The Proceedings of
The 6th International Symposiumof International Geoscience
Programme IGCP Project 608“Cretaceous Ecosystems
and Their Response to
Paleoenvironmental Changes
in Asia and the Western Pacific”

November 11-17, 2018
Khon Kaen-Kalasin, Thailand

The 6th International Symposiumof International Geoscience
Programme IGCP Project 608“Cretaceous Ecosystems
and Their Response to
Paleoenvironmental Changes
in Asia and the Western Pacific”

Copyright © 2018 All Right Reserved by the 6th IGCP608 Organizing Committee

PREFACE
We cordially invite you to participate in the 6th International
Symposium of IGCP608, which will be held from November 11 to 17,
2018 in Khon Kaen - Kalasin Province, Thailand.
The mechanisms underlying the evolution of the Asia-PacificCretaceous ecosystems are far from being fully understood. The IGCP608
project is aimed to reconstruct the Cretaceous ecosystems and thehistory of their responses to paleoenvironmental changes in Asia andthe Western Pacific. The Symposium will serve as a platform for participants to share their views on the paleoenvironmental changes impacts both on terrestrial and marine ecosystems. The scientific programme will cover a wide range of topics including paleoclimate,paleogeography, paleontology, stratigraphy, tectonics, and petroleum
geology.
The symposium is dedicated to the 10th anniversary of the Sirindhorn Museum. The Sirindhorn Museum is an important tourist attraction of Thailand. It is a well-known dinosaur museum containing
new dinosaur genera and species first found in Thailand. These new
dinosaurs are important additions to our knowledge of dinosaur diversity during the Mesozoic Era. Moreover, the museum is a research institution, and its beauty attracts large numbers of both Thai and foreign
tourists. Thus far, more than 3,000,000 people have visited the museum,and each passing year adds significantly to this total. The museum has
a conservation approach to tourism activities and promotes cooperation
with local communities, helping local people to supplement their income by producing and selling souvenirs.
The 6th International Symposium of the IGCP608 in Khon Kaen Kalasin Province will provide an opportunity for discussion of the latest
advances in studies of Asia-Pacific Cretaceous ecosystems. In addition
to scientific sessions, the pre-symposium field excursion will be organized in the Khorat Plateau, Northeastern Thailand to observe the Jurassic-Cretaceous non-marine deposits (Khorat Group) with abundantdinosaurs and other geo-conservation sites.

Executives
andOrganizing
Committee
IGCP 608 Project LeadersProf. 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

Organizing Committee of
the Sixth International Symposium of IGCP608• Director General,
Department of Mineral Resources (Honorary Chairman)• Deputy Director General,
Department of Mineral Resources (Chairman)• Deputy Director General,
Department of Mineral Resources (Co-Chairman)• Dr. Adichat Surinkum, Director of CCOP (Co-Chairman)• Mr. Naramase Teerarungsigul, Senior Expert,
Department of Mineral Resources (Vice-Chairman)• Mr. Surachai Siripongsatearn,
Director of Geological Survey Division (Vice-Chairman)• Mr. Suvapak Imsamut,
Director of Geological Resources Conservation and Management
Division (Vice-Chairman)• Mrs. Benja Sekthera,
Senior Expert, Department of Mineral Resources• Dr. Suree Teerarungsigul,
Director of Environmental Geology Division• Mr. Nimit Sornklang,
Director of Fossil Protection Division• Mr. Tinnakorn Tatong,
Director of Office of Mineral Resources Region 2• Dr. Apsorn Sardsud,
Director of Research Center• Mr. San Assavapatchara, Senior Geologist• Miss Pannipa Saetian, Senior Geologist• Mrs. Dhanyadhorn Thonnarat, Senior Geologist• Mr. Kitti Khaowiset, Senior Geologist• Dr. Pradit Nulay, Senior Geologist• Dr. Phornphen Chanthasit, Senior Geologist• Mr. Kajornphat Suksriboonampai, Senior Geologist• Miss Orn-Uma Summart, Director of Sirindhorn Museum(Symposium Secretary)

CONTENTS
PREFACEI

ORGANIZING COMMITTEEIICONTENTSVI

TIME SCHEDULE

XIX

PROGRAM SCHEDULE

XXIABSTRACT AND EXTENDED ABSTRACTXXXIA Cenomanian-Turonian Pelecypodal Faunule From the Upper Pan Laung
Formation, Kinda Area, Myittha Township, East Central Myanmar

1

A review of dinosaurs in Thailand

3

All about Sirindhorna khoratensis (Ornithopoda; Hadrosauroidea)

4

Belemnite diversity across the Jurassic–Cretaceous boundary in Russiannorthern Eurasia

6

Buchia associations and interregional correlation of the Jurassic–Cretaceous
boundary interval in Russian Boreal basins: new data from the Russian platform,
Siberia, and the Far East

8

Carettochelyid turtle from the Lower Cretaceous of Japan and the diversificationof the pan-trionychian turtles

10

CLMTV cooperation and compilation of the Jurassic and Cretaceous Mapping

12

Coal-forming Plants of The Early Cretaceous kuti formation (South-eastern
Transbaikalia, Russia)

14

By: Myo Myint and Thaw Tint

Varavudh Suteethorn, Suravech Suteethorn, Phornphen Chanthasit and Eric BuffetautIV

By: Masateru Shibata, Pratueng Jintasakul Yoichi Azuma, Duangsuda Chokchaloemwong andSoichiro Kawabe

By: O.S. Dzyuba

By: B.N. Shurygin, O.S. Urman and O.S. Dzyuba

By: Teppei Sonoda, Wilailuck Naksri, Masateru Shibata and Yoichi Azuma

By: Adichart Surinkham

By: E.V. Bugdaeva, V.S. Markevich, N.G. Yadrishchenskaya, A.V. Kurilenko, T.A. Kovaleva

Cretaceous Formation of part of East coast of India

18

Depositional environment of Lower Cretaceous lacustrine sedimentary rocks inCentral Mongolia

19

Depositional processes and transport mechanism of upper Ullyonsan
Conglomerates in the Cretaceous Yeongyang Subbasin of Gyeongsang
Sedimentary Basin, Korea

21

Detrital zircon U-Pb and radiolarian biostratigraphy in the Tethys Himalaya,southern Tibet: Constraints on the Timing of Initial Indian-Asia Collision22

Dinoflagellate cyst Biostratigraphy of Eocene in Duina, Yadong, Tibet, China

24

Distribution of Charophytes in the lower Cretaceous of the lake basins in
Mongolia and conditions of their growth27

Facies and geochemical analysis for basin evolution of the late Cretaceous Neungju Basin, SW Korea – a preliminary study

30

Flora of coal-bearing deposits of central Transbaikalia (Russia)

31

Holocene Climate and Environmental Changes in Mongolia as Recorded in The
Sediments of Lake: A Review

35Integrated study of volcano-stratigraphy, magneto-stratigraphy, reptilian
tetropods and palynology: tracking biotic and environmental changes acrossCretaceous-Palaeogene during Deccan volcanism.

36

By: Jayaraju, N

By: Bat-Orshikh Erdenetsogt, Sung Kyung Hong, Jiyoung Choi, Boldbaatar Gantulga, Niiden
Ichinnorov, Nyamsambuu, Odgerel, Gombosuren Tsolmon, Norov Baigalmaa1, Enkhbayar
Bolormaa

By: Ki-Hun Yu, Daekyo Cheong, Daewoo Kim

V

By: Tianyang WANG, Guobiao LI, Zhang Wenyuan, Xinfa LI and Xusong Ma

By: Wenyuan Zhang, Youjia Yao, Yuewei LI, Tianyang Wang, Xinfa LI and Guobiao LI

By: Gereltsetseg Lkhagva

By: Hyojong Lee and Taejin Choi

By: E.V. Bugdaeva, V.S. Markevich, T.A. Kovaleva

By: Oyunchimeg Tserentsegmid

By: Dhananjay M. Mohabey and Bandana Samant

CONTENTS
Late Cretaceous paleogeography of the Deccan Volcanic Province, peninsular
India: palynological evidence

39

Late Cretaceous Vertebrate Faunal Similarities between India and Madagascar:
Palaeobiogeographic Scenarios

40

Late Jurassic – Early Cretaceous Belemnites in Gyangze, Southern Tibet, China

41

Lithostratigraphy of the Berapit formation along the Malaysia-Thailand border

42

Lower Cretaceous oysters from Mangyshlak peninsula (northwestern
Kazakhstan) and Crimea peninsula: taxonomical composition and stratigraphic
distribution (preliminary data)43

Non-marine Cretaceous turtles of Japan and its significance forpaleoenvironmental analysis

47

Palaeoecology of a Maastrichtian lake during Deccan environmental transition:evidences from Malwa Plateau

49

Palynoflora and microfauna from Late Cretaceous Lameta sediments andIntertrappean sediments of Nand-Dongargaon and Salbardi-Belkher inland basinsof central India: age and paleoenvironment implications

51

Palynology studies of the Talbulag coal deposit, Eastern Mongolia

53

Plant Fossils from the Lower Cretaceous in Shandong Province, China

54

Preliminary study on the growth of Fukuiraptor kitadaniensis (Dinosauria:
Theropoda)

56

By: Vandana Prasad and Sunil Bajpai

By: Guntupalli V.R. Prasad

By: Liping Hu, Yuewei LI, Qi LI, Weiyuan ZHANG, Guobiao LI

By: Mat Niza bin Abdul Rahman and 2Mohamad Hussein bin Jamaluddin

VI

By: Igor N. Kosenko, Egor K. Metelkin

By: Ren Hirayama

By: Dhobale Anup, Dhananjay M. Mohabey, Deepesh Yadav and Bandana Samant

By: Hemant Sonkusare, Bandana Samant and D.M. Mohabey

By: Ichinnorov N., Tsolmon G., Eviikhuu A., Enerel G., Odgerel N.

By: Sun Bainian, Jin Peihong, Hua Yifan,Huang Rehan

By: Soki Hattori, Yoichi Azuma, Soichiro Kawabe

Preliminary study on the provenance of the Hayang Group sandstones in the
Gyeongsang Basin, Korea using detrital zircon geochronology

57

Provenance of the Cretaceous Neungju Basin, Korea

58

Refined chronostratigraphy of the late Mesozoic terrestrial strata in South China
and its tectono-stratigraphic evolution

59

Review and Revision of the socalled “Khorat GRoup”, NE, Thailand

60

Searching for the non-marine Jurassic/Cretaceous boundary in northeastern China

62

Sedimentology and stratigraphy of Phuwiang Dinosaur excavation sites, Khon
Kaen Province, northeastern Thailand

63

Significance of Cretaceous strata in the Japanese Islands: Cretaceous
continental arc-trench system

64

Stratigraphy and Structure of Jurassic – Cretaceous Rocks in the Thong San
Khan and Chat Trakan Areas, Northern Thailand.

66

Terrestrial climates in East Asia during the Cretaceous inferred from the stable
oxygen and carbon isotope compositions of vertebrate apatites; Further results

67

The depositional environments of the Late Jurassic-Early Cretaceous Phu Noi
dinosaur site, Phu Kradung Formation, Kalasin, northeastern Thailand

69

The Early Cretaceous angiosperm pollen of Transbaikalia and Primorye region (Russia)

70

By: Taejin Choi, Min Gyu Kwon

By: Min Gyu Kwon, Taejin Choi, Seung Won Shin

By: Xianghui Li, Chaokai Zhang, Yongxiang Li, Yin Wang and Ling Liu

By: Nares Sattayarak

By: Pitaksit Ditbanjong, Kritsada Moonpa, Nontawat Srisomporn, Nuttawat Obaom, Kamonlak
Wongko and Phornphen Chanthasit

By: Hisao Ando and Masaki Takahashi

By: Pongsathon Kanna, Weerapan Srichan, Phisit Limtrakun, Boontarika Srithai, Pitaksit
Ditbanjong and Rattanaporn Fongngern

By: Romain Amiot

By: Rattanaphorn Hanta, Phornphen Chanthasit, Kajeepan Sorndech, and Jiraporn Promthong

By: E.V. Bugdaeva, V.S. MarkevichVII

By: Gang Li, Atsushi Matsuoka

CONTENTS
The Early Cretaceous Birds from the Kitadani Formation, Katsuyama, Fukui,Japan: a Unique Window to the Extinct Avifauna in the Far East74

The Facies Analysis of Sedimentology of the Phu Tok Noi architecture, Phu Tok
Formation, Khorat Plateau, Northeast Thailand.

77

The Skull of Pelecanimimus Polyyodon (Theropoda, Lower Cretaceous, Spain):Comparative Approach to Asian Ornithomimosauria.

78

Through The Looking Glass: Insights From Radiolarian Research in Elucidating
The Geologic Evolution of The Philippines

81

Turtles from the Lower Cretaceous Khok Kruat Formation of Nakhon Ratchasima,Northeastern Thailand: New data83

Upper Cretaceous palynofloras from the Himenoura Group (South West Japan)
and consequences for the Normapolles and Aquilapollenites palynologicalprovinces in eastern Asia

84

Vertebrate remains from the Early Cretaceous fluvial deposits of Phu Wiang
Valley, Khon Kaen Province, Northeastern Thailand85

By: Imai, T., Azuma, Y., Shibata, M., Kawabe, S., Miyata, K., and Tsukiji, Y.

