan; Geobiological evolution of South Asia (Indo-Pak subcontinent)

M.S. Malkani

Geological Survey of Pakistan, Upper Chattar 130 D, str. 16, Muzaffarabad, Azad Kashmir, Pakistan; e-mail: [email protected]

Pakistan paleoclimate under greenhouse dus River systems which generally flow from conditions north to south and from northwest to southeast, Warm (greenhouse) climatic conditions as well as for the birth of Paleo Ganges and prevailed in Pakistan. Warm climates were dom- Paleo Brahmaputra rivers systems which gener- inant here during the Paleozoic except the Early ally flow from west to east. As a result of the col- Permian, when Tobra/Talchir beds were depos- lision, the northwestern margin of Indo-Pak be- ited. These beds show cold (icehouse) cli- came elevated in the latest Cretaceous, creating mate/glaciations (tillites-cemented angular to terrestrial environments for the deposition of the sub angular pebbles, cobbles and boulders with Vitakri and Indus formations. The Vitakri For- faceted, smoothed, polished, striated and pitted mation (red overbank muds and meandering rock fragments) in the Eastern Salt Range and sandstones) accumulated in the lower and mid- Potwar (upper Indus) Basin. In the Mesozoic dle Indus basins while the Indus Formation and Paleogene deposits of Pakistan, there are no (bauxites and laterites) accumulated in the up- evidences for icehouse climate, while the Pleis- per and uppermost Indus basins. During the tocene and Holocene in Kohistan-Ladakh, Hin- Early Eocene, the suture and surrounding areas dukush-Karakoram and northern extremity of were uplifted enough to originate the Paleo In- Azad Kashmir show glacial deposits, like tillites dus River systems supplying detritials/clasts from northwest and north. Major streams gener- and moraines (cemented and stratified), and tills ally flow from northwest to southeast in Sulaim- (nonsorted and non stratified), and fluvioglacial an (middle Indus) and from north to south in the deposits. So far only two icehouse records have Khyber-Hazara-Kashmir (uppermost Indus) and been found in Pakistan: Early Permian glacia- Kohat-Potwar (upper Indus) basins. During the tions in eastern Salt Range, and Quaternary gla- Late Eocene, the sea further regressed from the ciations in northern areas of Pakistan. uppermost, upper and middle Indus basins of Closure of Tethys from Pakistan Pakistan and was permanently closed. The Indo-Pak subcontinental plate first col- The Early Eocene deposits of Paleo Indus lided with Afghan block (close to Zhob- River system are represented by Shaheed Waziristan) of Asia at the latest Cretaceous (70– Ghat/Murgha Faqirzai shale (distal delta, mainly 67 Ma) and also docked with Kohistan-Ladakh shale with some sand lenses), Toi/Mina (green Tethyan belt. The latest Cretaceous collision is shale and sandstone) and Kingri/Shagala (red responsible for the birth of Kohistan-Ladakh shale and sandstone) formations of Chamalang magmatic arc. The magmatism ended in Ko- (Ghazij)/Shagala groups in the Sulaim- histan-Ladakh arc but it is continuing in Chagai an/Balochistan basins, and by Chorgali (green magmatic arc. Curves of sea-level fluctuations in shale, limestone and dolomite) and Kuldana the Tethyan Sulaiman (Middle Indus) and Ko- (red and green muds, limestone and dolomite, hat-Potwar basins show considerable drop at the and sandstone) formations of Kuldana Group in latest Cretaceous. During the Early Paleocene, the upper and uppermost Indus basins. Further the sea transgressed these areas. During the Late in the east (in India) the vertebrate-bearing Sub- Paleocene, the sea regressed from the western athu Formation (Sahni et al., 1983) was deposit- Sulaiman, northern Balochistan, upper and up- ed under the Paleo Indus River systems. The permost Indus basins due to further uplift and Kingri Formation (sandstone alternated with red continued collision of subcontinent. This first and maroon muds) in Sulaiman, the Shagala collision is responsible for the birth of Paleo In- Formation (sandstone alternated with red and

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maroon muds; fossils of land baluchithere mations were deposited in the lower Indus Ba- Pakitherium) in the northern Balochistan Basin, sin. The Tethys regressed permanently from the and the Kuldana Formation in the upper and lower Indus Basin at the Oligocene–Miocene uppermost Indus basins are the result of terres- boundary. The Tethys further retreated back- trial deposition. After their deposition a sea ward to the south at the beginning of the Mio- transgression occurred, and some other strata cene, and consequently the Manchar Group were deposited: the marine Drug and evaporitic (lower Indus Basin), the Vihowa, Litra and Baska, marine Middle Eocene Kahan Group Chaudhwan formations of the Vihowa Group (Habib Rahi marl and limestone, Domanda (northern Balochistan and middle Indus basins), shale, Pirkoh marl and limestone, and Drazinda the Murree Formation and Potwar Group (up- shale) in Sulaiman; the upper Kuldana in the per and uppermost Indus basins) and the Siwa- Kohat-Potwar and Khyber-Hazara-Kashmir ba- lik Group in India were deposited. sins; and the Mina/Panjgur Formation in south- During the Pleistocene–Holocene, the sea ern Balochistan basin. further retreated to the south. In Balochistan, the However, after the early Middle Eocene the Oligocene–Pliocene Talar (=Vihowa) Group Potwar and Khyber-Hazara-Kashmir basins up- (Parkini mudstone, Talar sandstone, and Chatti lifted, showing permanent closure of Tethys from mudstone) were deposited in southern Makran the Potwar and uppermost Indus basins. This Basin. The Sakhi Sarwar Group (conglomerate of was the start of closure of Tethys from Pakistan. the Dada Formation, and sandstone, mudstone At the Late Eocene, a major and hard colli- and conglomerate of the Sakhi Sarwar For- sion of Indo-Pak subcontinent with Asia oc- mation) in northern Balochistan, and lower and curred. As a result, the Tethys retreated further middle Indus basins as well as the Soan Group to the south, just close to the northern margin of in the upper Indus Basin and the Kirthar/lower Indus Basin (Fig. 1). Kech/Kamerod/Bostan in Balochistan Basin were The Oligocene shows no depositions in the deposited by high energy fluvial processes. Flu- Khyber-Hazara-Kashmir while the terrestrial vial systems represent much folding, faulting Chitarwata Formation was deposited in the and uplifting of Himalayas, Karakoram, Hin- middle Indus, and the marine Nari and Gaj for- dukush and advancing part of Indo-Pak plate.

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Geobiological evolution of South Asia sia while the Cenozoic vertebrates show Eura- (Indo-Pak subcontinent) sian affinity and migrated from Indo-Pak to The geobiological evolution of Indo-Pak is Eurasia or vice versa via Paleo Indus River sys- significant due to its present regional contact tems along western and northern Indus Suture, with Asia but with Gondwana in the past. India after the terminal Cretaceous collision of Indo- was the only source of information on dinosaurs Pak subcontinent with Asia. until 2000. In 2000 Pakistan appeared for the Indo-Pakistan separated from Madagas- first time in the world dinosaur map. A few fos- car at the Jurassic–Cretaceous boundary time sils of the Late Jurassic titanosaurian sauropod and started northward journey at the earliest (Brohisaurus kirthari) and Late Cretaceous Cretaceous (135 Ma). It migrated rapidly, cover- mesoeucrocodile/mesocrocodile (Khuzdarcroco ing more than 5000 km in about 60 Ma. Its zahri) were found in the lower Indus (Kirthar) northwestern corner for the first time collided Basin. In upper Indus (Kohat and Potwar) ba- with Afghan block of Tethys and Asia at the lat- sins, trackways of a herd of wide-gauge titano- est Cretaceous (about 70–67 Ma). This corner saurian sauropods (Malakhelisaurus mianwali) acted as a pivot point for counterclockwise rota- confronted by a running narrow-gauge thero- tion. Just after this collision the northern extrem- pod (Samanadrinda surghari) were recorded in ity of Indo-Pak docked with Kohistan-Ladakh the Middle Jurassic Samanasuk Limestone. In Tethyan belt. The main geoevents occurred at the middle Indus (Sulaiman) Basin, about 3000 the Pliocene–Pleistocene boundary time and re- fossils were collected from more than 30 locali- sulted in further retreat of sea from the Kirthar ties in the latest Cretaceous Vitakri Formation (lower/southern Indus) basin as the terrestrial (fluvial succession; two red mud horizons alter- Vihowa/Manchar Group was deposited. The last nated with two sandstone horizons). These fos- sils include titanosaurian sauropods, abelisauri- major episode occurred at the terminal Pleisto- an and noasaurian theropods, mesoeucrocodiles, cene resulting in further retreat of sea in the and pterosaurs (see Malkani in the present book south, folding and faulting. The northward of short papers). The trackways of titanosaurian movements of Indo-Pak plate are continuing so sauropod dinosaurs are found on the thick far. This orogeny is responsible for creating sandstone bed of the Vitakri Formation in Sor highest peaks and present morphology. Neo- Muzghai locality, Qila Saif Ullah District, Balo- tethys is remained in the east, south and mostly chistan, and this discovery is the first in Asia. in the west and is named now as Indian Ocean, The Mesozoic vertebrates show relatively and the subcontinent is named as South Asia close affinity to those of Gondwana than Laura- (Indo-Pak peninsula).

Reference

Sahni, A., Bhatia, S.B. Kumar, K., 1983. Faunal evi- Lesser Himalaya, Northwestern India. B. Soc. dence for the withdrawal of the Tethys in the Paleontol. Ital. 22 (1–2), 77–86.

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Assessing effects of Deccan volcanism on biota and environments of non-marine Maastrichtian–Palaeogene sediments of Central India

D.M. Mohabey and B. Samant

PG Department of Geology, RTM Nagpur University, Law College Square, Amravati Road, Nagpur 440001, India; e-mail: [email protected]

Link between Deccan Large Igneous Prov- studied volcano-, palyno-, and magnetostratig- ince (DLIP) and mass extinction at the Creta- raphy in the selected field transects in the EDVP ceous–Palaeogene (K–Pg) boundary is still an and CDVP. These transects include ongoing debate in spite that it is a best studied (i) Chandrapur-Wardha-Amravati-Yavatmal- LIP in the world. It is expected that effects of Nanded in the Sahyadri Group of Deccan Traps hostilities of Deccan volcanism by gas emissions targeting sediments at 13 stratigraphic levels (Renne et al., 2015) and by lava flows were more within the sequence of 28 basaltic flows between pronounced on the environment and biota of 200 and 498 m RL covering 30 localities, India during the Maastrichtian–Palaeogene tran- (ii) Chhindwara-Seoni in the Amarkantak Group sition. Chenet et al. (2007, 2008) considered that at 10 stratigraphic levels in the sequence of 31 Deccan flood basalts (DCFB) erupted in three flows between 530 and 870 m RL in 19 localities, phases: the first phase in C30n at 67.4 Ma, the and (iii) Dhar-Bagh in the Malwa Group at 8 second/main phase in C29r (200–100 ky before stratigraphic levels in the lower 18 flow se- the K–Pg boundary), and the third phase in C29r quence between 216 and 333 m RL in 14 locali- in the Danian. However, recent studies (Schöbel ties. We also studied the intertrappean beds at et al., 2014; Schoene et al., 2014; Renne et al., different stratigraphic levels in Saurashtra and 2015) show that the second phase lasted much Kutch. beyond the K–Pg boundary and outpoured over The Lameta outcrops are found scattered in 80% of the total Deccan lava eruptions. central and western India as thin narrow discon- Our investigation focuses on sedimentary tinuous bands round the borders of the trap beds at different stratigraphic levels in the Dec- country and are covered by earliest lava-flows in can volcanic sequence (DVS) of Central Deccan the basins. The sediments are not of any great Volcanic Province (CDVP) and Eastern Deccan vertical extent in comparison to its wide hori- Volcanic Province (EDVP). The multiple sedi- zontality. They are deposited (Mohabey, 1996) in mentary layers studied have an adequate strati- different inland basins: (1) Nand-Dongargaon graphic constraints provided by a flow-wise (N-D), (2) Jabalpur, (3) Sagar, (4) Ambikapur- mapping on 1:50K scale and volcano- Amarkantak, (5) Balasinor-Jhabua-Bagh (B-J-B), stratigraphy established by Geological Survey of (6) Salburdi, and (7) Adilabad and Ranga Reddy. India. The DVS in the geographically separated The timing of the arrival of the first lava flows areas have different sites and centres of mag- that terminated the sedimentation and arrival of matic eruptions. In the CDVP and EDVP, few the last flow is observed to be different in these flows are indicated to be chemical analogues of basins. Litho- and biofacies analysis shows that the flows of Western Deccan Volcanic Province sediments are pedogenically modified and are (WDVP) but such flows outpoured at different deposited in alluvial-limnic environments under magnetochrons. The sediments associated with semiarid climate. the DCFB are deposited in CDVP and EDVP as The sediments in different basins are time infratrappean/Lameta Formation before the ar- transgressive, they were deposited during the rival of the first lava flows that terminated sed- magnetochrons C30n to C29r of the Maastrichti- imentation or as intertrappean sediments depos- an (Hansen et al., 2005; Mohabey and Samant, ited at different stratigraphic levels during 2013). The B-J-B Basin sediments were deposited pauses in the volcanic eruptions. Sedimentary during C30n, whereas the sediments of N-D and record of environmental and biotic changes is Jabalpur basins were deposited during C30n– mainly influenced by the Deccan volcanism. We C29r. The sediments are rich in fossils of verte-

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific brates, including non-avian titanosaurid- the K–Pg boundary and disappeared completely abelisaurid dinosaurs, bothremydid turtles, Si- about 350 ky before the K–Pg boundary. The de- mosuchus crocodiles, madtsoid snakes, frogs, and cline in the diversity and abundance of dino- fishes; invertebrates, like molluscs and ostra- saurs is commensurate with beginning of vol- cods; pteridophyte-angiosperm dominated flora canic eruptions in the province. It is also (Huene and Matley, 1933; Mohabey, 1984; Wil- observed that eruption of the first Deccan vol- son et al., 2010; Samant and Mohabey, 2014). The canic flows markedly changed the existing floral intertrapean sedimentary beds between the lava composition, from a flora dominated by pteri- flows are mainly deposits of ponds and lakes dophytes and angiosperms to a flora dominated that developed over the fresh lava surface. Re- by gymnosperms and angiosperms; this event ports of marine or near-marine sediments are ra- appears to be close to the chrons C30n–C29r in re. The intertrappean sediments also yield diver- the Maastrichtian. Presence of Palaeocene paly- sified fauna comprising titanosaurs, turtles, noflora in sediments associated with flows, with lizards, crocodiles, frogs, fishes, micromammals, normal magnetic polarity interpreted as C30n is ostrocods, and molluscs; megaflora is dominat- recorded in the Sahyadri Group of Yavatmal ed by gymnosperms and angiosperms. and Amarkantak Group of Chhindwara area. The study shows that the appearance of an- We conclude that the Deccan volcanism in the giosperms and non-avian dinosaurs in India was CDVP and EDVP was initiated in C30n of the coeval and took place in the Maastrichtian chron Maastrichtian and lasted with an extended dura- C30n. Dinosaurs appeared about 550 ky before tion at least till C28n in the Palaeocene.

References

Chenet, A.L., Quidelleur, X., Fluteau, F., Courtillot, V., Mohabey, D.M., Samant, B., 2013. Deccan continental Bajpai, S., 2007. 40K–40Ar dating of the main flood basalt eruption terminated Indian dino- Deccan large igneous province: further evi- saurs before the Cretaceous–Paleogene bound- dence of KTB age and short duration. Earth ary. Geol. Soc. India Spec. Publ. 1, 260–267. Planet. Sci. Lett. 263, 1–15. Renne, P.R., Sprain, C.J., Richards, M.A., Self, S., Van- Chenet, A.L., Fluteau, F., Courtillot, V., Gerard, M., derkluysen, L., Pande, K., 2015. State shift in Subbarao, K.V., 2008. Determination of rapid Deccan volcanism at the Cretaceous– Deccan eruptions across the KTB using paleo- Paleogene boundary, possibly induced by im- magnetic secular variation: results from a pact. Science 350(6256), 76–78. 1200-m-thick section in the Mahabaleshwar es- Samant, B., Mohabey, D.M., 2014. Deccan volcanic carpment. J. Geophys. Res. 113, B04101. eruptions and their impact on flora: palynolog- Hansen, H.J., Mohabey, D.M., Lojen, S., Toft, P., ical evidence. Geol. Soc. Am., Spec. Pap. 505, Sarkar, A., 2005. Orbital cycles and stable car- 171–191. bon isotopes of sediments associated with Schöbel, S., de Wall, H., Ganerød, M., Pandit, M.K., Deccan volcanic suite, India: Implications for Rolf, Ch., 2014. Magnetostratigraphy and 40Ar– the stratigraphic correlation and Creta- 39Ar geochronology of the Malwa Plateau re- ceous/Tertiary boundary. Gondwana Geol. gion (Northern Deccan Traps), central western Mag. Spec. Vol. 8, 5–28. India: Significance and correlation with the Huene, F.B. von, Matley, C.A., 1933. The Cretaceous main Deccan Large Igneous Province sequenc- Saurischia and Ornithischia of the central es. J. Asian Earth Sci. 89, 28–45. provinces of India. Mem. Geol. Surv. India: Schoene, B., Samperton, K.M., Eddy, M.P., Keller G., Palaeontol. Indica 21, 1–24. Adatte, T., Bowring, S.A., Khadri, S.F.R., Mohabey, D.M., 1984. Study of dinosaurian eggs from Gertsch, B., 2014. U-Pb geochronology of the Infratrappean Limestone in Kheda District, Deccan Traps and relation to the end- Gujarat. J. Geol. Soc. India 25(6), 329–337. Cretaceous mass extinction. Science 347(6218), Mohabey, D.M., 1996. Depositional environment of 182–184. Lameta Formation (Late Cretaceous) of Nand- Wilson, J.A., Mohabey, D.M., Peters, S.E., Head, J.J., Dongargaon inland basin, Maharashtra: the 2010. Predation upon hatchling dinosaurs by a fossil and lithological evidences. Mem. Geol. new snake from the Late Cretaceous of India. Soc. India 37, 363–386. PLoS Bio. 8(3), 1–10.

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Environmental changes in Early Cretaceous palaeobasin of Western Siberia based on marine and terrestrial palynomorphs

E.B. Pestchevitskaya

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: [email protected]

Detailed biostratigraphic scales on dino- The T–R sequences in several sections are flagellates, spores and pollen of terrestrial plants supported by data on micro- and macrofauna are developed for the Lower Cretaceous of (Nikitenko et al., 2008; Pestcheviskaya et al., Western Siberia based on the investigations of 2009). There are two patterns: 1) palynological well materials and stratotype sections of Kha- successions from the sections located relatively tanga depression (Fig. 1). Palynological succes- close to the palaeo coastline are characterised sions are calibrated against the Boreal zonal by increasing microphytoplankton percentage standard. Key taxa allow the interregional corre- during the transgressions (Fig. 1); 2) palynolog- lations on several stratigraphic levels ical successions of offshore marine areas follow (Pestchevitskaya 2007a, 2007b, 2010). the reverse trend, when microphytoplankton These palynological stratigraphic scales percentage increases during the regressions. It serve as a basis for a detailed study of facial can be related to the distribution of nutrients changes and dynamics of the West Siberian and some other factors influencing microphy- palaeobasin. Taking into account the results of toplankton development. In recent marine ba- quantitative analysis of microphytoplankton sins, microphytoplankton concentrates in stable distribution in different sections, transgressive- marine environments with intensive mixing of regressive (T-R) trends of low-level are re- water and a high content of biogenic compo- vealed (Fig. 1). It should be note, that a com- nents. These are often quite deep areas of nerit- plete coincidence of T–R sequences in different ic zone. Apparently, in the Early Cretaceous, sections is impossible, as it is impossible to take such conditions occurred in coastal areas dur- samples exactly at the same stratigraphic levels. ing the transgressions of West Siberian palaeo- Nevertheless, some general regularities can be basin, and in inland areas during the regres- discussed. Against the background of general sions. Note, that T–R events are more evident regression trend from the Berriasian to the in in-shore areas, and less clear in central ones, Hauterivian, several minor T–R events can be sometimes showing no indications. In this case, determined including more pronounced re- additional information can be obtained from gression in the middle part of the dinocyst zone quantitative analysis of the distribution of pal- DZ 2 in the lower part of the Lower Valangini- aeoecological groups of terrestrial palyno- an and more pronounced transgression in the morphs (Fig. 1). upper part of the dinocyst zone DZ 3 in the Spores and pollen of terrestrial plants ar- middle part of the Lower Valanginian. In some rived within the palaeobasin mainly from cases, this sequence of T–R event allows more coastal areas, so the composition of spore-pollen accurate and reliable correlation of Siberian associations is not directly related to the T–R sections. It is especially important for the events. However, the composition of spore- southern regions of Western Siberia, where pollen associations indirectly reflects the chang- palynological assemblages often lack main key es in sedimentation features depending on the taxa, which are significant correlative markers composition of coastal vegetation and palaeo- in north Siberian biostratigraphic successions landscapes, which are largely changed due to (Pestchevitskaya et al., 2012). palaeobasin dynamics. It allows the definition of

Fig. 1. Distribution of some terrestrial palynomorphs reflecting T–R trends of Western Siberian palaeobasin (areas with sediment supply from the lowland).

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T–R trends based on quantitative ratio of spores areas with a supply of terrestrial palynomorphs and pollen of hydrophilous and drought- from the elevated areas. The first trend is charac- tolerant plants. In the Early Cretaceous of Sibe- terised by a decreasing percentage of spores and ria, hydrophilous plants included various ferns, pollen of hydrophilous plants and increasing mosses, lycopsids and some gymnosperms pro- quantity of drought-tolerant plants during the ducing the pollen of Alisporites and Piceapol- transgression. The second trend is characterised lenites types and some other morphotypes. by a reverse pattern. Interestingly, T–R trends Drought-tolerant plants in northern regions determined on terrestrial palynomorphs can be were mostly represented by ginkgophytes and identify not only in coastal areas, but also in the ancient conifers producing the pollen of Pi- central regions of West Siberian palaeobasin, nuspollenites type, while in southern regions, this where microphytoplankton data are sometimes group of plants was mainly represented by taxo- uninformative for the reconstruction of detailed dialeans. Two trends are revealed: 1) for palaeo- T–R sequences. basin areas, where spores and pollen of terres- This is a contribution to the programs 30 and 43 trial plants arrived from the lowland; 2) for of the Presidium of the RAS and IGCP 608, 632.

References

Nikitenko, B.L., Pestchevitskaya, E.B., Lebedeva, N.K., Pestchevitskaya, E.B., Urman, O.S., Shurygin, B.N., Ilyina, V.I., 2008. Micropalaeontological and paly- 2009. Early Valanginian associations of fauna nological analyses across the Jurassic–Cretaceous and palynomorphs from eastern margin of boundary on Nordvik Peninsula, Northeast Sibe- Western Siberian basin: Biostratigraphic and ria. Newslett. Stratigr. 42(3), 181–222. palaeoecological aspects, in: Paleontology and Pestchevitskaya, E.B., 2007a. Lower Cretaceous bio- improvement of stratigraphic basis of geological stratigraphy of Northern Siberia: Palynological mapping: Proceedings of LV session of the Pale- units and their correlation significance. Russ. ontological Society of RAS. St. Petersburg, Geol. Geophys. 48, 941–959. pp. 105–107 (in Russian). Pestchevitskaya, E.B., 2007b. Dinocyst biostratigraphy of the Lower Cretaceous in North Siberia. Pestchevitskaya, E.B., Smokotina, I.V., Baykalova, Stratigr. Geol. Correl. 15(6), 577–609. G.E., 2012. Lower Valanginian palynostratigra- Pestchevitskaya, E.B., 2010. Dinocysts and palynostra- phy of southeastern regions of Siberia, palaeoen- tigraphy of the Siberian Lower Cretaceous. Geo, vironment and vegetation reconstructions. J. Novosibirsk (in Russian). Stratigr. 36(2), 179–193.

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Palaeoenvironmental changes in the Early Cretaceous of Gydan region (NW Siberia)

E.B. Pestchevitskaya, O.D. Nikolenko, L.G. Vakulenko, S.V. Ershov and P.A. Yan

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: [email protected]

The paper presents the results of a compre- undulating and lenticular textures sometimes hensive study of the Lower Cretaceous section disturbed by deformation. The typical feature is in several boreholes from the west of Gydan the frequent active bioturbation. Carbonised Peninsula, which is an area the least explored by plant detritus rare occurs in core material. The drilling within Western Siberia. The study is formation of these deposits occurred in the faci- based on sedimentological and palynological es of periodic offshore progradation of coastal analyses and interpretation of well-log data. sedimentary systems resulted in continuous Some lithofacies corresponding to certain sedi- change from low-energy environments of mod- mentation environments as well as typical erately deep shelf to shallow shelf. trends in the changes of lithofacies sequences, Palynological data show shallow water ne- fixing sedimentation cycles of different scales, ritic zone. Palynological assemblages are con- are determined. stantly dominated by spores and pollen of ter- The lower part of the Cretaceous section restrial plants. Microphytoplankton is not consists of the Akhskaya Formation built on flat- abundant (5–20%) and mainly represented by lying clinoforms. Thin pack (20–40 m) of Berri- prasinophytes Leiosphaeridia. There is a regres- asian–Valanginian condensed deposits and sive trend upward in the section resulting in an mostly clayer Hauterivian sediments (up to overall reduction of microphytoplankton, espe- 250 m) lies at its base. Taking into consideration cially dinocysts represented here by taxa capable the lateral position of these sediments in clino- of surviving in coastal environment. These are form structure, we can conclude that they were mainly gonyaulacoid simple morphotypes of the formed at the foot or in the slope of “sedimen- group Escharisphaeridia–Sentusidinium and areo- tary” shelf. The base of the Hauterivian is stud- ligerceous dinocysts (Circulodinium). Slight in- ied in the core material from one of the bore- creases in the percentage and diversity of dino- holes. It is represented by black and brownish cysts indicate periodic short-term transgressions. mudstone interbedded with rare clayey silt- The composition of terrestrial palyno- stone. The rock is massive, with thin vague hori- morphs shows that terrigenous material derived zontal lamination and rare pyrite impregnations. from continental areas mainly occupied by co- There is a level with trace fossils Phycosiphon. niferous forests with an admixture of ginkgoale- According to lithological data, the formation of ans growing in rather wet and warm-temperate these deposits mainly occurred in the calm hy- climate. Spore-pollen assemblages contain con- drodynamic environments, and silt only occa- siderable percentages of poorly preserved sac- sionally supplied from shallow water areas. Pal- cate pollen of ancient coniferous plants (5–24%) ynological data evidence the middle part of and Alisporites–Pseudopicea group (2–20%), as neritic zone: palynological assemblages are well as Piceapollenites (1–8%) and Ginkgocycado- dominated by marine palynomorphs with phytus (2–7%). The pollen of Taxodiaceae is also abundant dinocysts, mostly represented by the revealed (2–5%). Spore-pollen assemblages in- families Gonyaulacaceae and Areoligeraceae. clude many species widespread in Siberia and The upper part of the Akhskaya Formation other Boreal regions: Protopinus subluteus, Pseu- is composed of alternating silty claystone and dopicea magnifica, Piceapollenites mesophyticus and silty sandstone (beds BG12, BG19, few meters up others. Pollen of heirolepidiaceous conifers to 40 m) of mostly progradation structure. Core (Classopollis) regarded as an indicator of hot and material is represented by light gray fine- arid climate, are not permanent component (0– grained sandstone and siltstone, often irregular 4%) of palynological assemblages. Wet areas interbedded with mudstone characterising by near the sea coast and river shores apparently