By: Kiattisak Sonpirom, PeangtaSatarugsa, and Natthawiroj Silaratana

By: Elena Cuesta, Francisco Ortega and José Luis Sanz

By: Edanjarlo J. Marquez, Karlo L. Queaño and Carla B. Dimalanta

VIII

By: Wilailuck Naksri, Teppei Sonoda, Duangsuda Chockchaloemwong, Masateru Shibata,
Yoichi Azuma and Pratueng Jintasakul

By: Julien Legrand, Toshifumi Komatsu, Yuka Miyake, Takanobu Tsuihiji and Makoto Manabe

By: Kamonlak Wongko, Phornphen Chanthasit and Chompoonoot Chanwicha

Diversity of Mesozoic crocodiles in the northeastern Thailand

86

By: Komsorn Lauprasert and Jérémy Martin

Academic Values of Mudeungsan UNESCO Global Geopark87

By: Min HUH, Yeon WOO and Jong-Sun KIM

Dinosaurs, Birds and Pterosaurs of Korea: A Paradise of Mesozoic Vertebrates
By: MIN HUH and JEONG YUL KIM

89

Sedimentary Environments of the Lower Formations of the Cretaceous
Yeongyang Subbasin of the Gyeongsang Sedimentary Basin in Bonghwa-gun,
Gyeongsangbuk-do, Korea

93

By: Eun-Hye Kong and Daekyo Cheong

Radiolarian assemblage of Barremian to Aptian interval in the
Tethys and the influence of the oceanic anoxic event (OAE) 1a

95

IX

By: Li Xin, Matsuoka Atsushi, Bertinelli Angela, Chiari Marco, and Wang Chengshan

GENERAL INFORMATION
11-17 November 2018 Thailand

XDetail of Scientific ProgrammeThursday, November 15, 2018
Srichan 1 Room, Charoen Thani HotelTIME

PROGRAMME

8.30-9.00

Registration

9.00-9.45

Welcome speech by: Address by the governor of Khon Kaen Province
Speech by: IGCP 608 leader
Opening address by: Director General of Department of Mineral ResourcesGroup Photo

9.45-10.00

Coffee break

10.00-10.30

Keynote: Review and Revision of the so-called ‘Khorat Group’, NE, Thailand
By: Nares Sattayarak

10.30.-11.00

Keynote: A reviews of Dinosaurs in Thailand
By: Varavudh Suteethorn

11.00-11.30

Keynote: Significance of Cretaceous strata in the Japanese Islands: Cretaceous
By: Hisao Ando, Masaki Takahashi

Cretaceous Terrestrial and Marine Environments in Asia and the Western Pacific
Chairman: Mr. Nares Sattayarak
11.30-11.45

UNESCO Global Geoparks of Korea: Focusing on Mudeungsan UGGp
By Min Huh

11.45-12.00

The facies analysis of sedimentology of the Phu Tok Noi architecture, Phu Tok
Formation, Khorat Plateau, Northeast Thailand.
By Kiattisak Sonpirom, Peangta Satarugsa, Natthawiroj Silaratana

12.00-13.00

Lunch

Cretaceous Terrestrial and Marine Environments in Asia and the Western Pacific
Chairman: Prof. Hisao Ando
13.00-13.15

CLMTV cooperation and compilation of the Jurassic and Cretaceous mapping
By Adichat Surinkum, Director of CCOP

13.15-13.30

Searching for the non-marine Jurassic/Cretaceous boundary in northeastern China
By Gang Li, Atsushi Matsuoka

13.30-13.45

Lithostratigraphy of the Berapit Formation along the Malaysia-Thailand border
By Mat Niza bin Abdul Rahman, Mohamad Hussein bin Jamaluddin

13.45-14.00

Through the looking glass: Insights from radiolarian research in elucidating thegeologic evolution of the Philippines
By Edanjarlo J. Marquez, Karlo L. Queaño, Carla B. Dimalanta

XI

continental arc–trench system

14.00-14.15

Facies and geochemical analysis for basin evolution of the Late Cretaceous Neungju
Basin, SW Korea – a preliminary study
By Hyojong Lee,Taejin Choi

14.15-14.30

Detrital zircon U-Pb and radiolarian biostratigraphy in the Tethys Himalaya, southern
Tibet: constraints on the timing of Initial Indian–Asia Collision
By Tianyang Wang, Guobiao Li, Zhang Wenyuan, Xinfa Li, Xusong Ma

14.30.14.45

Refined chronostratigraphy of the late Mesozoic terrestrial strata in South China and its
tectono-stratigraphic evolution
By Xianghui Li, Chaokai Zhang, Yongxiang Li, Yin Wang, Ling Liu

14.45-15.00

Coffee BreakCretaceous Terrestrial and Marine Environments in Asia and the Western Pacific
Chairman: Prof. Sunil Bajpai
15.00-15.15

Integrated study of volcano-stratigraphy, magneto-stratigraphy, reptilian tetropods andpalynology: tracking biotic and environmental changes across Cretaceous–Palaeogene
during Deccan volcanism
By Dhananjay M. Mohabey, Bandana Samant

15.15.15.30

Palaeoecology of a Maastrichtian lake during Deccan environmental transition:evidences from Malwa Plateau
By Dhobale Anup, Dhananjay M. Mohabey, Deepesh Yadav and Bandana Samant

15.30-15.45

XII

Palynoflora and microfauna from Late Cretaceous Lameta sediments and Intertrappean
sediments of Nand–Dongargaon and Salbardi–Belkher inland basins of central India:
age and paleoenvironment implications
By Hemant Sonkusare, Bandana Samant and D.M. Mohabey

15.45-16.00

Cretaceous formations of part of East Coast of India
By Jayaraju Nadimikeri

16.00.16.15

Terrestrial climates in East Asia during the Cretaceous inferred from the stable oxygenand carbon isotope compositions of vertebrate apatites: further results
By Romain Amiot

16.15-16.45

Poster Session

17.00-18.00

Culter programme

18.30-21.30

Welcome Dinner

Friday, November 16, 2018
Srichan 1 Room, Charoen Thani Hotel
Evolution of Cretaceous Terrestrial and Marine Ecosystems in Asia and the Western Pacific

Chairman: Dr. Dhananjay M. Mohabey
8.30-8.45

Plant fossils from the Lower Cretaceous in Shandong Province, China
By Sun Bainian, Jin Peihong, Hua Yifan, Huang Rehan

8.45-9.00

Flora of coal-bearing deposits of Central Transbaikalia (Russia)
By Eugenia V. Bugdaeva, Valentina S. Markevich, Tatiana A. Kovaleva

9.00-9.15

The Early Cretaceous angiosperm pollen of Transbaikalia and Primorye region (Russia)
By Eugenia V. Bugdaeva, Valentina S. Markevich

9.15-9.30

Palynology studies of the Talbulag coal deposit, Eastern Mongolia
By Niiden Ichinnorov, Gombosuren Tsolmon, Adiya Eviikhuu, Gantulga Enerel,
Nyamsambuu Odgerel

9.30-9.45

Late Cretaceous paleogeography of the Deccan Volcanic Province, peninsular India:
palynological evidence
By Vandana Prasad, Sunil Bajpai

9.45-10.00

Upper Cretaceous palynofloras from the Himenoura Group (Southwest Japan) andconsequences for the Normapolles and Aquilapollenites palynological provinces ineastern Asia
By Julien Legrand, Toshifumi Komatsu, Yuka Miyake, Takanobu Tsuihiji, Makoto Manabe

10.00-10.15

Coffee-breakEvolution of Cretaceous Terrestrial and Marine Ecosystems in Asia and the Western Pacific
Chairman: Prof. Daekyo Cheong
10.15-10.30

Belemnite diversity across the Jurassic–Cretaceous boundary in Russian northern Eurasia
By Oksana S. Dzyuba

10.30.-11.00

Buchia associations and interregional correlation of the Jurassic–Cretaceous boundary
Far East
By Boris N. Shurygin, Olga S. Urman and Oksana S. Dzyuba

11.00-11.30

Lower Cretaceous oysters from Mangyshlak peninsula (northwestern Kazakhstan) andCrimea peninsula: taxonomical composition and stratigraphic distribution (preliminary
data)
By Igor N. Kosenko, Egor K. Metelkin11.30-11.45

Radiolarian assemblage of Barremian to Aptian interval in the Tethys and the influenceof the oceanic anoxic event (OAE) 1a
By Xin Li

11.45-12.00

Dinoflagellate cyst biostratigraphy of Eocene in Duina, Yadong, Tibet, China
By Wenyuan Zhang, Youjia Yao, Yuewei Li, Tianyang Wang, Xinfa Li, Guobiao Li

12.00-13.00

Lunch

Evolution of Cretaceous Terrestrial and Marine Ecosystems in Asia and the Western Pacific

Chairman: Dr. Adichat Surikum
13.00-13.30

Keynote: Diversity of Mesozoic Crocodiles in the northeastern Thailand
By Komsorn Lauprasert

13.30-13.45

Vertebrate remains from the Early Cretaceous fluvial deposits of Phu Wiang Valley,
Khon Kaen Province, Northeastern Thailand
By Kamonlak Wongko, Phornphen Chanthasit, Pitaksit Ditbanjong

XIII

interval in Russian Boreal basins: new data from the Russian platform, Siberia, and the13.45-14.00

Non-marine Cretaceous turtles of Japan and its significance for paleoenvironmental
analysis
By Ren Hirayama

14.00-14.15

Carettochelyid turtle from the Lower Cretaceous of Japan and the diversification of the
pan-trionychian turtles
By Teppei Sonoda

14.15-14.30

Turtles from the Lower Cretaceous Khok Kruat Formation of Northeastern Thailand:
new data
By Wilailak Naksri

14.30-14.45

Coffee Break

Evolution of Cretaceous Terrestrial and Marine Ecosystems in Asia and the Western Pacific

Chairman: Dr. Romain Amiot
14.45-15.00

All about Sirindhorna khoratensis (Ornithopoda; Hadrosauroidea)
By Masateru Shibata

15.00-15.15

The Early Cretaceous Birds from the Kitadani Formation, Katsuyama, Fukui, Japan: aunique window to the extinct avifauna in the Far East
By Takuya Imai, Yoichi Azuma, Masateru Shibata, Soichiro Kawabe, Kazunori Miyata, Yuta
Tsukiji

15.15-15.30

Late Cretaceous Vertebrate faunal similarities between India and Madagascar:

XIV

palaeobiogeographic scenarios
By Guntupalli V.R. Prasad
15.30-15.45

Holocene climate and environmental changes in Mongolia as recorded in the sedimentsof lakes: a review.
By Oyunchimeg Tserentsegmid

15.45-16.00
16.00-16:45

Closing Symposium Session By the IGCP 608 leader
Project Summary of IGCP608 By Hisao Ando
Next new project proposal following IGCP608 By Gang Li

16.20-18.00

Business Meeting: Kaen Nakhon Room, Charoen Thani Hotel
Project Summary of IGCP608 (2013-2017+2018)
Next new project proposal following IGCP608

18.30-21.30

Farewell Party

Poster Presentation

2.

3.

4.

5.
6.

7.

8.
9.

10.

11.

12.

Depositional environment of Lower Cretaceous lacustrine sedimentaryrocks in Central Mongolia
By Bat-Orshikh Erdenetsogt, Sung Kyung Hong, Jiyoung Choi, Boldbaatar
Gantulga, Niiden Ichinnorov, Nyamsambuu Odgerel, Gombosuren Tsolmon,
Norov Baigalmaa, Enkhbayar Bolormaa
Depositional processes and transport mechanism of upper Ullyonsan Conglomerates in the Cretaceous Yeongyang Subbasin of Gyeongsang Sedimentary Basin, Korea
By Ki-Hun Yu, Daekyo Cheong, Daewoo Kim
The skull of Pelecanimimus polyodon (Theropoda, Lower Cretaceous,
Spain): comparative approach to Asian Ornithomimosauria
By Elena Cuesta, Francisco Ortega, José Luis Sanz
Distribution of Сharophytes in the lower Cretaceous of the lake basins in
Mongolia and conditions of their growth
By Gereltsetseg Lkhagvaa
Provenance of the Cretaceous Neungju Basin, Korea
By Min Gyu Kwon, Taejin Choi, Seung Won Shin
Sedimentology and stratigraphy of Phuwiang Dinosaur excavation sites,
Khon Kaen Province, Northeastern Thailand
By Pitaksit Ditbanjong, Kritsada Moonpa, Nontawat Srisomporn, Nuttawat
Obaom, Kamonlak Wongko, Phornphen Chanthasit
Depositional environments of the Early Jurassic Nam Phong Formation in
Nong Bua Daeng District, Chaiyaphum, northeastern Thailand
By Rattanaphorn Hanta
The cranial endocranial of Phuwiangosaurus sirindhonae
By Siripat Kaikaew
Preliminary study on the growth of Fukuiraptor kitadaniensis (Dinosauria:
Theropoda)
By Soki Hattori, Yoichi Azuma, Soichiro Kawabe
Preliminary study on the provenance of the Hayang Group sandstones in
the Gyeongsang Basin, Korea using detrital zircon geochronology
By Taejin Choi, Min Gyu Kwon
Stratigraphy and Structureof Jurassic – Cretaceous Rocks in the Thong San
Khan and Chat Trakan Areas, Northern Thailand
By Pongsathon Kanna, Weerapan Srichan, Phisit Limtrakun, Boontarika Srithai,Pitaksit Ditbanjong, Rungroj Benjakul and Rattanaporn Fongngern
Late Jurassic – Early Cretaceous Belemnites in Gyangze, Southern Tibet,
China
By Liping Hu, Yuewei Li, Qi Li, Weiyuan Zhang, Guobiao Li

XV

1.

XVI

ABSTRACTThe Sixth International Symposiumof International Geoscience Programme
IGCP Project 608“Cretaceous Ecosystems and Their Response
to Paleoenvironmental Changes in Asia andthe Western Pacific”
November 11-17, 2018, Khon Kaen-Kalasin, Thailand

1

The Sixth International Symposium of International Geoscience Programme IGCP Project 608

A Cenomanian-Turonian Pelecypodal Faunule From
the Upper Pan Laung Formation, Kinda Area, Myittha Township,
East Central Myanmar
Myo Myinta and Thaw Tintb
Department of Geology, University of Yangon, Myanmar
corresponding address: a: Department of Geosciences, Universiti Teknologi PERTONAS, Seri Iskandar, Perak, Malaysia
Hph: +60 11 2688 0789; email: myomyint61@yahoo.com/myo.myint@utp.edu.my

Abstract
The newly updated contribution herein highlights the Cenomanian-Turonian
pelecypodal faunule representing the upper most part of the Pan Lung Formation, which
was based on the part of master thesis submitted to Department of Geology, University of
Yangon, Myanmar, in 1990. A hitherto unknown Cenomanian-Turonian pelecypodal faunuleconsisting of Protocardium hillanim Sowerby, Inoceramus panlaungenesis n. sp. andChlamys pauciradiatus n. sp., and associated with fragments of naculids, was discoveredfrom interbedded mudstone and sandstone of the upper Pan Laung Formation exposed on
the west bank of the Pan Laung River, half-a-mile southwest of Peinhnebin village, Kinda
area, Myittha Township, which highlights the extension of the Cenomanian-Turonian marinetransgression over this segment of the western margin of the Shan-Thai Terrane called
Sibumasu Terrane (Figures 2, 3 and 4).
The Jurassic-Cretaceous Pan Laung Formation (Garson, et al.; 1976), carrying thePelecypodal faunule is described lies just on the west of the Pan Laung Fault Zone along
which the present Pan Laung River takes its course from the south to the north and which
delimits the eastern boundary of the Jurassic - Cretaceous sequence on the west that madeup the Tagondaing range (Myo Myint, 1990) (Figures 1). Moreover, The Pan Laung Formation isdefined as Necomian by Chit Saing (2000) and mid Jurassic to mid Cretaceous by Myint Theinet al (2000). The faunule bearing unit as exposed half-a-mile southwest of Peinhnebin village(Grid 819758, Map 93 C-8) is mainly gray calcareous siltstones and mudstones which havebeen extensively sheared and tightly folded. Further southwest and up the hill andunderlying the Cretaceous without any evidence of a stratigraphic lacuna is mudstone unitthat bears Thracia luducensis Hayami (1972) and other bivalves indicating Toarcian (MyoMyint, 1990). The entire Jurassic-Cretaceous sequence on the west bank has entirely dips
through the dip amounts and intensity of deformation considerably increase toward themain Pan Laung Fault Zone to the east. On the south and north of the CenomanianTuronian exposure that lies on the tip of the eastern spur of the Tagondaing range, run
oblique cross faults (NE-SW) that had cut off thenorthern and southern continuation of the Cretaceous exposure under discussion.
The regional structural pattern along the Pan Laung valley is such that Mesozoic units(Anisian? to Turonian) trapped west of the Shan-scarp Fault (Nwalabo-Ezwe Fault by Garson
et al, 1976) (Figure 2) and east of the post- Cretaceous granodiorite batholiths emplacement

2and its apophyses, have been cut up into N-S elongated conspicuous wedges by the main
longitudinal
Pan Laung Fault and its complementary sets of faults and a series of cross faults
resulting in isolated, disconnected blocks of different lithologic sequence and age, and also
assuming varying elevations all along this structural complex belt.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

A review of dinosaurs in Thailand
Varavudh Suteethorn1, Suravech Suteethorn1,2, Phornphen Chanthasit3 and Eric Buffetaut1,41

Palaeontological Research and Education Centre, Mahasarakham University, Maha Sarakham, Thailand 44150
2
Department of Biology, Faculty of Science, Mahasarakham University, Maha Sarakham, Thailand 44150
3
Sirindhorn Museum, Department of Mineral Resources, Sahatsakhan, Kalasin, 46140 Thailand
4
Centre National de la Recherche Scientifique, UMR 8538, Laboratoire de Géologie de l’Ecole Normale Supérieure, 24 rue
Lhomond, 75231 Paris Cedex 05, France

Abstract
Since the first dinosaur bone of Thailand found in 1980s, there were at least 34
species of dinosaur including 27 taxa from osteological evidences and 7 ichnotaxa. Most ofthem came from the members of Khorat plateau. While, the others were deposited in the
red bed from Phra Yao (northern), Trad (eastern) and Krabi (southern). The oldest dinosaurbone bed is started from the Triassic Nam Phong Formation in northeastern Thailand. Thisbone bed yielded one of the oldest sauropod dinosaurs, Isanosaurus attavipachi, andprosauropod. The younger formation was represented by the Late Jurassic Phu Kradung
Formation. New discovery has unveiled the dinosaur sanctuary. More than ve thousandbones of several dinosaurs taxa and individuals have been found, i.e., mamenchisaurid,
sinraptorid, stegosaurid and ornithichian. Also, crocodiliformes, turtles, bony fishes, fresh
water sharks and pterosaur were found from this locality. Recent studies have conclusively
shown this assemblage containing is very reminiscent of that from some Chinese formation,
notably the Upper Shaximiao Formation of Sichuan. Comparative studies from this locality
may lead to a better understanding of the palaeobiogeographical events linked with faunalchange during the Late Jurassic/Early Cretaceous in Southeast Asia. The dinosaur records ofSoutheast Asia is limiting at the Early Cretaceous period. Thus it seem that the evolutionaryof dinosaurs in Thailand were started from the Late Triassic-Early Jurassic period thenreplaced by the endemic Asian dinosaur assemblages during the Late Jurassic-Earliest
Cretaceous age and finally the Early Cretaceous dinosaurs were occupied over the Indochina
peninsula as evident in Thai, Laos and Malaysia.

4All about Sirindhorna khoratensis (Ornithopoda; Hadrosauroidea)
Masateru Shibata1,2*, Pratueng Jintasakul3 Yoichi Azuma1,2,
Duangsuda Chokchaloemwong3 and Soichiro Kawabe1,21Institute of Dinosaur Research, Fukui Prefectural University, 4-1-1 Matsuoka-Kenjojima, Eiheiji, Fukui 910-1195, Japan
2
Fukui Prefectural Dinosaur Museum, 51-11 Terao, Muroko, Katsuyama, Fukui 911-8601, Japan
3
Northeastern Research Institute of Petrified Wood and Mineral Resources, Nakhon Ratchasima Rajabhat University,
184 Moo 7 Suranaree Subdistrict, Mueang, Nakhon Ratchasima 30000, Thailand*Corresponding author. email: sdino@fpu.ac.jp

Abstract
Sirindhorna khoratensis, a basal hadrosauroid from the Lower Cretaceous of
Thailand, is the best-preserved ornithopod dinosaur in Southeast Asia. Shibata et al. (2015)
described skull elements, including premaxillla, maxillae, braincases, quadrate, andmandibles. Additionally, we have excavated abundant iguanodontian postcranial bones fromthe site. Those iguanodontian postcranial bones are assumed to belong to one taxon
because discovered five braincases show no features to imply the existence of multi-taxa.
Here, we introduce all about this great dinosaur; its postcranial skeleton and brain.
Postcranial skeleton: Composite restorations are produced for the postcranialskeleton because a few articulated elements have been known from the excavation site. In
axial skeleton, one small axis, one complete mid-cervical and several broken cervicalvertebra have been found. Interestingly, only one set of the articulated posterior cervical toanterior dorsal vertebrae was unearthed. In dorsal vertebrae, an isolated and well-preserved
one and several broken or unfused ones have been known. Completely fused sacrum,lacking the dorsal and anterior portion, consists of three and one broken sacral vertebrae. In
caudal vertebrae, no completely preserved one has been known, although more than tenvertebrae have been discovered. Anterior caudal vertebra shows well-developed transverse
processes. Posterior caudal vertebrae normally show an anteroposteriorly elongated andhexagonal-shaped centrum.
Appendicular skeleton is also reconstructable. The pectoral girdle and forelimbshows relatively a robust structure: the broad and expanded proximal portion of the scapula,
relatively small main body of the sternal with expanded caudolateral process, and the large
and distinct olecranon process of ulna. No manual elements have been identified. The
pelvic girdle and hindlimb bones also have been known. Although almost all bones arebroken and deformed, an assemblage of partially articulated pedal phalanges was found.
Variable sizes of femora are included.
Brain: CT-scanning of one well-preserved braincase of S. khoratensis shows theendocranial anatomy of S. khoratensis. The reconstructed endocast shows typicaldinosaurian brain morphology with rostrocaudally-elongated posture. The following generalendocast features of this animal resemble those of basal iguanodonitans A large peak of the
midbrain makes this brain a triangular shape in lateral aspect. The olfactory tract is projectedrostrally at the rostral end of the cerebrum. The cerebral hemisphere is broad and5

The Sixth International Symposium of International Geoscience Programme IGCP Project 608

dorsoventrally compressed. Caudal to the cerebrum, there is a weak constriction. A large
peak of the midbrain is possibly a pineal peak. The caudal region to this peak is constrictedagain, where the inner ear (endosseous labyrinth) is situated. The left endosseous labyrinth isalso well-reconstructed although lacking the ventral portion. The rostrocaudal length of theendocast is 136 mm and the width is 52 mm at the cerebrum. Significantly, the ratio of thevolume of the cerebrum to that of the endocast, which is approximately 30%, is muchhigher than any other non-hadrosaurid iguanodontians and close to those of hadrosaurids.
Despite a large number of fossil records of iguanodontians, the endocranial anatomy
information is still limited, particularly among non-hadorsaurid hadrosauroids. Therefore, S.
khoratensis provides fundamental information of the endocranial anatomy of nonhadrosaurid hadrosauroid.

6

Belemnite diversity across the Jurassic–Cretaceous boundary
in Russian northern Eurasia
O.S. Dzyuba
Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS,
Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: dzyubaos@ipgg.sbras.ru

Abstract
The taxonomic diversity of belemnites (Cylindroteuthididae) from the Volgian andRyazanian of northern East Siberia (Nordvik and Boyarka sections), northwestern West Siberia(Lopsiya, Maurynya, and Yatriya sections) and Central Russia (Gorodischi, Kashpir, Nikitino, andDurnenki sections) are studied. In Siberia, two different trends occurred in the dynamics ofbelemnite species diversity across the Jurassic–Cretaceous boundary. In the NW margin of
the West Siberian sea (Lyapin paleobay), the growth of belemnite diversity began at the endof the Middle Volgian and significantly increased in the Late Volgian. The peak of thebelemnite taxonomic diversity occurred in the terminal Volgian–beginning of the Ryazanian,i.e. it falls on the beginning of the Cretaceous (Dzyuba, 2013; Dzyuba et al., 2018). The West
Siberian ‘peak’ corresponds to a sharp decline on the species diversity curve of thebelemnites in the north of Eastern Siberia (Khatanga paleostrait). In the second half of the
Ryazanian, the number of species substantially decreased all over the Siberia. Belemnite
assemblages in the Central Russian sea did not experience any peculiar diversity changes(either positive or negative) across the Jurassic–Cretaceous boundary.
Belemnite assemblages were undoubtedly influenced by different global and regional
factors. The dynamics of belemnite diversity in the Lyapin paleobay correlates well withclimatic events. A gradual increase of species number during the Volgian–beginning of the
Ryazanian in Western Siberia as well as penetration of the Tethyan Hibolithes(Belemnopseidae) at the end of this time interval correspond to a global warming andtemperature elevation in Boreal basin, and the subsequent reduction of species diversity inthe second half of the Ryazanian is correlated with a gradual cooling (Dzyuba, 2013; Dzyuba
et al., 2013, 2018). Ryazanian belemnites of the Central Russian sea show the best
correlation between dynamics of belemnite diversity and transgressive–regressive events.
The correlation between belemnite diversity curves and eustatic or transgressive–
regressive curves is often not recorded. This can probably be attributed to the complicatedcharacter of this relationship; a decrease (or increase) in belemnite diversity can be linked toby either shallowing or deepening of their habitat. For example, the Kimmeridgian eustaticand transgressive events obviously favored a rise in biodiversity in Siberian seas; however, thefurther deepening of the West Siberian sea in the Volgian led to the formation ofpseudoabyssal depths (down to 500 m and below) in its central part and an almost
complete absence of belemnites, excluding juveniles transported by currents (Marinov et al.,2006). In northern East Siberia with the increased transgression and deepening of the basin
down to 200 m and over in the area of the modern Nordvik Peninsula, the number of

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

belemnites was reduced (Dzyuba, 2012; Zakharov et al., 2014). In the open sea deep-water
facies of Jurassic–Cretaceous transitional time, belemnites are missing despite the occurrenceof ammonites and numerous Buchias. A subsequent shallowing of deep areas invariably led
to the inverse process when belemnites returned to faunal communities and their taxonomic
diversity gradually increased (cf. Dzyuba, 2013). However, an extreme shallowing of thebasins in turn negatively influenced the species diversity. In the terminal Volgian, the Central
Russian sea became a shallow basin with highly abundant belemnites against the backgroundof very low species and generic diversity (Yanin, 2001).
At the superspecific level changes in Siberian belemnites in the Volgian and Ryazanian
are comparatively weak. Almost all genera occurring in the Upper Jurassic pass into the Lower
Cretaceous. The most perceptible change took place at the beginning of the Middle Volgian
when in the Lyapin Bay three cylindroteuthidid genera, Acroteuthis (Pachyteuthidinae),
Liobelus (Simobelinae), and Eulagonibelus (Lagonibelinae) first occurred. During the Volgianand Ryazanian ages none of the taxa superspecific in rank disappeared from the Siberian
belemnite assemblages, with the exception of southern migrants (Boreal-Atlantic genus
Eulagonibelus, and Tethyan genus Hibolithes) that penetrated into the western West Siberian
sea for a short time. By the terminal Middle Volgian in the Boreal-Atlantic seas
Cylindroteuthidinae, Lagonibelinae, and the genus Pachyteuthis disappeared sequentially, andtemporarily the genera Boreioteuthis and Simobelus (re-occurred in the Early Cretaceous). In
the Arctic seas, these taxa continued to exist and generated a number of new species. In theCentral Russian sea, as well as in shallow seas of NW Europe, only Acroteuthis and Liobelus
with dorsoventrally depressed and flattened on the ventral side rostra occurred at theJurassic–Cretaceous boundary as the most adapted to shallow environment.

References
Dzyuba, O.S., 2012. Belemnites and biostratigraphy of the Jurassic–Cretaceous boundary deposits ofnorthern East Siberia: new data on the Nordvik Peninsula. Stratigr. Geol. Correl. 20(1), 53–72.
Dzyuba, O.S., 2013. Belemnites in the Jurassic–Cretaceous boundary interval of the Mauryn’ya and Yatriya
River sections, Western Siberia: Biostratigraphic significance and dynamics of taxonomic diversity.
Stratigr. Geol. Correl. 21(2), 189–214.
Dzyuba, O.S., Izokh, O.P., Shurygin, B.N., 2013. Carbon isotope excursions in Boreal Jurassic–Cretaceous boundary
sections and their correlation potential. Palaeogeogr. Palaeoclimatol. Palaeoecol. 381–382, 33–46.
Dzyuba, O.S., Pestchevitskaya, E.B., Urman, O.S., Shurygin, B.N., Alifirov, A.S., Igolnikov, A.E., Kosenko, I.N.,
2018. The Maurynya section, West Siberia: a key section of the Jurassic–Cretaceous boundary
deposits of shallow marine genesis. Russ. Geol. Geophys. 59, 864–890.
Marinov, V.A., Meledina, S.V., Dzyuba, O.S., Urman, O.S., Yazikova, O.V., Luchinina, V.A., Zamirailova, A.G.,
Fomin, A.N., 2006. Biofacies of Upper Jurassic and Lower Cretaceous sediments of central West
Siberia. Stratigr. Geol. Correl. 14(4), 418–432.
Yanin, B.T., 2001. The Volgian biota of the Central Russian sea. Paper 1. Major evolutionary tendencies.
Vestn. Mosk. Univ., Ser. Geol. 5, 10–15.
Zakharov, V.A., Rogov, M.A., Dzyuba, O.S., Žák, K., Košt’ák, M., Pruner, P., Skupien, P., Chadima, M., Mazuch,
M., Nikitenko, B.L., 2014. Palaeoenvironments and palaeoceanography changes across theJurassic/Cretaceous boundary in the Arctic realm: case study of the Nordvik section (north Siberia,
Russia). Polar Res. 33, 19714.