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 were mostly occupied by cyatheaceous and dip- lamination. The typical feature is plant detritus teridaceuos ferns: smooth trilete spores of Cy- with frequent siderite inclusions. There are some athidites–Biretisporites group are most abundant levels with clayey and rarer carbonaceous intra- (12–41%). Its percentage increases in northern clasts as well as contorted texture and trace fos- and northeastern boreholes, whereas coniferous sils Skolithos and Ophiomorpha. The layers of silty pollen is more typical for western regions. Het- claystone separated sandy beds are often carbo- erogeneous composition of the main compo- naceous, they contain rather abundant root nents of spore-pollen assemblages throughout plants and plant imprints of medium and well studied area can be explained by terrigenous preservation. The areas of thin intercalation of material supply from the areas with different siltstone and claystone exhibit contortion and vegetation. Probable terrigenous supply from rarer local erosion, and deformation under grav- northern or northwestern regions is evidenced ity loading. Siderite inclusions are common by insufficient quantity of gleicheniaceous ferns here. The formation of the sediments from this (2–7%). Its percentage in palynological assem- part of the section mainly occurred in the envi- blages of the Hauterivian and Barremian in ronments of delta complex. Sandstone was ac- northeastern regions of Western Siberia is very cumulated in fluvial deltaic arms, and siltstone low, while western regions are characterised by and claystone were deposited in delta plains of- its increased amount. ten undergone waterlogging. The Lower Tanopcha Subformation (Upper The Upper Tanopcha Subformation (509– Hauterivian–lowermost Aptian) is of 433–460 m 556 m, Aptian) is represented by irregular alter- thick in the studied area. Its base is composed of nation of sandstone and siltstone (beds TP1– light grey fine-grained sandstone, silty to vary- TP14, up to 102 m thick) with silty claystone and ing degrees, formed the beds BG10 (10–18 m) rare thin layers and lenses of coal. Core material and BG11 (18–29 m) of Late Hauterivian age. mainly consists of fine- and medium-grained Uneven low-angle and cross-undulating lamina- sandstones and rarer siltstone. Textures are tion is caused by disposal of clayey and carbo- massive and cross-bedded due to accumulation naceous material with frequent siderite inclu- of small and large particles of plant detritus sions. Sandy layers in this part of section were sometimes containing siderite inclusions. Well- mainly formed in the environments of migrating preserved plant fossils and several layers with delta distributaries, and to a less extent in estua- clayey and carbonaceous intraclasts are re- rine bars. Silty claystone is characterised by con- vealed. The layers separated sandy beds are torted texture and fine bioturbation, it contains mostly composed of intercalation of clayey silt- small detritus particles and siderite inclusions. stone, claystone and clay. The typical features The formation of these sediments occurred in are plant detritus, siderite concretions, root the environments of delta plains and prodeltas. plants and carbon-bearing inclusions. These sed- The overlying layers of the Lower iments were formed within large alluvial plain Barremian (56–91 m, beds TP24–TP23) are repre- with meandering rivers. The upper part of the sented by continental sediments mostly formed Upper Tanopcha Subformation (beds TA1–TP2- as the filling of large alluvial channels. Core ma- 3 and separating layers) was accumulated in del- terial mainly consists of light grey fine- and me- tas and coastal marine environments. Their typi- dium-grained sandstone with massive texture cal features are progradation character of sedi- and rare low-angle cross lamination due to dis- mentary sequences, undulating lamination of posal of plant detritus. The beds of silty clay- silty and clayey layers including glauconite, stone are less common, and they were apparent- fragments of bivalve shells, and rare root plants. ly formed within alluvial floodplains. Brackish or continental environments in the The upper part of the Lower Tanopcha Sub- Barremian and Aptian are confirmed by palyno- formation (beds TP15–TP22, the Upper logical data. Palynological assemblages contain Barremian–Lower Aptian) is composed of fine- low percentage of microphytoplankton mostly grained and sometimes silty sandstone. Predom- represented by prasinophytes (Leiosphaeridia). inant textures are massive and cross-bedded Small-scale transgressive events in the middle of with rare current ripples, flaser and horizontal the Barremian and in some levels of the Aptian

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific are indicated by dinocysts. The spore-pollen da- creased abundance and diversity of schizaea- ta evidence gradual change of land vegetation ceous ferns in the Barremian could have been re- on the areas of sediment source, that was caused lated to the development of the river network by both evolutionary processes and changes in and occurrences of wet, but drained areas with palaeoenvironments. The quantity of taxodia- sufficient light input along river shores. Gradu- ceous pollen increases from the Barremian to the ally increased abundance of sphagnaceous Aptian characterised by appearance of first an- mosses in the uppermost Barremian and Aptian giosperms. Later, these palynomorphs gradually may have been due to expansion of wetlands. become the main components in the Late Creta- This is a contribution to the programs 30 and 43 ceous plant communities. At the same time, in- of the Presidium of the RAS and IGCP 608, 632.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Palynological study of intertrappean sediments in the central and eastern parts of Deccan volcanic province of India to understand age and depositional environment

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

PG Department of Geology, RTM Nagpur University, Law College Square, Amravati Road, Nagpur 440001, India; e-mail: [email protected]

The Deccan volcanic eruptions covering an Intertrappean deposits of the Chandrapur area of about 500.000 km2 with eruptive volume and Yavatmal districts occur in the lowermost of 1.3x106 km3 in western, central and southern Ajanta Formation of Sahyadri Group, and inter- part of India in the Late Cretaceous–Early Paleo- trappean sediments of Naskal and Rangpur in cene are one of the largest volcanic eruptions in Rangareddy District occur between the lower the Earth’s history. Whether volcanism or flows of the Deccan volcanic sequence (DVS) in Chicxulub impact caused global mass extinction the area. Eight intertrappean beds including six at the Cretaceous–Paleogene (K–Pg) boundary is beds in Yavatmal and Chandrapur districts still a matter of debate. However, recent studies (Shibla, Shankar lodi, Bari, Mauda, Maria pat- suggest that both volcanism and impact played nam and Lendi gauda beds) and two beds in important role in global environmental deterio- Rangareddy District (Naskal and Rangpur beds) ration (Schoene et al., 2014; Renne et al., 2015) in were palynologically investigated. Out of these, the Late Cretaceous–Early Paleocene. If volcan- six intertrappean localities yielded palynoas- ism can cause global environmental changes, semblage. then its impact on Indian subcontinent is ex- Palynoflora of Chandrapur–Yavatmal locali- pected to be pronounced due to its proximity to ties show presence of pollen grains of pterido- source of eruption. We conducted palynological phytes, gymnosperms, angiosperms, and fungal study of the intertrappean sediments in the ad- spores. Pollen grains of Proxapertites operculatus, joining eastern and southern parts of Deccan Gabonisporis vigourouxii and Sparaganiaceaepol- volcanic province in the Yavatmal and Chan- lenites sp. are the dominating taxa. Incrotonipollis drapur districts of Maharashtra and the Ran- neyvelii and Lygodiumsporites also form significant gareddy District of Telangana. The findings are member of these intertrappeans. The presence of significant as the palynological information on palynotaxa such as Aquilapollenites bengalensis, the intertrappean sediments from the present Gabonisporis vigourouxii, Sparganiaceaepollenites, study area is either absent or meager in compar- Jiangsupollis and Azolla cretacea suggests Maas- ison to the information on mega- and microflora trichtian age for these intertrappean. One inter- bearing intertrappean localities to the north- trappean near village Shibla is rich in megaflora, eastern part of the Deccan volcanic province especially fossil woods of palms. Megaflora such (DVP). as roots of the family Cyperaceae, woods Ai- Flows in the Deccan volcanic province are lanthoxylon indicum of the family Simaroubaceae divided into four groups, namely Mandla and and seeds Indovitis chitaleyae of the family Vita- Malwa groups to the north of Narmada River, ceae have been recorded from this intertrappean. Satpura Group to the south of Narmada River The palynoassemblage of Rangpur intertrappean up to Tapti River, and Sahyadri Group to the shows dominance of Sparganiaceaepollenites sp. south of Tapti River in the central and southern and Mulleripollis bolpurensis. Significantly, part of DVP. The volcanic flows in the north- Proxapertites operculatus form dominant taxa of western part are still unclassified (Nair and Chandrapur–Yavatmal intertrappean beds. Zet- Bhusari, 1991). The intertrappean sediments are ter et al. (2001) consider that pollen grains of mostly found in the fringe areas of the Deccan Proxapertites shows possible affinity with Arace- volcanic sequence. The study of biota associated ae and it could be an herb living in coastal envi- with intertrappean sediments is important to ronment along the shores of river channels and know age, correlation and assessing impact of lagoons. Singh et al. (2007) recorded pollen volcanism in space and time. grains of Proxapertites, Spinizonocolpites (Nypa)

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific and Lithopyrophysis from Naskal intertrappean. estuarine or distant estuarine conditions in this Hence, data suggest possibility of existence of part of DVS.

References

Nair, K.K.K., Bhusari, B., 2001. Stratigraphy of Deccan B., 2014. U-Pb geochronology of the Deccan Traps: A review. Geol. Surv. India Spec. Publ. 64, Traps and relation to the end-Cretaceous mass 477–491. extinction. Science 347(6218), 182–184. Renne, P.R., Sprain, C.J., Richards, M.A., Self, S., Van- Singh, R.S., Kar, R., Prasad, G.V.R., 2006. Deccan in- derkluysen, L., Pande, K., 2015. State shift in tertrappean beds of Naskal, Rangareddi District, Deccan volcanism at the Cretaceous–Paleogene Andhra Pradesh. Curr. Sci. 90, 1281–1285. boundary, possibly induced by impact. Science Zetter, R., Hesse, M., Frosch-Radivo, A., 2001. Early 350(6256), 76–78. Eocene zona-aperturate pollen grains of the Schoene, B., Samperton, K.M., Eddy, M.P., Keller G., Proxapertites type with affinity to Araceae. Rev. Adatte, T., Bowring, S.A., Khadri, S.F.R., Gertsch, Palaeobot. Palynol. 117(4), 267–279.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

The Cretaceous flora of Mongolia and its paleoenvironment

Uranbileg L.1, Ichinnorov N.1 and Eviikhuu A.2

1Institute of Paleontology and Geology, Mongolian Academy of Sciences, S. Danzan str. 3/1, Ulaanbaatar 15160, Mongolia; e-mail: [email protected] 2Uyan Geo Resource LLC, Sambuu str. 13/2, Ulaanbaatar 15160, Mongolia

Introduction gist Ichinnorov (1995, 1999, 2002, 2003, 2004, In Central Asia, Mongolia is one of the 2012) were carrying out studies on leafy plants countries extremely rich in fossil flora. There are and spore-pollens of Early Cretaceous flora of widespread sediments that accumulated here Mongolia, respectively; and they have partici- during the most geological stages and are de- pated in the classification of stratigraphic con- termined by unique combinations of the stages’ clusions based on paleoflora of the certain peri- own plants. The sediments containing Creta- od. Their research works were mainly carried ceous plants are mainly restricted to Central and out to place labeled Gurvan-Ereen, Baruun- Eastern Mongolia. Non-sufficient number of Erdene Mt., Böön-tsagaan Lake, Kholboot-Gol findings from the lower and middle parts of the River, Tsagaantsav, Shine-khudag, and Manlai. Upper Cretaceous has been observed. In sum- According to Vakhrameev (1990), the Lower mary, more than 30 localities yielding remains of Cretaceous floras of Mongolia are represented Cretaceous plants were identified in the country. by the following plants: maidenhair trees such This abstract highlights the key results and brief as ginkgoaleans Ginkgoites, Baiera, Sphenobaiera, summary of the research works that focused on and Karkenia (seeds), bennettitaleans such as flora composition and paleoenvironment in the Otozamites, Neozamites, Pterophyllum, Nilssoniop- Cretaceous in Mongolia. teria, and Cycadolepis, conifers such as Araucaria mongolica, heyrolepids such as Brachyphyllum, Cretaceous flora and Podozamits, and ancient pine trees such as By the Early Cretaceous, paleogeographic Pseudolarix, Pityophyllum, Pityospermum, and landscapes in regions of Mongolian Altai, Khan- Schizolepis. gai, Huvsgul and Khentii were changed, and ac- Cretaceous flora of Mongolia contains the cumulation of sediments was generally directed following plants: Muscites ostracodiferus, Lyco- from west to east, from southwest to northeast, podites falcatus, Equisetites lateralis, Limnothetis go- and to latitudinal direction as it had been pre- biensis, Limnoniobe insignis, Onychopsis psilotoides, dominating in earlier periods. The most im- Karkenia mongolica, Cladophlebis denticulate, Ptero- portant event in the flora is that plants flour- phyllum burjense, P. sutchanense, P. angulatum, ished and, moreover, ferns, some of Nilssoniopteris denticulata, Cycadolepis sp., Otoza- gymnosperms, lycopods were spreading; coni- mites lacustris, Ginkgoites mongoliensis, Ginkgo sp., fers reached their maximum development. First Sphenobaiera ikorfatensis, S. altaica, Baierella has- information about Early Cretaceous plants of tate, Baiera manchurica, Leptostrobis sp., Hartzia Mongolia was originally created as result of multifolia, Pheonicopsis angustifolia, Swedenborgia Third Expedition into Central Asia by American junior, S. longilobia, Darneya angusta, Araucarites Museum of Natural History (Cockerell, 1924). mongolicus, Brachyphyllum densiramosum, B. sulca- Later, the studies have been carried out by Neu- tum, Pseudolarix erensis, P. asiatica, Samaropsis au- burg (1932), Krassilov and Martinson (1982), rita, S. sagittata, Schizolepis drepanoides, Willsi- Jahnichen and Kahlert (1972), Vakhrameev ostrobus latisaccus, Pityanthus microsaccus, (1988; Vakhrameev et al., 1970), Krassilov and Gurvanella dictyopers, Erenia stenoptera, Tuphaera Makulbekov (2003, 2004). Most significant work fusiformis, Williamsonia whitbiensis, Arctopteris summarizing Lower Cretaceous paleobotanical sp., Naozamites vachrameevii, Adiantites ko- studies of Mongolia has been performed by chibeanus, Sephalotaxopsis sp., Lobifolia ajakensis, Krassilov (1979, 1985, 2003, 1982). Mongolian Araucaria gobiensis, Sequoia microlepis, and Cedrus paleobotanist Sodov (1980, 1981) and palynolo- sp. Since the previous studies, the main results

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific of the studies that are conducted with participa- mine site labeled Shivee-Ovoo in Central Mon- tion of Mongolian scientists nowadays are brief- golia. According to results of spore-pollen study ly below. (Ichinnnorov, 1995, 1996, 1999), the coal-bearing Mongolian–Russian–Swedish joint research sediments are belonged to the Aptian–Albian works are carried out on the Baganuur coal (Lower Cretaceous). Further studies should in- mine, Lake Böön-tsagaan, Bakhar Area, clude research of megaflora and repeating of Tsagaan-chikh, Zuunbayan and Baruunbayan spore-pollen studies and should elaborate on the areas in Central and Southeastern Mongolia age classification of the coal-bearing sediments. (Kodrul et al., 2012), achieving new results. Dur- At the moment, a number of remnants of fossil ing this study, regional distribution and some is- plants, such as Sphenopteris, Onychopsis, Phoe- sues of stratigraphic boundaries and Cretaceous nicopsis, Pityophyllum and Ginkgoites, as well as paleogeography were clarified on the base of many kinds of seeds have been found at Shivee- newly discovered complex of Lower Cretaceous Ovoo, and the plants are considered to be Early plants in Central Mongolia (Vakhrameev, 1988, Cretaceous. The site has high potential for dis- 1991; Vakhrameev et al., 1970). Within frame of covery of a number of interesting fossils in fu- the study, the plants which were found in mark- ture. In the next stage, the repeating studies will ered sites of Central Mongolia are close to Creta- determine classification (based on compounds of ceous flora that has been found in Siberia; there- the participating plants) of the complexes of co- fore, in terms of paleogeography, the Central existed flora that will be recovered from the Mongolia rather belongs to Siberian-Canadian coal-bearing sediments. Belt than to Euro-Sinian Belt. As a result of the Paleoenvironments studies of spore-pollen assemblages of the Zuunbayan and Baruunbayan formations, it was The climate was dry and warm during the concluded that studied areas belonged to Amur earliest Early Cretaceous while the wet climate Province, Siberia-Canadian Belt. It was also stat- predominated during the latest Early Creta- ed that warm and dry climate predominated ceous, causing formation of large caustobiolithic there (Kodrul et al., 2012). deposits of brown coal and peats. Therefore, the Mongolian–American joint research works. paleobotanic studies have importance to reveal The Shine-khudag markered flora site is located the spatial distribution and timing of Cretaceous in Southern Mongolia. The paleofloras found at coal deposits in Mongolia. In the latest Early the site were studied by famous Russian scien- Cretaceous, coal-bearing sediments were accu- tist V.A. Krassilov for many years, and his data mulated in the areas located at Dundgovi, Nyal- are being the markered studies for Cretaceous ga, Dornogovi, Tamtsagbulag, Bayantumen, in plants of Mongolia. However, Mongolian– the Onon-Balj Basin and Central Khalkha uplift- American cooperating studies started only two ed regions. years ago. During these studies, most of plant In general, during the Cretaceous Period, species that had been found and determined by cooler and wet climate was predominating (not V.A. Krassilov, have been identified. Nonethe- too hot); although territory of low mountains less, there is stated number of issues, which and plateaus were enlarged, in same time, val- need further classification. Now the main part of leys, hollows and intermontane troughs filled the expedition’s activity focuses on those flora large territories, too. remnants which are contained in coal and study- Conclusion ing them in details; this kind of research way is very familiar worldwide, in last time. Also, It is significantly important to find out new Mongolian–American joint research team pays places prospective for studies and to carry out attention to investigation of seeds; research comparative studies of Cretaceous paleoenvi- works are continuing in the sector. ronments and plant assemblages composed of Mongolian research team. One of the major similar flora on certain coal-bearing basins or areas of the expedition’s study is brown coal mine sites.

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

Discontinuous euxinia during the early Aptian oceanic anoxic event (OAE 1a): A case study from the Russian Platform

S.O. Zorina and O.V. Pavlova

Kazan Federal University, Kremlyovskaya str. 4, Kazan 420008, Russia; e-mail: [email protected]

The Cretaceous is marked by several epi- ary limestone. The first one includes homogene- sodes of widespread anoxia in the oceans, re- ous dense flaky aggregate of chlorite and sulted in black shale deposits known as Oceanic montmorillonite (Fig. 1A) with rare plant debris Anoxic Events (OAE) (Schlanger and Jenkyns, and pyrite framboids. The energy-dispersive 1976). Extremely warm paleotemperatures con- spectrum of the pyrite framboid in the bitumi- nected to a global sea-level highstand such as in nous siltstone shows a high value of carbon the early Aptian support the idea of glacio- (50%). The size of framboid is about 8 µm. eustasy even during hot greenhouse phases of First appearance of foraminifera from the Earth climate (e.g., Sames et al., 2016). Lower Aptian Mjatliukaena aptiensis– Bituminous shales interbedded by concre- Haplophragmoides aptiensis Zone is about 10 m tionary limestones (“Aptian Slab”) which accu- below the base of the bituminous shales. The mulated in the shallow epicontinental sea on the whole complex of this zone is fully restored di- Russian Platform are widely interpreted as be- rectly above the bituminous shale and it be- ing a regional manifestation of the global anoxic comes even more numerous. episode OAE la (Gavrilov et al., 2002; Zorina, Noteworthy, lamination caused by quiet 2016; Zakharov et al., 2013). depositional conditions and the lack of bioturba- The studied “Tatar-Shatrashany” borehole tion (Oschmann, 2011) means the termination of section is located on the Russian Platform. Dur- the sea currents, sudden appearance of euxinic ing the Early Aptian, this site belonged to the conditions leading to stratiphying water column northern-eastern part of the Peri-Tethys, being and preventing organic matter from dissolution. situated within a sea-strait connecting the Te- Pyrite framboids are raspberry-shaped, thys Ocean with the Boreal-Arctic Sea. The Low- spherical aggregates (2–50 µm in diameter) that er Aptian strata reported to correlate with OAE consist of cubo-octahedron to octahedron, equi- 1a (Gavrilov et al., 2002; Zorina, 2016) include bi- morphic microcrystals (0.5–2 µm) (Cavalazzi et tuminous shales (“Aptian Slab”), 4.2 m in thick- al., 2014; Park et al., 2003). Pyrite framboids are ness consist of dark brown thin-laminated silt- very common component for black shales being stones and clays (1–5 mm thick) cemented by formed in weakly reducing euxinic conditions as pyrite. The value of TOC in the bituminous shales synsedimentary precipitates due to bacterially from the “Tatar-Shatrashany” section is 7.55%. driven iron- and sulfate-reduction (Cavalazzi et Importantly, BF have not been found in the al., 2014; Wignall et al., 2005). bituminous shales. The bedding surfaces are There is no agreement on the origin of py- covered by numerous ammonites from the Des- rite framboids, probably because they could be hayesites volgensis Zone and embrional ammonite formed under different environmental condi- conchs. Upward the section, a level of the light tions. We adhere to the hypothesis suggested the concretionary massive limestone, 0.8 m thick is possibility of magnetotactic bacteria containing traced at a distance of more than hundred kilo- ferromagnetic sulphides (Sawlowicz, 1993). Fa- meters (Gavrilov et al., 2002; Zorina, 2016). rina et al. (1990) showed that a colony of magne- The SEM study and microprobe analyzes totactic bacteria is similar to framboids in ap- undertaken at the Institute of Geology and Pe- pearance and size (5–10 µm). troleum Technologies of Kazan Federal Univer- As homogenization of framboids usually sity (the Research Analyst B. Galiullin) revealed spreads from the centre to the surface of the that the strata corresponding to the OAE1a are spherules, organic matter and clayey particles represented by two lithological types – bitumi- may be captured as inclusions (Sawlowicz, nous micaceous clayey siltstone and concretion- 1993). 74

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

This probably explains a high value of C the basin, but about euxinia, a state with toxic (50%), the presence of Si, Al, Na and Ca in the levels of hydrogen sulfide concentrations. energy dispersive spectra taken from the pyrite The intercalations of concretionary lime- framboid of the studied bituminous shale stones underlying and overlying by the bitumi- (Fig. 1A). nous shales are of great interest. They are com- Pyrite framboids evidently indicate the eux- posed of assemblage of well-preserved skeletons inic (sulfidic) condition (Meyer and Kump, 2008) of coccoliths from the Lower Aptian Rhagodiscus with increased organic matter preservation. So, angustus NC7 nannofossil Zone (Fig. 1B, C) it is more correct to speak not about anoxia in (Bralower et al., 1995).

Fig. 1. (А) SEM images and energy-dispersive spectra of the Lower Aptian rocks from the “Tatar-Shatrashany” sec- tion. Plant particle (Pla) and pyrite framboid (Pyr) in the carbonate clayey matrix of the bituminous shale. (В, C) SEM images of the limestone with well preserved coccolith skeletons. 75

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016

These limestones indicate that the OAE 1a had been a sharp increase in bioefficiency of na- on the Russian Platform was heterogeneous. The noplankton. But stagnation and euxinity have total euxinia had been interrupted by a short ep- been recovered as quickly as they stopped. This isode of rapid oxidization, and restoration of is evidenced by the renewed accumulation of bi- normal marine conditions. At that time there tuminous shales overlying limestones.

References

Bralower, T.J., Leckie, R.M., Sliter, W.V., Thierstein, Sames, B., Wagreich, M., Wendler, J.E., Haq, B.U., H.R., 1995. An integrated Cretaceous microfossil Conrad, C.P., Melinte-Dobrinescu, M.C., Hu, X., biostratigraphy. SEPM Spec. Publ. 54, 65–79. Wendler, I., Wolfgring, E., Yilmaz, I.Ö., Zorina, Cavalazzi, B., Agangi, A., Barbieri, R., Franchi, F., S.O., 2016. Review: Short-term sea-level changes Gasparotto, G., 2014. The formation of low- in a greenhouse world – A view from the Creta- temperature sedimentary pyrite and its relation- ceous. Palaeogeogr. Palaeoclimatol. Palaeoecol. ship with biologically-induced processes. Geolo- 441(3), 393–411. gy of oil deposits 56, 395–408. Sawlowicz, Z., 1993. Pyrite framboids and their de- Farina, F., Esquivel, D.M.S., Lins de Barros, H.G.P., velopment: a new conceptual mechanism. Geol. 1990. Magnetic iron-sulphur crystals from a Rundschau 82, 148–156. magnetotactic microorganism. Nature 343, 256– Schlanger, S.O., Jenkyns, H.C., 1976. Cretaceous oce- 258. anic anoxic events: Causes and consequences. Gavrilov, Yu.O., Shchepetova, E.V., Baraboshkin, Geol. Mijnbouw 55, 179–184. Wignall, P.B., Newton, R., Brookfield, M.E., 2005. Py- E.Yu., Shcherbinina, E.A., 2002. The Early Creta- rite framboid evidence for oxygen poor deposi- ceous anoxic basin of the Russian Plate: Sedi- tion during the Permian–Triassic crisis in Kash- mentology and geochemistry. Lithol. Miner. Re- mir. Palaeogeogr. Palaeoclimatol. Palaeoecol. sour. 37(4), 310–329. 216, 183–88. Meyer, K.M., Kump, L.R., 2008. Oceanic euxinia in Zakharov, Yu.D., Baraboshkin, E.Yu., Weissert, H., Earth history: Causes and consequences. Ann. Michailova, I.A., Smyshlyaeva, O.P., Safronov, Rev. Earth Planet. Sci. 36, 251–88. P.P., 2013. Late Barremian–early Aptian climate Oschmann, W., 2011. Black shales, in: Reitner, J., of the northern middle latitudes: Stable isotope Thiel, V. (Eds.), Encyclopedia of Geobiology. evidence from bivalve and cephalopod molluscs Springer Science+Business Media B.V., Dor- of the Russian Platform. Cretaceous Res. 44, 183– drecht, pp. 201–210. 201. Park, M.-H., Kim, I.-S., Ryu, B.-J., 2003. Framboidal Zorina, S.O., 2016. Sea-level and climatic controls on pyrites in late Quaternary core sediments of the Aptian depositional environments of the Eastern East Sea and their paleoenvironmental implica- Russian Platform. Palaeogeogr. Palaeoclimatol. tions. Geosci. J. 7(3), 209–215. Palaeoecol. 441(3), 599–609.

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Session 4 Cretaceous stratigraphy and sedimentology

Chronostratigraphy of the Jurassic–Cretaceous lacustrine deposits in southeast Mongolia: Brief results of Japan–Mongolia Joint research project

H. Ando1, H. Hasegawa2, Ichinnorov N.3, N. Hasebe4, T. Ohta5, T. Hasegawa6, M. Yamamoto7, G.B. Li8, Erdenetsogt B.9 and U. Heimhofer10

1Department of Earth Sciences, Faculty of Science, Ibaraki University, Mito 310-8512, Japan; e-mail: [email protected] 2Nagoya University Museum, Nagoya University, Nagoya 464-8601, Japan 3Paleontological Center, Mongolian Academy of Sciences, Ulaanbaatar 210351, Mongolia 4Division of Earth Environmental Technology, Kanazawa University, Ishikawa 920-1192, Japan 5Department of Earth Sciences, Faculty of Education and Integrated Arts and Sciences, Waseda University, Tokyo 169-8050, Japan 6Department of Earth Sciences, Faculty of Science, Kanazawa University, Ishikawa 920-1192, Japan 7Faculty of Environmental Earth Science, Hokkaido University, Sapporo 060-0810, Japan 8Nanjing Institutes of Geology and Palaeontology, Chinese Academy of Science, Nanjing 210008, China 9Department of Geology and Geophysics, National University of Mongolia, Ulaanbaatar 13320, Mongolia 10Institute of Geology, Leibniz University Hannover, D-30167 Hannover, Germany

Lower Cretaceous lacustrine oil shale de- beds. In the type locality of the Khootin Khoto- posits (Shinekhudag Formation) are widely dis- gor area, the 150 m thick Eedemt Formation tributed in southeastern Mongolia. Their high overlies the coal-bearing fluvial deposits of the organic carbon content has motivated many ge- Khootin Khotogor Formation. ochemical and petroleum exploratory studies. To establish the chronostratigraphy of these Most of the lacustrine oil shales are considered lacustrine deposits, fission-track and U–Pb age to be of Early Cretaceous age, but our recent dating of zircon in intercalated tuff and K–Ar studies revealed that some of them are of Mid- age dating of intercalated basalt were conduct- dle Jurassic age (Li et al., 2014). Thus, the pre- ed. Based on that radiometric age dating, the sent study aims are to explore the spatial and Shinekhudag Formation is considered to be de- temporal distribution of the Mongolian oil posited between ca. 123–119 Ma (Early Aptian), shales, establishing the chronostratigraphy of while the Eedemt Formation straddles 165 Ma or the Jurassic–Cretaceous lacustrine deposits in the late Middle Jurassic. Mongolia. This study has been conducted as the The Shinekhudag Formation is composed Japan–Mongolia–China joint researches since mainly of alternating beds of dark greyish paper 2009 (Ando et al., 2011; Hasegawa et al., in shale (oil shale), greyish calcareous shale, light press). greyish dolomitic marl, and yellowish to brown- The Shinekhudag Formation (250 m thick) ish dolomite. The shale and dolomite succes- exposed in the Shine Khudag (type) area of sions are rhythmically alternated (decimeter-, Shaazangiin Gobi region below the fluvio- meter-, tens of meter-scale), possibly controlled lacustrine Tsagantsav Formation and above the by orbitally driven changes in lake level and coal-bearing fluvial Khuhuteg Formation is lake productivity changes reflecting precipita- studied to cover the majority of terrestrial se- tion changes. Paper shale contains micrometer- quences for constructing a composite section scale laminations (ca. 60–100 µm thick), which (Jerzykiewicz and Russell, 1991; Hasegawa et al., are most likely of varve origin. Fluorescent mi- 2012). croscopic inspection reveals that they are com- The Middle Jurassic lacustrine deposits of posed of repetitive couplets of algal organic mat- the Eedemt Formation encompass alternating ter-rich and detrital mineral-rich lamina. The shale, dolomitic marl, siltstone and sandstone estimated sedimentation rate is ca. 6.3–12.5 77

The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 cm/k.y. by the varve-counting methods on thin max values (430–440°C), and all the samples are sections. Thus, the Shinekhudag Formation has composed of Type I–II OM. Palynofacies analy- a potential to record the annual-scale climatic sis further indicated the dominance of Botryococ- change and seasonal changes in mid-latitude cus colonies in dolomite layers, whereas shale Asia during the Aptian time. To obtain the con- layers are abundant in amorphous OM, algal tinuous paleoclimatic record of this unique la- cysts, and terrestrial palynomorphs. custrine deposit, we have drilled two scientific Therefore, the dolomite layers are inferred research cores (CSH01, 02) in Shine Khudag area to be formed during low lake levels by microbi- in 2013 and 2014 summer seasons. CSH01 core is ally mediated precipitation in highly alkaline 150 m long and covers the lower to middle part lake waters. Botryococcus colonies were abun- of the formation. CSH02 core is 192 m long and dant under such oligotrophic and euryhaline covers the middle to upper part of the for- conditions. On the other hand, the shale layers mation. were deposited during high lake levels, which In order to clarify the depositional envi- were characterized by higher algal productivity ronments and the controlling factors for the and increased inputs of detrital minerals. rhythmically alternating lithofacies changes, we Both of the Jurassic–Cretaceous lacustrine conducted XRD analysis, elemental analysis (C, oil shale deposits took place in intra-continental N, S), Rock-Eval pyrolysis, and a quantitative rift basins at middle latitude of the paleo-Asian study of palynofacies to evaluate the organic continent. Although basin evolution tectonics matter (OM) composition. The mineral composi- tion results confirmed the cyclic alternations (ca. may have been involved in the deposition of 1.5 m cycle) of dolomite abundant layers and de- these lacustrine oil shale, it is enhanced precipi- tritus minerals and calcite rich layers. C/N val- tation under a humid climatic setting during the ues are significantly low (<10) in the dolomite Early Aptian and the late Middle Jurassic times samples and higher (>15) in shale samples. that is more likely to be a key factor in the wide- Rock-Eval analysis shows significantly high hy- spread occurrence of lacustrine environments in drogen index (>650 mg/g) with relatively high T- southeast Mongolia.