8

Buchia associations and interregional correlation of theJurassic–Cretaceous boundary interval in Russian Boreal basins:
new data from the Russian platform, Siberia, and the Far East
B.N. Shurygin1,2, O.S. Urman1 and O.S. Dzyuba1
1

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS,
Acad. Koptyug av. 3, Novosibirsk 630090, Russia; e-mail: dzyubaos@ipgg.sbras.ru
2
Novosibirsk State University, Pirogova str. 2, Novosibirsk 630090, Russia

Abstract
Bivalves attributed to the genus Buchia (Buchiidae) are widely used in the Upper
Jurassic–Lower Cretaceous biostratigraphy of Boreal and adjacent areas. A eurybionticity ofrepresentatives of the Buchia determined the similarity of their association in various facial
sections of the Jurassic–Cretaceous boundary interval for different biogeographic areas of
Boreal paleobasins (Zakharov, 1981). It is evident that the precise position of the Jurassic–
Cretaceous boundary, determined in the Tethyan section, will never be determined in Boreal
sections (Shurygin and Dzyuba, 2015). The problem of identification of this level in Boreal
sections can be solved only using a combination of data obtained by paleontological andnonpaleontological methods of stratigraphy. The magnetostratigraphic calibration of theBuchia succession was recently proposed for the Jurassic–Cretaceous boundary interval on
the base of material from northern Siberia (Bragin et al., 2013) and Central Russia(Baraboshkin et al., 2016).
In Central Russia, abundant bivalves from the Middle Volgian–Ryazanian of the
Kashpir section (Middle Volga Basin) as well as from the Ryazanian of the Nikitino, Durnenki
and Chernaya Rechka sections (Oka River Basin) have been preliminary studied (Dzyuba et al.,2015; Urman et al., 2016). Bivalve assemblages are mainly represented by both typicallyBoreal and Subboreal forms. The following beds and zones based on Buchia are traced inCentral Russia: B. russiensis-mosquensis Beds, B. terebratuloides Zone, B. obliqua Zone, B.
unschensis Zone, B. volgensis Zone, B. okensis Zone, B. jasikovi Zone, and B. tolmatschowi
Zone. In general, this buchiid succession repeats that of the Boreal standard (Zakharov et al.,
1997; Nikitenko et al., 2013).
Buchiids are numerous in the Komsomolsk Group of the Northern Sikhote-Alin(Russian Far East), and we studied them in the key section at right bank of the Amur River
opposite to Komsomolsk-on-Amur (Urman et al., 2014). The analysis of stratigraphic
distribution of buchiids in the Upper Volgian–Lower Valanginian deposits allowed us to reveal
the sequence of Buchia-bearing beds: this is well correlated with the Buchia zonal scales ofmany Boreal regions. Here, from the base upward, there have been recognized the following:
Buchia terebratuloides Beds, B. unschensis & B. terebratuloides Beds, B. volgensis Beds, andB. inflata & B. keyserlingi Beds. The B. unschensis & B. terebratuloides Beds also yielded the
Berriasian ammonite Pseudosubplanites? sp. of Tethyan affinity. Judging by finds ofPseudosubplanites cf. grandis, P. aff. combesi and Berriasella ex gr. jacobi in the Southern

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Primorye (Sey and Kalacheva, 1999), the penetration of Tethyan ammonites up to theNorthern Sikhote-Alin latitudes is more likely in the Jacobi–Grandis phases. Earlier, in theuppermost part of the Komsomolsk section, Kalacheva (Sey and Kalacheva, 1999)
determined the Valanginian ammonite Sarasinella cf. varians, which was considered by
Kalinin (2006) as representative of the genus Kilianella. The obtained paleontological data
permit us to refine the age spans of the local stratigraphic units.
Our investigation allowed us to produce a more detailed Buchia scale for the regional
stratigraphic schemes of the Russian Platform and the Russian Far East in the Jurassic–
Cretaceous boundary interval, and to correlate these schemes with bio- andmagnetostratigraphic zonations of Siberia.

References
Baraboshkin, E.Yu., Rogov, M.A., Guzhikov, A.Yu., Dzyuba, O.S., Urman, O.S., Shurygin, B.N., Pestchevitskaya, E.B.,
Manikin, A.G., 2016. Kashpir section (Volga River, Russia), the proposed auxiliary section for the J/K
interval in Subboreal Realm, in: Michalík, J., Fekete, K. (Eds.), XIIth Jurassica Conference. Workshop of the
ICS Berriasian Group and IGCP 632 (Smolenice, Slovakia): Field Trip Guide and Abstr. Book. Bratislava, pp.
109–112.
Bragin, V.Yu., Dzyuba, O.S., Kazansky, A.Yu., Shurygin, B.N., 2013. New data on the magnetostratigraphy of theJurassic–Cretaceous boundary interval, Nordvik Peninsula (northern East Siberia). Russ. Geol. Geophys. 54,
329–342.
Dzyuba, O.S., Urman, O.S., Shurygin, B.N., 2015. Belemnites and bivalves from the Jurassic−Cretaceous boundaryinterval of the Kashpir section, Middle Volga Basin, Russia: Implications for biostratigraphy and Panboreal
correlation, in: Baraboshkin, E.Yu., Bykov, D.E. (Resp. Eds.), The International Scientific Conference on theJurassic/Cretaceous boundary, Samara: Proc. volume. Kassandra, Togliatti, pp. 36−41.
Kalinin, E.A., 2006. Beds with Buchia in the Jurassic–Lower Cretaceous sequence along the Amur River(Khabarovsk Krai) and their correlation with the Boreal zonal standard, in: Paleontology, Biostratigraphy,
and Paleogeography of the Boreal Mesozoic. GEO, Novosibirsk, pp. 93−97 (in Russian).
Nikitenko, B.L., Shurygin, B.N., Knyazev, V.G., Meledina, S.V., Dzyuba, O.S., Lebedeva, N.K., Peshchevitskaya, E.B.,
Glinskikh, L.A., Goryacheva, A.A., Khafaeva, S.N., 2013. Jurassic and Cretaceous stratigraphy of the Anabar
area (Arctic Siberia, Laptev Sea coast) and the Boreal zonal standard. Russ. Geol. Geophys. 54, 808–837.
Sey, I.I., Kalacheva, E.D., 1999. Early Cretaceous ammonites of the Sikhote Alin system and their biostratigraphic
and biogeographical significance. Tikhookean. Geol. 18(6), 83–92 (in Russian).
Shurygin, B.N., Dzyuba, O.S., 2015. The Jurassic/Cretaceous boundary in northern Siberia and Boreal–Tethyancorrelation of the boundary beds. Russ. Geol. Geophys. 56, 652–662.
Urman, O.S., Dzyuba, O.S., Kirillova, G.L., Shurygin, B.N., 2014. Buchia faunas and biostratigraphy of the Jurassic–
Cretaceous boundary deposits in the Komsomolsk section (Russian Far East). Russ. J. Pac. Geol. 8(5), 346–
359.
Urman, O.S., Shurygin, B.N., Dzyuba, O.S., 2016. New data on buchias and belemnites from the Ryazanian of the
Oka River Basin (Central Russia), in: Baraboshkin, E.Yu. (Ed.), Cretaceous system of Russia and CIS
countries: problems of stratigraphy and paleogeography: Proceedings. Chernomorpress Publishing House,
Simferopol, pp. 279–281 (in Russian).
Zakharov, V.A., Bogomolov, Yu.I., Il'ina, V.I., Konstantinov, A.G., Kurushin, N.I., Lebedeva, N.K., Meledina, S.V.,
Nikitenko, B.L., Sobolev, E.S., Shurygin, B.N., 1997. Boreal zonal standard and biostratigraphy of theSiberian Mesozoic. Russ. Geol. Geophys. 38, 965–993.
Zakharov, V. A., 1981. Buchiids and Biostratigraphy of the Boreal Upper Jurassic and Neocomian. Nauka, Moscow(in Russian).

10

Carettochelyid turtle from the Lower Cretaceous of Japan and thediversification of the pan-trionychian turtles
Teppei Sonoda1*, Wilailuck Naksri2, Masateru Shibata1,3, Yoichi Azuma1,3
1

Fukui Prefectural Dinosaur Museum, 51-11 Terao, Muroko, Katsuyama, Fukui 911-8601, Japan
2
Northeastern Research Institute of Petrified Wood and Mineral Resources, Nakhon
Ratchasima Rajabhat University, 184 Moo 7 Suranaree Subdistrict, Mueang, Nakhon Ratchasima 30000, Thailand
3
Dinosaur Research Institute, Fukui Prefectural University, 4-1-1 Kenjojima, Matsuoka,
Eiheiji, Fukui 910-1195, Japan*Corresponding author: t-sonoda@dinosaur.pref.fukui.jp

Abstract
The Carettochelyidae (Trionychia, Testudines), a sister group of soft-shelled turtles(the Trionychidae), is known from the Lower Cretaceous of Laos and Thailand as the oldest
record. The distribution has been restricted in Asia during the Cretaceous, although it has
spread widely onto Europe, North America, and Asia during the Eocene (Joyce et al., 2004).
In the present day, only one living species Carettochelys insculpta is distributed in thenorthern Australia and the southern New Guinea. Here we report the first occurrence of
carettochelyid turtle from the Early Cretaceous of Japan. New materials of carettochelyids
are three disarticulated shell elements including a peripheral and right and left hypoplastron.
These are collected from the dinosaur quarry at Katsuyama city in Fukui Prefecture, central
Japan, where fluvial deposits of the Kitadani Formation (Aptian) of the Tetori Group are
exposed. The Surface of shells are covered by characteristic sculpture that consists ofirregular fine pits, grooves, and tubercles. The hypoplastron with very narrow bridge is quite
similar to anosteirine Kyzylkumemys and Anosteira in shape. The carapace length isestimated about 9 cm long.
All four families of pan-trionychia, Trionychidae, Carettochelyidae, Adocidae, andNanhsiungchelyidae, are here recognized from the Kitadani Formation. In contrast, one or
two groups of pan-trionychia have been occurred from the other sites of the Lower
Cretaceous such as Kyrgyzstan, China, Korea, Laos and Thailand (e.g., Hirayama et al., 2000;
Lapparent de Broin, 2004; Tong et al., 2009; Li et al., 2015). The Kuwajima (Hauterivian? Barremian) and Akaiwa (Barremian? -Aptian) formations underlying the Kitadani Formation
yields more basal pan-trionychian turtles that have no synapomorphy as any families (e.g.,
Hirayama et al., 2000, 2005, 2012). It suggests that the morphological evolution of pantrionychian turtles might have been occurred around Aptian age, and four families of pantrionychia might have appeared at the almost same period in the coastal region of Asia.
Keywords: turtle, Trionychia, Lower Cretaceous, Kitadani Formation, Tetori Group11

The Sixth International Symposium of International Geoscience Programme IGCP Project 608

References
Hirayama, R., Brinkman, D. B. and Danilov, I. G., 2000. Distribution and biogeography of non–marine
Cretaceous turtles. Russian Journal of Herpetology, 7 (3), 181–198.
Hirayama, R., Isaji, S. and Hibino, T., 2012. Kappachelys okurai gen. et sp. nov., a new stem soft-shelledturtle from the Early Cretaceous of Japan. In Brinkman, D. B., Holroid, P. A. and Gardner, J. D. (eds.),
Morphology and Evolution of Turtles, Vertebrate Paleontology and Paleoanthropology, 179–185.
Joyce, W. G., Klein, N., and Mörs, T., 2004. Carettochelyine Turtle from the Neogene of Europe. Copeia, 2,
406–411.
Lapparent de Broin F. de. 2004. A new Shachemydinae (Chelonii, Cryptodira) from the Lower Cretaceousof Laos: preliminary data. Comptes Rendus Palevol, 3, 387–396.
Li, L., Joyce, W. G., and Liu, J., 2015. The first soft-shelled turtle from the Jehol biota of China. Journal of
Vertebrate Paleontology, 35 (2). doi: 10.1080/02724634.2014.909450.
Tong, H., Claude, J., Suteethorn, V., Naksri, W., and Buffetaut, E., 2009. Turtle assemblages of the Khorat
Group (Late Jurassic-Early Cretaceous) of NE Thailand and their palaeobiogeographical significance.
In: Buffetaut, E., Cuny, G., Loeuff, J., & Suteethorn, V. (eds.), Late Palaeozoic and Mesozoic
Ecosystems in SE Asia. London, Geological Society, Special Publication, 315, 141–152.

12

CLMTV cooperation and compilation of the Jurassic
and Cretaceous Mapping
Adichart Surinkum
CCOP Building, 75/10 Rama 6 Road, Phayathai, Ratchathewi, Bangkok 10400 THAILAND
Tel: (662) 644 5468 Fax: (662) 644 5429

Abstract
During 1990 to 2000, oceanic plate stratigraphy of East and Southeast Asia was themain issue for all geologists who involved in Gondwana study. It was because of it is a key
to the implication on the Tectonic evolution of the region. The studies showed that there
are many suture zones commenced differently both on times and settings. It was also led us
to have more understanding on mineral deposits related to subduction zones. Many mines
were opened, particularly along the borderline from Western Indonesia extended northward
to Southern China. Furthermore, the information on Tectonic related mineral deposits wereapplied in many places where similarity is identified.
At that time, fault contacts were the noted along the borderline of two countries,
either on rock type or age. The verification by field survey was impossible because of theaccessibility was so limited, military or minority issues. Therefore the best way to delineate
the fault contacts was sharing information through the seminars or workshops organized byinternational organization, such as IGCP GEOSEA CCOP. As of IGCP working system, both on
information sharing and capacity building, groups of geologist were formed to tackle a
specific subject. Many success case studies were made thereafter, such as Permian strata
from Western Thailand to Northwest Myanmar, Carboniferous fossil along borderline
between Malaysia and J/K boundaries transect between Vietnam Lao PDR Thailand andMyanmar.
Starting from 2002, Geological Survey of Japan initiated through CCOP to have asharing mechanism on geoscience information, on Metadata project. Later on in 2006,
Metadata Phase II and One Geology were started where both geoscience information
including the Harmonized 2M scale geologic maps. Many CCOP countries also publishedtheir own 1M scale geologic map with the ISO for Geographic Information Metadata. At
present, 1M scale geologic map of CCOP (ASEAN) Member Countries program is in progress,
expected to be published by 2020. There are two (2) focused groups separated by major
geological settings, Cambodia Lao PDR Myanmar Thailand and Vietnam (CLMTV) as one group
and another group of PNG TML Indonesia Philippines Brunei Singapore and Malaysia.
Moreover, there are many cooperation programs on Transboundary area in CLMTV
countries, based on the current interesting topics. Water and Groundwater interaction
program is focused on Mekong region, both for water management and water pollution. Geohazard program, on Active fault and landslide, is focused on sharing information, capacity
building and community-based mitigation. Many programs are also focused to support theestablishment of Geopark, especially in the Countries are not yet a member of the UNESCO

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Geopark. It has been proved also that working on mutual respect with mutual benefit basis
is the best approach for these programs.
Recently, Jurassic to Cretaceous Transboundary Geoscience program was started in
CLMTV countries. This program is also focused on promoting the young geologists throughYES Network established during 2007 International Year of Planet Earth. Two workshops,
firstly in 2017 and then again 2018, were organized in Bangkok, with cooperation from CCOP,
Geological Society of Thailand and Thai Department of Mineral Resources. Most recent
studies from CLMTVT countries, especially on the transboundary topics were presented inthis annually workshop. Map of specific geoscience information, such as groundwater, index
fossil, mineral resources and tectonic evolution of J/K, are shared and discussed among theparticipant where international standard is applied.
The first expected output of these cooperation programs is on the data andinformation sharing. However during the commencing, knowledge enhancement and capacity
buildings are focused for all stakeholders too. Finally, we, CCOP, would like to have all of
the geoscience information be ready-to-used via internet on CCOP and CLMTV WebGIS
portal. Eventually, Outreach or Geoscience for the Public is our final output of thesetransboundary programs.