References

Ando, H., Hasegawa, H., Hasegawa, T., Ohta, T., Drastic shrinking of the Hadley circulation during Yamamoto, M., Hasebe, N., Li, G., Ichinnorov, the mid-Cretaceous Supergreenhouse. Clim. Past N., 2011. Jurassic–Cretaceous lacustrine deposits 8, 1323–1337. in the East Gobi Basin, southeast Mongolia. J. Jerzykiewicz, T., Russell, D.A., 1991. Late Mesozoic Geol. Soc. Japan. 117, XI–XII. stratigraphy and vertebrates of the Gobi Basin. Hasegawa, H., Ando, H., Hasebe, N., Ichinnorov, N., Cretaceous Res. 12, 345–377. Ohta, T., Hasegawa, T., Yamamoto, M., Li, G., Li, G., Ando, H., Hasegawa, H., Yamamoto, M., Erdenetsogt, B., Murata, T., Shinya, H., Enerel, G., Oyunjargal, G., Munkhtsetseg, O., Buyantegsh, B., Hasegawa, T., Ohata, T., Hasebe, N., Ichinnorov, Enkhbat, D., Suzuki, N., Irino, T., Yamamoto, K., N., 2014. Confirmation of a Middle Jurassic age Kouchi, Y., Orihashi, Y., Heimhofer, U., in press. for the Eedemt Formation in Dundgobi Province, Island Arc. southeast Mongolia: Constraints from the dis- Hasegawa, H., Tada, R., Jiang, X., Suganuma, Y., Imsamut, covery of new spinicaudatans (clam shrimps). S., Charusiri, P., Ichinnorov, N., Khand, Y., 2012. Alcheringa 38, 305–316.

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Supersequenses in the Upper Jurassic and Lower Cretaceous of Western Siberia

A.L. Beisel

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e–mail: [email protected]

There are very different stereotypes in the Notable ‘violations’ in the work of the development of stratigraphic schemes of the Ju- mechanism of cyclogenesis are obviously associ- rassic and Lower Cretaceous of Western Siberia ated with widespread boreal transgression be- due to both objective and subjective reasons. gun in the end of the Bathonian and in the Cal- However, these categories are difficult in some lovian. This marine transgression has evolved in cases. The West Siberian stratigraphic scheme of several stages, reaching a maximum at the the Jurassic reflects the structure of the incisions, Kimmeridgian–Volgian boundary. It was fol- but the Cretaceous scheme is built largely on bi- lowed by general regression, which was slow in ostratigraphic basis. the Volgian and became more rapid in the Early It should be noted that during the compara- Cretaceous, reaching its maximum in the Val- tive analysis of the structure of the sections, we anginian–Early Hauterivian. In this case, the Ba- need to adhere to a unified perspective on a key zhenovo Horizon composed of oil shales occurs mechanism of formation of the sedimentary cy- in the initial step of the regression. The Volgian cles, as they can be different in the Jurassic and is overall regressive, as it is evidenced by the Lower Cretaceous. According to the author, that study of the outcrops and well sections in differ- ent regions of Western Siberia. mechanism is the geographical conversion cy- Clinoform complex of the Lower Cretaceous cles of relief – rejuvenation due to tectonic ac- of Western Siberia is traditionally displayed as tivity and subsequent smoothing by exogenous an expressive series of clinoforms, which are processes. Regarding the sedimentary basins, it limited by the top of the Bazhenovo Horizon in is expressed in periodic subsidence of the seabed the lower part, while the upper part of clinoform and the subsequent filling of the formed con- complex is less certain. In western regions, west- tainers by the sediments. Thus, the sedimentary erly-dipping clinoforms meet the opposite cycles have the tectono-sedimentary nature. This branch of easterly-dipping clinoforms, and east- mechanism is characteristic of the entire sedi- ern regions are characterized by uncertain struc- mentary cover, including the Lower Cretaceous ture. Clinoform stratum of transitional zone is part of the section. characterized by different structure, which is The formation of regular tectonic– poorly studied. sedimentary cycles in the pool occurred in the By analyzing the Lower Cretaceous cli- Jurassic. The lower part of these cycles is repre- noforms of the Yenisei-Khatanga trough, V.A. sented by clayey rocks, and the upper part con- Kontorovich et al. (2014) identify the southern sists of sandy sediments substantially composed boundary of the area with clinoform structure of cyclites of a lower order. Alternating clayey and define the area, where the clinoforms are ab- and sandy strata are the basis for the allocation sent. The width of this region is of hundreds of of regional lithostratigraphic units, the horizons. kilometers. Structure of the sections in the mar- In the transitional Jurassic–Cretaceous in- gins of the trough is shown by the author (Beisel, terval, there is a continuous succession of three 2014) on the example of the reference Lower Cre- clayey horizons: Georgievka, Bazhenovo hori- taceous section situated on the Boyarka River zons, and unnamed Lower Cretaceous clayey (south margin of the Khatanga depression). In strata located between the Bazhenovo Horizon general, the section is represented by parase- and so-called ‘offshore’ Neocomian sandstones. quences that become more clear in the upper part The Cretaceous Kulomzino, Tara, etc. horizons of the section. Their hierarchical order corre- allocated here have a completely different mean- sponds to the West Siberian clinoforms that is ing in comparison to the preceding horizons and proved by the coincidence of their number (about do not reflect the structure of the section. 15 in the Valanginian–Lower Hauterivian).

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Fig. 1. Suresequenses in the Kharampurskaya-314 Well section (NE Western Siberia), based on well log data. 1 – predominantly sand, 2 – silt, 3 – clay, 4 – oil shale. 80

Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

Thus, clinoforms were formed in relatively by erosion of the Upper Jurassic rocks, changing deep-water part of the basin, and ordinary para- of sedimentation conditions, etc. sequences occur in the coastal zone. Another Thus, the analysis of section structure important feature of the reference section on the shows that there is no fundamental difference Boyarka River is the absence of the progradation between the Lower Cretaceous and Jurassic in Western Siberia. Here, the formation of se- of coastal facies. This section was formed in 15 quences and parasequences is related to the cy- km from the paleocoast characterizing by per- cles of rejuvenation and smoothing of the relief. manent location during the Neocomian. A prominent episode of rejuvenation of the re- In Western Siberia, there are three superse- lief occurred in the Neocomian, near the Berri- quences in the Upper Jurassic and lower part of asian–Valanginian boundary, and was followed the Lower Cretaceous: the Vasyugan, Georgiev- by the formation of a new transgressive- ka–Bazhenovo and Megion supersequences regressive cycle with the layers of clay at the (Fig. 1). The last two supersequences are pro- bottom and at the top of progradational sand- posed for the first time. The boundary between stone. The Georgievka–Bazhenovo and Megion supersequences have not been previously de- the second and third supersequences presuma- fined, because their boundaries are regarded as bly corresponds to the Berriasian–Valanginian changing in time. However, it is not confirmed boundary. In northern Siberia, this boundary is by reliable biostratigraphic data. characterized by some features evidencing on a This is a contribution to the IGCP608 and pro- major geological event, which was accompanied gram 43 of the Presidium of the RAS.

References

Beisel, A.L., 2014. The value of the reference sections participation (September 10–15, 2014, Vladivos- of the Lower Cretaceous of Siberia in the tok). Dalnauka, Vladivostok, pp. 52–54 (in Rus- knowledge of the clinoform structure of the Ne- sian). ocomian of Western Siberia, in: Baraboshkin, Kontorovich, V.A., Lapkovski, V.V., Lunev, B.V., E.Yu., et al. (Eds.), Cretaceous System of Russia 2014. Model of formation of the Neocomian cli- and the near abroad: problems of stratigraphy noform complex, West Siberian oil and gas prov- and paleogeography. Proceedings of the 7th ince, taking into account isostasy. Oil Gas Geol. Russian Scientific Conference with international 1, 65–72 (in Russian).

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The Jurassic–Cretaceous boundary in the Asian part of Russia

O.S. Dzyuba1 and B.N. Shurygin1,2

1Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: [email protected] 2Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia

The Global Stratotype Section and Point and Chetaites chetae ammonite zones. In Siberia, (GSSP) for the Berriasian, the basal stage of the the uncertainty interval is quite narrow, corre- Cretaceous, is currently under examination by sponding to the upper part of the C. taimyrensis the International Subcommission on Cretaceous Zone – a cointerval of this zone with the Arcto- Stratigraphy (ISCS) and the ISCS Berriasian teuthis tehamaensis belemnite Zone (Shurygin Working Group. Marine sections in Tethys are and Dzyuba, 2015). However, the separation of only considered for the definition of the Juras- the Jacobi and Grandis subzones is still difficult sic–Cretaceous (J–K) boundary. These sections, in practice, and neither the base of the Grandis especially in western Tethys, are easily accessi- Subzone nor the base of M18r is supported by ble and highly fossiliferous, and they were in- majority of members of the Berriasian WG as a tensively studied during the last decades. How- primary marker (Wimbledon, 2016). ever, a small number of continuous, non- Despite controversies, the position of the J–K condensed J–K sections, which are also to be boundary at the base of the Calpionella alpina characterised by palaeontological and non- Subzone (i.e., at the base of the Calpionella Zone) palaeontological key markers, is still a problem is currently largely accepted. The boundary falls for formal Berriasian GSSP proposal. in the pre-Brodno part of M19n, commonly in The traditional J–K boundary, which was the middle part of M19n.2n, and is constrained defined by the first appearance of ammonite by the FADs of some nannofossil species. In Bo- Berriasella jacobi in the West Mediterranean re- real regions, this level falls within the middle gion (Flandrin et al., 1975), gradually loses its part of the Upper Volgian (see Shurygin and defining value owing to widespread endemism Dzyuba, 2015). C. alpina, mostly large forms of in ammonites and their scarcity in the J–K transi- this species is a common element of the Tithoni- tion beds at many sites. Therefore, other events an Crassicollaria Zone, while the boundary be- (not only biological, but also physical and chem- tween the Crassicollaria and Calpionella zones is ical) have been analysed as potential primary defined by an ‘explosion’ event in abundance of and supporting markers of the J–K boundary. small globular C. alpina. According to Michalík Many efforts were made by Russian stratig- and Reháková (2011), this event was soon fol- raphers to search for the most preferable level lowed by the onset of the monospecific C. alpina or, at least, interval for determination of the Ber- association that is the reflection of environmen- riasian GSSP (for references see Zakharov, 2011; tal instability related to eustatic lowering of the Guzhikov, 2013; Arkadiev et al., 2014; Shurygin sea level. and Dzyuba, 2015). Recently it was concluded The Boreal–Tethyan correlation of the J–K that the least interval of the uncertainty of the boundary interval is a stratigraphic problem that position of the J–K boundary in Siberian and cannot be solved solely by using the biostrati- some other sections will be ensured by the selec- graphic method. This problem is rooted in the tion of one of two markers: biostratigraphic fact that the latest Jurassic and earliest Creta- (base of the Grandis Subzone) or magnetostrati- ceous was a time of extreme differences between graphic (base of the M18r). Both these markers the Boreal and Tethyan marine biota. As a result, are located within the upper part of the Upper the Tithonian and Berriasian stages, which are Volgian, close to several other important mark- between the Kimmeridgian and Valanginian ers: the Brodno (M19n.r1) Subzone, the widely stages, are assigned to the Tethyan scale, while traceable positive δ13C excursion, and the the Volgian and Ryazanian stages are assigned boundary between the Craspedites taimyrensis to the Boreal scale. Unlike the Tithonian–

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Berriasian boundary, only the Volgian– topic events, while two significant positive δ13C Ryazanian boundary in Boreal sections has reli- excursions have been established at Nordvik. able bioevent markers. In Siberia, it was as- The first excursion was defined in M20n1n, and signed to the base of the Chetaites sibiricus or the second positive event marks M19n–M18r Praetollia maynci ammonite zones. transition (Dzyuba et al., 2013). The J–K boundary deposits are observed in In Western Siberia, the most stratigraphical- a huge territory of the Asian part of Russia, ly-complete section spanning the J–K boundary mainly in its northern and eastern regions. is located in the foothills of the Northern Urals These deposits are dominated by terrigenous on the Maurynya River. Ammonite-based and rocks of marine and continental geneses, which belemnite-based biostratigraphy, and high- are of very different lithologic compositions; but resolution C- and O-isotope stratigraphy have in eastern areas of Russia, the siliceous- been clarified for the Maurynya section. The terrigenous and volcano-siliceous deposits are δ13C values in the section show two large posi- also developed. Typically ‘Boreal’ fossils charac- tive excursions (Dzyuba et al., 2013). The first terise the J–K boundary beds in Siberia and ma- excursion found in the lowermost part of the jor part of the Russian Far East; only a few section is well correlated with the positive ex- ‘Tethyan’ fossils have been recorded from the cursion defined within M20n1n of northern East Southern Primorye and Sikhote-Alin. Siberia (Dzyuba et al., 2013; Zakharov et al., The best integrated stratigraphic study of 2014) and Tethys (Weissert et al., 2008). The sec- the J–K boundary interval in the Asian part of ond excursion found within the Craspedites tai- Russia was performed for the Nordvik section myrensis Zone corresponds to the positive excur- located in northern East Siberia. Here, the J–K sion recognised near the boundary of boundary beds contain ammonites, belemnites, M19n−M18r in northern East Siberia. Addition- bivalves, foraminifers and dinocysts, which pro- ally, the first Sr isotope data were recently re- vide a precise biostratigraphy for the section ported from the Maurynya section (Izokh et al., (Zakharov et al., 2014). Both δ13C and δ18O 2015). curves have been reconstructed for the J–K The J–K boundary beds at Maurynya have boundary interval of the Nordvik section not yet received the palaeomagnetic characteris- (Dzyuba et al., 2013; Zakharov et al., 2014). tics, and Arctoteuthis tehamaensis belemnite has Moreover, a continuous succession of magneto- not been found here. The position of the J–K zones from M20n to M16r, including two im- boundary can be provisionally defined at the portant subzones (M20n.1r, the Kysuca Subzone, base of the Simobelus compactus belemnite beds and M19n.1r, the Brodno Subzone), was estab- (age analogue of the A. tehamaensis Zone), be- lished here (Houša et al., 2007; Bragin et al., tween two positive δ13C excursions but closer to 2013). Chrons M19n to M17r reveal apparently upper one. lower sedimentation rates (up to 0.5–2.0 m/m.y.) In the northeastern Russia, there are a num- comparable to those from ammonitico rosso fa- cies (Bragin et al., 2013; Wierzbowski and ber of sites with continuous J–K transition suc- Grabowski, 2013). cessions (Burgakhchan, Bannaya, Tantyn, Il- Note that the most of magnetozone M19n in guveem, and Perevalnaya rivers, etc.), where the Nordvik section belongs to an ammonite- biostratigraphic frame is based mainly on Buchia free interval (Rogov et al., 2015; Schnabl et al., (Paraketsov and Paraketsova, 1989). Among 2015). Only one biostratigraphic marker, the ammonites, only Chetaites sp. has been found base of the Arctoteuthis tehamaensis belemnite here within the interval under consideration Zone was undoubtedly recorded within M19n, (Pezhenka River). All these sections were not close to the middle part of M19n.2n (see Shu- restudied during a long time mainly because of rygin and Dzyuba, 2015). However, it cannot be their inaccessibility. Magneto- and chemostrati- excluded that the base of the Craspedites tai- graphic works have not been conducted here at myrensis ammonite Zone is also close to this lev- all. The J–K boundary is within the wide ranging el, but this issue needs further investigation. The Buchia terebratuloides–B. tenuicollis Zone (Upper middle part of M19n.2n does not show any iso- Volgian–lowermost Ryazanian).

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In the Russian Far East, the Komsomolsk data, but the presence of magnetozone M19n section located in the Northern Sikhote-Alin is was not established in this section with certain- also mainly characterised by Buchia-based bio- ty. Boreal bivalves (Buchia) and foraminifers stratigraphic succession (Urman et al., 2014). have been revealed here, and palynological ob- The J–K boundary is within the wide ranging jects (pollen and spores, dinocysts, etc.) were al- Buchia unschensis–B. terebratuloides beds (upper- so studied. However, the real stratigraphic most Upper Volgian–lowermost Ryazanian), ranges of all these fossils in the section need fur- which also yield ammonite Pseudosubplanites? ther investigation. sp. of Tethyan affinity. Thus, the J–K boundary defined in Tethys Integrated bio- and magnetostratigraphic by the morphological change of Calpionella alpina study of the J–K boundary in the Russian Far cannot be strictly recognised in the Asian part of East was recently performed for the Chigan sec- Russia. The problem of identification of approx- tion, Southern Primorye (Guzhikov et al., 2016). imate position of this level can be solved only Several Tethyan ammonites, characteristic for using a combination of data obtained by palae- the Jacobi Zone, are known from this section: ontological and non-palaeontological methods Dalmasiceras orientale, Berriasella cf. jacobi, B. ex of stratigraphy. gr. jacobi, Pseudosubplanites cf. combesi, P. aff. combesi, and P. cf. grandis. Investigations show This is a contribution to the IGCP608 and pro- the possibility of obtaining of palaeomagnetic grams 30 and 43 of the Presidium of the RAS.

References

Arkadiev, V.V., Baraboshkin, E.Yu., Guzhikov, A.Yu., gion, Russia), in: Michalík, J., Fekete, K. (Eds.), 2014. About Jurassic–Cretaceous boundary, in: XIIth Jurassica, IGCP 632 and ICS Berriasian Baraboshkin, E.Yu., et al. (Eds.), Cretaceous Sys- workshop: Field Trip Guide and Abstracts Book. tem of Russia and the near abroad: problems of ESI SAS, Bratislava, pp. 101–104. stratigraphy and paleogeography. Proceedings Houša, V., Pruner, P., Zakharov, V.A., Kostak, M., of the 7th Russian Scientific Conference with in- Chadima, M., Rogov, M.A., Šlechta, S., Mazuch, ternational participation. Dalnauka, Vladivostok, M., 2007. Boreal–Tethyan correlation of the Ju- pp. 27–30 (in Russian). rassic–Cretaceous boundary interval by magne- Bragin, V.Yu., Dzyuba, O.S., Kazansky, A.Yu., Shur- to- and biostratigraphy. Stratigr. Geol. Correl. 15, ygin, B.N., 2013. New data on the magnetostra- 297–309. tigraphy of the Jurassic–Cretaceous boundary in- Izokh, O.P., Kuznetsov, A.B., Dzyuba, O.S., Kosenko, terval, Nordvik Peninsula (northern East I.N., Shurygin, B.N., 2015. Short-term perturba- Siberia). Russ. Geol. Geophys. 54, 329–342. tions of marine 87Sr/86Sr near the Jurassic– Dzyuba, O.S., Izokh, O.P., Shurygin, B.N., 2013. Car- Cretaceous boundary in the Maurynya Section, bon isotope excursions in Boreal Jurassic– West Siberia: Potential causes and correlative Cretaceous boundary sections and their correla- value. Ber. Inst. Erdwiss. K.-F.-Univ. Graz 21, tion potential. Palaeogeogr. Palaeoclimatol. Pal- 181. aeoecol. 381–382, 33–46. Flandrin, J., Schaer, J.P., Enay, R., Remane, J., Rio, M., Michalík, J., Reháková, D., 2011. Possible markers of Kubler, B., Le Hégarat, G., Mouterde, R., Thieu- the Jurassic/Cretaceous boundary in the Mediter- loy, J.P., 1975. Discussion générale préliminaire ranean Tethys: A review and state of art. GSF au dépôt des motions. Colloque sur la limite Ju- 2(4), 475–490. rassique–Crétacé, Lyon–Neuchâtel, September Paraketsov, K.V., Paraketsova, G.I., 1989. Stratigraphy 1973. Mém. B.R.G.M. 86, pp. 386–393. and fauna of the Upper Jurassic and Lower Cre- Guzhikov, A.Yu., 2013. Solving unsolvable problems taceous deposits of Northeast USSR. Nedra, in stratigraphy. Russ. Geol. Geophys. 54, 349– Moscow (in Russian). 354. Rogov, M.A., Alifirov, A.S., Igolnikov, A.E., 2015. Re- Guzhikov, A.Yu., Arkadiev, V.V., Baraboshkin, E.Yu., vised ammonite succession of the upper Volgian Feodorova, A.A., Shurekova, O.V., Baraboshkin, of Nordvik section: Zonal boundaries and uncer- E.E., Manikin, A.G., Golozubov, V.V., Kasatkin, tainties, in: Baraboshkin, E.Yu., Bykov, D.E. S.A., Nechaev, V.P., 2016. New bio- and magne- (Eds.), The International Scientific Conference on tostratigraphic data at the Jurassic–Cretaceous the Jurassic/Cretaceous boundary: Proceedings boundary of the Chigan Сape (Vladivostok re- volume. Kassandra, Togliatti, pp. 70–76.

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Schnabl, P., Pruner, P., Wimbledon, W.A.P., 2015. A Wimbledon, W.A.P., 2016. Resolving the positioning review of magnetostratigraphic results from the of the Tithonian/Berriasian stage boundary and Tithonian–Berriasian of Nordvik (Siberia) and the base of the Cretaceous System, in: Michalík, possible biostratigraphic constraints. Geol. Car- J., Fekete, K. (Eds.), XIIth Jurassica, IGCP 632 and pathica 66(6), 489–498. ICS Berriasian workshop: Field Trip Guide and Shurygin, B.N., Dzyuba, O.S., 2015. The Juras- Abstracts Book. ESI SAS, Bratislava, pp. 128–130. sic/Cretaceous boundary in northern Siberia and Zakharov, V.A., 2011. The Jurassic–Cretaceous Boreal–Tethyan correlation of the boundary boundary and Berriasian GSSP: is there light at beds. Russ. Geol. Geophys. 56, 652–662. the end of the tunnel? (Comments to proposals Urman, O.S., Dzyuba, O.S., Kirillova, G.L., Shurygin, on the Jurassic–Cretaceous boundary by Berri- B.N., 2014. Buchia faunas and biostratigraphy of asian Working Group). News Paleontol. Stratigr. the Jurassic–Cretaceous boundary deposits in the 16–17 (Suppl. Russ. Geol. Geophys. 52), 69–86 (in Komsomolsk section (Russian Far East). Russ. J. Russian with English summary). Pac. Geol. 8(5), 346–359. Zakharov, V.A., Rogov, M.A., Dzyuba, O.S., Žák, K., Weissert, H., Joachimski, M., Sarnthein, M., 2008. Košt’ák, M., Pruner, P., Skupien, P., Chadima, Chemostratigraphy. Newsl. Stratigr. 42(3), 145– M., Mazuch, M., Nikitenko, B.L., 2014. Palaeoen- 179. vironments and palaeoceanography changes Wierzbowski, A., Grabowski, J., 2013. The meteorite across the Jurassic/Cretaceous boundary in the Mjølnir crater in the Barents Sea in stratigraph- Arctic realm: case study of the Nordvik section ical interpretations. Prz. Geol. 61: 516–522. (north Siberia, Russia). Polar Res. 33, 19714.

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Lower Cretaceous formations and palynology of the Matad area (Tamsag Basin), southeastern Mongolia

Ichinnorov N.1, Ch.–Ch. Hofmann2, H. Hasegawa3 and Uranbileg L.1

1Institute of Paleontology and Geology, Mongolian Academy of Sciences, S. Danzan str. 3/1, Ulaanbaatar 15160, Mongolia; e-mail: [email protected] 2Department of Paleontology, University of Vienna, Austria 3Nagoya University Museum, Nagoya University, Nagoya 464-8601, Japan

Introduction represent the characteristics of offshore lacus- In Mongolia, Upper Jurassic to Cretaceous trine facies in large (extensive), perennial lakes. non-marine sedimentary rocks are widely dis- The formation is about 300 to 700 m thick and is tributed. The Lower Cretaceous rocks contain widely distributed in the Khangai, Mongol Al- important mineral resources, such as coal, oil, tai, Gobi Altai, Central Gobi, East Gobi, Nyalga, bituminous shales, gypsum, quart, fluorite, zeo- and Choibalsan basins (Shuvalov, 1975; lite, rare metals, and gold. Jerzykiewicz and Russell, 1991). In Eastern Mongolia, the Lower Cretaceous Paleontological age constraints of the sedimentary sequence is classified into several Shinekhudag Formation had been controversial. different formations in different basins. Although abundant molluscan and ostracod fos- The stratigraphy of Lower Cretaceous strata sils have been cited as evidence of the Barremian in the Tamsag Basin has been studied by Mari- to Hauterivian age (Martinson and Shuvalov, nov et al. (1973), Khosbayar (1996), Tooruul and 1975; Khand et al., 2000), the Aptian age of the Makhbadar (1990), PAM report (1990), Tomor- formation was suggested by floral, concostra- togoo (1998), Geerdts (2007) assigned these rocks cans, and palynological evidence (Krassilov, to the Tsagaantsav and Zuunbayan (also spelled 1982; Jerzykiewicz and Russell, 1991; Dzunbayan and Dzun Bayan) formations (Shu- Ichinnorov, 1998; Graham et al., 2001; valov, 1975). The Zuunbayan Formation is the Ichinnorov, 2005; Yuan and Chan, 2005; thickest unit in the Tamsag Basin. It is divided Ichinnorov and Hofmann, 2012). Martinson and into the upper and lower formations, based on Shuvalov (1975) previously considered the Hau- depositional environment dominance. terivian–Barremian age for the formation, based The Lower Zuunbayan Formation is called on the conchostracan assemblage of Bairdestheria Shinekhudag Formation in Southeastern Gobi sinensis (Chi), B. mattoxi Kras., Pseudograpta asa- (Martinson and Shuvalov, 1973; Shuvalov, 1980, noi (Kob. et Kus) from the lower part of the 2003; Jerzykiewicz and Russell, 1991; Badam- Zuunbayan Formation of East Gobi. Some of la- garav et al., 1995; Graham et al., 2001; custrine shales within the Tsagantsav Formation Ichinnorov and Hofmann, 2012), in Eastern may be mistakenly correlated to the Mongolia (Bat–Erdene, 1992; Yamamoto et. al., Shinekhudag Formation, as it is also pointed out 1993) and consists mainly of deep lacustrine by Graham et al. (2001). On the other hand, shale rich in organic matter. The Upper Zuun- Krassilov (1982) defined the age of the bayan Formation is called Khukhteeg Formation Shinekhudag Formation as Aptian on the basis in Southeastern Gobi (Martinson and Shuvalov, of two floral assemblage zones of Baierella has- 1973; Shuvalov, 1980, 2003; Jerzykiewicz and tata–Araucaria mongolica, and Limnothetis go- Russell, 1991; Badamgarav et al., 1995; Graham biensis–Limnoniobe insignis, which also occurred et al., 2001; Ichinnorov and Hofmann, 2012), and in dated strata in eastern Siberia. Based on the in Eastern Mongolia (Bat–Erdene, 1992; Yama- conchostracan assemblage in the Shine Khudag moto et al., 1993). In this study, we use the locality, Yuan and Chen (2005) concluded that Shinekhudag and Khukhteeg formations. the Shinekhudag Formation is correlated to the The Shinekhudag Formation is composed of Jiufotang Formation of Liaoaning Province due paper shale (well-laminated shale), dolomitic to the similar faunal occurrence, whose age was marls, dolomite, siltstone and sandstone, which assigned to the Early Aptian (Sha, 2007). In addi-