14

Coal-forming Plants of The Early Cretaceous kuti formation(South-eastern Transbaikalia, Russia)
E.V. Bugdaeva1, V.S. Markevich1, N.G. Yadrishchenskaya2, A.V. Kurilenko2, T.A. Kovaleva3
1

Federal Scientific Center of the East Asia Terrestrial Biodiversity, Far Eastern Branch of Russian
Academy of Sciences, Vladivostok, Russia, bugdaeva@biosoil.ru
2
Joint-stock Company “Siberian Production Geological Organization”, Chita, Russia
3
Research Center of Paleontology and Stratigraphy, Jilin University, Changchun, China
email: bugdaeva@biosoil.ru

Abstract
The Lower Cretaceous deposits of the south-eastern Transbaikalia are widelydistributed, filling the riftogenic depressions of the Transbaikalian type. The Lower
Cretaceous is divided into the Turga and Kuti formations. The former stratigraphic unit
includes the volcanic-sedimentary rocks. The volcanites refer to an andesite-basalt series.
The Kuti Formation overlies the Turga Formation in the marginal parts of the basins withunconformity, in the central parts – with gradual transitions. The Kuti Formation isrepresented by the coal-bearing alluvial-lacustrine and swamp sediments. These rocks are
facially replaced by coarse detrital proluvial deposits to marginal areas of basins. Brown
coals are distributed mainly in the upper part of the Kuti Formation; where up to 27 coalseams occur having thickness from 0.3 to 5.3 m, sometimes up to 22 m.
The Turga-Kharanor Basin is located in the southeastern part of Transbaikalia. Its
sedimentary cover includes the volcanic-sedimentary Turga Formation, overlain by the coalbearing Kuti Formation. The thickness of the first reaches 1,100 m. The Kuti Formation is
subdivided into two subformations; the lower one of which is characterized by a different
interbeddings of sandstones, siltstones and mudstones with rare layers of gravel sandstones,
conglomerates, and conglomerate breccias. An admixture of coal detritus is characteristic for
sediments, rather often coaly mudstones and brown coals (2-6 m) occur. The thickness ofthe subformation is variable and reaches 500 m. The Upper Kuti subformation is composedof often alternating aleuritic sandstones and siltstones with interlayers and lenses ofsiderites, mudstones, gravelites. This part of the section contains numerous coal beds often
having considerable thickness (from the first meters to 49 m). The thickness of the Upper
Kuti subformation is 300-400 m.
The coal-bearing strata is a complex paragenetic series of lacustrine, swamp, alluvial
and proluvial facies, often sharply variable and replacing each other both vertically andlaterally. The clastic beds of the Kuti Formation are polymictic or oligomictic. The cement ofrocks is represented by kaolinite, montmorillonite with an admixture of hydromica, silica,
carbonates (siderite, calcite, dolomite, ankerite). The stratification in coarse-grained clastic
rocks is wavy, lenticular, oblique, in fine-grained clastic rocks - horizontally laminated. The
rocks are weakly cemented and diagenised.
For the Kuti Formation the Early Cretaceous palynological assemblage with
angiosperm pollen Asteropollis asteroides Hedlund et Norris was obtained. It was revealed

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diverse paleontological remains here: bivalves Limnocyrena ovalis (Rammelmeier), L.
hupehensis (Grabau), Unio obrutschewi Martinson, insects, such as caddisflies Folindusia sp.,
Terrindusia sp. We found the fossil plants Nilssoniopteris aff. prynadae Samylina, Ginkgo
manchurica (Yabe et Oishi) Meng et Chen, Sphenobaiera cf. starukhiniae Bugd.,
Pseudotorellia kharanorica Bugdaeva, Tomharrisia sp.A, Pagiophyllum sp., Pityophyllum sp.,
Pityospermum sp., Pityostrobus sp. (Bugdaeva, 1992, 1995).
We studied the coals sampled from the Kharanor Coal Mine and Urtuy Coal Minelocated in the south-eastern Transbaikalia. The latter is situated in East Urulyunguy Basin, 10
km north of the city of Krasnokamensk. The Kuti Formation developed in this basin contains
several coal seams, the thickest of which is the coal seam “Moshchny” having thickness 6-60
m. The Kharanor Coal Mine is located in Turga-Kharanor Basin, 260 km south-west of Chita
city. The upper horizon of the coal layers of the Kuti Formation has up to 20 coal seams.
The main coal seam is the "Novy I"; its thickness reaches 49 m, in the southeastern part ofbasin it is split into the strata "Novy 1-A" (thickness is about 13 m) and "Novy 1-B" (the coal
bed mainly has a thickness of 17-22 m, and only in the southwestern part of mine reduced
to 6-10 m). The coal seam "Novy II" (8.3 m) lies above. The thickness of the uppermost coalseam "Novy III" is unstable, and this coal bed has no industrial significance.
In 2018 the geologist of the Kharanor Coal Mine O.D. Gilfanova sent us the samples ofcoals from the "Novy" coal seam. After chemical maceration of the coals with the use of
nitric acid and alkali, dispersed cuticles of the following plants were obtained. The coal bed"Novy 1-A" contains the remains of plants Pseudotorellia sp. A, Elatides sp. A,
Czekanowskiales? sp. indet., Cheirolepidiaceae? sp. indet., coal bed "Novy III-A" Nilssoniopteris aff. prynadae Samyl. (Table I, figs. 4-5), Pseudotorellia kharanorica (Table I,
fig. 7), Elatides cf. zhoui Shi, Leslie, Herendeen, Ichinnorov, Takahashi, Knopf et Crane; coal
bed "Novy III-B" – N. aff. prynadae, P. kharanorica, Arctopitys sp. A (Table I, Figures 8-12),
Pagiophyllum sp. (Table I, fig. 6), E. cf. zhoui.
In 2018 the geologists of the Urtuy Coal Mine S.V. Chikov and N.V. Ovcharenko sent
us the samples of coals from the "Moshchny" coal seam. We revealed that Pseudotorellia sp.
A (Table I, fig. 1-2), Elatides sp. A (Table I, fig. 3) formed this coal.
Thus, the main coal-forming plants of the "Novy" coal seam of the Kharanor Coal
Mine are representatives of the bennettites Nilssoniopteris aff. prynadae, ancient ginkgoalean
Pseudotorellia, conifers Elatides sp. A, E. cf. zhoui, Arctopitys sp. A, Pagiophyllum sp. The
plant communities of slopes consisted of ginkgoalean Ginkgo manchurica, Tomharrisia sp. A,
and also plants having affinity with Pinaceae.
The main coal-forming plants of the "Moshchny" coal seam are Pseudotorellia andElatides.
The significant role in the swamp vegetation played the ginkgoaleans and conifers,
next in importance were bennettites. Also the share in buried phytomass of the ferns (basedon palynological analysis) was very high.

16

Acknowledgments
The authors are grateful to geologist of the Kharanor Coal Mine O.D. Gilfanova andgeologists S.V. Chikov and N.V. Ovcharenko of the Urtuy Coal Mine (Transbaikalian Region), to
N.P. Domra (Federal Scientific Center of the East Asia Terrestrial Biodiversity, Far Eastern
Branch of Russian Academy of Sciences) for processing of the palynological samples. Our
research was supported by Russian Foundation for Basic Research (grant 17-04-01582).

References
Bugdaeva E.V. The Early Cretaceous flora of Transbaikalia // In: Aspects of non-marine Cretaceous geology,(Eds.: N. Mateer, Chen P.-J.). Beijing: Ocean Press, China, 1992. P. 193-199.
Bugdaeva E.V. Pseudotorellia from the Lower Cretaceous coal-bearing deposits of Eastern Transbaikalia //Paleontological Journal. 1995. Vol. 29, N 1A. P. 182-184.
Table I. The coal-forming plants of the Early Cretaceous Kuti formation (South-eastern Transbaikalia,
Russia)Captions: figs. 1-2 – ginkgoalean Pseudotorellia sp. A., Urtuy Coal Mine, coal seam “M”, 1 – leaf, lower andupper cuticle, SEM, scale bar 200 μ; 2 – two stomata on the lower cuticle, scale bar 10 μ; fig. 3 –conifer Elatides sp.A, Urtuy Coal Mine, coal seam “M”, stomatal band, scale bar 200 μ; fig. 4-5 –bennettite Nilssoniopteris aff. prynadae Samyl., Kharanor Coal Mine, coal seam «Novy III-B», 4 –lower cuticle of leaf, costal and intercostals zones, scale bar 100 μ; 5 – stoma, SEM, scale bar 10 μ;fig. 6 – conifer Pagiophyllum sp., Kharanor Coal Mine, coal seam «Novy III-B», stomata, scale bar 100
μ; fig. 7 – ginkgoalean Pseudotorellia kharanorica Bugd., stoma, SEM, Kharanor Coal Mine, coal seam
«Novy III-B», scale bar 10 μ; figs. 8-12 – conifer Arctopitys sp. A, Kharanor Coal Mine, coal seam
«Novy III-B», 8 - leaf, scale bar 1 mm; 9 – groove with stomata bordered by papillae, scale bar 100
μ; 10 - two stomata, one of them is destroyed, SEM, scale bar 10 μ, 11 - groove with stomata
bordered by papillae, SEM, scale bar 20 μ, 12 - lower part of leaf, in its upper part the groove withpapillae, scale bar 100 μ.

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18

Cretaceous Formation of part of East coast of India
Jayaraju, N
Department of Geology, Yogi Vemana University, KADAPA-516003, AP, INDIA
e-mail: nadimikeri@gmail.com

Abstract
The Cretaceous period was one of the most eventful time –spans in the Indian
geological history. The study area occupied one of the important palaeogeographicallocations in Indo-Pacific region during the Cretaceous period. The marine transgression andregression sedimentary sequences of the study area have acted as repositories for theaccumulation of varying litho-units with rich faunal and floral assemblages and are more
helpful in the inter-regional correlation of the Indo-Pacific region. Based on their distribution,
tectonic setting and geographical position, the Indian Cretaceous basins have been grouped
as follows: i) East Coast Basin, ii) Narmada Trough and Lameta Basin, iii) Kutch Shelf, iv)
Jaiselmer Shelf, v) Bengal-Assam Basin, vi) Basins of the Himalayan belt and vii) Basins of theIndo Burma-Andaman . The East Coast basin consists of the Cauvery, Palar, Krishna-Godaveri
and Mahanadi basins. The Cretaceous succession in Cauvery, Palar and KrishnaGodaveri
together from South Indian Cretaceous. Of these geographic areas, the outcrop exposed in
the vicinity of the Tiruchirapalli area is the largest one. The deep wells drilled for exploratory
purpose by ONGC in the different parts of the basin indicate that the thickness of thesedimentary rocks is nearly 4 to 6 km thick which is ranging from Early Cretaceous to Recent
age .The study also reveals the two third sedimentary sequences were deposited in the
Cretaceous time. The paper attempts to deal with the economic importance of hydrocarbon
deposits, mineral wealth etc., of the Cretaceous Basins of part of East Coast of India .

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Depositional environment of Lower Cretaceous lacustrine sedimentaryrocks in Central Mongolia
Bat-Orshikh Erdenetsogt1*, Sung Kyung Hong2, Jiyoung Choi2, Boldbaatar Gantulga3, Niiden
Ichinnorov4, Nyamsambuu, Odgerel1, Gombosuren Tsolmon4, Norov Baigalmaa1, Enkhbayar
Bolormaa1
1

National University of Mongolia, Ulaanbaatar, Mongolia (tsogo@num.edu.mn),
Korea Institute of Geoscience and Mineral Resources, Daejeon, South Korea,
3
Erdenes-Tavantolgoi JSC, Ulaanbaatar, Mongolia,
4Institute of Paleontology and Geology, Ulaanbaatar, Mongolia,

2

Abstract
The depositional environment of Cretaceous sedimentary facies in Mongolia is poorly
known and only few studies have been published so far (Traynor and Sladen, 1995; Sladen
and Traynor, 2000; Yamamoto et al., 1998; Johnson et al., 2003; Hasegawa et al., 2018). Thus,
43 samples of Lower Cretaceous lacustrine oil shale were collected from 9 locations inCentral Mongolia to improve understanding of their depositional environment as well as
petroleum potential. Most of the samples are taken from outcrops of oil shale seams andintercalated carbonate layers, but also include 17 core samples from a borehole.
Total organic carbon (TOC) content and rock-Eval pyrolysis of the samples were
performed using Rock-Eval 6 instrument equipped with TOC module. Organic carbon andtotal nitrogen isotopic compositions were analyzed using a stable isotope ratio mass
spectrometer system with element analyzer (Vision-EA, IsoPrime, UK). Based on the results ofbulk geochemical analysis (Rock-Eval), 7 oil shale samples were selected for biomarker
analysis. The GCMS analyses were conducted with a Thermo Scientific Trace 1310 GC system
coupled to a Thermo Scientific ISQ single quadrupole mass spectrometer.
Results indicate that Lower Cretaceous oil shale samples have highly oil prone type I
kerogen, emphasized by high TOC (avg.10.1 %), S2 (68.7 mgHC/g rock) and HI (avg. 619
mgHC/g TOC). Organic matter (OM) in oil shales is accumulated in stratified lakes with anoxic
bottom water, reflected by low Pr/Ph ratios (<0.28) and highly negative 13Corg (avg. -30.6‰)
and highly positive 15Nt (avg. +10.5‰) values. The salinity of lakes was different, suggested
by variable gammacerane index ranging from 0.03 to 0.44. In studied oil shale, aquatic plant
was dominant OM source (0.42 to 0.7 of nC21-25) with contribution from algae and land plantderived OM.
Early Cretaceous lakes in eastern Mongolia were developed in small discrete riftbasins and there were minor differences among the basins, e.g., sedimentation rate etc.
(Sladen and Traynor, 2000), and the lakes repeatedly expanded and contracted during rifting(Graham et al., 2001; Johnson et al., 2003). Because of its smaller size and instability, salinity,
redox condition and OM input type in lake was changed easily and therefore variable among
the lakes. The depositional environment of oil shale forming lakes in Central Mongolia was20

similar to that of paleolakes in eastern and southeastern Mongolia as well as Erlain basin in
China (Yamamoto et al., 1998; Johnson et al., 2003; Chen et al., 2014).