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific tion, Ichinnorov (1998, 2005) and Ichinnorov and Palynological results Hofmann (2012) demonstrated pollen and spore The encountered specimens are character- assemblages of the Shinekhudag Formation ized by 26–33% spores, 67–74% gymnosperm from Bayan Erkhet, Matad, and Shine Khudag pollen. We recovered 46 fossil species of spores localities, and concluded an Aptian age of the and 31 species of gymnosperm in the Aptian– formation. Albian sediments of the lower Khukhteeg For- The Khukhteeg Formation is composed mation. mainly of dark greyish coaly mudstone, light Spores of pteridophytes, most of them prob- greyish sandstone, and conglomerate. It is wide- ably ferns, are common in the assemblage. A sin- spread in the east and center of Mongolia with a gle monolete form is present. It is assigned to the characteristic feature of abundant coal seams species Laevigatosporites ovatus. Among the (e.g., Shivee Ovoo, Tevshin Gobi, Bayan Erkhet, spores, the species of trilete spores are dominat- Khuren Dukh, Nalaikh, Baga Nuur localities). ed: Aequitriradites spinulosus, Cooksonites variabilis, Basic volcanics of different thickness (up to Foraminsporis asymmetricus, Cicatricosisporites hal- 100 m), as well as oval sandstone concretions, lei, Cicatricosisporites australiensis, Cicatricosisporites partial tree trunks, and other water-borne organic dorogensis, Appendicisporites tricornitatus, Pilo- materials are intercalated in this formation. The sisporites trichopapillosus, Pilosisporites notensis, thickness of the Khukhteeg Formation is about Kuylisporites lunarius, Leptolepidites verrucatus, Bi- 150–300 m. In the type section of the Khukh Teeg retisporites potoniaei, Glecheniidites senonicus, hill, near the Shine Khudag locality of East Gobi, Sphagnumsporites spilatus, and Osmundacidites there are abundant remains of stromatolites wellmannii. About 15 spores of pteridophytes (Sochava, 1977). The Khukhteeg Formation yields were identified to the generic level. aquatic champsosaurs (Shuvalov, 2000). Angio- Non-saccate gymnosperm pollen are repre- sperms and some species of ferns occurred in all sented by Araucaricidites, Inaperturapollenites, areas, but ginkgo pollen were less abundant Ephedripites, Ginkgocycadophytus, Monosulcites, (Ichinnorov, 1998, 2005; Ichinnorov and Hof- and Cycadopites. mann, 2012). The Khukhteeg Formation is dated In our assemblage, the specimens of bisac- as Albian or Aptian–Albian based on the occur- cate coniferous pollen are mostly assigned to the rences of turtles and mammals (Dosh Uul, Khar genera Piceapollenites, Pinuspollenites, Cedripidites Khutul, Khukh Teeg; Shuvalov, 1975), molluscs and Podocarpidites. The following taxa are com- (Khamaryn, Khural), and pollen–spore (Nichols mon: Alisporites sp., Keteleriapollenites sp., Pi- et al., 2006; Ichinnorov, 1998, 2005; Ichinnorov nuspollenites divulgatus, Pinuspollenites minimus, and Hofmann, 2012). In the Trans-Altai Gobi, the Pinuspollenites cf. concessus, Pinuspollenites sp. 1, Khukhteeg deposits ascribed to the Doshuul Pinuspollenites sp. 2, Piceapollenites exiloides, Pice- Formation contain a horizon of basalts, whose ra- apollenites mesophyticus, Protopiceapollenites ex- diometric age is 110–113 Ma (Shuvalov, 2000). iloides, Piceapollenites sp., Podocarpidites multi- Based on plant megafossils Krassilov (1982) sug- formis, Podocarpidites dettmannii, Podocarpidites gested that the deposits are Late Aptian to Albian decorus, Podocarpidites sp., Cedripites libaniformis, in age due to the floral similarity with the equiva- Cedripites cretaceous, and Cedripites sp. lent strata in the Amur Basin, Japan and north- eastern China (Shuvalov, 1975; Martinson, 1982). Discussion The Khukhteeg Formation contains the remains This palynological assemblage is completely of elasmobranchs, which also occur in the sedi- different from palynological assemblages dis- ments of Aptian age in Soviet mid-Asia. The covered from (Ichinnorov, 2005) and (PAM, Khukhteeg Formation has yet to yield trionychid 1997), concluded that the age of these sediments turtles, which first appeared in the Late Albian in is Hauterivian–Barremian. Our palynological as- Soviet mid-Asia, while it is known from the over- semblage includes many different species of lying Bayanshiree Formation (Nessov, 1985; Vitek pteridophyte spores. Aequitriradites spinulosus, and Danilov, 2014). This evidence indicates that Appendicisporites tricornitatus, Cicatricosisporites the deposition of the Khukhteeg Formation end- hallei, Cicatricosisporites australiensis, Cicatri- ed before the Late Albian. cosisporites dorogensis, Pilosisporites trichopapillo-

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 sus, Pilosisporites notensis, Leptolepidites verruca- the top of the Berriasian to the Albian. It has tus, Biretisporites potoniaei, and Glecheniidites been recorded from the Aptian–Albian of Eng- senonicus are the typical Neocomian species, but land (Kemp, 1970) and Mongolia (PAM, 1997), most of them were found in the Aptian–Albian and from the Maastrichtian of Wyoming (Mi- Khukhteeg Formation of Mongolia (Bratseva chael et al., 1986). and Novodvorskaya, 1975; Ichinnorov, 2003, According to the occurrences of spores and 2005; PAM, 1997). Foraminsporis asymmetricus, pollen listed above and absence of angiosperms, Cooksonites variabilis, Laevigatosporites ovatus have the palynological assemblage is dated as Apti- been found in the Aptian–Albian of Mongolia an–Albian (the lowest Khukhteeg Formation), (Ichinnorov, 2003, 2005), Russia (Kotova, 1970), and it is well correlated with the Aptian–Albian and western Canada (Pocock, 1962; Singh, 1964), assemblage of the locality Shivee–Ovoo in the Albian–Cenomanian of Central Alberta (Ichinnorov, 2003, 2005). The palynological evi- (Norris, 1967). Appendicisporites tricornitatus is a dence is consistent with a humid and warm typical Lower Cretaceous species ranging from paleoclimate.

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Ryazanian (Boreal Berriasian) ammonite succession of the Nordvik section (Russian Arctic): Revision and new data

A.E. Igolnikov1,2, M.A. Rogov3 and A.S. Alifirov1,2

1Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia 2Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia e-mail: [email protected] 3Geological Institute of the RAS, Pyzhevskii per. 7, Moscow 119017, Russia

The section on the Nordvik Peninsula (the The assemblage of the Chetaites sibiricus Laptev Sea coast, Anabar Bay) is studied since Zone generally consists of various Praetollia as the 50th of last century that provides a lot of ma- well as rare Craspedites (Taimyroceras), Bore- terial. Nevertheless, it requires new revision. ophylloceras, and Borealites (?). New data show This investigation is based on some samples that previous occurrences of Borealites at such collected by V.A. Zakharov, Yu.I. Bogomolov, low stratigraphic level (Igolnikov, 2010) cannot V.A. Marinov, but major part of the material be considered as definitive, because some large was collected by the authors during 2003, 2009, shells of Praetollia can have rather clear rib dif- 2011, and 2014 field seasons. The published data ferentiations, typical for Borealites. were analyzed (Basov et al., 1970; Zakharov et The base of second Ryazanian zone, Hec- al., 1983; Bogomolov, 1989), and the N.I. Shulgi- toroceras kochi (about 8.9 m thick), is defined by na’s collection located in the CSRGS museum first appearance of index species and confined to (Saint Petersburg) was investigated. the base of massive concretion horizon in the The entire Ryazanian stage is here exposed bed 23 (Fig. 1). It confirms the initial point of comprising five ammonite zones. The base of the view on the location of zone base (Basov et al., first Chetaites sibiricus Zone (about 3.5 m thick) is 1970) that is supported by new occurrences of commonly defined in the Nordvik section at the H. kochi at this level. In the lower third of the base of thin bed 18 (3–5 cm) of phosphatic chalk zone, various Praetollia continue to prevail (Fig. 1) according to the first occurrence of Prae- among ammonites, several specimens of Boreal- tollia. It should be noted that there are some ites (Borealites) and single Chetaites, Bochianites, questions on Chetaites occurrences from C. sibiri- and Biasaloceras are found. Well preserved am- cus Zone in the Nordvik section. The specimens monites are rare in the middle part of the section of C. cf. sibiricus previously represented by commonly containing rare concretions, but there N.I. Shulgina (Zakharov et al., 1983) cannot be are some imprints defined as Borealites (?) sp. attributed to this genus, because they are charac- ind. There are plenty of ammonites in the upper terized by Craspeditidae-like suture pattern and part of the zone: Borealites (Borealites) and Boreal- a moderately tight umbilicus that allows the re- ites (Pseudocraspedites) are the most abundant, liable identification of these forms as Praetollia. and Boreophylloceras and Anabaroceras are rare C. cf. sibiricus shown by Zakharov and Rogov here. As the last one concerned, we should note (2008; Table II, Fig. 8) is hardly belongs to this that these are not the first findings outside the genus; C. aff. sibiricus mentioned in the same type locality (Anabar River lower reaches), but publication (Ibid, Table II, Fig. 9) is character- they are most ancient (type collection contains ized by a Craspeditidae-like suture pattern. This Valanginian specimens) (Repin, 2012). form is close to Craspedites (Taimyroceras), but New data on the succession of Surites from differs in its large size in comparison to other the analogus group fully comply with previous Craspedites (Taimyroceras). In the collection of the results (Basov et al., 1970; Zakharov et al., 1983), authors, there is an exclusive specimen with and the base of the Surites analogus Zone (4.3 m) wide umbilicus, which is important diagnostic is defined at the base of the bed 31 (Fig. 1). feature of the genus Chetaites. However, this Along with Surites, the assemblage also com- specimen was found in the next higher ammo- prises Borealites (Pseudocraspedites) and Borealites nite zone, i.e. Hectoroceras kochi Zone. (Ronkinites), but they are less frequent.

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Fig. 1. Distribution of all known Ryazanian ammonite records in the Nordvik section (1967–2014). 1 – stage/substage, 2 – ammonite zones (Boreal standard), 3 – Borealites beds (A.E. Igolnikov), 4 – paleomagnetic zones; 5–8 – lithology: 5 – silty clays to claystones, 6 – phosphatic chalk, 7 – carbonate concretions, 8 – massive concretion horizon; 9–11 – lo- calities: 9 – Outcrop 32, 10 – Outcrop 33, 11 – Outcrop 31; 12 – approximate position or loose occurrences from bed. Numbers of beds are after Zakharov et al. (1983) for the outcrops 32 and 33, and after A.E. Igolnikov (field data 2014) for the Outcrop 31. Thickness scale 1 m.

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The Bojarkia mesezhnikowi and Tollia tolli ceous with very rare ammonites can be only zones, the uppermost two Ryazanian zones in found in the pits. All specimens of C. sibiricus the Nordvik section, are defined according to were found in the large bun-shaped concretions Yu.I. Bogomolov (1989). There are no fundamen- of calcareous siltstones from the rock debris of tally new data on these intervals, but the occur- lower stratigraphic level that is evidenced by rence of Boreophylloceras sp. in the rock debris of rock structure, as opposed to the visible section B. mesezhnikowi Zone should be noted. basement in the publications of predecessors The continuous Ryazanian from the (Saks, 1972; Alekseev, 1984; Zakharov, 1990). In Nordvik outcrops with abundant ammonites this case, it is important either to select the ne- and distinct zone boundaries can be regarded as ostratotype for the C. sibiricus Zone or use Prae- a reference section for the north of Siberia. For tollia maynci as index species for the lowermost instance, Praetollia confined only to the bottom zone of the Ryazanian stage in Siberia. of the Chetaites sibiricus Zone in the Kheta River Chetaites and Borealites successions in the section (Alekseev, 1984) remained unexplainable Nordvik section show that S.N. Alekseev’s for a long time. Praetollia and Hectoroceras were (1984) tripartite division of the Hectoroceras kochi previously reported from the Nordvik Peninsula Zone can be extended. Approximately 5 m of the and Greenland (Basov et al., 1970; Zakharov et section between the layers containing Hec- al., 1983; Surlyk, 1973), and they are recently toroceras and the last Chetaites, which can be found in the Hectoroceras kochi Zone in the Lena compared with the H. kochi Subzone, and the River (Rogov et al., 2011) and in the North Sea level marked by the first appearance of Borealites regions (Abbink et al., 2001). Thus, the part of (Borealites) constans do not contain any ammo- the Kheta River section previously assigned to nites (Fig. 1). This lacuna corresponds to the lay- the C. sibiricus Zone (Saks, 1972; Alekseev, 1984) ers with B. (B.) antiquus. can be now considered as the H. kochi Zone due Using the data on ammonite succession in to co-occurrence of Chetaites sp. and Hectoroceras the Nordvik section, the boundaries of the Hec- sp. in the base of the section (Saks, 1972; Zakha- toroceras kochi Zone can be more accurately de- rov, 1990). The base of the H. kochi Zone must be fined in the absence index species. The section in identified by the first appearance of Hectoroceras the Lena River lower reaches can be used as an (Casey et al., 1988). Nevertheless, Hectoroceras example (Rogov et al., 2011). Here, there is the specimens from the Kheta River have never Chetaites sibiricus Zone with Chetaites, Praetollia, been described in the publications and they are and Borealites in the bottom of the Ryazanian absent in the collection (excluding the specimen part of the section. This assemblage is typical for from the rock debris apparently of the higher the lower third of the H. kochi Zone, so the C. stratigraphic levels), so it is impossible to check sibiricus Zone may be absent in the region. the accuracy of their definitions. According to This work is supported by the Geological Insti- the field data of M.A. Rogov (2015 season), Out- tute of RAS (project 0135-2014-0064), and is a contri- crop 21 in the Kheta River completely consists of bution to the IGCP608 and programs 30, 32 and 43 of Quaternary rock debris, and the Lower Creta- the Presidium of the RAS.

References Abbink, O.A., Callomon, J.H., Riding, J.B., Williams, Basov, V.A., Zakharov, V.A., Ivanova, E.P. et al., 1970. P.D.B., Wolfard, A., 2001. Biostratigraphy of Ju- Zonal classification of the Upper Jurassic and rassic–Cretaceous boundary strata in the Ter- Lower Cretaceous deposits on Urdyuk–Khaya schelling Basin, the Netherlands. Proc. Yorkshire Cape (Pakhsa Peninsula, Anabar Bay), in: Gerke, Geol. Soc. 53, 275–302. A.A. (Ed.), Science memoirs NIIGA. Palaeontol- Alekseev, S.N., 1984. New data on a zonal subdivision ogy and biostratigraphy. NIIGA, Leningrad, pp. of the Berriasian in the north of Siberia, in: Men- 14–31 (in Russian). ner, V.V. (Ed.), The Jurassic and Cretaceous Bogomolov, Yu.I., 1989. Polyptychites (Ammonoids) boundary stages. Nauka, Moscow, pp. 81–106 (in and biostratigraphy of the Boreal Valanginian. Russian). Nauka, Novosibirsk (in Russian).

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Casey, R., Mesezhnikow, M.S., Shulgina, N.I., 1988. Saks, V.N. (Ed.), 1972. Jurassic–Cretaceous boundary Ammonite zones in Jurassic–Cretaceous bounda- and Berriasian stage in Boreal realm. Nauka, ry sediments of the Boreal realm. News AS Novosibirsk (in Russian). USSR. Geol. Ser. 10, 71–84 (in Russian). Surlyk, F., 1973. The Jurassic–Cretaceous boundary in Igolnikov, A.E., 2010. New ammonite’s finds from Jameson Land, East Greenland. Geol. J., Spec. Iss. Berriasian of the Nordvik Peninsula, in: Proc. 5th 5, 81–100. All-Russia meeting “Cretaceous system of Russia Zakharov, V.A., 1990. Definition of Jurassic– and near Overseas: problems of stratigraphy and Cretaceous boundary on buchias, in: A boundary paleogeography”. UlGU, Ulyanovsk, pp. 163–165 of Jurassic–Cretaceous system. Nauka, Moscow, (in Russian). pp. 115–128 (in Russian). Repin, Yu.S., 2012. The endemic branch of the Phyl- Zakharov, V.A., Rogov, M.A., 2008. The Upper Vol- loceratida (Ammonoidea) of Arctic Mesozoic, in: gian substage in northeast Siberia (Nordvik Pen- Proc. conf. “Contributions to current cephalopod insula) and its Panboreal correlation based on research: Morphology, systematics, evolution, ammonites. Stratigr. Geol. Correl. 16, 423–436. ecology and biostratigraphy”. PIN, Moscow, pp. Zakharov, V.A., Nalnyaeva, T.I., Shulgina, N.I., 1983. 73–76 (in Russian). New data on the biostratigraphy of the Upper Rogov, M.A., Zakharov, V.A., Ershova, V.B., 2011. De- Jurassic and Lower Cretaceous deposits on Paksa tailed stratigraphy of the Jurassic–Cretaceous Peninsula, Anabar Embayment (north of the boundary beds of the Lena River lower reached Middle Siberia), in: Jurassic and Cretaceous based on ammonites and Buchiids. Stratigr. Geol. paleobiogeography and biostratigraphy of Sibe- Correl. 19, 641–662. ria. Nauka, Moscow, pp. 56–99 (in Russian).

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The closing age of Himalayan Tethys: New evidence from planktic foraminifera

G.B. Li

China University of Geosciences, Beijing 100083, China; e-mail: [email protected]

The Yadong area was located at the residual which conformably contact each other. Abundant basin of the Neotethys during the Paleogene, benthic and planktic foraminifera are respectively which develops a set of youngest marine deposi- revealed in the Limestone and Shale members tion of the Tethyan Himalayas, and therefore the (Fig. 2). This paper focuses on the planktic foram- biostratigraphic data from the Tingri-Gamba- iniferal biostratigraphy of the Shale Member. Yadong area are essential to constrain the age of Examination of foraminiferal tests and thin- the India–Asia collision. section fossils of the Shale Member has yielded Planktic foraminifera study is usually con- 135 species of 28 planktic foraminiferal genera, sidered to be one of the most important methods and ten planktic foraminiferal biozones were to determine the age of Meso-Cenozoic marine recognized, in ascending order: M. formosa for- sediments and thus can be used to define the mosa, M. aragonensis, A. pentacamerata, H. nut- age of latest sediments in Tethyan Himalayas, talli, G. subconglobata subconglobata, M. lehneri, which can provide well-constrained age of the O. beckmanni, T. rohri, G. semiinvoluta, and India–Asia collision (Wan, 1990; Willems et al., T. cerroazulensis s.l. zones. The planktic forami- 1996; Rowley, 1998; Wang et al., 2002; Li and nifera retrieved from the Shale Member give an Wan, 2003; Li et al., 2004, 2005, 2006; Najman et Eocene age, spanning the interval from the mid- al., 2010). dle Ypresian to the latest Priabonian (P7–P17, A detailed investigation of planktic deposited ~52–34 Ma) and indicating that the fi- foraminfers was firstly provided for the newly nal closure of the Tethys seaway in this region discovered marine horizon (Zhepure Formation should occur later than ~34 Ma. of Paleogene age) in the Gulupu section, Duina, Keywords Yadong, southern Tibet (Fig. 1). The Zhepure Planktic foraminifera, Zhepure Formation, Formation was further divided into underlying Tethyan Himalaya, Gulupu, Yadong, Priabonian, Eo- Limestone Member and overlying Shale Member, cene.

Fig. 1. Geological setting and locality of the studied section. 93

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Fig. 2. The representative species of planktic foraminiferal assemblages from the Gulupu section. 1–5 – Globigerina lozanol Colom; 4–6 – Morozovella spinulosa (Cushman); 7–9, 13–15 – Morozovella aequa (Cushman et Renz); 10–12 – Mo- rozovella aragonensis (Nuttall); 16–21 – Turborotalia boweri (Bolli); 22–24 – Turborotalia cerroazulensis possagnoensis (Toumarkine et Bolli); 25–30 – Turborotalia cerroazulensis pomeroli (Toumarkine et Bolli); 31–33 – Globorotaloides eovariabilis Huber et Pearson; 34–36 – Globigerina senni (Beckmann); 37–39 – Morozovella conicotruncata (Subbotina); 40–42 – Acarinina primitiva (Finlay). Scale bar equals 100 µm.

References

Li, G.B., Wan, X.Q., 2003. Eocence microfossils in Li, G.B., Wan, X.Q., Liu, W.C., 2005. Paleogene micro- southern Tibet and the final closing of the Tibet– paleontology and basin evolution of southern Tethys. J. Stratigr. 27, 99–108. Tibet. Geological Publishing House, Beijing. Li, G.B., Wan, X.Q., Ding, L., Liu, W.C., Gao, L.F., Li, X.H., Wang, C.S., Luba, J., Hu, X.M., 2006. Age of 2004. The Paleogene foreland basin and sedimen- tary responses in the southern Tibet: Analysis on initiation of the India–Asia collision in the east- sequence stratigraphy. Acta Sedimentol. Sinica central Himalaya: A discussion. J. Geol. 114, 637– 22, 455–464. 640. 94

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Najman, Y., Appel, E., Boudaghe-Fade, M.B., Bown, thys–Himalayan sea. Acta Micropalaeontol. Sini- P., Carter, A., Garzanti, E., Godin, L., Han, J.T., ca 7, 169–186. Liebke, U. Oliver, G., Parrish, R., Vezzoli, G., Wang, C.S., Li, X.H., Hu, X.M., Jansa, L., 2002. Latest 2010. The timing of India–Asia collision: Geolog- marine horizon north of Qomolangma (Mt. Ever- ical, biostratigraphic and palaeomagnetic con- est): Implications for closure of Tethys seaway straints. J. Geophys. Res. 115, B12416. and collision tectonics. Terra Nova 14, 114–120. Rowley, D.B., 1998. Minimum age of initiation of col- Willems, H., Zhou, Z.Y., Zhang, B.G., Gräfe, K.-U., lision between India and Asia north of Everest based on the subsidence history of the Zhepure 1996. Stratigraphy of the Upper Cretaceous and Mountain section. J. Geol. 106, 229–235. Lower Tertiary strata in the Tethyan Himalayas Wan, X.Q., 1990. Cretaceous–Early Tertiary foraminif- of Tibet (Tingri area, China). Geol. Rundschau era of Xizang (Tibet) and evolution of the Te- 85, 723–754.

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Revised stratigraphy of Indus Basin (Pakistan): Sea level changes

M.S. Malkani

Geological Survey of Pakistan, Upper Chattar 130 D, str. 16, Muzaffarabad, Azad Kashmir, Pakistan; e-mail: [email protected]

The Indus Basin is located in the central and overlain by the Sakesar Formation (its lateral fa- eastern part of Pakistan and further subdivided cies substitution is the Lockhart Formation). The into the uppermost (Khyber–Hazara–Kashmir), Eocene Kuldana Group represents fine clastic upper (Kohat–Potwar), middle (Sulaiman) and Chorgali Formation and Kuldana Formation lower (Kirthar) basins. The Indus Basin is situat- comprising red and varicoloured mudstone, ed in the west and north of Indo-Pak subconti- sandstone, and dolomitic limestone. In this ba- nent, which belongs to Gondwana lands (south- sin, first clastic material derived from the north ern earth). The sediments of Pakistan underwent showing first and feeble collision of Indo-Pak significant tectonic deformation during the colli- plate with Asia. The lower part of the Kuldana sion of Asian and Indo-Pak continental plates Formation is mostly continental; it is correlated that started in the latest Cretaceous. As a result, with the Toi and Kingri formations of the mid- strata were folded, faulted and elevated along dle Indus Basin. The upper part of the Kuldana with many variations of sea level (Fig. 1). Formation shows the transgression of the sea. It is correlated with the Habib Rahi, Domanda, Revised stratigraphy of the Khyber-Hazara- Pirkoh and Drazinda formations of the Kahan Kashmir (uppermost Indus) Basin Group of the middle Indus Basin. The next The uppermost Indus Basin is the lateral ex- member of northern stratigraphic succeccion is tension of the upper Indus Basin in the down- the Miocene–Pliocene Murree Formation com- ward slopes. In the upper Indus Basin, the alter- posed of fine to coarse clastic rocks, showing nating terrestrial and marine conditions were hard collision of Indo-Pak with Asia. The Soan dominant, while the marine conditions were Group is represented by the Pleistocene Lei common in the uppermost Indus Basin. The ex- Formation with mainly conglomerate and coarse ample is the Datta Formation, which was depos- clastic facies, and the Holocene Soan Formation ited in terrestrial environments in the upper In- comprising clay, sandstone and subordinate dus Basin and marine environments in the conglomerate and relatively fine clastic facies. uppermost Indus Basin. There are some problems in correlation of The comprehensive and revised stratigraph- the Murree, Kamlial, Chinji, Nagri and Dhok Pa- ic succession in the southern part of the Khyber- than formations, especially in Azad Kashmir Hazara-Kashmir (uppermost Indus) Basin com- and northern Potwar. So, the Murree Formation prises the Hazara and Tanawal Quartzite for- is the senior synonym of the Kamlial Formation. mations (Precambrian), the Abbottabad and Thus, the revised succession in the Khyber- Hazira formations (Cambrian), the Chalk Jabbi Hazara-Kashmir areas are the Murree and Soan Formation (Triassic), the Datta and Samanasuk formations, and in the Potwar area – the Murree, formations (Jurassic), and the Chichali and Ka- Chinji, Nagri and Dhok Pathan formations of the wagarh formations (Cretaceous). Potwar Group. In the Khyber area, the for- In the northern part, the succeccion includes mation names are based on local names; it needs the Panjal Formation with volcanic rocks, the the revision and correlation to the Hazara- Indus Formation with bauxite, chamosite and Kashmir area of the uppermost Indus Basin. laterite of latest Cretaceous age, and the latest Cretaceous to Late Paleocene Hangu Formation. Revised stratigraphy of the Kohat-Potwar The Patala Formation is a lateral facies substitu- (upper Indus) Basin tion of the Hangu Formation; its age is latest Indo-Pakistan shield is represented by the Cretaceous to Early Paleocene, because it is well Precambrian Nagar Parker granite in south- correlated with the Vitakri coal of Kingri area in ern/lower Indus Basin and the Kirana Group the Sulaiman Basin. The Hangu Formation is composed of slate, quartzite and igneous rocks

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Fig. 1. Mesozoic and Cenozoic sea level curves for Sulaiman (middle Indus) and Kohat-Potwar (upper Indus) basins of Pakistan.

in the northern/upper Indus Basin. Stratigraphic na (light green dolomite and shale), Baghanwala succession in central and western Kohat sub- (red shale alternated with flaggy sandstone), basin of the Kohat-Potwar Basin is following: the and Khisor (gypsum with shale and dolomite) Precambrian Salt Range Formation composed of formations; the Permian Tobra (tillite conglom- marl, gypsum, salt, and shale; the Cambrian erate and sandstone), Dandot (sandstone and Khewra (purple to brown sandstone), Kussak shale), Warcha (sandstone with some shale), (greenish grey and glauconitic sandstone), Juta- Sardhi (shale with minor sandstone and silt-

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 stone), Amb (sandstone, limestone, and shale), Sulaiman Basin stratigraphy. The sedimentary Wargal (limestone and dolomite), and Chidru section in Pezu to Parachinar area (Kurram (shale and sandstone) formations; the Triassic Agency) is composed of interfingering strata of Mianwali (shale, limestone, and sandstone), the middle and upper Indus basins. Tredian (sandstone), and Kingriali (dolomite Revised stratigraphy of the Sulaiman (middle and limestone with minor shale) formations; the Indus) and Kirthar (lower Indus) basins Jurassic Datta (fluvial sandstone with minor shale), Shinawari (shale, limestone, and sand- The Sulaiman Basin shows the different up- stone), and Samana Suk (limestone with subor- dated succession of lithological units (Malkani dinate shale) formations; the Cretaceous Chicha- 2010, 2012; Fig. 1). The Triassic Khanozai Group li (glauconitic sandstone and shale), Lumshiwal is represented by the Gwal Formation with shale (white sandstone and shale), and Kawagarh and thin bedded limestone and the Wulgai For- (limestone, marl, and shale) formations; the pre- mation composed of shale with medium bedded Tertiary Indus Formation composed of bauxite, limestone. The Jurassic Sulaiman Group is rep- laterite, chamositic and glauconitic iron; the lat- resented by the Spingwar Formation consisted est Cretaceous–Paleocene Hangu Formation of shale, marl and limestone with some igneous with sandstone, shale, and coal (the synonym is sills/dykes found close to the western Indus Su- the Patala Formation), the Sakesar Formation ture, the Loralai Formation composed of lime- composed of nodular limestone with minor stone with minor shale, and the Chiltan For- shale (synonyms are the Lockhart and Margala mation with limestone. The Cretaceous Parh hill limestone), the Panoba Formation with Group is represented by the Sembar Formation shale, the Gurguri Formation (synonym is the with shale, the Goru Formation with shale and Chashmai Formation, which is coeval with the marl, and the Parh Formation composed of Toi Formation of Sulaiman), the Shekhan For- limestone with some volcanic sills/dykes found mation with limestone and shale, the Bahadurk- close to the western Indus Suture); the Fort hel Formation with halite salt, the Jatta For- Munro Group is represented by the Mughal Kot mation composed of gypsum with minor clay, Formation consisted of shale/mudstone, sand- the Habib Rahi Formation composed of lime- stone, marl and limestone with some volcanics stone with marl and shale (coeval with the Ko- found close to western Indus Suture, the Fort hat Formation), and the Domanda Formation Munro Formation with limestone, the Pab For- (synonym is the Sirki Formation). mation composed of sandstone with subordinate In Potwar, Hazara, Kashmir and eastern shale with some evidences of Deccan volcanism, Kohat, the Kuldana Group includes the Chorgali and the Vitakri Formation consisded of red Formation with shale and dolomitic limestone muds which is the host of dinosaurs and grey to and Kuldana Formation composed of red and white sandstone. The Paleocene Sangiali Group varicoloured shale, sandstone, and dolomitic is represented by the Sangiali Formation com- limestone. The Miocene–Pliocene Murree For- posed of limestone, glauconitic sandstone and mation comprises sandstone, conglomerate, and shale, the Rakhi Gaj Formation with the Girdu shale (synonym is the Kamlial Formation), the Member composed of glauconitic and hematitic Chinji Formation consists of red clays, sandstone sandstone and the Bawata Member composed of and conglomerate, and the Nagri Formation is alternation of shale and sandstone, and by the composed of sandstone with minor shale and Dungan Formation with limestone and shale. conglomerate. The Pliocene Dhok Pathan For- The Eocene Chamalang (Ghazij) Group is repre- mation comprises clays with subordinate sand- sented by the Shaheed Ghat Formation with stone and conglomerate. The Pleistocene Lei shale, the Toi Formation composed of sand- Formation contains conglomerate. The Holocene stone, shale, rubbly limestone and coal, the Soan Formation is composed of clay, conglom- Kingri Formation composed ofred shale/mud, erate, and sandstone; the subrecent and recent grey and white sandstone, the Drug Formation surface rocks are represented by alluvium, col- composed of rubbly limestone, marl, and shale, luvium and eolian deposits (Fig. 1). The Waziri- and the Baska Formation with gypsum beds and stan–Kurram areas show the extension of shale; the Kahan Group is represented by the

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Habib Rahi Formation with limestone, marl, and ternary, but it varies in the Tertiary. The Paleo- shale, the Domanda Formation composed of cene Ranikot Group is represented by the shale with one bed of gypsum, the Pir Koh For- Khadro Formation composed of sandstone, mation with limestone, marl, and shale, and the shale, limestone, and volcanics derived from Drazinda Formation composed of shale with Deccan volcanism, the Bara Formation com- subordinate marl and Sulaimanitherium dhanotri posed of sandstone with minor limestone, coal (Basilosauridae) – the king of basal whale. The and volcanics, and the Lakhra Formation with Oligocene–Pliocene Vihowa Group is represent- limestone and shale. The Early Eocene Cha- ed by the Chitarwata Formation composed of malang/Ghazij Group (north source) has been grey ferruginous sandstone, conglomerate and recognized in northern Kirthar. In southern mud with Baluchitherium osborni, the largest land Kirthar, the Laki Group is represented by laterit- mammal Buzdartherium gulkirao, and fresh water ic clay, ochre, coal and limestone of the Sohnari crocodile Asifcroco retrai, the Vihowa Formation Formation and shale and limestone of the Laki composed of red ferruginous shale/mud, sand- Formation. The Kirthar Group is represented by stone and conglomerate, the Litra Formation the Kirthar Formation composed of shale and comprised of greenish grey sandstone with sub- limestone, and the Gorag Formation mainly ordinate conglomerate and mud with host of comprised resistant limestone. The Oligocene large proboscidean Gomphotherium buzdari, and Gaj Group is represented by the Nari Formation the Chaudhwan Formation composed of mud, composed of ferruginous sandstone, shale, lime- conglomerate and sandstone. The Pleistocene stone, and the Gaj Formation composed of shale Dada Formation is composed of conglomerate with subordinate sandstone and limestone. The with subordinate mud and sandstone, subrecent Miocene–Pliocene Manchar Group is represent- and recent fluvial, eolian and colluvial deposits. ed by sandstone, conglomerate, and mud. Sub- In general, the Kirthar Basin shows the recent and recent surface sediments are repre- same succession of lithological units like in the sented by alluvium, colluvium, eolian, Sulaiman basin during the Mesozoic and Qua- lacustrine, and evaporite deposits.

References

Malkani, M.S., 2010. Updated stratigraphy and min- Malkani, M.S., 2012. Revised lithostratigraphy of eral potential of Sulaiman (middle Indus) basin, Sulaiman and Kirthar basins, Pakistan, in: Earth Pakistan. Sindh Univ. Res. J., Sci. Ser. 42(2), 39– Sciences Pakistan 2012, Baragali Summer Cam- 66. pus, University of Peshawar, June 23–24, 2012, Pakistan: Abstract Volume and Program. J. Him- alayan Earth Sci. 45(2), 72.

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Stratigraphy of Jurassic–Cretaceous rocks of Thung Yai–Khlong Thom area, peninsular Thailand

N. Teerarungsigul

Department of Mineral Resources, Rama 6, Ratchatawi, Bangkok 10400, Thailand; e-mail: [email protected]

The Thung Yai–Khlong Thom area is locat- hummocky and flaser bedding. The fossils as- ed in the peninsular Thailand covering approx- semblages in the lower part reflect lagoonal en- imately 1.160 sq. km. The topography of the area vironment gradually changing over to lacustrine is generally high mountainous and undulating to the fluvial environment. The rocks of the Lam landforms. The present investigation embraces Thap Formation were believed to be deposited defining the lithostratigraphy of non-marine in meandering stream, floodplain, and alluvial Mesozoic rocks distributed in the Thung Yai– fan environments. The paleo-currents are mainly Khlong Thom area, southern Thailand. Addi- characterized by east to west directions (285 di- tional attempt has been made to analyze the sed- rections). The conglomerate and conglomeratic imentary sequences in terms of sedimentary fa- sandstone of the Sam Chom Formation com- cies and to reconstruct the depositional monly exhibit sharp contacts, graded bedding, environment in the area. The oldest rocks of and finning upward the sequence in some areas, Thung Yai–Khlong Thom area is believed to be reflecting the braided stream and alluvial fan or- the Permian limestone and marine Triassic igins. The fine-grained sandstone is character- rocks. These rocks unconformably underlie the ized by red to reddish brown color with com- sedimentary sequences of non-marine Mesozoic monly trough and planar cross-bedding of the rocks of the Trang Group. Phun Phin Formation indicating braided stream The Jurassic–Cretaceous rocks (Trang with east direction of the paleocurrent in the Group) unconformably overlie the Permian to lower part, and northeast direction in the upper Triassic basement rocks. This group consists of part. The sharp contact, matrix-supported, and four formations: the Khlong Min Formation, the variety of clasts in the fanglomerate of the upper Lam Thap Formation, the Sam Chom Formation, part of the Phun Phin Formation indicate debris and the Phun Phin Formation (in ascending or- flow origin. From stratigraphic and paleontolog- der). The total thickness varies from 65 to ical evidences, the age of the Trang Group 1.145 m. should be determined as early Middle Jurassic– The Khlong Min Formation is represented Late Cretaceous. by mudstone intercalated with fossiliferous Keywords limestone with abundant vertebrate and inver- Jurassic–Cretaceous rocks, Thung Yai–Khlong tebrate fossils, and primary structures, i.e., Thom, peninsular Thailand.

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Palynology and magnetostratigraphy of Deccan volcanic associated sedimentary sequence of Amarkantak Group in Central India: Age and paleoenvironment

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

PG Department of Geology, RTM Nagpur University, Law College Square, Amravati Road, Nagpur 440001, India; e-mail: [email protected]

The Deccan Continental Flood Basalt the important and newly recorded palyno- (DCFB) province covers an area of about 500.000 morphs are Ephedripites spp., Crenwellia sp. A, km2 in central and western India. The study area Dipterocarpuspollenites retipilatus, Farabeipollis falls in Chhindwara–Jabalpur–Seoni–Mandla minutes, Intratricolpites brevis, Incrotonipollis ney- (CJSM) sector of the eastern part of the Deccan velli, Jingsupollis spp., Paleosantalaceaepites mioce- Volcanic Province (EDVP) (Yedekar et al., 1996), nicus, Proteacidites spp., Psilodiporites erdtmanii, which has ~431 m thick lava pile comprising of Racemonocolpites maximus, Retibrevitricolporites 34 flows and eight formations, namely the spp., Retidiporites megadalensis, Scollardia conferta, Mandla, Dhuma, Piperdehi, Linga, Multai, Am- Sparaganiaceaepollenites spp., Spinizonocolpites arwara, Khampa, and Kuleru formations (as- spp., Tribrevicolporites sp., and Tricolpites spp. cending stratigraphic order) (Geological Survey Overall, palynological assemblage of MKWS is of India, 2000). Detailed palynological study of dominated by Ephedripites, Proxaperties and 23 intertrappean sections at nine stratigraphic Spinizonocolpites. levels was carried out to understand the flora, The overlying MKFF intertrappean domi- age and depositional environmental of the sed- nated by chert yielded palynomorphs mainly iments. For better age constraint, paleomagnetic from two sections, namely the Nala section and study of associated volcanic flows was also car- the section near Keriya village. The palynologi- ried out. cal taxa in MKFF are represented by 11 genera The lowermost intertrappean, i.e. Mohgaon and 32 species. Some of the important taxa rec- Kalan Well Section (MKWS), is mainly encoun- orded from MKFF are Aquilapollenites ben- tered in the dug wells, and the upper intertrap- galensis, Azolla cretacea, Gabonisporis vigourouxii, pean, i.e. Mohgaon Kalan Fossil Forest (MKFF) Proxapertites operculatus, Spinizonocolpites echina- rich in megaflora, is exposed in an area of about tus, Jiagsupollis spp., and the pollen of Nor- 100 km2. Both these intertrappeans occur in be- mapolles group. Dominating forms are Aqui- tween the Mandla and Dhuma formations. lapollenites bengalensis, Azolla cretacea and Gabonisporis vigourouxii. Palynology Overall, palynological assemblage from For palynological investigations, nine new both intertrappean deposits shows close similar- dug well sections, namely the Government Well, ity, but palynoflora of MKWS is more diverse. Srivastava Well, Shriwas Well, Lodhi Well, Ha- The presence of Aquilapollenites bengalensis, Az- kim-1 Well, Jamil Well, Idbi bano Well, Hakim olla cretacea, Gabonisporis vigourouxii, Crenwellia Well, and Vishwakarma Well represented by sp. A, Scollardia conferta, Farabeipollis minutes and various lithofacies (green shales, highly fossilif- Jiagsupollis spp. indicate Maastrichtian age for erous black lignitic shales, and carbonaceous both intertrappean deposits. The presence of clay), were studied. The samples from six dug dominating Spinizonocolpites (Nypa) and wells (Government Well, Srivastava Well, Proxapertites (Arecaceae) suggests estuarine con- Shriwas Well, Lodhi Well, Hakim Well, and ditions at the time of deposition. High concen- Vishwakarma Well) yielded very good concen- tration of fungal remains and epiphyllous fungi tration of palynomorphs. The palynoflora is rep- (Microthyriaceae (Phragmothyrites), Dicellaespo- resented by pteridophytes, gymnosperms, angi- rites fusiformis, and Frasnacritetrus indicus) indi- osperms, fungal spores, fungal fruit bodies, and cates the prevalence of humid conditions (Cook- algal remains. The recovered palynomorphs are son, 1947; Dilcher, 1965; Selkirk, 1975; Samant assigned to 35 genera and 63 species. Some of and Mohabey, 2009).

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The Jhilmili intertrappean occurs in be- purensis. The stratigraphic position of the Pindrai, tween the Dhuma and Pipardehi formations. Surli and Tenadi intertrappean deposits is higher Paleocene intertrappean deposits comprise for- than the Jhilmili intertrappean, which has been aminifers of P1a Zone (Keller et al., 2009). They dated as Paleocene on the basis of foraminifera of do not yield palynomorphs, but contain abun- P0–P1 age (Keller et al., 2009). Palynology and dant diatoms and sponge spicules. The succes- stratigraphy suggest Paleocene age for the Pin- sively overlying Machagora, Bhutera and Loha- drai, Surli and Tenadi intertrappean deposits. ra intertrappean deposits occur in between the Magnetostratigraphy Pipardehi and Linga formations, and the Umaria Isra, Imlikheda and Ghat Parasia intertrappean The study of magnetic polarity of 19 volcan- deposits occur in between the Linga and Multai ic flows associated with intertrappean beds at formations. They yielded biodegraded organic nine stratigraphic levels between RL 525 to 850 m material and Glomus-like mycorrhizal fungi on- was carried out. The lowermost volcanic flow at ly. The palynoflora is recorded from the succes- the contact of Precambrian basement and suc- sively overlying Pindrai, Surli and Tenadi inter- cessively overlying flow, i.e., upper flow of trappen beds occur in between the Multai– MKWS, and the lower flow of Jhilmili indicate Amarwara, Amarwara–Khampa and Khampa– normal polarity. The upper flow of MKFF shows Kuleru formations, respectively. The important mixed polarity. The basaltic flow overlying palynotaxa recorded from these intertrappean Jhilmili intertrappean, which contains foramini- deposits are Cyathidites australis, Ericipites sahnii, fers of P1a Zone of Early Paleocene age, indi- Haloragacidites amolosus, Rhoipites spp., Psilodi- cates reverse polarity. The volcanic flow under- porites erdtmanii, Retidiporites spp., Liliacidites lying the Ghat Parasia intertrappean indicates spp., Incrotonipollis neyvelli, Longapertites reverse polarity. After that, all the flows, i.e., vaneendenburgi, Mulleripollis bolpurensis, Palmaeo- flow overlying the Ghat Parasia, and upper and pollenites spp., Proxapertites operculatus, and lower flows of Pindrai, Surli and Tenadi inter- Sparganiaceaepollenites. Spinizonocolpites and trappean deposits, indicate normal polarity. The Proxapertites, which were dominant in the low- magnetic polarity data indicate 30N–29R–29N ermost intertrappean, are not present in these in- sequence in the study area. tertrappean deposits. These intertrappeans are Summing up, palynology and magnetic po- also characterized by high concentration of fun- larity data in the study area indicate deposition gal fruit bodies of fungi microthyriaceae (Phrag- of sediments in humid–semiarid–sub-humid mothyrites) as well as Pediastrum and algae climate under estuarine to increasingly fresh wa- Kalviwadithyrites saxenae. The overlying Tenadi ter depositional conditions during the chrons intertrappean in between the Khampa and Kule- 30N–29R–29N of Late Maactrichtian to Early ru formations yielded mainly Mulleripollis bol- Paleocene.

References

Cookson, I.C., 1947. Plant microfosssils from the lig- Samant, B, Mohabey, D.M., 2009. Palynoflora from nite of Kergulen Archipelago, in: BAN2ARE Re- Deccan volcano-sedimentary sequence (Creta- port, Ser. A, II, pp.127–148. ceous–Palaeocene transition) of central India; Dilcher, D.L., 1965. Epiphyllous fungi from Eocene implications for spatio-temporal correlation. J. deposits in western Tennessee USA. Palaeonto- Biosci. 34, 811–823. graphica B 116, 1–156. Selkirk, D.R., 1975. Tertiary fossil fungi from Kiandra, Geological Survey of India, 2000. District resource New South Wales. Proc. Linn. Soc. N.S.W. 100, map, Chhindwara District, Madhya Pradesh. 70–94. Keller, G., Adatte, T., Bajpai, S., Mohabey, D.M., Yedekar, D.B.S., Aramaki, T., Fujii, T., Sano, T., 1996. Widdowson, M., Khosla, A., Sharma, R., Khosla, Geochemical signature and stratigraphy of S.C., Getsch, B., Fleitmann, D., Sahani, A., 2009. Chhindwara–Jabalpur–Seoni–Mandla sector of K–T transition in Deccan Traps of Central India the Eastern Deccan Volcanic province and prob- marks major marine seaway across India. Earth lem of its correlation. Gondwana Geol. Maga- Planet. Sci. Lett. 282, 10–23. zine, Spec. Vol. 2, 49–58.

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Bio- and lithostratigraphy of the Jurassic–Cretaceous boundary deposits in the Komsomolsk section (Russian Far East)

O.S. Urman1, O.S. Dzyuba1, B.N. Shurygin1,2 and G.L. Kirillova3

1Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: [email protected] 2Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia 3Kosygin Institute of Tectonics and Geophysics, Far Eastern Branch of RAS, Kim Yu Chen str. 65, Khabarovsk 680000, Russia

The Komsomolsk section (also known as the here, its thickness reaches 700 m. The rhythmic Pivan section) crops out in a series of exposures alternation of sand and siltstone and the subor- at the right bank of the Amur River opposite to dinate layers and lenses of gravelite and con- Komsomolsk-on-Amur and runs for over 18 km. glomerate are characteristic for the stratum. In 1960s, the clastic strata of 6000 m thick were During the 2001 Russian–Japanese expedition to subdivided into six formations in the area near the Komsomolsk section, this stratum was sam- Komsomolsk-on-Amur, namely the Ulbin For- pled for radiolarian. In the NE stratum’s out- mation, the Silinka Formation, the Padali For- crop, the cherty siltstone with felsic tuff layers mation, the Gorin Formation, the Pioneer For- yielded, according to K. Isida (Kirillova et al., mation, and the Pivan Formation. The latter 2002), the Late Tithonian radiolarians. The same three were usually joined into the Komsomolsk stratum contains an exotic block of tectonic me- Group (e.g., Vereshchagin, 1977). The section’s lange (120 m); this block comprises chert, cherly folded structure was considered as a limb of a mudstone slate, and limestone and produced the large anticline with a dominant monoclinal Early–earliest Late Jurassic radiolarians. southeast dip. The anticline hinge was suggest- The middle siltstone stratum comprises silt- ed to be northwesterly off the Komsomolsk sec- stone, silty sandstone, and a subordinate tion. amount of small-grained and fine-grained sand- Later, during the more detailed mapping stone. The most complete section of the siltstone and investigation of the folding character, a set stratum (stratotype of the former Pioneer For- of large isoclinal folds locally faulted was re- mation) was described in the Komsomolsk sec- vealed. It was assumed that the sediments pre- tion; here, its thickness reaches 1100 m. For this viously ascribed to the Ulbin, Padali and Pioneer stratum, vast lists of bivalves (Buchia, Anopaea, formations, having similar rock compositions, Inoceramus, and Lima) were compiled by are actually the same single unit. This conclu- V.N. Vereschagin, T.D. Zonova, A.A. Kapitsa, sion was then confirmed by different fauna, L.D. Tretiakova, V.P. Pokhialainen, and which in all the earlier isolated formations are K.V. Paraketsov along with sparse record of represented by the Volgian–Valanginian species ammonite (Thurmanniceras? thurmanni) and oc- (e.g., Kirillova, 2009). The Silinka and Pivan casional plant remnants (e.g., Vereshchagin, formations occurring in syncline hinges also 1977; Kirillova, 2009). Only a few of them have turned out to be a single unit having a higher been illustrated: Buchia aff. jasikovi, Anopaea stratigraphic position. Finally, three nameless pivanensis, A. stempeli, A. savrasovi, A. gerasimovi, strata were recognised: (1) the stratum of Inoceramus vereshagini, I. cf. vereshagini, I. glasun- rhythmic alternation of Volgian age, (2) the sili- ovi, I. koslovi, I. acuticostatus, I. subardonensis, and ceous–siltstone stratum of Volgian–Valanginian Lima (Lima) aff. consobrina (e.g., Pokhialainen, age, and (3) the sandstone Valanginian stratum 1969; Kapitsa, 1978; Sey et al., 2004). (e.g., Kirillova et al., 2002; Kirillova, 2009). The The upper sandstone stratum conformably rhythmic alternation stratum is correlated with overlies the siltstone one. The former is domi- the former Gorin Formation. nated by medium-grained coarse-layered sand- The most complete section of the rhythmic stone with sparse coarse-grained sandstone, alternation stratum was described at the right gravelite, sedimentary breccia, siltstone, and bank of the Amur River near the Pivan wharf; beds of alternation of sandstone and siltstone.

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The stratum sequence is most fully presented in shells of B. terebratuloides, B. fischeriana (close to the Komsomolsk section; however, it lacks there the bottom), B. unschensis, and probably B. aff. its upper horizons. The stratum’s total thickness jasikovi illustrated by Sey et al. (2004). Some of is about 800 m. The publications contain illustra- inoceramids, illustrated by A.A. Kapitsa (1978), tions of bivalves Anopaea amurensis and Inocer- were found in this part of the section (for dis- amus quasineocomiensis (Kapitsa, 1978), and am- cussion see Urman et al., 2014). Beds with B. vol- monite Sarasinella cf. varians (Sey et al., 2004). gensis correlate with the eponymous Buchia zone Apparently, the same strata (the formation was of Siberia, the Pechora River basin, and Svalbard not mentioned) yielded Buchia keyserlingi and (e.g., Zakharov, 1981, 1987). B. ex gr. keyserlingi (Sey et al., 2004). Beds with B. inflata and B. keyserlingi were An analysis of the stratigraphic distribution established in the “sandstone stratum”. They are of the Buchia assemblages in the Komsomolsk comparable to two buchiazones widespread in section allowed us to establish four successive the Boreal sections: the B. inflata Zone (lower beds with Buchia (Urman et al., 2014). upper part of the Lower Valanginian; in some Beds with B. terebratuloides were identified regions, it also includes the uppermost Berri- in the “rhythmic alternation stratum” in which asian) and the B. keyserlingi Zone (upper part of B. terebratuloides has been found along with the Lower Valanginian). A more detailed subdi- Buchia sp. ind., Malletia sp. ind., and an indefin- vision of these beds in the Komsomolsk section able fragment of ammonite. The upper bounda- did not succeed, because the B. keyserlingi was ry of the beds is defined by the change of buchi- seen rarely and was not recorded separately id assemblages and the first appearance of from B. inflata. Therefore, it is possible that beds B. unschensis. These beds are comparable with with B. inflata and B. keyserlingi embrace here on- the B. obliqua Zone, which was recognised in the ly the B. inflata Zone. same volume as the lowermost Upper Volgian Cephalopod remains in the Komsomolsk Craspedites okensis ammonite Zone in Siberia, in section are very rare. However, certain intervals the Pechora River basin, and on Franz Josef of the section may be correlated with the Berri- Land (Rogov and Zakharov, 2009). At the base asian (based on the findings of Pseudosub- of the B. obliqua Zone, according to V.A. Zakha- planites? sp.) and Valanginian (the findings of rov (1981, 1987), there are representatives of the Sarasinella cf. varians). The complete absence of index species along with B. terebratuloides. belemnites in the Komsomolsk section possibly Beds with B. unschensis and B. terebratuloides may be explained by the relatively deep envi- were identified in the middle part of the “silt- ronment of its formation. In the modern palaeo- stone stratum,” in which numerous B. terebratu- geographic scheme of the East-Asian continental loides, B. fischeriana, and B. unschensis typical of margin for the Jurassic–Cretaceous transition the Volgian–Ryazanian boundary layers have (Volgian–Valanginian), the Komsomolsk section been found. These layers in the Komsomolsk territory fits the zone of a moderately deep- section also provided sparse bivalves Lima sp. water continental slope (Kirillova, 2009). Nota- ind. and Inoceramus sp. ind., and a Tethyan am- bly, cylindroteuthid belemnites preferred to in- monite provisionally determined as Pseudosub- habit shallow depths of probably less than 200 m planites? sp. The B. unschensis Zone has been (e.g., Dzyuba, 2013). recognised in many Boreal sections (e.g., Zakha- Thus, the stratigraphic subdivision and cor- rov, 1981, 1987; Jeletzky, 1984); this zone corre- relation of the Komsomolsk section with sec- sponds to the beds with B. unschensis and B. tere- tions in adjacent regions is based mainly on bratuloides of East Greenland (Surlyk, 1982), and buchiids. An analysis of the stratigraphic distri- these are the same beds as identified in the bution of the Buchia assemblages allowed us to Komsomolsk section. establish here a sequence of beds with Buchia Beds with B. volgensis were recognised at that is well comparable with the buchiid zonal the top part of the “siltstone stratum” by finds of scales of many Boreal regions. Ammonite find- typical Berriasian B. volgensis and B. okensis. The ings permitted us to correlate some intervals of latter species is found only in the lower half of the section with the Berriasian and the Val- the beds. The beds also contain scattered rare anginian. On the basis of the revision of the pal-

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific aeontological characteristics and biostratigraph- dicate the presence of the large synclinal fold in ic studies, the Komsomolsk section has gained the studied outcrops: while approaching toward significantly updated ages of strata recognised the alleged location of the large synclin’s hinge, here. It was established that the “rhythmic alter- the layers gradually youthen from both the nation stratum” is an earliest Late Volgian in southwest and northeast. age, the “siltstone stratum” is a latest Late Vol- gian–Ryazanian, and the “sandstone stratum” is This is a contribution to the IGCP608 and pro- an Early Valanginian. Palaeontological data in- gram 30 of the Presidium of the RAS.

References

Dzyuba, O.S., 2013. Belemnites in the Jurassic– Cretaceous inocerams of Northwest USSR. Cretaceous boundary interval of the Mauryn’ya SVKNII, Magadan, pp. 124–162 (in Russian). and Yatriya River sections, Western Siberia: Bio- Rogov, M., Zakharov, V., 2009. Ammonite and bi- stratigraphic significance and dynamics of taxo- valve based biostratigraphy and Panboreal corre- nomic diversity. Stratigr. Geol. Correl. 21(2), 189– lation of the Volgian Stage. Sci. China Ser. 214. D-Earth Sci. 52(12), 1890–1909. Jeletzky, J.A., 1984. Jurassic–Cretaceous boundary Sey, I.I., Okuneva, T.M., Zonova, T.D., et al., 2004. At- beds of Western and Arctic Canada and the las of the Mesozoic marine fauna of the Russian problem of the Tithonian–Berriasian stages in the Far East. VSEGEI, St. Petersburg (in Russian). Boreal Realm. Geol. Assoc. Canada, Spec. Pap. 2, Surlyk, F., Zakharov, V.A., 1982. Buchiid bivalves 175–255. from the Upper Jurassic and Lower Cretaceous Kapitsa, A.A., 1978. New species of the Lower Creta- of East Greenland. Palaeontol. 25, 727–753. ceous inoceramids of the Lower Amur region, in: Urman, O.S., Dzyuba, O.S., Kirillova, G.L., Shurygin, Biostratigraphy of the Southern Far East (Phan- B.N., 2014. Buchia faunas and biostratigraphy of erozoic). Vladivostok, pp. 65–77 (in Russian). the Jurassic–Cretaceous boundary deposits in the Kirillova, G. L., Natal’in, B.A., Zyabrev S.V., et al., Komsomolsk section (Russian Far East). Russ. J. 2002. Upper Jurassic–Cretaceous deposits of East Pac. Geol. 8(5), 346–359. Asian continental margin along the Amur River, Vereshchagin, V.N., 1977. Far East Cretaceous System. in: Kirillova, G.L. (Ed.), Field excursion guide- Nedra, Leningrad (in Russian). book. Khabarovsk. Zakharov, V.A., 1981. Buchiids and biostratigraphy of Kirillova, G.L. (Ed.), 2009. Middle Amur sedimentary the Boreal Upper Jurassic and Neocomian. Nau- basin: Geology, geodynamics, and fuel-energetic ka, Moscow (in Russian). resources. DVO RAN, Vladivostok (in Russian). Zakharov, V.A., 1987. The bivalve Buchia and the Ju- Pokhialainen, V.P., 1969. Neocomian inoceramids of rassic–Cretaceous boundary in the Boreal Prov- the Anadyr–Koryak fold area, in: Jurassic and ince. Cretaceous Res. 8, 141–153.