References
Chen, Z., Liu, G., Huang, Z., Lu, X., Luo, Q., Ding, X., 2014. Controls of oil family distribution andcomposition in nonmarine petroleum systems: a case study from Inner Mongolia Erlian Basin,
Northern China. Journal of Asian Earth Sciences 92, 36-52
Graham et al., 2001. Graham, S.A., Hendrix, M.S., Johnson, C.L., Badamgarav,D., Badarch, G., Amory, J.,
Porter,M., Barsbold, R., Webb, L.E., Hacker, B.R., 2001. Sedimentary record and tectonic implicationsof Mesozoic rifting in Southeast Mongolia. Geological Society of America Bulletin 113, 1560–1579.
Johnson, C.L., Greene, T.J., Zinniker, D.A., Moldowan, J.M., Hendrix, M.S., Carroll, A.R., 2003. Geochemical
characteristics and correlation of oil and nonmarine source rocks from Mongolia. AAPG Bulletin 87,
817–846.
Traynor, J.J., Sladen, C., 1995. Tectonic and stratigraphic evolution of the Mongolian People's Republic andits influence on hydrocarbon geology and potential. Marine and Petroleum Geology 12, 35–52.
Sladen, C., Traynor, J.J., 2000. Lakes during the evolution of Mongolia. In: Gierlowski-Kordesch, E.H. and
Kelts, K.P. (Eds.), Lake basin through space and time: AAPG Studies in Geology 46, pp. 35-57.
Yamamoto, M., Bat-Erdene, D., Ulziihutag, P., Watanabe, Y., Imai, N., Kajiwara, Y., Takeda, N., Nakajima, T.,1998. Organic geochemistry and palynology of Lower cretaceous Zuunbayan oil shales, Mongolia.
Geological Survey of Japan Bulletin 49, 257–274.
Hasegawa, H., Ando, H., Hasebe, N., Ichinnorov, N., Ohta, T., Hasegawa, T., Yamamoto, M., Li, G.,
Erdenetsogt, B., Heimhofer, U., Murata, T., Shinya, H., Enerel, G., Oyunjargal, G., Munkhtsetseg, O.,
Buyantegsh, B., Enkhbat, D., Suzuki, N., Irino, T., Yamamoto, K., Kouchi, Y., Orihashi, Y. (2018)
Chronostratigraphy of the Jurassic–Cretaceous lacustrine deposits in southeast Mongolia. Island Arc
27, e12243. DOI: 10.1111/iar.12243

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Depositional processes and transport mechanism of upper Ullyonsan
Conglomerates in the Cretaceous Yeongyang Subbasin of Gyeongsang
Sedimentary Basin, Korea
Ki-Hun Yu, Daekyo Cheong, Daewoo Kim
Department of Geology, Graduate School, Kangwon National University, Korea

Abstract
The sedimentary rocks of the Cretaceous sedimentary basins located in thesoutheastern part of the Korean Peninsula were analyzed by sedimentological study and the
dynamic characteristics of sediment gravity flows. The clastic sedimentary rocks of the
Ullyonsan Formation are mainly composed of conglomerate and sandstone. In particular, theupper sedimentary rocks are composed of reddish pebbly sandstone layers andconglomerate layers repeatedly and boulder-size clasts constituting the conglomerate haveangular roundness and are larger than 1m in diameter. It is presumed that these
conglomerates are formed while the sediments move and are accumulated in a short timeat the source area adjacent to the fault scarp. Detailed sketches of the sedimentary rocks
were drawn to understand the sedimentary structure, size, shape, composition, particle
contact, geometry and size of the sedimentary rocks. The dynamic characteristics and thesedimentation process of gravity flow are interpreted based on the field data ofconglomerate and sandstone layers. The conglomerate layer composed of cobble toboulder size clast was formed by high density fluids showing the dynamic characteristics ofcohesionless debris flow carrying and depositing coarse sediments. The pebbly sandstone
and conglomerate layer composed of pebble size clast was considered to be formed bytransporting and depositing sediments by high density fluid showing dynamic characteristics
of normal stream flows. Due to the characteristics of the proximal part of an alluvial fan, thecontinuous migration of the channels occurred. High-density fluids flowing in these channels
are supposed to have the sediment content of a range of about 20-60% and continuallyexperience changes in velocity, density, viscosity, and fluidity depending on time and space.
Also it is believed that the dynamical characteristics similar to high-concentration turbidity
current should change into the normal stream flow, and finally into the cohesionless debris
flow as the flow velocity decreases.
Keywords : Proximal alluvial fan, normal stream flow, cohesionless debris flow, highdensity fluid, landslide

22

Detrital zircon U-Pb and radiolarian biostratigraphy in the Tethys
Himalaya, southern Tibet: Constraints on the Timing of Initial IndianAsia Collision
Tianyang WANG 1, 2, Guobiao LI 1, 2, *, Zhang Wenyuan 1, 2,, Xinfa LI 1, 2 and Xusong Ma 1, 2
1State Key Laboratory of Environmental Geology and Biogeology, China University of Geosciences, Beijing 100083, China
2
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China*email: liguobiao@cugb.edu.cn

Abstract
Upper Cretaceous to Eocene marine sedimentary sequences which consist of Asianmargin strata of the Gangdese arc and Indian-margin strata of the northern Tethys Himalaya
provide constraints on the initial India-Asia collision and the closure time of the Neo-Tethys
Ocean. We report sedimentological, petrographic, biostratigraphic and geochemical data on
Cretaceous to Paleogene strata in the Beijia area, near Gyangze, located along the YarlungZangbo Suture Zone in southern Tibet. Abundant radiolarian fossils were obtained from theZongzhuo Formation andSeventy-three species of fifty genera were identified and assigned asfollows: Thanarla pulchra-Holocrytocanium barbui, Pseudoeucyrtis spinose, Dictyomitra
formosa, D. koslovae and Amphipyndax pseudoconulus the late Cretaceous Zones, andBuryella tetradica and Bekoma campechensis the late Paleocene zones. The late Paleocene
Radiolarian zones from this succession can be compared with the radiolarian zones RP5 andRP6 in New Zealand, indicating a time interval of 61.5-55.5 Ma. The sandstones of Upper
Cretaceous to Eocene Zongzhuo Formation and Beijia conglomerateare dominated byzircons younger than 200 Ma, showing a major peak at 76-134 Ma, comparable to those fromthe Gangdese arc. By contrast, the Lower Cretaceous Gyabula Formation is dominated bydetrital zircons with Archean to Cambrian U-Pb ages, which we interpret to be derived fromthe Indian continent. The change in sedimentary provenance between the Gyabula andZongzhuo formations from the southern Indian continent to the northern Gangdese arc andthe radiolarian fauna in the Zongzhuo Formation denote the initiation of India-Asia collisionoccurred no later than 55.5 Ma.
Key words: India-Asia collision, Tethys Himalaya, Radiolarian, provenance analysis,
detrital zircons

Acknowledgements
This research is supported by the Strategic Project of Science and Technology ofChinese Academy of Sciences (XDB050105003), the State Scholarship Fund of China(41272030), the National Basic Research Program of China (2012CB822001), and IGCP608.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

References
Aitchison, J.C., Badengzhu, Davis, A.M., Liu, J.B., Luo, H., Malpas, J.G., McDermid, I.R.C., Wu, H.Y., Ziabrev,
S.V., Zhou, M.F., 2000. Remnants of a Cretaceous intra-oceanic subduction system within the
Yarlung-Zangbo suture (southern Tibet). Earth Planet. Sci.Lett. 183, 231–244.
Aitchison, J.C., Ali, J.R., Davis, A.M., 2007a. When and where did India and Asia collide? J.Geophys. Res. 112,
B05423 doi: 10.1029/2006JB004706.
Ding, L., Kapp, P., Wan, X., 2005. Paleocene–Eocene record of ophilite obduction andinitial India–Asian
collision, south central Tibet. Tectonics 24. doi:10.1029/2004TC001729 TC3001.
Li, G.B., Jiang, G.Q., Hu, X.M., Wan, X.Q., 2009a. New biostratigraphic data from the Cretaceous Bolinxiala
Formation in Zanda, southwestern Tibet of China andtheir paleogeographic and paleoceanographic
implications. Cretaceous Res.30, 1005–1018.
Li, G.B., Jiang, G.Q., Wan, X.Q., 2011. The age of the Chuangde Formation in Kangmar, southern Tibet of
China: implications for the origin of Cretaceous oceanic red beds (CORBs) in the northern Tethyan
Himalaya. Sed. Geol. 235, 111–121.
Li, G.B., Wan, X.Q., Liu, W.C., Bucher, H., Li, H.S., Goudemand, N., 2009b. A new Cretaceous age for theSaiqu “mélange”, southern Tibet, evidence from radiolaria.Cretaceous Res. 30, 35–40.
Li, G.B., Wan, X.X., Liu, W.C., Liang, D.Y., Hyesu, Y., 2005a. Discovery of Paleogene marine stratum along thesouthern side of Yarlung–Zangbo suture zone and its implications in tectonics. Sci. China, Ser. D. 48,
647–661.

24

Dinoflagellate cyst Biostratigraphy of Eocene in Duina,
Yadong, Tibet, China
Wenyuan Zhang 1, 2, Youjia Yao1, 2, Yuewei LI 1, 2, Tianyang Wang1, 2,
Xinfa LI 1, 2 and Guobiao LI 1, 2 *1State Key Laboratory of Environmental Geology and Biogeology, China University of Geosciences, Beijing 100083, China
2
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China*email: liguobiao@cugb.edu.cn

Abstract
The Tibetan Plateau located in the southern part of the Asian continent and known
as the "roof of the world" and the "third pole" was caused by the collision between the India
plate and the Asian plate. The uplift of the Himalayas and the Qinghai-Tibet Plateau has had
a profound impact on the changes in global geology, geochemistry and climate, so Chineseand foreign scholars have paid great attention to the collision between the Eurasian plate
and the Indian plate. But there is still a lot of controversy about the starting time of thecollision. The study of the closing time of the Tethys Ocean can provide the most direct
constraint for the start time of the collision between the Eurasian plate and the Indian plate.
The era of the highest marine strata in the region represents the time of the closure and thefull collision of the Tethys.
In China, most of the Paleogene strata are continental sedimentary, and the marine
paleoclimatic strata are only developed in Tibet, Xinjiang and parts of Taiwan. The southernpart of the continent preserved a continuous marine paleocene to the Eocene strata, which
are rich in fossils and can be used for stratigraphic division and contrast. A set of wellpreserved Eocene marine strata developed in the East Asia Basin, which is rich in large
amounts of sporopollen and dinoflagellate fossils. This paper focuses on the detailed study
and identification of the fossils of the Eocene strata in the stacked reservoir, which 88
species of 63 dinoflagellate genus are identified and 4 assemblage zones are recognized asfollows (Fig.1): Apteodinium donghaiense - Apteodinium rohmbiforme, Chalesdowniea
rhombiodalis - Hystrichokolpoma salacia, Membranilarnacia variata - Wetzeliella xinjian andCleistosphaeridium shandongense - Luxadinium elongatum assemblage zones. Based on the
research and analysis of the fossils in the reservoir, it is concluded that the sedimentary
period of the sandstone shale section of the study area can reach the late Eocene.
Key words: Eocene, Tethys, Dinoflagellate, Biostratigraphy, Yadong, Duina

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Fig.1 Represent elements of Eocence dinoflagellate assemblage in Duina, Tibet(Scale: x 400)

26

Acknowledgements
This research is supported by the Strategic Project of Science and Technology ofChinese Academy of Sciences (XDB050105003), the State Scholarship Fund of China(41272030), the National Basic Research Program of China (2012CB822001), and IGCP608.

References
Erica M. C., Pi Suhr Willumsen, Denise K. K.. 2014. A revised Paleocene (Teurian) dinoflagellate cyst
zonation from eastern New Zealand. Review of Palaeobotany and Palynology, 202: 47–79.
Hamid Slimani, Koré Élysée Guédé, Graham L.Williams. 2016. Campanian to Eocene dino flagellate cyst
biostratigraphy from the Tahar and Sekada sections at Arba Ayacha, western External Rif, Morocco.
Review of Palaeobotany and Palynology, 228: 26–46.
Hiroshi Kurita. 2004. Paleogene dinoflagellate cyst biostratigraphy of northern Japan. Micropaleontology, 50(suppl. no. 2): 2004.
Li, G.B., Wan, X.X., Liu, W.C., Liang, D.Y., Hyesu, Y., 2005a. Discovery of Paleogene marine stratum along thesouthern side of Yarlung–Zangbo suture zone and its implications in tectonics. Sci. China, Ser. D. 48,
647–661.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Distribution of Charophytes in the lower Cretaceous of the lake basinsin Mongolia and conditions of their growthGereltsetseg Lkhagva
Institute of Paleontology and Geology, Mongolian Academy of Sciences, Chingeltei district,
S.Danzan street 3/1, P.O.B: 46/650, Ulaanbaatar-15160, Mongolia.
e-mail: gerel6341@gmail.com, gerel63@yahoo.com

Abstract
Introduction: Currently factual and literature data on charophytes have been
accumulated which allow to trace their development within the vast territory of Mongolia
and neighboring areas of Middle and Central Asia since the Late Mesozoic till present days.
Results: During the Early Cretaceous for the territory of Mongolia characterizeddevelopment of the extensive lake basins and humid climatic conditions.
Despite the extensive lacustrine basins of Lower Cretaceous in Mongolia, theCharophytes are found irregularly.
Lower Cretaceous
In the Neocomian (Hauterivian-Barremian) deposits of Charophytes were found in
vicinity of Lake Ogii nuur and Bakhar (fig. 1.2.3) the Central Mongolia (Shinekhudag
Formation). Among them are Aclistochara caii Wang, Raskyella sp. Mesochara sp..
Aclistochara caii Wang are known from the Lower Cretaceous sediments of China.
The Aptian-Albian (Khokhteeg Formation) assemblage of Charophytes is Atopochara
trivolvis Peck, Mesochara voluta (Peck) Shaikin, M. tuzsoni Rasky, M. tarica Kyansep-Rom., M.
sainshandinica Kyansep-Rom., Mesochara sp., Aclistochara caii Wang, A. aff. lata Peck,
Flabellochara aff. harrisi (Peck) Grambast, Flabellochara sp., Raskyella sp., Praechara sp.,Porochara sp., Sphaerochara verticilata (Peck) Horn af Rantzien. Charophytes were found in
the Western and Central Mongolia, Southern Gobi and South - East Gobi.
Aclistochara lata, Flabellochara harrisi, Sphaerochara verticilata, Atopochara
trivolvis are known from the Aptian sediments of North America (Peck, 1938a, 1938b, 1957)
and Aptian-Albian sediments of Asia, Europe (N.P.Kyansep-Romashkina, 1967, 1969, 1974;
Rasky, 1941, 1945, 1958; Prosnyakova, Shaikin, 1969). Mesochara tarica are known from theAptian sediments of Fergana (Uzbekstan) (N.P.Kyansep-Romashkina, 1974). Mesochara voluta(Peck) Shaikin are known from the Aptian-Albian sediments of North America (Peck, 1938a,
1938b, 1957) and from the Upper Jurassic sediments of Donbassa and from the Lower
Cretaceous sediments of Moldava and Krima. Mesochara tuzsoni are known from the Aptian
sediments of Hungaria.
The Albian-Cenomanian (Baruunbayan Formation) assemblage of Charophytes:
Mesochara sainsandinica Kyansep-Rom., Mesochara tuzsoni Rasky, Atopochara trivolvis
Peck. Charophytes were found in the Southern Gobi and South - East Gobi.
Mesochara sainsandinica are known from the Aptian-Maastrichtian sediments ofSouthern Gobi and South - East Gobi.