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Environments of conservation of the dinosaurs in the Mesozoic deposits of south- eastern West Siberia (Shestakovskii Yar section)

O.N. Zlobina

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: [email protected]

A skull and partial skeleton of a small Psit- The nearby rocks are visibly homogeneous. tacosaurus named Psittacosaurus sibiricus were They are represented by light-greenish, weakly discovered in the coastal cliff of the Kiya River cemented silty sandstone or sandy silt, without near Shestakovo village (Kemerovo Oblast) in any inclusions, and with massive texture. Rare 1953. The age of the deposits comprising skeletal thin fragments of charred plant detritus were remains of the dinosaur was dated as an Early only documented using microscopic study. Par- Cretaceous. It is based on the widely spread ticle-size distribution in the sample taken from opinion that the psittacosaurs reached their ac- the surface on which psittacosaurs were stand- me in Central Asia in the Early Cretaceous, so ing or lying, demonstrates perfect symmetrical fossils of this fauna group serve as indicators of monomodal spectrum, where the moda is the this epoch. Deposits built up the coastal cliff of size of the most commonly encountered grains the Kiya River were attributed to the continental (in this case up to 9.7%) corresponds to 74 mi- Ilek Formation. According to the stratotype, its crons (Fig. 1a). This type of distribution appears distinctive feature is the intercalation of calcare- to be the most typical for the sublittoral sedi- ous clay or marl (reddish-brown or cherry-red in ments (underwater coastal slope), formed on the color, often with bluish-green or purple stains), continental shelf below the level of the lowest brown and greenish siltstone, and green fine- tide. Deposits characterized by more complex grained sandstone (Khlonova et al., 1990). The and usually bimodal curves are formed in the Ilek Formation (100–760 m thick) formed in the environments of tideland zone (upper littoral by Chulym-Yenisei facial area during the Berriasian Sverdrup et al., 1942). Spectrum changes in the and Valanginian was studied in natural out- layer lying two centimeters above (Fig. 1b). crops and drill cores, and dated by the rare Mode corresponds to the size of 176 microns, freshwater fauna, skeletal remains of the dino- and the number of clasts with such diameter is saur, spores and pollen. 8.6%. The cumulative percentage at the level of A major discovery was made in this outcrop mode (the total content of all particles with a di- in the end of 20th century. Monolithic blocks ameter smaller than that of the most common were sawed out at different levels and moved grains) is 73.5. The distribution curve becomes down to for preparation. Further layer-by-layer asymmetrical. The rocks overlying the skeletal preparation (top down) of one block revealed remains tend to be more poorly sorted (Fig. 1c). well preserved skeletal remains, similarly ori- The number of grains with the dominant diame- ented and arranged on one surface, one next to ter (148 microns) constitutes only 7%, with the the other, and belonging at least to three psitta- cumulative percentage at the level of mode be- cosaurs. In this connection, a hypothesis of their ing 69.3. At this, the content of pelitic fractions possible burial during the lifetime was suggest- (particles with a diameter smaller than 0.01 mm) ed. Such occurrences are rare and unique. More- is almost unchanged in the sediments, ranging over, a smaller animal was found in the other within 7.9–10.4% from the base to the top of the monolith block, probably belonging to a differ- monolith block. The nature of the change of the ent species. The lithological study of the nearby curves indicates the input of coarser material in- deposits provided the evidence of undisturbed to the sedimentation area from the deposits with burial of the first group of dinosaurs confirmed distribution type close to symmetric. The break- by grain size distribution and mineralogical ing rocks probably also represented facies of the composition of the sediments, studied in differ- underwater coastal slope, cropping out onto the ent layers of the section. surface as a result of significantly lowered sea-

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Fig. 1. Particle size distribution in the weakly cemented silty sandstone or sandy silt, enclosing Psittacosaurus skeletal remains.

level. The polymodal type of the distribution is type of cement was formed during postsedimen- typical for the sandstone from another monolith tary transformations by perecrystallization of block (with smaller animal) (Fig. 1d). the first type. Well crystallized calcite crystals The mineral composition of siltstone and without any micropores are observed in the in- sandstone from different sections appears to be terstices between the fragments (Fig. 2b). In identical, and it comprises calcite (36%) includ- some sites, their aggregates form basal type of ing pellets, outigenic cement and part of the cementation. clasts. Nevertheless, basal type of cementation is Small concentrations of organic carbon in not solid, and it is quickly destructed in the wa- the rocks and the absence of life traces of the ter. Scanning electron microscopy investigation benthic organisms indicate undeveloped trophic allows the determination of two types of the cal- base. It is assumed, that the herbivorous dino- careous cement (Fig. 2). The first one was saurs would roam on the slope in search of food formed in the process of sedimentation of crusts during spans of low tide, looking for food in the fouling on calcareous clastic grains as a result of niches of coastal cliff or hiding there from the biochemogenic precipitation of the microcrystal- predators. Probably, the algal mass accumulated line calcite from seawater. Crusts are round in in niches due to wave processes attracted the shape with a diameter up to 10 microns, and psittacosaurs. Thus, a group of the pasturing an- they overlap each other forming microstructures imals could be buried under the rock-fall caused similar to the roof tiles. All fragments of a ‘roof by weathering of sediments formed a steep cliff tiles’ are penetrated by frequent and equally ori- and readily swelled on the wetting. Part of ented tubular micropores (Fig. 2a). The second moved sediments occurred above the sea level

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Fig. 2. Types of the calcareous cement.

for a long time that resulted in its transformation are not observed in this section, and carbonized into reddish-brown clay silt of the weathering plant detritus of different dimensions is rare. At crust. Their color is resulted from the oxidation the same time, skeletal remains of dinosaurs, processes of Fe-, Ti-, Cr- containing minerals crocodiles, turtles, fish, birds and mammals (rep- (fayalite, amphibole, chromespinellids etc.) pre- resentatives of the orders Triconodonta and sented in clastic parts of the rocks. Several such Symmetrodonta) were revealed. According to lenticular horizons ranging in thickness from tens many experts, the extinction of the representa- of centimeters to several meters are observed in tives of Symmetrodonta occurred in the Late Ju- natural outcrops in Shestakovskii Yar. Apparent- rassic. Thus, the deposits from the Shestakovskii ly, the described events repeatedly took place on Yar section were probably formed in the latest Ju- the paleobasin coast indicating significant fluctu- rassic–earliest Cretaceous. Taking it into account, ations in sea level. The obtained results contradict the south-east regions of Western Siberia can be the continental genesis of the Ilek Formation considered as the ancestral homeland of psittaco- (Khlonova et al., 1990). Classical alluvial rhythms saurs occupied different regions of Central Asia and remains of the root system of ancient plants in the Early Cretaceous.

References

Khlonova, A.F., Papulov, G.N., Purtova, S.I., Strep- Sverdrup, H.U., Johnson, M.W., Fleming, R.H., 1942. etilova V.G., 1990. Non-marine Cretaceous of The oceans: Their physics, chemistry, and biolo- Western Siberia, in: Continental Cretaceous gy. Prentice Hall, New York. USSR. FEB AS USSR, Vladivostok.

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Session 5 Cretaceous vertebrates of Asia and the Western Pacific

Stable isotope composition of modern and fossil archosaur eggshells as a tracer of animal ecology, living environment and reproductive strategy

R. Amiot, N. Lazzerini, Ch. Lécuyer and F. Fourel

CNRS UMR 5276, Université Claude Bernard Lyon 1 and Ecole Normale Supérieure de Lyon, 2 Rue Raphaël Dubois, 69622 Villeurbanne Cedex, France; e-mail: [email protected]

Stable oxygen and carbon isotope composi- as oxygen isotope fractionations between calcite, tions of fossil remains from vertebrate mineral- body fluids and drinking water have not been ized tissues (bones, teeth, scales) have been determined yet. widely used to infer past ecologies (Clementz For this purpose, eggshell, albumen and and Koch, 2001; Amiot et al., 2010) and envi- drinking water of extant birds and crocodilians ronmental conditions (Suarez et al., 2014; Amiot have been analyzed for their oxygen and carbon et al., 2015; Domingo et al., 2015; Goedert et al., isotope compositions. Relative enrichments in 2016). Tooth enamel is of primary interest due to 18O relative to 16O between body fluids and its strong resistance to diagenetic processes, and drinking water of about +2‰ for semi-aquatic its stable oxygen and carbon isotope composi- birds and of about +4‰ for terrestrial ones are tions of phosphate and carbonate can retain observed. Surprisingly, no dependence to body primary isotopic record, even for fossil remains temperature on the oxygen isotope fractionation dating back to the early Paleozoic (Trotter et al., between eggshell calcite and body fluids is ob- 2008). However, some vertebrates such as birds served, suggesting that bird and crocodile egg- and some dinosaurs are toothless and their bony shells, for which we determined similar frac- remains can be more easily altered, thus limiting tionation factors between body water and their use as biological or environmental indica- eggshell calcite, precipitate out of equilibrium. tors based on their stable isotope compositions. Two empirical equations relating the δ18Ocalc On the other hand, eggshell remains are abun- value of eggshell calcite to the δ18Ow value of in- dant in the sedimentary record and have been gested water have been established for terrestri- found in deposits dated back to the Late Trias- al and semi-aquatic birds. sic. Due to their calcitic nature, oxygen and car- These various equations have been applied bon isotope compositions of fossil bird and di- to fossil eggshells and allowed to demonstrate nosaur eggshells (δ18Ocalc and δ13Ccalc) are their potential use as a tracer of past environ- regularly used to reconstruct paleoenvironmen- ments (in terms of air temperature, aridity), tal conditions (Sarkar et al., 1991; Montanari et ecology (in terms of aquatic or terrestrial life- al., 2013). However, the interpretation of δ18Ocalc style) and reproductive strategy (in terms of egg values of fossil eggshells has been limited to formation periods, either seasonal or all year qualitative variations in local climatic conditions round).

References

Amiot, R., Buffetaut, E., Lécuyer, C., Wang, X., Bou- habits among spinosaurid theropods. Geology dad, L., Ding, Z., Fourel, F., Hutt, S., Martineau, 38, 139–142. F., Medeiros, M.A., Mo, J., Simon, L., Suteethorn, Amiot, R., Wang, X., Zhou, Z., Wang, X., Lécuyer, C., V., Sweetman, S., Tong, H., Zhang, F., Zhou, Z., Buffetaut, E., Fluteau, F., Ding, Z., Kusuhashi, 2010. Oxygen isotope evidence for semi-aquatic N., Mo, J., Philippe, M., Suteethom, V., Wang, Y., 109

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Xu, X., 2015. Environment and ecology of East Montanari, S., Higgins, P., Norell, M.A., 2013. Dino- Asian dinosaurs during the Early Cretaceous in- saur eggshell and tooth enamel geochemistry as ferred from stable oxygen and carbon isotopes in an indicator of Mongolian Late Cretaceous pale- apatite. J. Asian Earth Sci. 98, 358–370. oenvironments. Palaeogeogr. Palaeoclimatol. Clementz, M.T., Koch, P.L., 2001. Differentiating Palaeoecol. 370, 158–166. aquatic mammal habitat and foraging ecology Sarkar, A., Bhattacharya, S.K., Mohabey, D.M., 1991. with stable isotopes in tooth enamel. Oecologia Stable-isotope analyses of dinosaur eggshells: 129, 461–472. Paleoenvironmental implications. Geology 19, Domingo, L., Barroso-Barcenilla, F., Cambra-Moo, O., 1068–1071. 2015. Seasonality and paleoecology of the Late Suarez, C.A., González, L.A., Ludvigson, G.A., Kirk- Cretaceous multi-taxa vertebrate assemblage of land, J.I., Cifelli, R.L., Kohn, M.J., 2014. Multi- “Lo Hueco” (Central Eastern Spain). PloS One taxa isotopic investigation of paleohydrology in 10, e0119968. the Lower Cretaceous Cedar Mountain For- Goedert, J., Amiot, R., Boudad, L., Buffetaut, E., Fou- mation, Eastern Utah, USA: Deciphering effects rel, F., Godefroit, P., Kusuhashi, N., Suteethom, of the Nevadaplano Plateau on regional climate. V., Tong, H., Watanabe, M.E., Lécuyer, C., 2016. J. Sediment. Res. 84, 975–987. Preliminary investigation of seasonal patterns Trotter, J.A., Williams, I.S., Barnes, C.R., Lécuyer, C., recorded in the oxygen isotope composition of Nicoll, R.S., 2008. Did cooling oceans trigger Or- theropod dinosaur tooth enamel. Palaios 31, 10– dovician biodiversification? Evidence from co- 19. nodont thermometry. Science 321, 550–554.

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Late Cretaceous (Maastrichtian) vertebrate fossils from inland basins of Indian peninsula – their palaeogeographic significance

A. Bhadran

Geological Survey of India, 27 Jawarlal Nehru Road, Kolkata 700016, India; e-mail: [email protected]

The Indian subcontinent had a dynamic ge- The Lameta beds of Maharashtra deposited in ographic and geologic history, i.e., key to under- alluvial-limnic semi-arid conditions during the standing major palaeobiogeographic and mac- Maastrichtian (Mohabey, 1990, 1996; Udhoji and roevolutionary events in Earth history, Mohabey, 1991; Mohabey and Udhoji, 1993). including the Cretaceous–Paleogene (K–Pg) Balasinor–Jhabua. This inland basin is im- mass extinction event. In Central India, the Up- portant because of well preservation of skeletal per Cretaceous (Maastrichtian) is represented by remains, egg nests and eggs of dinosaurs in the the Lameta Formation in Jabalpur, Bagh area in Balasinor and Rahioli localities of the Kheda and Jhabua and Dhar districts of Madhya Pradesh, Panchmahal districts in Gujarat. It is interpreted Pisdura–Dongargaon area in Chandrapur and to be the deposits of sheet washed into palus- Nagpur districts of Maharashtra, and Balasinor– trine environment (Mohabey, 1998, 2001a,b). Di- Rahioli area of Kheda and Panchmahal districts nosaur remains consist of Antarctosaurs septen- of Gujarat. In all these areas, the Lameta For- trionalis (sauropods) and Rajasaurus narmadensis mation is characterised by its vertebrate fossil (thereopods) (Huene and Matley, 1933; Mo- content, particularly dinosaurs. Several workers habey, 1987; Wilson and Upchurch, 2003; Wilson described faunal assemblages from the Lameta et al., 2003). Nests and eggs include Megaolo- Formation in these areas from time to time. lithus rahioliensis, M. phensaniesis, M. khempuensis, There are some important features of vertebrate M. megadermus, and M. balasinorensis (Huene faunal assemblages. and Matley, 1933; Mohabey, 1983, 1998; Khosla Jabalpur. The Jabalpur Lameta beds are and Sahni, 1995). Using oxygen and carbon iso- considered to be more significant due to rich tope analysis, fluvial or mostly lacustrine envi- preservation of dinosaurian remains. Rich as- ronment of deposition were proposed, particu- semblage consists of caudal vertebrae, tooth, larly for the egg-bearing horizons. coprolites and skulls of Sauropoda, Theropoda, Salbardi basin. The Lameta sedimentation and Ornithopoda, i.e., Titanosaurus indicus and in Salbardi took place after Gondwana sedimen- Antarctosaurus septentrionalis (sauropods); In- tation. The lower part of the Lameta succession dosuchus raptorius, I. matleyi, Lametasaurus indi- is mainly represented by arenaceous and argilla- cus, Composuchus solus, Laevisuchus indicus, Jub- ceous sediments that show a change in the ener- balppuria tenuis, Dryptosauroides (?) grandis, gy conditions in the depositing medium. In the Ornithomimoides mobilis, and O. barasimlensis upper part, the succession is mostly calcareous, (theropods); Brachypodasaurus gravis (ornitho- evidencing the shallowing of the basin and alka- pods) (Lydekker, 1877; Matley, 1924; Huene and line nature of the depositing medium (Roopesh Matley, 1933; Chatterjee, 1978; Mohabey, 1987; and Srivastava, 2015). Salbardi basin is found to Jain and Bandopadyay, 1997; Loyal et al., 1998; be productive for dinosaurian remains. It con- Demic et al., 2009). Egg nests and eggs are repre- tains fragmentary bones preserved in light sented by Megaloolithus dhoridungriensis (Mo- green-coloured, medium-grained sandstone. habey, 1996, 1998, 2000, 2001a,b). Srivastava and Mankar (2013, 2015) have report- Nand–Dongargaon. Dinosaur remains con- ed fragmentary remains of right ulna of Titano- sists of Titanosaurus indicus, T. blandfordi, T. col- saurus colberti, egg nest and eggs belonging to berti, and Laplatasurus madagascariensis (Lydek- Megaloolithus oogenus of the family Megaloo- ker, 1890; Chakravarti, 1934; Chatterjee, 1978; lithidae. Arun and Varsha (Aglawe and Carrano et al., 2010). Egg nests and eggs include Bhadran, 2014; Bhadran and Aglawe, 2015) re- Megaloolithus matleyi and M. megadermus (Jain ported turtle and theropod (abelisaurid?) bones and Sahini, 1985; Shukla and Srivastava, 2008). from the same locality. 111

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Comparison of the Salbardi area with oth- study of this new location allows the modifi- er areas of the Lameta Formation occurrence cation of earlier proposed palaeogeography of shows that it was nearly similar in size as the Lameta sedimentation in larger geographical Jabalpur, Rahioli and Nand–Dongargaon ba- extent. In conclusion, a new inland basin has sins. The dinosaurian remains including bones been identified for Lameta sedimentation, i.e. and eggs are indicative of channel to point bar the Salbardi–Belkher (Roopesh and Srivastava, deposition under sub-arid condition. The 2015).

References

Aglawe, V.A., Bhadran, A., 2014. First report of turtle Lydekker, R., 1877. Note of new and other vertebrates bones and occurrence of dinosaurian bones from from Indian Tertiary and Secondary rocks. Rec. Lameta Formation, Ghorpend village, Salbuldi Geol. Surv. India 10, 38–41. area, Betul District, Madhya Pradesh. e-News 30, Lydekker, R., 1890. Note on certain vertebrate re- GSI, CR. mains from Nagpur district. Rec. Geol. Surv. In- Bhadran, A., Aglawe, V.A., 2015. First report of a The- dia XXIII, 20–24. ropod (Dinosauria) from Upper Cretaceous Matley, C.A., 1924. Note on an armoured dinosaur (Maastrichtian) Lameta Formation of Salbardi from the Lameta beds of Jubbulpore. Rec. Geol. Basin, Betul District, Madhya Pradesh. Indian J. Surv. India 55, 142–164. Geosci. 69, 131–136. Mohabey, D.M., 1983. Note on the occurrence of dino- Carrano, M.T., Wilson, J.A., Barrett, P.M., 2010. The saurian fossil eggs from infratrappean limestone history of dinosaur collecting in Central India, in Kheda district, Gujarat. Curr. Sci. 52, 1194. 1828–1947. Geol. Soc. London Spec. Publ. 343, Mohabey, D.M., 1987. Juvenile sauropod dinosaur 161–173. from Upper Cretaceous Lameta Formation of Chakravarti, D.K., 1934. On a stegosaurian humerus Panchmahal district, Gujarat, India. J. Geol. Soc. from the Lameta beds of Jubbulpore. Q. J. Geol. India 30, 210–216. Min. Metall. Soc. India 5, 75–79. Mohabey, D.M., 1990. Dinosaur eggs from Lameta Chatterjee, S., 1978. Indosuchus and Indosaurus, Cre- Formation of Western and Central India: Their taceous carnosaurs from India. J. Paleontol. 52, occurrence and nesting behaviour, in: Sahni, A., 570–580. Jolly, A. (Eds.), Cretaceous event stratigraphy Demic, M.D., Wilson, J.A., Chatterjee, S., 2009. The ti- and correlation of the Indian non-marine strata. tanosaur (Dinosauria: Sauropoda) osteoderm Panjab University, Chandigarh, pp. 18–21. record: review and first definitive specimen from Mohabey, D.M., 1996. Depositional environment of India. J. Vertebr. Paleontol. 29, 165–177. Lameta Formation (Late Cretaceous) of Nand- Huene, F.B. von, Matley, C.A., 1933. The Cretaceous Dongergaon inland basin, Maharshtra: The fossil Saurischia and Ornithischia of the Central and lithological evidences. Mem. Geol. Soc. India Provinces of India. Mem. Geol. Surv. India. 37, 363–386. Paleontol. Indica 21, 1–74. Mohabey, D.M., 1998. Systematics of Indian Upper Jain, S.L., Bandopadyay, S., 1997. New titanosaurid Cretaceous dinosaur and chelonian eggshells. J. (Dinosauria: Sauropopda) from the Late Creta- Vertebr. Paleontol. 18, 384–362. ceous of Central India. J. Vertebr. Paleontol. 17, Mohabey, D.M., 2000. Understanding community 114–136. structure, nesting and extinction of Upper Creta- Jain, S.L., Sahni, A., 1985. Dinosaur eggshell frag- ceous (Maastrichtian) Indian dinosaurs: Evi- ments from the Lameta Formation at Pisdura, dences from eggs and nests. Gondawana Geol. Chandrapur district, Maharashtra. Geosci. J. 2, Magazine 15, 1–23. 211–220. Mohabey, D.M., 2001a. Dinosaurs eggs and dung (fe- Khosla, A., Sahni, A., 1995. Parataxonomic classifica- cal mass) from the Late Cretaceous of Central tion of Late Cretaceous dinosaur eggshell from India, dietary implications. Geol. Surv. India, India. J. Palaeontol. Soc. India 40, 87–102. Spec. Publ. 64, 605–615. Loyal, R.S., Mohabey, D.M., Khosla, A., Sahni, A., Mohabey, D.M., 2001b. Indian dinosaur eggs: 1998. Status and palaeobiology of the Late Creta- A review. J. Geol. Soc. India 58, 479–508. ceous Indian theropods with description of new Mohabey, D.M., Udhoji, S.G., 1993. Palaeoenviron- theropod eggshell oogenus and oospecies, Ellip- mental interpretation of Lameta Formation (Late soolithus khedaensis from the Lameta Formation, Cretaceous) of Nand area, Nagpur district, Ma- district Kheda, Gujarat, western India. GAIA 15, harashtra. Gondwana Geol. Magazine, Spec. Vol. 379–387. 2, 349–364. 112

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Roopesh S.M., Srivastava, A.K., 2015. Salbardi– and Betul, Madhya Pradesh. J. Geol. Soc. India Belkher inland basin: A new site of Lameta sed- 85, 457–462. imentation at the border of districts Amravati, Udhoji, S.G., Mohabey, D.M., 1991. A final report on Maharashtra and Betul, Madhya Pradesh, Cen- palaeontological studies of fresh water tral India. Curr. Sci. 109, 1337–1344. intertrappean (Lametas) and intertrappean Shukla, U.K., Srivastava, R., 2008. Lizard eggs from formations in part of Maharshtra (under IGCP Upper Cretaceous Lameta Formation of Jabal- Project 216), in: Unpublished Rep. F. S. 1984–85 pur, Central India, with interpretation of deposi- to 1988–89, pp. 49. tional environments of the nest-bearing horizon. Wilson, J.A., Upchurch, P.A., 2003. Revision of Titano- Cretaceous Res. 29, 674–686. saurus Lydekker (Dinosauria–Sauropoda), the Srivastava, A.K., Mankar, R.S., 2013. A dinosaurian first dinosaur genus with Gondwana distribu- ulna from a new locality of Lameta Succession, tuon. J. Syst. Palaeontol. 1, 125–160. Salbardi Area, districts Amravati, Maharashtra Wilson, J.A., Sereno, P.C., Srivastava, S., Batt, D.K., and Betul, Madhya Pradesh. Curr. Sci. 105, 900– Khosla, A., Sahni, A., 2003. A new abelisaurid 901. (Dinosauria–Sauropoda) from the Lameta For- Srivastava, A.K., Mankar, R.S., 2015. Megaloolithus mation (Cretaceous: Maastrichtian) of India. dinosaur nest from the Lameta Formation of Contrib. Mus. Palaeontol. Univ. Michigan 31, l– Salbardi area, districts Amravati, Maharashtra 42.

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Results of paleontological excavations 2014–2015 held by the Kemerovo Regional Museum at the Early Cretaceous Shestakovo vertebrate localities

N.V. Demidenko1 and E.N. Maschenko2

1Kemerovo Regional Museum, Sovetsky av. 55, Kemerovo 650000, Russia; e–mail: [email protected] 2Borissiak Paleontological Institute of the RAS, Street trade–Union 123, Moscow 117647, Russia

Introduction Saint Petersburg State University and Tomsk The Russia’s largest complex of localities of State University. Early Cretaceous vertebrates is situated near the In 2013, a major complex research was car- village Shestakovo (Chebulа District, Kemerovo ried out by KRM at the Shestakovo locality and Oblast). In 2013, the Kemerovo Regional Muse- adopted to the research program “Paleontologi- um (KRM) adopted the program, which includ- cal study of fossils in Paleozoic and Mesozoic ed excavation in the Shestakovo 3 locality. In deposits of the Kemerovo region”. The license 2014–2015, the excavations were carried out by for the use of subsurface resources aimed at col- the joint team of KRM and Borissiak Paleonto- lecting mineralogical, paleontological and other logical Institute of the Russian Academy of Sci- geological samples in the area of “Kiya support- ences (PIN RAS, Moscow). The result of the ex- ing open–pit", "Kiya–Sertinsky complex”, and cavation was the discovery of site of the unique “Antibes” located in Tisul, Chebula and Mar- mass death of at least 12 individuals of Psittaco- iinsk districts of the Kemerovo Oblast was ob- saurus sibiricus and other terrestrial vertebrates tained. In 2015, this license was extended until (Lopatin et al., 2015). 2020. The Shestakovo is the second paleontologi- In 2013, KRM fulfilled organizational and cal site of Russia, where the burial of complete managerial works including legal registration of skeletons of Early Cretaceous dinosaurs was activities at the Shestakovo localities and con- discovered (Maschenko et al., 2014). In addition, cluded a partner’s agreement with PIN RAS to the specimens of diverse fauna of terrestrial ver- undertake a joint research of the Shestakovo site. tebrates belonging to more than eight groups It was considered necessary due to the fact that were found there (Rozhdestvensky, 1960; Lesh- PIN RAS is the leading specialized scientific or- chinskiy et al., 1997, 2000; Voronkevich, 1998; ganization in Russia conducting paleontological Alifanov et al., 1999; Efimov and Leshchinskiy, researches as a part of scientific programs and 2000). Since 1953, dozens of identifiable bones, grants offered by the Government of the Russian teeth, hundreds of fragments belonging not only Federation. to different types of dinosaurs, flying reptiles, Since 2014, the field works have been car- amphibians, birds, but also to other groups of ried out in the Chebula District at two localities reptiles (turtles, crocodiles, lizards, etc.), and of Early Cretaceous terrestrial fauna: the Shesta- Mesozoic mammals were revealed in the kovo 1 (Kiya River bluff), about 500 m down- Shestakovo site (Leshchinskiy et al., 1997; Mas- stream from the Shestakovo village, and the chenko and Lopatin, 1998; Averianov et al., Shestakovo 3, about 1.5 km south-east from the 2002; Lopatin et al., 2010). Shestakovo village. The fossils were regularly collected at the Results and discussion slopes of the Kiya River bluff (Shestakovo 1). In Psittacosaurus sibiricus discovered at the the course of these studies, a large number of Shestakovo localities is a separated group of Late Pleistocene mammals were found includ- Psittacosurus dinosaurs endemic to Kuzbass area ing woolly mammoth, Pleistocene bison, wool- (Averianov et al., 2006). ly rhinoceros, wolf, reindeer, Pleistocene hors. Until 2013, the excavations and research of In addition to these, the fossils of Early Creta- the fossils from the Shestacovo localities were ceous vertebrates, such as giant dinosaurs (sau- carried out on irregular base by the researchers ropods) and tyrannosaurid dinosaurs were of PIN RAS, Zoological Institute of the RAS, found.

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific

In 2014, KRM started the excavation in the Conclusion area of 2x8 m with the altitude of 7 m above the The scientific description of the discovered road level. In 1 m below the soil, a level of Early paleontological materials obtained during the Cretaceous alluvial deposits including terrestrial excavations in 2014–2015 is being performed by vertebrate fossils was discovered. The bon-bad the researchers of KRM Department of Nature. layer is composed of brownish-red and greenish- Their research activities are systematically an- gray solid clay. Sculls, fractions of bones and nounced to museum visitors. The materials fragments of skeletons of Early Cretaceous verte- serve as the basis of the “Shestakovo Dinosaurs” brates (Protosuchia, Tagarosuchus kulemzini, Lacer- section of the new exhibition “Kemerovo region tilia (Agamidae) and dinosaur Psittacosaurus sibi- as a unique natural monument” opened in Au- ricus) were found there. The bone-bearing lens gust 2015. The fragments and complete skele- was located at the level of 0.3 m under bon-bad tons of Psittacosaurus sibiricus, Crocodylomorpha, layer. The characters of the bone-bearing lens ta- the fragments of sauropod skeletons found at phonomy demonstrated that the examined piece Shestakovo 1 as well as the traces of sand ripple of about 1 m wide and 4.5 m long is extended from the soundings of shallow sea are exhibited from north-east to south-west. The thickness of there. A joint exhibition of KRM and PIN RAS the lens was approximately 60–70 cm. has been prepared. The exhibition will be held The lens is unique including a lot of com- as a part of the permanent display in the Dino- plete Psittacosaurus skeletons presented in ana- saur Hall of PIN RAS Paleontological Museum tomic position in situ. The taphonomy peculiari- in Moscow. ties suggest that the death of dinosaur group, The project includes: (1) study and restora- consisting of specimen of different ages, was the tion of the largest Psittacosaurus sibiricus skele- result of a catastrophe. It is probable that mov- ton; (2) creation of a virtual model of Psittaco- ing along the temporary stream bed they were saurus sibiricus on the basis of measuring and buried by a mud flow. Such type of a taphono- scanning of original and restored bones; (3) con- my has never been previously obtained from the struction of a volumetric authentic Psittacosaurus Shestakovo locality or at any other locality in skeleton supported by a still construction; and Russia (Averianov et al., 2006; Lopatin et al., (4) preparation of a full-sized plastic copy of the 2015). dinosaur. The field season 2015 revealed the diverse In the course of the dinosaur’s skeleton factors of genesis of the Shestakovo deposits and examination, the scientists study the lifestyle, relatively diverse conditions of Early Cretaceous morphology and some behavioral features of vertebrates’ burials. Within the Ilek Formation, these reptiles. Skeleton model is prepared in the researchers of PIN RAS discovered at least the quadrupedal position using the support- two layers with traces of sand ripple divided ing firm construction also showing the ability with a 10 cm thick layer of siltstone at the 220– of bipedal motion, which is the result of eco- 240 cm from the basement of the altitude scale of logical peculiarities of dinosaur’s habitat and the Shestakovo 3 locality. These layers are pre- lifestyle. served areas of a shallow sea lagoon with traces This exhibition is a significant event in cul- of marine invertebrates (presumably the chan- tural and scientific life, because Russian muse- nels of polychaete worms), where clay deposits ums have not yet displayed complete dinosaurs containing fossil vertebrates were formed. Such excavated in Russia. traces were revealed for the first time in the Ear- ly Cretaceous lagoon in the Shestokovo site. It is Keywords the true evidence of the formation of a part of Kemerovo Regional Museum, Early Cretaceous, the Ilek Formation in the soundings of shallow Shestakovo localities, Psittacosaurus sibiricus, excava- sea. tion, field work.

References Alifanov, V.R., Efimov, M.B., Novikov, I.V., Morales, (Southern Siberia). Rep. Acad. Sci. USSR 369, 491– M., 1999. A new psittacosaur complex of tetrapods 493 (in Russian). from the Lower Cretaceous Shestakovo locality 115

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Averianov, A.O., Voronkevich, A.V, Maschenko, E.N., Regional Conference of the Geologists of Siberia, Leshchinskiy, S.V., Fayngertz, A.V., 2002. A sau- Far East, and North East of Russia, Vol. 2. ropod foot from the Early Cretaceous of Western GalaPress, Tomsk, pp. 363–366 (in Russian). Siberia, Russia. Acta Palaeontol. Polonica 47, Lopatin, A.V., Maschenko, E.N., Averianov, A.O., 117–124. 2010. A new genus of triconodont mammals Averianov, A.O., Voronkevich, A.V, Leshchinskiy, from the Early Cretaceous of Western Siberia. S.V., Fayngertz, A.V., 2006. A ceratopsian dino- Dokl. Biol. Sci. 433, 282–285. saur Psittacosaurus sibiricus from the Early Creta- Lopatin, A.V., Maschenko, E.N., Tarasenko, К.К., ceous of West Siberia, Russia and its phylogenet- Podlesnov, А.V., Demidenko, N.V., Kuzmina, ic relationships. J. Syst. Palaeontol. 4, 359–395. Е.А., 2015. A unique burial site of Early Creta- Efimov, M.B., Leshchinskiy, S.V., 2000. The first find- ceous vertebrates in Western Siberia (the Shesta- ing of a fossil crocodile skull in Siberia, in: Ko- kovo 3 locality, Kemerovo Province, Russia). marov, A.V. (Ed.), Materials of the Regional Con- Dokl. Biol. Sci. 462, 148–151. ference of the Geologists of Siberia, Far East, and Maschenko, E.N., Lopatin, A.V., 1998. First record of North East of Russia, Vol. 2. GalaPress, Tomsk, an Early Cretaceous triconodont mammal in Si- pp. 361–363 (in Russian). beria. Bull. Inst. R. Sci. Nat. Belg., Sci. Terre 68, Leshchinskiy, S.V., Voronkevich, A.V., Fayngertz, 233–236. A.V., Schikhovtzeva, L.G., 1997. Some aspects of Maschenko, E.N., Feofanova, О.А., Demidenko, N.V., taphonomy and stratigraphic position of the lo- Kuzmina, Е.А., 2014. Looking for a Siberian di- calities of the Shestakovo complex of Early Cre- nosaur. Sci. Life 11, 74–80 (in Russian). taceous vertebrates, in: Podobina, V.M. (Ed.), Rozhdestvensky, A.K., 1960. Locality of Lower Creta- Questions of geology and palaeontology of Sibe- ceous dinosaurs in Kuzbass. Paleontol. Zh. 2, 165 ria. Tomskii Gos. Univ., Tomsk, pp. 83–90 (in (in Russian). Russian). Voronkevich, A.V., 1998. A large representative of the Leshchinskiy, S.V., Fayngertz, A.V., Voronkevich, genus Psittacosaurus from the locality Shestako- A.V., Maschenko, E.N., Averianov, A.O., 2000. vo-3, in: Vyltsan, I.A. (Ed.), Actual questions of Preliminary results of the investigation of the the geology and geography of Siberia: Materials Shestakovo localities of Early Cretaceous verte- of the scientific conference. Vol. 1. Tomskii Gos. brates, in: Komarov, A.V. (Ed.), Materials of the Univ., Tomsk, pp. 190–193 (in Russian).

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Historical stages of natural science collection formation in the Kemerovo Regional Museum

O.A. Feofanova

Kemerovo Regional Museum, Sovetsky av. 51, Kemerovo 650000, Russia; e–mail: [email protected]

In the Kemerovo Regional Museum, there There is little information left on the consti- are more than 2.000 depositary items related to tution of the natural science collection formed in natural science collections. These are geological, the early years of the Kemerovo Regional Muse- zoological, botanical and paleontological collec- um. Archive was lost, as the museum had re- tions. peatedly moved, especially during the Great The museum and its collections have nearly Patriotic War. That is why many exhibits and 100 years of history. In 1926, the Shcheglovsk documents were lost (Kravtsova, 1999). Only city (now the Kemerovo city) became the admin- some of the geological and paleontological sam- istrative center of the Kuznetsk Uyezd (now the ples, stuffed animals and skins remained. Kemerovo Oblast) (Tivyakov, 1995). This young A new stage of museum’s history began in town and the region witnessed an active con- 1957, when it was moved to the building on the struction of industrial enterprises as well as a Sovetsky Avenue (now it is a building number constant flow of people. There was a need for 55) and was reopened after a massive reorgani- education and training of workers and young zation. Since the early 1960’s, museum workers people. To fill this need, some sectors of political started to collect new exhibits, their systematiza- education were formed. In particular, a resolu- tion, study and display. Ethnographical, histori- tion for the formation of the Regional Museum cal and archaeological expeditions were orga- was adopted at the session of a planned meeting nized, that also provide the collections of natural under the District Committee of Public Educa- materials. tion on September 27, 1927 (Kitova, 1999). It was In 1970s–80s, the museum staff organized assumed that the museum will display the ma- multipurpose expeditions on the territory of the terials showing the economic state of the region, Kemerovo Oblast, where museum materials on its environmental conditions, the history of specific topics were collected: industry, agricul- revolution and ethnography. The museum was ture, education, culture, environment, everyday opened on October 6, 1929. After renaming of life, etc. During this period, the museum orga- the Shcheglovsk in 1932, the museum got the nized several expeditions focused on the miner- name Kemerovo City Museum. al search and plants collecting for the herbaria, Development of museum holdings was animal skins and stuffed animals were also started by the members of the Kuznetsk District bought. During 1960s–1980s, the museum Society of Local History in 1928 even before worked in close collaboration with geological the museum opened to the public. By the exploration organizations and coal-mining en- opening day, the collection exhibits reached terprises. Through such cooperation, the collec- about 600 units. In the process of collecting tion was enriched with a large number of geo- exhibits and creating displays, the priority logical items. During the exploration and was given to the industrial and agricultural development of mineral deposits, geologists and development of the region. This direction of miners revealed numerous fossils, including museum development was determined by the mammoth fauna, animal bones, remains of cal- Communist Party and the Soviet government. careous skeletons of marine invertebrates, petri- Years before, the war was resulted in accelera- fied wood and leaf imprints. tion of industrial development associated with In the early 2000’s, the number of new con- the strengthening of the state's defense poten- tributions decreased. The difficulties derived tial. In this regard, the main goal of regional from the change of enterprises ownership forms museums was to study industrial forces of the as well as the lack of sufficient funds for the country (Ivanova, 1963). purchase of rare and valuable items.

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Today, the Kemerovo Regional Museum fossils in Paleozoic and Mesozoic deposits of the has developed and adopted scientific concept Kemerovo Region”, and also got a license for the for the acquisition of exhibits. It is based on the use of subsurface resources in order to collect analysis of available collections, the definition of geological materials. In 2015, the license was ex- main directions for a long-term acquisition. One tended until 2020. of such directions is the collection of paleonto- The first stage of the implementation of logical objects and the creation of a new perma- paleontological research program was the or- nent exhibition that reflects the evolution of life ganization of excavations in the Shestakovo lo- on the Kuzbass territory. cality. An agreement between the museum and The new exhibition should represent the Borissiak Paleontological Institute of the Russian unique geological and paleontological nature Academy of Sciences (PIN RAS) was signed to monuments of the Kemerovo Oblast and show implement joint researches in Shestakovo locali- the formation of the modern image of the re- ty. In 2014, the museum expedition started the gion. To achieve this goal, the Kemerovo Re- excavations in the Shestakovo 3 locality in col- gional Museum implemented several projects. laboration with PIN RAS team. The first one was the temporary exhibition Today, the museum has reached new out- called “12 Steps of Evolution” dedicated to the standing results in the research of the Shestako- 70th anniversary of the Kemerovo Oblast. The vo locality. During the expeditions of 2014–2015, exposition was opened in KRM Department of more than 1.500 paleontological items were col- Nature on October 15, 2012 and consisted of lected, and new bone-bearing layers were also three sections: “The Ancient Inhabitants of the discovered with mass burials of skeletons of Seas”, “Terrible Lizards – the Dinosaurs” and Psittacosaurus sibiricus (Lopatin et al., 2015). “Ice Age” covering long time interval from the The next stage of the program involves the Paleozoic to the Cenozoic. The exhibition dis- creation of a scientific center on the basis of the played paleontological items collected on the Kemerovo Regional Museum. This year, the de- territory of Kuzbass and in other regions of partment of research and expeditions called the world. Skeletons of Psittacosaurus sibiricus “Paleontological Research Laboratory” was es- Voronkevich et Averianov found near the vil- tablished at the museum. The department has lage Shestakovo were displayed for the first modern equipment for mechanical cleaning and time. chemical treatment of fossils. The members of However, most of the exhibition items are the department currently organize expeditions owned by Mr. Grebnev, a private collector from to collect paleontological materials and to per- Novosibirsk, including fossils of dinosaurs from form excavations in the Shestakovo locality. the Shestakovo locality. In order to create a They also make preparation of paleontological permanent exhibition, the museum must have fossils obtained in the course of excavations as its own collection of depositary items. At that well as prepare them to be displayed. time, museum’s paleontological collection had In the future, we plan to deepen the cooper- almost no fossils representing life forms of ation and to organize joint work with scientific Paleozoic and Mesozoic eras. At the same time, and educational institutions in the region and it is a promising region for paleontological the Russian Federation. Thus, the Kemerovo Re- study, as it is the homeland of some Devonian gional Museum will be a platform for long-term marine invertebrates and Cretaceous continental scientific research carried out by scientists and fauna. In 2013, the Kemerovo Regional Museum Ph.D. students in the field of paleontology. initiated the organization of scientific research of Moreover, new department will serve as a Early Cretaceous deposits containing vertebrates ground for various cultural and educational ac- in the Shestakovo locality, one of the largest and tivities that contribute to the popularization of most promising dinosaurs burials in Russia (Ali- paleontology among people. fanov et al., 1999; Mashchenko et al., 2014). The museum developed a program of scientific and Keywords exhibition research “Paleontological study of Collection, museum, historical stages, Shestakovo.

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References Alifanov, V.R., Efimov, M.B., Novikov, I.V., Morales, Kravtsova, L.P., 1999. Kemerovo Regional Museum: M., 1999. A new psittacosaur complex of tetra- Meeting the anniversary. Research: Regional pods from the Lower Cretaceous Shestakovo lo- History Yearbook 5, 7–11 (in Russian). Lopatin, A.V., Maschenko, E.N., Tarasenko, К.К., cality (Southern Siberia). Rep. Acad. Sci. USSR Podlesnov, А.V., Demidenko, N.V., Kuzmina, 369, 491–493 (in Russian). Е.А., 2015. A unique burial site of Early Creta- Ivanova, O.V., 1963. Museum construction in the time ceous vertebrates in Western Siberia (the Shesta- of prewar five-year plans (1928–1941), in: kovo 3 locality, Kemerovo Province, Russia). Razgon, A.M. (Ed.), Essays on the history of Dokl. Biol. Sci. 462, 148–151. museology in the USSR. Sovetskaya Rossiya, Maschenko, E.N., Feofanova, О.А., Demidenko, N.V., Kuzmina, Е.А., 2014. Looking for a Siberian di- Moscow, 86–89 (in Russian). nosaur. Sci. Life 11, 74–80 (in Russian). Kitova, L.Y., 1999. History of Kemerovo Regional Mu- Tivyakov, S.D., 1995. Administrative and territorial seum creation (1920s–1930s). Research: Regional division of Kuznetsk land. Research: Regional History Yearbook 5, 11–22 (in Russian). History Yearbook 4, 8–9 (in Russian).

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Fossil vertebrates from the Late Cretaceous Tamagawa Formation (Turonian) of Kuji City, Iwate Prefecture, northeastern Japan

R. Hirayama1, T. Takisawa2, K. Sasaki3, T. Sonoda4, M. Yoshida5, A. Takekawa5, Sh. Mitsuzuka6, Y. Kobayashi7, T. Tsuihiji8, R. Matsumoto9, M. Kurosu10, Y. Takakuwa11, S. Miyata12 and Y. Tsutsumi13

1School of International Liberal Studies, Waseda University, Nishiwaseda 1-6-1, Shinjuku-ku, Tokyo 169-8050, Japan; e-mail: [email protected] 2Kuji Amber Museum, Kuji, Japan 3Kuji City Office, Kuji, Japan 4Fukui Prefectural Dinosaur Museum, Katsuyama, Japan 5Graduate School of Science, the University of Tokyo, Tokyo, Japan 6Nippon Koei Co., Ltd., Shizuoka, Japan 7Faculty of Science, Hokkaido University, Sapporo, Japan 8Faculty of Science, the University of Tokyo, Tokyo, Japan 9Kanagawa Prefectural Museum of Natural History, Odawara, Japan 10China University of Geosciences, Beijing, China 11Gunma Museum of Natural History, Tomioka, Japan 12Josai University, Tokyo, Japan 13National Museum of Nature and Science, Tsukuba, Japan

The Tamagawa Formation in Kuji Group of Crocodiles (order Crocodyliformes) are next Kuji City, Iwate Prefecture of northeastern Japan abundant group (105 specimens in total). Its is the richest geological unit bearing the Late amphicoelous vertebrae, osteoderms and dental Cretaceous terrestrial vertebrates as well as rich morphology suggest that they were the mem- ambers in this country. More than one thousand bers of neosuchian grade, possibly close to the vertebrate fossils have been found from about genus Paralligator. the 20 cm thick coaly mudstone layer and over- Twenty three isolated almost cylindrical lying 1 m thick marine sandstone bed of the teeth of sauropods (order Saurischia) have been Tamagawa Formation since 2005. Fission track collected, whereas other dinosaurs (Theropoda dating carried out in the volcanic tuff layer inter- and Ornithischia) are known by few limb bones bedded between the mudstone and marine and isolated teeth. A wing digital bone of medi- sandstone units indicates a Turonian age (Tsu- um size pterosaur (order Pterosauria) was found tsumi, in preparation). in 2010. Two isolated vertebrae from the sand- Sharks (elasmobranchs) are known by 110 stone bed are identified as the first known isolated teeth of Scapanorhynchus, Cretolamna, Cre- Choristodera from the Upper Cretaceous of todus, and Protolamna as well as by vertebrae and Asia. presumed coprolites from the sandstone bed. Except two partially articulated turtle shell Turtles (order Testudines) are the most of Adocus, all terrestrial vertebrate fossils from abundant vertebrates (441 specimens in total), bone bed inter-bedded by marine sandstone lay- identified as the Adocidae (genus Adocus), Trio- ers are isolated and fragmentary. This occur- nychidae, Nanhsiungchelyidae, Lind- holmemydidae, and Carettochelyidae. Most of rence suggests that they were transported by turtle remains are isolated shell elements, river stream near the mouth. Abundance of sau- whereas few cranial and appendicular materials ropod teeth seems unique as the Late Cretaceous were collected. Adocus sp. from the Tamagawa biota. Formation seems the most derived species of Fauna and flora of the Kuji Group are one this genus in the possession of extremely wide of the most expectable examples of both non- marginal scales and the loss of cervical scale of marine and marine vertebrates of the Late Cre- carapace. Largest specimen of Adocus in this lo- taceous in Japan. Our excavation will be contin- cality suggests an individual with 70 cm long ued in the coming years for more plentiful re- shell. sults.

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The Lower Cretaceous continental vertebrate fauna from the Shestakovo locality (West Siberia): Results of 20-year research

S.V. Ivantsov1, A.V. Fayngerts1, S.V. Leshchinskiy1, A.S. Rezviy2, P.P. Skutschas1 and A.O. Averianov1

1Laboratory of Mesozoic and Cenozoic Continental Ecosystems, Tomsk State University, Lenin av. 36, Tomsk 634050, Russia; e-mail: [email protected] 2Museum of Nature and Man, Mira str. 11, Khanty-Mansiysk 628011, Russia

The year of 2013 witnessed the 60th anniver- logical structure (Fayngerts and Leshchinskiy, sary of the discovery of the Lower Cretaceous 2000) and taphonomic features (Voronkevich, continental vertebrates in the Shestakovo site. 2000) are presented in several papers. Each lo- Several localities are situated on the right bank cality is characterized by specific features of sed- of the Kiya River in the vicinity of the Shestako- imentation, and therefore special burial condi- vo village (Chebula District of the Kemerovo tions. Microvertebrate assemblage from the Oblast). Shestakovo 1, being the typical section for the The discovery was not easy. A.R. Anan’yev, Ilek Formation, provides a complete overview of assistant professor of Tomsk State University the composition of vertebrate fauna. It was (TSU), mentioned: “In spite of careful search, formed in alluvial conditions, while the Shesta- neither plant, nor animal fossils are not found in kovo 3 characterized by complete skeletons, the Ilek Formation” (Anan’yev, 1948). their fragments in anatomical position and sepa- In 1953, a geologist A.A. Mossakovskiy and rate bones and teeth represents the crevasse assistant professor of TSU I.V. Lebedev discov- splay facies. ered the incomplete skeleton and the skull with At present time, the following taxa are re- forelimb of the small ornitischian dinosaur re- vealed in the complex of the Shestakovo 1: Pal- ferred to Psittacosaurus at the base of the Shesta- aeonisciformes indet., Sinamiidae indet., Kiyatri- kovo section (Rozhdestvenskiy, 1960). ton leshchinskiyi, Caudata indet., Kirgizemys sp., In the early 1960s, A.A. Bulynnikova and Choristodera indet., Xenosauridae indet., Par- L.Ya. Trushkova (1967) found the remains of a macellodus sp., Scincomorpha indet., Gekkota larger dinosaur, which was sent to A.K. Rozh- indet. (Averianov and Voronkevich, 2002; destvenskiy (Paleontological Institute) for iden- Skutschas, 2006, 2014; Skutschas and Vitenko, tification. 2015), Tagarosuchus kulemzini, Kyasuchus saevi The further findings of the Early Cretaceous (Efimov and Leshchinskiy, 2000), Pterodactyloi- vertebrates from the Shestakovo site were made dea indet., Ornithocheiridae indet., Troodonti- only in 1994, when E.N. Maschenko discovered dae indet., Dromaeosauridae indet., Therizino- a phalanx of sauropod dinosaur and the molari- sauroidea indet., Theropoda indet., form of the theromorph tritylodont in the talus Titanosauriformes indet., Stegosauridae indet., of the Shestakovo outcrops. The last one was the Ornithopoda indet., Hypsilophodontidae indet., first tritylodontid from the Lower Cretaceous. Psittacosaurus sibiricus (Averianov et al., 2002, Previously, they assumed to be extinct in the Ju- 2003, 2004, 2006; Averianov and Sues, 2007), rassic. In 1995, the members of the Department Mystiornis cyrili (Kurochkin et al., 2011), Evge- of Paleontology and Historical Geology of TSU, navis nobilis (O’Connor et al., 2014), Xenocreto- prospecting in Tegul’det depression of West Si- suchus sibiricus, Sibirotherium rossicus (Tatarinov beria, found the bones of the large dinosaurs in and Maschenko, 1999; Maschenko et al., 2002; the outcrop of Shestakovo steep bank. Besides, Lopatin et al., 2009), Gobiconodontidae (Lopatin several new sites were discovered (Shestako- and Averianov, 2015), Acinacodus tagaricus, vo 2, 3; Smolenskii Yar; Ust’-Kolba) (Saev and Yermakia domitor, Kiyatherium cardiodens (Lopatin Leshchinskiy, 1997). et al., 2005, 2010). The Shestakovo complex of vertebrate local- The composition of this vertebrate assem- ities is rather well studied. The data on its geo- blage is heterogeneous and includes vertebrates

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 with Jurassic (e.g., paramacellodid lizard, “pro- Since the first years of the research, the large tosuchian” and shartegosuchid crocodyliforms, bones of sauropod were washed out from the tritylodonts, docodont mammals) and Creta- Shestakovo 1 outcrop. The pedal ungulal phal- ceous (e.g., “macrobaenid” turtles, dromaeo- anx of a therizinosaurid was found at the same saurid and troodontid theropods, ceratopsian place in 2010. There are still undescribed taxa of Psittacosaurus sibiricus) affinities (Leshchinskiy et theropods of large, medium and small size rep- al., 2001). Thus, the presence of refugium in the resented by fragmentary materials. Only prelim- south-east of West Siberia is proposed. inary results are published on turtles and liz- There is still a potential for describing new ards. Only small portion of Shestakovo 3 taxa of vertebrates from the Shestakovo section. perspective area was excavated in the past years.

References Anan’ev, A.R., 1948. Geology of Mesozoic deposits ference of the Geologists of Siberia, Far East, and near Ust’-Serta village on Kiya River. Uch. Zap. North East of Russia, Vol. 2. GalaPress, Tomsk, Tomskogo Gos. Univ. 10 (in Russian). pp. 361–363 (in Russian). Averianov, A.O., Sues, H.-D., 2007. A new troodontid Fayngerts, A.V., Leshchinskiy, S.V., 2000. Early Creta- (Dinosauria: Theropoda) from the Cenomanian ceous Chulym-Enisey paleobasin: Conditions of of Uzbekistan, with a review of troodontid rec- sedimentation and habitat of vertebrate fauna, ords from the territories of the former Soviet Un- in: Sreda i zhizn’ v geologicheskom proshlom, ion. J. Vert. Paleontol. 27, 87–98. Tez. dokl. Novosibirsk, pp. 47–48 (in Russian). Averianov, A.O., Voronkevich, A.V., 2002. A new Kurochkin, E.N., Zelenkov, N.V., Averianov, A.O., crown-group salamander from the Early Creta- Leshchinskiy, S.V., 2011. A new taxon of birds ceous of Western Siberia. Russ. J. Herpetol. 9, (Aves) from the Early Cretaceous of Western Si- 209–214. beria, Russia. J. Syst. Palaeontol. 9, 109–117. Averianov, A.O., Voronkevich, A.V, Maschenko, E.N., Leshchinskiy, S.V, Voronkevich, A.V., Fayngertz, Leshchinskiy, S.V., Fayngertz, A.V., 2002. A sau- A.V., Maschenko, E.N., Lopatin, A.V., Averi- ropod foot from the Early Cretaceous of Western anov, A.O., 2001. Early Cretaceous vertebrate lo- Siberia, Russia. Acta Palaeontol. Polonica 47, cality Shestakovo, Western Siberia, Russia: A re- 117–124. fugium for Jurassic relicts? J. Vert. Paleontol. 21, Averianov, A.O., Leshchinskiy, S.V., Skutschas, P.P., 73A. Rezvyi, A.S., 2003. Pterosaur teeth from the Lopatin, A.V., Averianov, A.O., 2015. Gobiconodon Lower Cretaceous of Russia and Uzbekistan. (Mammalia) from the Early Cretaceous of Mon- Sovrem. Gerpetol. 2, 5–11 (in Russian). golia and revision of Gobiconodontidae. J. Averianov, A.O., Leshchinskiy, S.V., Skutschas, P.P., Mammal. Evol. 22(1), 17–43. Fayngertz, A.V., Rezvyi, A.S., 2004. Dinosaurs Lopatin, A.V., Maschenko, E.N., Averianov, A.O., from the Early Cretaceous Ilek Formation in Rezvyi, A.S., Skutschas, P.P., Leshchinskiy, S.V., West Siberia, Russia, in: Second European Asso- 2005. Early Cretaceous mammals from Western ciation of Vertebrate Paleontologists Meeting: Siberia: 1. Tinodontidae. Paleontol. J. 39, 523–534. Abstracts of papers. Moravian Museum, Brno, Lopatin, A.V., Averianov, A.O., Maschenko, E.N., p. 6. Leshchinskiy, S.V., 2009. Early Cretaceous Averianov, A.O., Voronkevich, A.V, Leshchinskiy, mammals of Western Siberia: 2. Tegotheriidae. S.V., Fayngertz, A.V., 2006. A ceratopsian dino- Paleontol. J. 43, 453–462. saur Psittacosaurus sibiricus from the Early Creta- Lopatin, A.V., Averianov, A.O., Maschenko, E.N., ceous of West Siberia, Russia and its phylogenet- Leshchinskiy, S.V., 2010. Early Cretaceous ic relationships. J. Syst. Palaeontol. 4, 359–395. mammals of Western Siberia: 3. Zhangheothe- Bulynnikova, A.A., Trushkova, L.Ya., 1967. Continen- riidae. Paleontol. J. 44, 573–583. tal Cretaceous deposits of eastern and central Maschenko, E.N., Lopatin, A.V., Voronkevich A.V., parts of the Western Siberian lowland, in: Mar- 2002. A new Early Cretaceous mammal from tinson, G.G. (Ed.), Stratigraphy and palaeontolo- Western Siberia. Dokl. Biol. Sci. 386, 475–477. gy of Mesozoic and Palaeogene–Neogene conti- O'Connor, J.K., Averianov, A.O., Zelenkov, N.V., nental deposits of the Asiatic part of the USSR. 2014. A confuciusornithiform (Aves, Pygostylia)- Nauka, Leningrad, pp. 40–46 (in Russian). like tarsometatarsus from the Early Cretaceous Efimov, M.B., Leshchinskiy, S.V., 2000. The first find- of Siberia and a discussion of the evolution of ing of a fossil crocodile skull in Siberia, in: Ko- avian hind limb musculature. J. Vert. Paleontol. marov, A.V. (Ed.), Materials of the Regional Con- 34, 647–656.

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Rozhdestvensky, A.K., 1960. Locality of Lower Creta- mander from the Lower Cretaceous of Western ceous dinosaurs in Kuzbass. Paleontol. Zh. 2, 165 Siberia, Russia. Cretaceous Res. 51, 88–94. (in Russian). Skutschas, P.P., Vitenko, D.D., 2015. On a record of Saev, V.I., Leshchinskiy, S.V., 1997. New findings of choristoderes (Diapsida, Choristodera) from the dinosaurs in Siberia, in: Podobina, V.M., Savina, Lower Cretaceous of Western Siberia. Paleontol. N.I., Kuznetsova, K.I., Muzylev, N.G. (Eds.), Bio- J. 49, 507–511. stratigraphy and microorganisms of the Phaner- Tatarinov, L.P., Maschenko, E.N., 1999. A find of an ozoic of Eurasia. Geos, Moscow, p. 268 (in Rus- aberrant tritylodont (Reptilia, Cynodontia) in the sian). Lower Cretaceous of Kemerovo Region. Paleon- Skutschas, P.P., 2006. Biostratigraphy of the Late tol. Zh. 4, 85–92 (in Russian). Mesozoic tetrapod assemblages of Siberia, in: Voronkevich, A.V., 2000. Taphonomic features of bur- Rozanov, A.Yu., Lopatin, A.V., Parkhaev, P.Yu. ial of vertebrates’ remains in the deposits of Ilek (Eds.), Classical and new methods: Second All- Svita, in: Komarov, A.V. (Ed.), Materials of the Russian school – 2005. Moscow, pp. 87–96. Regional Conference of the Geologists of Siberia, Skutschas, P.P., 2014. Kiyatriton leshchinskiyi Averi- Far East, and North East of Russia, Vol. 2. anov et Voronkevich, 2001, a crown-group sala- GalaPress, Tomsk, pp. 359–360 (in Russian).