28

The Lower Cretaceous deposits of the Mongolia are poor in fossils oogonia
Charophytes. Lake basin was lightly salted waters, deep in the Lower Cretaceous, probably
closed and more or less oligotrophic by its hydrology.
Keywords: Charophytes, Lower Cretaceous, Mongolia.

абFig. 1 Aclistochara caii а/ lateral view, б/ basal view

а

б

в

Fig. 2 Mesochara sp. төрөл а/ apical view б/ lateral view, в/ basal viewа
Fig. 3 Raskyella sp. төрөл а/ apical view, б/ lateral viewб

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

References
Barsbold R, Khand Yo. 2014. “Cretaceous of Mongolia” Second International Symposium of International
Geoscience Programme (IGCP) Project 608. Abstract volume. P.127-130
Kyansep-Romashkina N.P. “Значение харовых водорслей для стратиграфий Мезозойских
отложений Ферганы и палеолимнологических реконструкций“//The Problems of thestudy Ancient Lacustrine Basins in Eurasia. 1974. 21-37. In russian
Kyansep-Romashkina N.P. “Некоторые позднеюрские и меловые харофиты Монголии“//Joint
Soviet-Mongolian Paleont. Exp.Transaction - 2. 1975, р. 181-204. In russian
Kyansep-Romashkina N.P. “Позднемеловые харовые водорсли из озерных отложений
Монголии и Закавказья“//Limnobions of Ancient Lacustrine Basins in Eurasia, 1980. 71-90. In
russian
Kyansep-Romashkina N.P. “Распространение харовых водорслей Мезозойских озерных
бассейнах Монголии и условия их произрастания“// Mesozoic Lacustrine Basins in
Mongolia. 1982. 158-180. In russian
Grambast L. Classification de l,embrachement des Charophytes. – Natur Monspeliensia, ser.bot., 1962, 14,
63-86
Grambast – Fessard N. Description de deux especes nouvelles d,Atopochara Peck (Clavatoraceae,
Charophyta). – Geobios, 1980, N13, fasc. 1, Lyon, p.129-135
Horn af Rantzien H. Comparative studies of some modern, Cenozoic and Mesozoic charophyte
fructifications. – Ibidem, 1959-1960, 5, 1, 1-17.
Peck R.E. A new family of Charophyta from the Lower Cretaceous of Texas. – J.Paleontol., 1938, 12, N1,
p.173-176.
Peck R.E. North American mesozoic Charophyta. – U.S.Geol.Survey, Prof. Papers, 1957, N294-A, III, p.1-44.
Rasky K. Fossile Charophyten-Fruchtt aus Ungarn. – Ungar. Naturwiss. Mus., Naturwiss. Monogr., 1945, 2,
S.1-74.
Wang Zhen. Cretaceous Charophytes from the Yangtze – Han River Basin with a note on the classificationof Porocharaceae and Characeae. – Mem. Nanjing Inst.Geol.Paleont.Acad.Sinica, 1978, 9, 5, 61-88.

30

Facies and geochemical analysis for basin evolution of the late
Cretaceous Neungju Basin, SW Korea – a preliminary study
Hyojong Lee1* and Taejin Choi2
1

School of Earth and Environmental Sciences, Seoul National University, South Korea (barefox@gmail.com)
Department of Energy and Resources Engineering, Chosun University, South Korea (tchoi@Chosun.ac.kr)

2

Abstract
During the Cretaceous, the East Asian continental margin including the Korean
Peninsula was under a back-arc to intra-arc setting due to oblique subduction of the Izanagi
Plate. Under an extensional/transtensional tectonic regime, more than 10 small basins wereformed in the southwestern Korean Peninsula along the NE-SW-trending strike-slip fault
systems. Although volcanic activities as well as climatic changes might strongly influence on
the development of these basins, they have been less focused in previous studies. The
Neungju Basin, the largest one of these basins, was deposited under alluvial to lacustrine
environments, experiencing episodic volcanism. The basin-fill may provide a good
opportunity to assess the roles of multiple controls including volcanic activities, climatechange and tectonics for the development of the Cretaceous pull-apart basins in the Korean
Peninsula. In this study, thus, facies and geochemical analyses were carried out toreconstruct basin development history and assess the controlling factors for the non-marine
succession of the Neungju Basin.
As a preliminary result, we report facies transition and environmental changes for the
sedimentary succession of the Neungju Basin. The entire basin-fill is subdivided into threestratigraphic intervals, representing temporal paleoenvironmental changes throughout thebasin evolution. The lower interval is composed of distal alluvial fan facies. The alluvial fanswere developed in hinterlands on the west, supplying sediments east- and southeast-ward.
The middle interval is composed two regressive cycles, each showing an upward transition
from marginal lake to sandflat facies. Volcaniclastic sediments occur at the bottoms of these
regressive cycles, supplied from the south along the basin axis. The upper interval iscomposed of alluvial fan facies and shows a transition from distal to proximal alluvial fans.
The deepening of the basin in the middle interval might be caused by increase in basin
subsidence related to fault displacement, or climatic wetting and consequent increase of
precipitation/evaporation ratio. The occurrence of volcaniclastic sediments before thedeposition of marginal lake facies, however, suggests that crustal loading on the south
induced by volcanic eruptions was more likely to cause flexural subsidence and the
deepening. Further study will focus on petrographic and geochemical analyses of the nonmarine sediments to constrain climatic changes and tectonic events during their deposition.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Flora of coal-bearing deposits of central Transbaikalia (Russia)
E.V. Bugdaeva1, V.S. Markevich1, T.A. Kovaleva2
1

Federal Scientific Center of the East Asia Terrestrial Biodiversity, Far Eastern Branchof Russian Academy of Sciences, Vladivostok, bugdaeva@biosoil.ru
2
Research Center of Paleontology and Stratigraphy, Jilin University, Changchun, China

Extended Abstract
Introduction
The Olon-Shibir Coal Mine is the main deposit in the Central Transbaikalia. This coal
field is located in the north-eastern part of the Tugnuy Basin. From the north and the east,
this basin is bordered by the Tsagan-Daban and Zagan ranges, in the south by the anticlinal
fold of the Kapsal Mountain. The sedimentary sequence of Tugnuy Basin consists of
volcanogenic Ichetuy Formation and coal-bearing Tugnuy Formation. The latter includes 22
coal seams; their total area is about 41 km2. This stratigraphic unit is composed of normallysedimentary, continental, alluvial-lacustrine-marshy sediments, mainly sandstones andsiltstones, among which there are beds and lenses of coal. The thickness of the Tugnuy
Formation in this coal field is about 150 m (Skoblo et al., 2001; Coal Base of Russia, 2001).
The formation of peat bogs in the Early Tugnuy time was the result of the swamping of avast lake occupied most of the basin. There were rivers that flowed into this lake from thesoutheastern side of the Tugnuy Basin. Basically peat accumulation took place in constantly
swamping lakes of a wide river floodplain. The age of the Tugnuy Formation was proposed
by V.M. Skoblo as the Middle Jurassic based on ostracods, conchostracans, and mollusks(Skoblo et al., 2001).

Material and method
The geologist of the Open Joint Stock Company “Tugnuy Coal Mine” G.D. Chimitov
sampled for us the specimens of coals from the Olon-Shibir Coal Mine.
Palynological samples from the clastic and coal beds of the 8th, 15th, 17th, and 18th
coal seams of the Olon-Shibir Coal Mine were processed using standard methods. Coals weretreated with nitric acid and alkali, and then thoroughly washed out with distilled water toextract the phytoleims. Dispersed cuticles were prepared for study under an Axioscop 40
optical microscope equipped with an Axiocam HRc camera (Carl Zeiss).
The palynological spectra contain rather diverse and abundant palynomorphs. The
dispersed cuticle Pseudotorellia sp. was obtained from coals.
The coal seam 8 has relatively simple structure. Its thickness varies from 1.2 to 2.5 m.
In several separate disconnected lenses, the anomalous thickness can reach 6-8 m.
The palynological spectra from both clastic and coal layers of coal seam 8 aredominated by spores of cyatheaceous ferns. Sometimes these spores were found as
unbroken sporangia, what evidences the vicinity that ferns habitat to the burial. Next in32

importance is bisaccate pollen having affinity with Pinaceae. Most often in the third positionin palynological spectra from coals is the monosulcate pollen Ginkgocycadophytus, although
in those from sandstones this role belongs to osmundaceous spores.
The coal seam 15 has thickness from 0.3 to 1 m. In the palynospectra of this seam,
spores of Cyatheaceae dominate; the second in importance are bisaccate pollen and
Ginkgocycadophytus. The diversity of palynomorphs increases. The percentage of spores oflower plants and pollen of Podozamitaceae becomes higher.
The coal seam 17 is mainly of simple, less moderately complex structure. The
thickness is 1.5-2.5 m. The palynospectra of the coal and sill are dominated by Cyatheaceae,
as in the palynospectrum of the roof of the coal the latter is replaced by Osmundaceae. On
the second place in the spectra from the clastic beds is bisaccate pollen having affinity with
Pinaceae, while in the coals - Ginkgocycadophytus. Also the amount of Podozamites pollen
in the clastic increases, in coals its percentage drops.
The coal seam 18 is thick (1.60 to 8 m), sometimes very thick (up to 40-50 m). It is
distributed over the whole area of coal field. The palynospectra are dominated by
Cyatheaceae, next in importance is bisaccate pollen Pinaceae, in the third place Osmundaceae or Ginkgocycadophytus.
For the purpose of palynological analysis, spores and pollen were united into themain groups: (1) Bryopsida and Lycopsida; (2) Dicksoniaceae and Cyatheaceae; (3)Schizaeaceae; (4) Ginkgocycadophytus; (5) bisaccate pollen having affinity with Pinaceae; (6)Araucariaceae; (7) Taxodiaceae; (8) others, including representatives of other groups of ferns,
as well as Podozamitaceae, Cheirolepidiaceae, and angiosperms.

Results
The taxonomic composition of the palynospectra from the coal and clastic beds of
the Olon-Shibir Coal Mine is approximately similar: they are dominated by Cyatheaceae,
Pinaceae; the subdominants are Osmundaceae and Ginkgocycadophytus. The ferns andconiferous trees supplied the main phytomass for the formation of coal and, apparently,
these plants formed coastal vegetation of the vast river valley. With the increased influx ofterrigenous sand material into lowlands of basin, possibly as a result of floods, the amountof spores and pollen of plants of slope vegetation increased in the burials. For example, inthe palynospectra of terrigenous layers, the role of Osmundaceae and Araucariaceae often
increases.
The amount of pollen Podozamites is quite stable. It is not excluded that its
producers or formed thickets between slope and lowland vegetation, or in a small amount
were part of the latter. The absence of Podozamites cuticle in coals suggests the first
assumption.
Pollen Ginkgocycadophytus, as is known, could be produced by different plants, suchas representatives of Ginkgoales, Czekanowskiales, Bennettitales, Cycadales and some othergroups. The findings of the dispersed cuticle Pseudotorellia in coals, the absence of finds ofmegafossils of bennettites and cycads suggest that it was produced by ginkgoaleans. It is not
excluded and the role of the Czekanowskia as parent plant. This genus was found earlier by

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

paleobotanists V.A. Vakhrameev and I.N. Srebrodolskaya from these deposits, but we did not
find its remains in this locality. It should be noted that leaves of the czekanowskialeanspossessed a fairly characteristic thick and resistant cuticle, which is well preserved in theburials; however, during the chemical maceration of coals such cuticle was not revealed.
This pattern is characteristic of all Late Mesozoic coals in the south of Siberia and theRussian Far East.
It was much unexpected to found extremely rare pollen of angiosperms Tricolpites
sp. and Clavatipollenites incisus Chlon. in almost all spectra from different sedimentologicalenvironments of the Olon-Shibir Coal Mine. It should be noted that usually the appearanceof the first angiosperms is marked by the appearance of single pollen grains, the number ofpalynomorphs along the section regularly increases, and their species diversity is increasing,for example, in the Barremian-Albian sections of Portugal (Heimhofer et al., 2007). V.A.
Vakhrameev and I.Z. Kotova (1977) have found angiosperm pollen Asteropollis asteroides
Hedl. et Norr. in the Barremian-Aptian (pre-Albian) continental deposits of the Zaza (Baisa
locality), Beklemishevo, Chita-Ingoda, East Urulunguy, Konda, and Arbagar basins ofTransbaikalia. We collected paleobotanical material from Baisa locality of the Zaza Basin.
According to our data, the composition of angiosperms in the palynospectra from thissection is more diverse. In addition to their find, we also obtained Clavatipollenites hughesii
Coup. and Tricolpites sp.
The Middle Jurassic age of the Tugnuy Formation was first substantiated by G.G.
Martinsson (1961) and Ch.M. Kolesnikov (1964) on the basis of finds of fossil bivalves. A.N.
Oleynikov (1975) and E.K. Trussova (Jurassic continental biocenoses, 1985) also considered
the age of this stratigraphic unit as the Early-Middle Jurassic based on the study ofconchostracans. V.M. Skoblo, based on ostracods, also supported the Middle Jurassic age(2001). According to VA. Vakhrameev, fossil plants (collections of V.M. Skoblo) have a wide
stratigraphic distribution - the Jurassic and Early Cretaceous. They have some similarities with
the Middle Jurassic floras of the Irkutsk Basin and Tuva (Siberia). Thus, Vakhrameev bent infavor ("although not with full guarantee") of the Middle Jurassic age of the Tugnuy Formation(Skoblo et al, 2001).
The discovery of angiosperms in the palynological assemblage of the Tugnuy
Formation leads to a new look at its age and place in the stratigraphic chart of Transbaikalia,
and also at the time of coal formation in this region. We consider the age of thepalynospectra of the Tugnuy Formation from the Olon-Shibir Coal Mine as the Early
Cretaceous (apparently Barremian-Aptian). In addition to angiosperms, spores of ferns having
affinity with the Schizaeaceae (Cicatricosisporites sp., Impardecisporites apiveruccatus (Coup.)
Venkat., Kar. et Raza, Concavissimisporites asper Poc., and Pilosisporites setiferus (Verb.)
Verb.), Polypodiaceae (Laevigatosporites ovatus Wils. et Webst., L. ovoideus Takah.), pollenof plants having affinity with the Pinaceae (Alisporites aequalis (Bolch.) Chlon., A. bilateralis
Rouse, A. similis (Balme) Dett.) were revealed. These taxa are usually characteristic of the
Early Cretaceous palynofloras of the Siberia-Canadian floristic region.
Summarizing the above, we consider the age of the coal-bearing deposits of theOlon-Shibir Coal Mine, belonging to the Tugnuy Formation, as the Barremian-Aptian. Our

34main conclusion of our studies - the Mesozoic coal formation in Transbaikalia wasmanifested only in the mid-Cretaceous.