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The history of discovery and research of the Shestakovo locality of Early Cretaceous vertebrates

A.E. Kostyunin

Kemerovo Regional Museum, Department of the Nature, Sovetsky av. 55, Kemerovo 650000, Russia; e–mail: [email protected]

Research history of the Shestakovo locality Systematic investigations of the Shestakovo of Early Cretaceous vertebrates was started in locality were started in the early 90th. In 1994, the first part of 50th years of the last century. In E.N. Maschenko from the Paleontological Insti- 1953, a geologist A.A. Mossakovsky (Geological tute of the Russian Academy of Sciences (PIN Institute of the Academy of Sciences of the RAS) discovered teeth of tritilodontid, some- USSR, Moscow) discovered fragments of a fore times ago identified as Xenocretosuchus sibiricus limb of medium-sized herbivorous dinosaur. Tatarinov et Matchenko (Tatarinov and Mas- The fossils were found near the Shestakovo vil- chenko, 1999), and phalange of sauropod lage in the precipice of the Kiya River (center of (Averianov et al., 2002). Next year he found a the Shestakovskii ravine location, also known fragment of jaw of Mesozoic mammal Gobicono- as the Shestakovo 1). In the same year, the do- don borissiaki Trofimov (Maschenko and Lopatin, cent of Tomsk Polytechnic Institute I.V. Lebe- 1998). dev found a cranium and a fore limb belonging Since 1995, the staff of Tomsk State Univer- to other specimen of the same species of dino- sity (TSU) has performed excavation and strati- saurs. graphical operations resulted in the discovery of The fragments discovered by A.A. Mossa- two new bone burial locations (Shestakovo 2 kovsky and I.V. Lebedev were transferred to the and Shestakovo 3) (Saev and Leshchinskiy, Paleontological Institute of the Academy of Sci- 1997). ences of the USSR. Afterwards, these fragments In 1995–1996, the group of Tomsk paleon- were identified as remains of a dinosaur of the tologists found the fragments of foot and verte- genus Psittacosaurus (Rozhdestvensky, 1955). brae of sauropod, jointed fragments of Psittaco- After delivery of skeleton to Moscow, A.K. saurus skeleton as well as other paleontological Rozhdestvensky (expert on dinosaurs from the materials (Leshchinskiy et al., 1997; Vo- Paleontological Institute) was sent to Shestakovo ronkevich, 1998; Efimov and Leshchinskiy, 2000; to prospect the locality, but he could not make Averianov et al., 2002). A spread of remains in excavation, because bone-bearing layers were the even-aged layer of Early Cretaceous blankets inaccessible due to high water level. A.K. Rozh- on the limited area lets to associate three locali- destvensky was forced to perform the geological ties in the united complex (Leshchinskiy et al., investigation of the Shestakovskii ravine as well 1997; Alifanov et al., 1999). as the nearest precipices and outcrops along the In 1997, the research group from PIN RAS Kiya River and its feeder, the Serte River (Rozh- in collaboration and under financial support of destvensky, 1960). the Museum of Natural History (North Arizona, Since the finding of the first remains of Psit- USA) worked under the direction of V.R. Ali- tacosaurus until the early 90th, no special investi- fanov in the Shestakovo locality (Alifanov et al., gations have been carried out in the neighbor- 1999). In this expedition, Psittacosaurus skeleton hood of the Shestakovo village. At the same and single bones of the same species of dino- time, there is a mention in the literature about saurs were found, but these materials have not the finding of big bones in the Shestakovo 1 yet been published. (Bulynnikova and Trushkova, 1967). It may be Since 1997, the staff of PIN RAS has per- suggested that these remains could belong to a formed washing of bone-bearing layers of the dinosaur from sauropods (Averianov et al., Shestakovo locality to find the micro balances of 2002). It is unknown what has happened with terrestrial vertebrates. As a result of these inves- this finding. tigations carried out for more than 10 years, the

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific extensive paleontological material was obtained established that it includes a large number of (Averianov et al., 2003; Lopatin et al., 2005, 2009, relic forms, which were typical for the Late Ju- 2010a,b). In addition, the staff of TSU periodical- rassic epoch. It allows us to suggest that a refu- ly collected fossil remains of different groups of gium existed in this territory in the Early Creta- terrestrial vertebrates at the Shestakovo 3 ceous (Leshchinskiy et al., 2001). (O'Connor et al., 2014). These works continued A new stage in the study of the Cretaceous until 2012. fauna of the Shestakovo localities began in In 1999, A.V. Voronkevich (TSU) found two 2014, when employees of the Kemerovo Re- complete Psittacosaurus skeletons in anatomic gional Museum in cooperation with the staff of synarthrosis at the Shestakovo 3. These skele- PIN RAS resumed excavations in that area. As tons became the base for the detachment and a result of this work, a new bone-bearing lens description of the separate species named Psitta- with a large burial of Psittacosaurus skeletons cosaurus sibiricus Voronkevich et Averianov and other paleontological materials were dis- (Leshchinskiy et al., 2000). Until that moment, covered (Lopatin et al., 2015). Currently, the this species was considered as a form of Psittaco- excavations at the Shestakovo 3 and the wash- saurus mongoliensis Osborn (Voronkevich, 1998; ing of the Ilek Formation rocks at the Shestako- Alifanov et al., 1999). vo 1 are performed. Thus, during the research of Early Creta- ceous vertebrates from the Shestakovo locality, Keywords the rich fauna including more than 25 species Cretaceous, West Siberia, Shestakovo locality, was discovered (Averianov et al., 2006). It was history of discovery.

References

Alifanov, V.R., Efimov, M.B., Novikov, I.V., Morales, North East of Russia, Vol. 2. GalaPress, Tomsk, M., 1999. A new psittacosaur complex of tetra- pp. 361–363 (in Russian). pods from the Lower Cretaceous Shestakovo lo- Leshchinskiy, S.V., Voronkevich, A.V., Fayngertz, cality (Southern Siberia). Rep. Acad. Sci. USSR A.V., Schikhovtzeva, L.G., 1997. Some aspects of 369, 491–493 (in Russian). taphonomy and stratigraphic position of the lo- Averianov, A.O., Voronkevich, A.V, Maschenko, E.N., calities of the Shestakovo complex of Early Cre- Leshchinskiy, S.V., Fayngertz, A.V., 2002. A sau- taceous vertebrates, in: Podobina, V.M. (Ed.), ropod foot from the Early Cretaceous of Western Questions of geology and palaeontology of Sibe- Siberia, Russia. Acta Palaeontol. Polonica 47, ria. Tomskii Gos. Univ., Tomsk, pp. 83–90 (in 117–124. Russian). Averianov, A.O., Leshchinskiy, S.V., Skutschas, P.P., Leshchinskiy, S.V., Fayngertz, A.V., Voronkevich, Rezvyi, A.S., 2003. Pterosaur teeth from the A.V., Maschenko, E.N., Averianov, A.O., 2000. Lower Cretaceous of Russia and Uzbekistan. Preliminary results of the investigation of the Sovrem. Gerpetol. 2, 5–11 (in Russian). Shestakovo localities of Early Cretaceous verte- Averianov, A.O., Voronkevich, A.V, Leshchinskiy, brates, in: Komarov, A.V. (Ed.), Materials of the S.V., Fayngertz, A.V., 2006. A ceratopsian dino- Regional Conference of the Geologists of Siberia, saur Psittacosaurus sibiricus from the Early Creta- Far East, and North East of Russia, Vol. 2. ceous of West Siberia, Russia and its phylogenet- GalaPress, Tomsk, pp. 363–366 (in Russian). ic relationships. J. Syst. Palaeontol. 4, 359–395. Leshchinskiy, S.V, Voronkevich, A.V., Fayngertz, Bulynnikova, A.A., Trushkova, L.Ya., 1967. Continen- A.V., Maschenko, E.N., Lopatin, A.V., Averi- tal Cretaceous deposits of eastern and central anov, A.O., 2001. Early Cretaceous vertebrate lo- parts of the Western Siberian lowland, in: Mar- cality Shestakovo, Western Siberia, Russia: A re- tinson, G.G. (Ed.), Stratigraphy and palaeontolo- fugium for Jurassic relicts? J. Vert. Paleontol. 21, gy of Mesozoic and Palaeogene–Neogene conti- 73A. nental deposits of the Asiatic part of the USSR. Lopatin, A.V., Maschenko, E.N., Averianov, A.O., Nauka, Leningrad, pp. 40–46 (in Russian). Rezvyi, A.S., Skutschas, P.P., Leshchinskiy, S.V., Efimov, M.B., Leshchinskiy, S.V., 2000. The first find- 2005. Early Cretaceous mammals from Western ing of a fossil crocodile skull in Siberia, in: Ko- Siberia: 1. Tinodontidae. Paleontol. J. 39, 523–534. marov, A.V. (Ed.), Materials of the Regional Con- Lopatin, A.V., Averianov, A.O., Maschenko, E.N., ference of the Geologists of Siberia, Far East, and Leshchinskiy, S.V., 2009. Early Cretaceous

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mammals of Western Siberia: 2. Tegotheriidae. avian hind limb musculature. J. Vert. Paleontol. Paleontol. J. 43, 453–462. 34, 647–656. Lopatin, A.V., Averianov, A.O., Maschenko, E.N., Rozhdestvensky, A.K., 1955. New data on psittaco- Leshchinskiy, S.V., 2010a. Early Cretaceous saurs – Cretaceous ornithopods. Questions Geol. mammals of Western Siberia: 3. Zhangheothe- Asia 2, 783–788 (in Russian). riidae. Paleontol. J. 44, 573–583. Rozhdestvensky, A.K., 1960. Locality of Lower Creta- Lopatin, A.V., Maschenko, E.N., Averianov, A.O., ceous dinosaurs in Kuzbass. Paleontol. J. 2, 165 2010b. A new genus of triconodont mammals (in Russian). from the Early Cretaceous of Western Siberia. Saev, V.I., Leshchinskiy, S.V., 1997. New findings of Dokl. Biol. Sci. 433, 282–285. dinosaurs in Siberia, in: Podobina, V.M., Savina, Lopatin, A.V., Maschenko, E.N., Tarasenko, К.К., N.I., Kuznetsova, K.I., Muzylev, N.G. (Eds.), Bio- Podlesnov, А.V., Demidenko, N.V., Kuzmina, stratigraphy and microorganisms of the Phaner- Е.А., 2015. A unique burial site of Early Creta- ozoic of Eurasia. Geos, Moscow, p. 268 (in Rus- ceous vertebrates in Western Siberia (the Shesta- sian). kovo 3 locality, Kemerovo Province, Russia). Tatarinov, L.P., Maschenko, E.N., 1999. A find of an Dokl. Biol. Sci. 462, 148–151. aberrant tritylodont (Reptilia, Cynodontia) in the Maschenko, E.N., Lopatin, A.V., 1998. First record of Lower Cretaceous of Kemerovo Region. Paleon- an Early Cretaceous triconodont mammal in Si- tol. Zh. 4, 85–92 (in Russian). beria. Bull. Inst. R. Sci. Nat. Belg., Sci. Terre 68, Voronkevich, A.V., 1998. A large representative of the 233–236. genus Psittacosaurus from the locality Shestako- O'Connor, J.K., Averianov, A.O., Zelenkov, N.V., vo-3, in: Vyltsan, I.A. (Ed.), Actual questions of 2014. A confuciusornithiform (Aves, Pygostylia)- the geology and geography of Siberia: Materials like tarsometatarsus from the Early Cretaceous of the scientific conference. Vol. 1. Tomskii Gos. of Siberia and a discussion of the evolution of Univ., Tomsk, pp. 190–193 (in Russian).

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Reinvestigation of an Early Cretaceous eutherian mammal Endotherium niinomii

N. Kusuhashi1, Y.-Q. Wang2 and C.-K. Li2

1Graduate School of Science and Engineering, Ehime University, Matsuyama, Ehime 790-8577, Japan; e-mail: [email protected] 2Key Laboratory of Vertebrate Evolution and Human Origins of Chinese Academy of Sciences, Institute of Vertebrate Paleontology and Paleoanthropology, Chinese Academy of Sciences, Beijing 100044, P.R. China

Various mammalian fossils have been dis- not sufficiently described and illustrated in the covered from the Lower Cretaceous (Aptian– paper. Therefore, the species is rarely mentioned Albian) Fuxin Formation in western Liaoning in recent papers on Mesozoic eutherians, and Province, northeastern China. They include eu- sometimes treated as a nomen dubium (e.g., triconodontans (three described species of two Kielan-Jaworowska and Cifelli, 2001). However, genera and a few other undescribed species), the coaly rock containing the remaining part of multituberculates (four described species of the type specimen is still housed in the Dalian three genera and a few other undescribed spe- Museum of Natural History, and the impres- cies), at least one undescribed species of spala- sions of the missing parts are preserved on it. cotheriids, and eutherians (Endotherium niinomii We reexamined the morphology of the type and other undescribed species) (Shikama, 1947; specimen based on the impressions and the orig- Kusuhashi et al., 2009a,b, 2010, 2015). inal description of Shikama (1947), preceding to The number of eutherian specimens collect- the study on our eutherian specimens from the ed from the Fuxin Formation reaches 40% of the Fuxin Formation. total collection. It implies that they were a dom- The dentaries of Endotherium niinomii are inant group of the mammalian fauna in East relatively slender and highly probably had five Asia at that time. Another dominant group is premolars and three molars. The entoconid and multituberculates, also constituting 40%. This hypoconulid of lower molars are not closely faunal composition is very different from that of twinned. These features imply that Shikama’s the Jehol Group, which is also distributed in (1947) attribution of the species to the Eutheria western Liaoning but is slightly older than the is reasonable. The species also has following Fuxin Formation; multituberculates and eutheri- characteristics: sizes of lower molars diminish ans were obviously minor elements in the distally; the height difference between the mammalian fauna from the group (Meng, 2014). trigonid and talonid of lower molars are mod- Eutherians from the Fuxin Formation, therefore, erate and smaller than those of other Early Cre- might provide the information about early di- taceous eutherians; lower molar cusps are versification of the group in East Asia. blunt; the protoconid is the largest among the Endotherium niinomii is a eutherian mammal trigonid cusps; the paraconid is as tall as the reported from the Fuxin Formation by Shikama metaconid. This suite of characters is enough (1947). Unfortunately, the important part of the diagnostic among Cretaceous eutherians, and type specimen including molars was lost some- we thus consider that E. niinomii is a valid spe- time after his observation, and the specimen was cies.

References

Kielan-Jaworowska, Z., Cifelli, R.L., 2001. Primitive Kusuhashi, N., Hu, Y.-M., Wang, Y.-Q., Setoguchi, boreosphenidan mammal (?Deltatheroida) from T., Matsuoka, H., 2009b. Two eobaatarid (Mul- the Early Cretaceous of Oklahoma. Acta Palaeon- tituberculata; Mammalia) genera from the Low- tol. Polonica 46, 377–391. er Cretaceous Shahai and Fuxin formations, Kusuhashi, N., Hu, Y.-M., Wang, Y.-Q., Hirasawa, S., northeastern China. J. Vert. Paleontol. 29, 1264– Matsuoka, H., 2009a. New triconodontids 1288. (Mammalia) from the Lower Cretaceous Shahai Kusuhashi, N., Hu, Y.-M., Wang, Y.-Q., Setoguchi, T., and Fuxin formations, northeastern China. Geo- Matsuoka, H., 2010. New multituberculate bios 42, 765–781. mammals from the Lower Cretaceous (Shahai

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and Fuxin formations), northeastern China. J. Meng, J., 2014. Mesozoic mammals of China: Implica- Vert. Paleontol. 30, 1501–1514. tions for phylogeny and early evolution of Kusuhashi, N., Wang, Y.-Q., Li, C.-K., Jin, X., 2015. mammals. Nat. Sci. Rev. 1, 521–542. Two new species of Gobiconodon (Mammalia, Eu- Shikama, T., 1947. Teilhardosaurus and Endotherium, triconodonta, Gobiconodontidae) from the Low- new Jurassic Reptilia and Mammalia from the er Cretaceous Shahai and Fuxin formations, Husin Coal-Field, south Manchuria. Proc. Japan northeastern China. Hist. Biol. 28, 14–26. Acad. 23, 76–84.

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Vitakri Dome of Pakistan – a richest graveyard of titanosaurian sauropod dinosaurs and mesoeucrocodiles in Asia

M.S. Malkani

Geological Survey of Pakistan, Upper Chattar 130 D, str. 16, Muzaffarabad, Azad Kashmir, Pakistan; e-mail: [email protected]

Titanosauriform/early titanosaurian sauropod Gspsaurus pakistani is based on most com- dinosaurs from Pakistan plete relatively large skull. The anterior dentary Brohisaurus kirthari is found in the lowest symphysis seems to be weak. The anterior por- part of the Upper Jurassic of the Sembar For- tions of dentary rami are V-shaped. It has rela- mation from Kirthar Range, Khuzdar District, tively long, narrow, slightly oval, slender and Balochistan. It is based on some poorly recog- slightly recurved teeth. nized postcranial elements. It shows apparent Saraikimasoom vitakri rostrum is of generally pneumaticity in thoracic ribs and a strongly an- long, narrow and moderate shallow shape (with teroposteriorly compressed femoral midshaft. 40° inclinations from horizontal). The anterior portions of upper and lower jaws are broadly Titanosaurian sauropod dinosaurs from arched forming U-shape. Teeth are long, narrow Pakistan and slender. A tooth slenderness index seems to Khetranisaurus barkhani is characterized by be 3–5. Its teeth are robust and straight relative slightly broad to sub squarish midcaudals. Its to Gspsaurus. It shows dental formula 4, 13/11– centrum is unique among Pakiforms having 17(?). The teeth row of left upper jaw seems to broad ventral centrum width than dorsal cen- be complete, and it gives the best information on trum width (Fig.1). the Titanosauria at a global level. Generally, the Sulaimanisaurus gingerichi is characterized titanosaurs were considered as bearing a Diplo- by long and squarish mid caudals, and it is docus-type skull, but moderate incline and mod- based on fragmentary caudal vertebrae and erate long well developed skulls are now found many referred vertebrae and bones from Sangi- in Pakistan (Fig. 1). ali, Shalghara and Mari Bohri localities. Nicksaurus razashahi is based on axial and Pakisaurus balochistani is based on four asso- limb elements and includes a pair of femora (left ciated tall caudal centra and also attributed full femur, right partial femur), a pair of stocky many fragmentary, associated and articulated distal tibiae, partial humerus parts; proximal ra- bones and pieces of bones belong to crania/skull, dius, five teeth in jaw ramus, chevron, cervi- vertebrae, ribs, sternal, scapulae, humerai, radi- cal/dorsal centrum (Fig. 1). The very broad na- us, ulnae, ilia, femora, tibia, fibula, foot bones, ture of holotypic caudals shows its relation to osteoderms, pieces of coprolite, etc. the family Saltasauridae. Marisaurus jeffi is based on six heavy and Maojandino alami is a titanosaurian sauro- slightly tall to squarish midcaudals. The ratio of pod with a thickest, broad and long neck, mid-dorsal width to mid-ventral width of mid short tail, heavy and stocky body. The holo- and posterior caudals is about 1.5. It is attributed typic materials include about 6 cervical, 4 dor- by cranial and postcranial materials. sal, and 10 caudal vertebrae along with partial Balochisaurus malkani were relatively most left femur, partial left and right tibiae, partial stocky and large bodied with stocky limbs. It is radius, a pair of partial distal scapulae, partial based on seven associated heavy and broad to sternal plate/ilia, some neural arch and lamina squarish (heart shape mid caudals) caudal ver- covered partially by yellow brown muds, etc. tebrae and also attributed many fragmentary, (Fig. 1). Although they are fragmentary and associated and articulated bones and pieces of disarticulated, they are associated, because all bones like postcrania, osteoderms, pieces of cop- of this material is found within one site of the rolite, etc. The ratio of mid-dorsal width to mid- same locality. M. alami may belong to the fam- ventral width of mid and posterior caudals is ily Balochisauridae of titanosaurian sauro- about 2. pods. 129

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New locomotion style of titanosaurs from Pakisauridae (titanosaurian sauropods) from Pakistan Pakistan. The distal scapula in Pakisaurus (and Less and more wide-gauge movements possibly other taxa of Pakisauridae) is deflected originally appeared in Balochisauridae and laterodorsally creating more wide gauge move-

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Cretaceous Ecosystems and Their Responses to Paleoenvironmental Changes in Asia and the Western Pacific ments, while the distal scapula in Marisaurus Theropod dinosaurs from Pakistan (and probably, Balochisaurus) of Balochisauridae Vitakridrinda sulaimani is a large bodied is straight or inclined slightly medially with less abelisaurian, based on a pair of left and right wide gauge movements. The features like prox- proximal femora as well as basioccipital condyle imal femur deflected medially, femoral eccen- alongwith partial braincase. It has referred many tricity, laterally beveled and fibular condyle of vertebrae and limb bones. Vitakrisaurus saraiki is femur, broad sacrum and ilia, laterodorsally de- a small-sized noasaurian based on isolated pes. flected distal scapula and large sternal plates are The large ratio between phalanges II–2 and II–1 the basic elements resulted in wide-gauge and proximally narrow metatarsal II (in dorsal movement parten of Pakiforms. view) also suggest noasaurids affinities, while Tail features of titanosaurs from Pakistan phalanx II–2 is longer than Velocisaurus (com- pared to phalanx II–1). Many smaller bones and A specific fossil tail with trispinous distal- phalanges are found just below the claw, which most caudal centrum, found in Pakistan for the may be the bones of left pes of Vitakrisaurus or first time, provides a new look on Titanosauria. may belong to the birds or other flying reptiles It has been found in the uppermost Cretaceous like pterosaurs. The noasaurids are represented Vitakri Formation (Sulaiman Basin, Pakistan). by Composuchus, Jubbulpuria, Laevisuchus, Fossil tail of titanosaurs from Pakistan is unique. Masiakasaurus, Noasaurus, Ornithomimoides, Ve- It seems to be robust and relatively short, and it locisaurus, and Vitakrisaurus. may serve for different purposes being a good defending tool from its foe, balancing body as a Footprints and trackways of dinosaurs from third support while searching food in tall tree, Pakistan – the fossils reported from Asia and mating. So far, this discovery shows an en- for the first time demic nature of Pakisauridae and Balochisauri- A herd of early titanosaurs (Malakhelisaurus dae. mianwali) has been revealed in Pakistan con- Osteoderms and dermal plates of dinosaurs from fronted by a running large theropod (Sa- Pakistan – the fossils reported from Asia for manadrinda surghari), that represents a confronta- the first time tion scenario. A couple of small theropods have been also found (Himalayadrinda potwari) (Fig. 1). Malkani (2003) reported four types of oste- The footprints and trackways of the titanosaur oderms of titanosaurs from Pakistan, for the first Pashtosaurus zhobi are found on the thick sand- time from Asia. Osteoderm scutes of mosaic stone bed of the latest Cretaceous Vitakri For- type are assigned to Marisaurus, large dermal mation (Balochistan, Pakistan). This discovery is armor of ellipsoid type is assigned to Balochisau- significant, because the bones and footprints are rus, and large dermal armor of ellipsoid type found in the same horizon and the same basin. with median cut is assigned to Pakisaurus. Some other bulb and root type osteoderms are also Pterosaur from the Latest Cretaceous Vitakri found in Pakistan. Formation of Pakistan Saraikisaurus minhui is based on dentary Coprolites of dinosaurs from Pakistan ramus with eight teeth. This ramus shows inter- Diverse coprolites of dinosaurs are found in nal pneumatic texture/structure. The teeth are India, but some small rounded to surrounded, oval to suboval, some overlapped. The total spongy/vesicular pieces of coprolites with diam- length of preserved dentary ramus is 5.8 cm. The eter of 5–7 cm are revealed in Pakistan (Fig. 1). dentary is slender. A dentary without teeth and These coprolite pieces are spongy. No grassy some limb bones with thick hollow and thin pe- material is visible by naked eye. ripheral bone and small size show their assign- Eggs of dinosaurs from India and Pakistan ment to pterosaur or bird (Fig. 1). Well preserved and diverse eggs of dino- Mesoeucrocodiles from Pakistan saurs were reported from India. The snake Pabwehshi pakistanensis is based on rostrum bones are found in one nest. Nevertheless, no and articulated partial dentary. The Sulaima- well recognized eggs are found in Pakistan. nisuchus kinwai is based on anterior dentary and

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The Fourth International Symposium of IGCP Project 608 – Novosibirsk 2016 splenial. The Induszalim bala is based on rostrum Induszalim, the large teeth dia is relatively more (Fig. 1), which shows anteriorly/anterodorsally than Pabwehshi tooth diameter, and there are pits directed external nares, very high/very deep and with anteroposterior lineation on the lateral side narrow rostrum, the laterally compressed teeth of maxillary ramus. Pabwehshi has no lineation. of ziphodont type (oval to D-shape, heterodont Induszalim shows marked boundary/contact be- in size), and thick rostral elements. In Induszalim, tween palatal shelves and maxillary wall, but the snout depth is equal to width, while in Pabwehshi shows no boundary/contact between Pabwehshi the depth is ¾ of width. In Induszalim, palatal shelves and maxillary wall. Induszalim is the maxillary ramus is relatively far away/down similar to Pabwehshi in having saggital torus on to palatal contact, while in Pabwehshi the maxil- palatal shelves. The Khuzdarcroco zahri is based lary ramus is just close to the palatal contact. In on one partial rib and referred half egg.

References

Malkani, M.S., 2003. Pakistani Titanosauria; are ar- moured dinosaurs? Geol. Bull. Univ. Peshawar 36, 85–91.

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Lithostratigraphy and biota of the Late Cretaceous dinosaur bearing Lameta and intertrappean sediments along Salbardi fault in Betul and Amravati districts of Central India

H. Sonkusare, B. Samant and D.M. Mohabey

PG Department of Geology, RTM Nagpur University, Law College Square, Amravati Road, Nagpur 440001, India; e-mail: [email protected]

The Deccan volcanic associated sediments with clay pockets in the basal part, and medium are designated as the infratrappean (Lameta to coarse grained sandstone, which is concre- Formation) occurring just below the earliest vol- tized in the upper parts covered with thin ve- canic flow in the basin and the intertrappean neer of chert. The 6–7 m thick calcretes formed deposited between the flows during the break in after the sandstone are nodular to massive at the volcanic activity. The sediments forming the different levels, with thin chert partings. The Lameta Formation are deposited in different in- calcretes at the top are mostly capped by chert land basins including the Salbardi basin in the (silcretes). Dinosaur and turtle bones are present Amravati District of Maharashtra and the ad- in the green sandstone, whereas the nests and joining Betul District of Madhya Pradesh in Cen- eggs are recorded in the upper part of the se- tral India. The Lameta sediments (Maastrichtian) quence in the calcretes. Parataxonomically, the rests over the Archaean basement or Gondwana eggs are of Megaloolithus affinity. Group of rocks, and are overlain by Deccan vol- To the south-west of Salbardi village, the canic sequence with intertrappean sediments good outcrops of intertrappean beds up to 2 m deposited at different stratigraphic levels. The thick are exposed in the localities at Hiradehi Gondwana shows faulted contact with Lameta and Topidhana. The sediments comprise black and Deccan trap. A thick pile of Deccan volcanic and gray chert, clay, shale, cherty shale and flows are present in the area, and they are classi- shaly marly limestone. Molluscs mainly repre- fied as the Satpura Group to the north and the sented by Physa, Paludina, Lymneae and Unio are Sahyadri Group to the south of Salbardi fault. present in the sediments with scarce wood The associated intertrappean beds in the area fragments. During the palynological study, dif- lithologically comprise chert, cherty and nodular ferent types of pennate diatoms characterised by limestone, clay, shale, cherty and tuffaceous rectangular elongate and square shape were re- shale. covered from the Topidhana sections, whereas The 14 m thick Lameta Formation in the mycorrhizal fungi, cuticles of plants and other lower part comprises 5–6 m thick conglomeratic microflora were recovered from the Hiradehi and pebbly green to grey sandstone associated sections.

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Early Cretaceous fossil sites in Kalasin Province, Thailand

O.-U. Summart, K. Wongko and Ph. Chantasit

Department of Mineral Resource, Rama VI Road, Bangkok 10400, Thailand; e-mail: [email protected]

Since the 1980s, Thai–French Research Pro- More than 700 pieces of bones and five new jects on the Mesozoic vertebrates of Thailand species are found in the Sao Khua Formation have resulted in the discovery of many dinosaur (Early Cretaceous) at Phu Khum Kao hill of Kal- localities ranging in age from Late Triassic to asin Province. One of the specimens is the most Early Cretaceous. After the discovery, the study complete dinosaur skeleton found to date in of the dinosaurs of Thailand has increased con- Thailand. It was named as a “dinosaur’s grave- siderably. yard”. The Phu Faek Park is other place in the Thai dinosaurs, recorded non-marine Mes- Kalasin Province that discovered theropod foot- ozoic environments, are quite abundant on the prints of various sizes. No skeletal remains of Khorat Plateau. The Khorat Group is a rock dinosaurs have yet been found in the Phra Wi- group that is represented by the deposits of the han Formation (Early Cretaceous). The last Cre- Khorat Plateau in the northeastern part of Thai- taceous fossil site is located beside of the Lam land, ranging in age from 100 to 230 million Pao River. The large bone of sauropod, teeth of years. This red bed has yielded 16 species of di- spinosaurid and accompanying vertebrate fossil nosaurs, including the allosaurid or metriacan- fauna are found here. thosaurid (Siamotyrannus) and the oldest known The discovery of fossil sites in this area pro- sauropod (Isanosaurus) in the world. In North- vides the important paleontological data for the east Thailand, dinosaurs are abundant in the Sao study of dinosaur successions in Thailand. Con- Khua Formation containing various theropods sequently, Department of Mineral Resources has and sauropods. The Kalasin Province is one of developed large dinosaur museum and paleon- the most important areas for dinosaur discovery tology institute, which become the significant in Thailand. Dinosaur bones, other vertebrate tourist attraction and learning center of Thailand fossils and dinosaur trackways are found in and Southeast Asia. three Cretaceous formations: the Sao Khua For- Keywords mation, the Phra Wihan Formation, and the Thai dinosaurs, Khorat Group, Mesozoic verte- Khok Kruat Formation. brates.

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Научное издание

Меловые экосистемы и их реакции на изменения палеосреды в Азии и Западной Пацифике

Материалы Четвертого Международного Симпозиума Международной программы по геонаукам МПГК проект 608

15–20 августа 2016 г. Новосибирск, Россия

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