Acknowledgments
The authors are grateful to G.D. Chimitov and V.N. Kuletsky (Open Joint Stock
Company “Tugnuy Coal Mine”, the Buryat Republic), N.P. Domra (Federal Scientific Center ofthe East Asia Terrestrial Biodiversity, Far Eastern Branch of Russian Academy of Sciences,
Vladivostok).
Our study was supported by the Russian Foundation for Basic Research (grant 17-0401582).

References
Coal Base of Russia. Volume IV. Coal Basins and Deposits of Eastern Siberia (Tunguska and Taimyr basins,
Deposits of Transbaikalia). Ed. by V.F. Cherepovskii. Moscow: ZAO “Geoinformmark”, 2001. 493 p. [inRussian].
Heimhoffer U., Hochuli P.A., Burla S., Weissert H. New records of Early Cretaceous angiosperm pollen from
Portuguese coastal deposits: Implications for the timing of the early angiosperm radiation. Review of
Palaeobotany and Palynology. 2007. Vol. 144. P. 39–76.
Jurassic continental biocenoses of Southern Siberia and adjacent territories. Ed. by A.P. Rasnitsyn. Moscow:
Nauka, 1985. 199 p. [in Russian]
Kolesnikov Ch.M. Stratigraphy of the continental Mesozoic of Transbaikalia. In: G.G. Martinsson (ed.),Stratigraphy and paleontology of the Mesozoic and Cenozoic deposits of East Siberia and the Far
East. Moscow-Leningrad: Nauka, 1964. P. 5-138 [in Russian]Martinsson G.G. The Mesozoic and Cenozoic mollusks of the continental deposits of the Siberian platform,
Transbaikalia and Mongolia. Moscow-Leningrad: AN SSSR, 1961. 322 pp. [in Russian]
Oleynikov A.N. Stratigraphy and phyllopods of the Jurassic and Cretaceous of Eastern Transbaikalia.
Transactions of VSEGEI. Vol. 138. 1975. 172 p. [in Russian]
Skoblo V.M., Lyamina N.A., Rudnev A.F., Luzina I.V. The Continental Upper Mesozoic of the Pribaikalia andTransbaikalia (stratigraphy, depositional environments, correlation). Novosibirsk: Publishing House of
the SB RAS. 2001. 332 p. [in Russian]Vachrameev V.A. and Kotova I.Z. Drevnie pokrytosemennye I soputstvuyushchie im rasteniya iz
nizhnemelovykh otlozheniy Zabaikalya (The early angiosperms and the associated plants from theLower Cretaceous deposits of Transbaikalia). Paleontologicheskii zhurnal (Paleontological Journal).
1977. 4. P. 101-109. [in Russian]

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Holocene Climate and Environmental Changes in Mongolia as
Recorded in The Sediments of Lake: A Review
Oyunchimeg Tserentsegmid
Institute of Paleontology and Geology Mongolian Academy of Sciencese-mail: oyuna0401@gmail.com

Abstract
The Mongolian plateau is located at the dry land and semidry land region, and isaffected by global-scale climate systems: the North Atlantic Oscillations (NAO), and the East
Asian summer monsoon which is associated with the El Nino-Southern Oscillations (ENSO)
and Intertropical Convergence Zone in the tropical Pacific (Tudhope et al., 2001). Mongolia
has extreme continental climate with very cold winters and warm summers. The climate
becomes increasingly moist from south to north due to decreases in temperature andincreases in precipitation. Lake sediments is very good archive for past climatic conditions fora variety of reasons. In particular, lakes with a deep central basin are likely to containcontinuous sedimentary geologic records. Lake levels are a sensitive index of regional
effective moisture. Using mollusc profiles from lake sediments, Grunert et al., (2000) foundthat Uvs Nuur and adjacent Bayan Nuur reached their highest stands in the upper late glacialand early Holocene, between 11,230±60 yr BP and 9,690 yr BP. During a generally regressive
phase, lake level in the Uvs Nuur has been dated between 7,310±90 yr BP and 3,250±70 yr
BP (An et al., 2008). Lastly, lacustrine sedimentation occurred during the late Holocene
between 3,010±50 yr BP and 4,030±50 yr BP (An et al., 2008). Lake Hovsgol of northern
Mongolia has been studied (Altunbaev and Samarina, 1977: Dorofeyuk and Trasov, 1998;
Fedotov et al., 2001, 2004; Prokopenko et al., 2003; 2005; 2008; 2009; Tserentsegmid et al.,2008). The climate biogenic indicators SiO2biog, Corg, diatoms and elements are indicated
Holocene/Pleistocene-11.5 ky BP, a warm period Bolling-Allerod (BA, 15-13 ky BP) in the endof Pleistocene, a cold period Younger Dryas (YD, 13-11.5 ky BP) (Tserentsegmid et al., 2008).
In Northern Mongolia at the Gun Nuur lake core corresponding to warm period from 9,000 to7000 yr BP and colder dry climate about 7,000 to 5,000 yr BP. This interpretation isconsistent with dry period in sedimentary proxy from Lake Telmen-north-central Mongolia(Pecl et al., 2002; Fowel et al., 2003).
Keywords: Climate change, lake sediments, lake levels, Bolling-Allerod, Younger Dryas

36

Integrated study of volcano-stratigraphy, magneto-stratigraphy,
reptilian tetropods and palynology: tracking biotic and environmental
changes across Cretaceous-Palaeogene during Deccan volcanism.
Dhananjay M. Mohabey and Bandana Samant
Department of Geology, RTM Nagpur University, Law College Campus, Amravati road, Nagpur-440001, India.
email: dinomohabey@yahoo.com

Abstract

The voluminous eruption (ca. 1.3 x 106 km3) of Deccan contimental flood basalts(DCFB) is considered to have erupted at least in three phases over a period of at least 6-7
million years (69-63 My- Jay and Widdowson, 2008, 68-61 My Sheth et al. 2001). Mostly
based on the study of lava flows of Western Ghats in the main Deccan volcanic province(DVP) it is hypothesised that these three discreet phases of volcanism were represented by
the earliest one at ca. 67.5 Ma near C30r-C30n transition followed by second ( also main)
phase within C29r just before the K-Pg boundary and the third or last phase within
Palaeogene spanning C29r-C29n (Chenet et al. 2007, 2009; Keller et al. 2008). Recently
Schoene and others (2014) based on U-Pb zircon dating suggested that the main phase of
eruptions was initiated at least 250,000 ky before the K-Pg boundary and the 1.1 Km3 oflava erupted in 750,000 ky. Also based on study in Western Ghat Renne et al. (2015)concluded that with the boloid impact at Chicxulub at K-Pg more than 70% of the Deccan
lava with more massive and episodic was erupted suggesting a causal-link between the
volcanism and boloid impact. However, it has been difficut to test any hypothesis for timing
and durations of the phases for lack of accurate estimates of total volume of magma
eruptions in geographically separated Deccan provinces and their chronostratigraphic
constraints on the lava piles. Present aerial extent of Deccan volcanic province is over 500,
000 km2 between the latitudes 150 10'-24030' N and longitude 70'10'-82000'E (Geological
Survey of India, 1993) that could originally be much large exceeding 1,5000,000 km2(Hooper,1999). The Deccan provinces viz. Western Deccan volcanic province, Eastern Deccan
volcanic province, Northern Deccan volcanic Province and undesignated sequences of
Saurashtra and Kutch are spatio-temporarily separated having separate sites and source of
eruptions and also the different timing and duration of eruptions (Mohabey, 2013, Samantand Mohabey, 2014, Schoebel et al. 2014). The stratigraphic correlation of lava flows basedon chemo-stratigraphy is difficult as similar chemo-strato types are found in diffrent
magnetochrons in different provinces. The volcanic sequences are associated with sediments(infratrappean/Lameta and deposited at 'Ground Zero' before covered with the first flows
arriving locally and the sediments (intertrappean) deposited at multiple stratigrphic levels
during the period of repose in the volcanism.
It is crucial to observe relatioship if any between the changing biota and Deccan
volcanic eruptions, especially their nature and magnitude in three different phases of
eruptions. We studied over 150 geographically separated sections in different DVP to37

The Sixth International Symposium of International Geoscience Programme IGCP Project 608

observe biotic and environmental changes during the eruptive history of different provinces.
For tracking biotic or environmental changes the sedimentary layers at multiple stratigraphic
levels were targeted in the volcanic sequences having chronostratigraphic constraints
provided mainly by volcano-stratigraphy, magneto-stratigraphy and available radiomatricdating of lava flows. The infratrappean sediments at 'Ground Zero' are time-transgressive
semi-arid alluvial-limnic deposits of C30n to C29r (Maastrichtian) in different provinces/basins,
whereas the intertrappean are mainly the lake sediments of C30n to C28r MaastrichtianPaleocene (Samant and Mohabey, 2014) deposited over the fresh lava surface.
Vertebrates recovered from the sediments mostly included tetrapods- frogs(Indobatrachus pusilus), turtles (Shweboemys /Bothremydid/Kumademydinae -Sankuchemys
and Kuramademys), Lizards (Agma, Litakis, Pristiguana), Crocodylimorphs (Notosuchids,
Simosuchus), snakes- (Althenophid madtsoiids - Sanajeh indicus, Madtsoia pisdurensis Wilson
et al. 2010, Mohabey et al. 2011), titanosauriforme sauropods (Isisaurus, Jainosaurus),
abelisaurid theropods- Rajasaurus, Rahiolisarus, Indosuchus, Indosaurus and noasauridsLaevisuchus indicus (Huene and Matley, 1933, Wilson et al. 2003, Novas et al. 2010) andnumerous mammal teeth. The taxanomic affinity of these Indian reptiles favours connection
between Indian subcontinent and Madagascar that persisted till stage of late Cretaceous andconsequent endemism after its separation from Madagascar. The studies strongly suggestthat the Indian Late Cretaceous (Maastrichtian) reptiles were adversely impacted by the
initiation of Deccan volcanism and arrival of first lava flows locally in different provinces.
Relatively, more diversity and abundance of reptlilian fauna is observable at 'Ground Zero'conditions before the advent of volcanism. The titanosauriforme and abelisaurids maketheir first appearance coeval with angiosperms in the C30n Maastrichtian on the Indian
subcontinent 500,000 ky before the K-Pg boundary but only one or two species oftitanosaurs survived the initial onslaught by volcanic eruptions and totally disappear atleast 350 ky before the K-Pg boundary. A distinct change from angiosperm-gymnosperm
dominant flora to angiosperm-pteridophyte association with the advent of volcanic activity isrecorded in the Indian Maastrichtian. Further, at higher stratigraphic level in the Deccan
volcanic sequences a change over from Maastrichtian marker palynoflora to Paleocene
marker palyflora is recorded (Samant and Mohabey 2014). It is observed that a change inthe diversity of reptiles and extinction of dinosaurs commensurate much before the K-Pg
boundary as response to advent of Deccan volcanism and arrival of first lava flows locally.
The timing of such biotic changes is noticeably different from North Americal terrestrial KPg boundary sections that is linked to the boloid impact.

References
Chenet, A. L., X. Quidelleur, F. Fluteau, and V. Courtillot (2007), 40K-40Ar dating of the main Deccan large
igneous province: Further evidence of KTB age and short duration, Earth Planet. Sci. Lett., 263, 1–15,
doi:10.1016/j.epsl.2007.07.011.
Chenet, A.L., V. Courtillot, Fre´de´ric Fluteau, M. Ge´rard, Xavier Quidelleur, S. F. R. Khadri, K. V. Subbarao, andThor Thordarson (2009). Determination of rapid Deccan eruptions across the Cretaceous-Tertiaryboundary using paleomagnetic secular variation: Constraints from analysis of eight new sections and38synthesis for a 3500-m-thick composite section. J. Geophys. Res., 114, B06103,doi:10.1029/2008JB005644, 2009.
Geological Survy of India (1993). Geological Map of India, 1:5 million scale. Government of India, Publication,
Kolkata.
Hooper, P. R. (1999). The timing of crustal extension and the eruption of continental flood basalts. Nature,345(6272), 246- 249.
Jay, A. E., Widdowson, M. (2008). Stratigraphy, structure and volcanology of the SE Deccan continental floodbasalt province: implications for eruptive extent and volumes. J. Geological Society, 165, 177-188.
Keller, G., T. Adatte, S. Gardin, A. Bartolini, and S. Bajpai (2008), Main Deccan Volcanism phase ends near the
K-T boundary: Evidence from the Krishna Godavari Basin, SE India, Earth Planet. Sci. Lett., 268, 293–
311, doi:10.1016/j.epsl.2008.01.015.
Mohabey D. M., Head J.J. (2011). A new species of the snake Madtsoia from the Upper Cretaceous of Indiaand its palaeobiogeographic implications. J. Vert. Pal., v. 31(3), pp. 588-595.
Mohabey D.M and Samant Bandana (2013). Deccan Continental Flood Basalt Eruption Terminated Indian
Dinosaurs before the Cretaceous-Paleogene Boundary. Geological Society of India, Special Publication
No. 1, 2013, pp.260-267.
Novas, F.E., Chaterjee, S., Rudra, .K. and Dutta, P.M. (2010) Rahiolisaurus gujaratensis, n. gen. n. sp., a newabelisaurid theropod from the Late Cretaceous of India. In: S. Bhandopadhyay (eds) New Aspects of
Mesozoic Biodiversity, Lecture notes in Earth Sciences, 132, DOI 10.1007/978-3-642-10311-7_3,@Springer-verlag berlin Heidelberg 2010.
Paul R. Renne, Courtney J. Sprain, Mark A. Richards, Stephen Self, Loÿc Vanderkluysen and Kanchan Pande.
(2015). State shift in Deccanvolcanism at the Cretaceous-Paleogene boundary, possibly induced by
impact. Science, 350 (6256), 76-78.
Samant B. and Mohabey D.M. (2014). Deccan volcanic eruptions and their impact on ora: Palynologicalevidence. The Geological Society of America Special Paper 505, 171–191, doi:10.1130/2014.2505(08).
Schoene, B., Samperton K.M,. Eddy, M. P., Keller, G., Adatte, T., Bowring S A., Khadri, S.F.R.. and Gertsch, B.
(2014). U-Pb geochronology of Deccan traps and relation to end Cretaceous mass extinction. Science
express, 10.1126/science.aaa0118, 1-5.
Sheth, H.C., Pande Kanchan and Bhutani, R. (2001) 40Ar-Ar39 age of a national monument: the Gilbert Hillbasalt, Deccan Trap, Bombay, Curr. Sci., v. 80, pp. 1437-1440.
Von Huene F.B. and Matley, C.A. (1933) Cretaceous-Saurischia and Ornithischia of the Central Provinces ofIndia, Geol. Surv.India, Mem. 1, Pal. India, No. 21, pp. 1-24.
Wilson J. A., Paul C. S., Srivastava S., Bhatt, D. K., Khosla, A. and Sahni, A. (2003). A new abelisaurid (Dinosauria,
Theropoda) from the Lameta Fomation (Cretaceous, Maastrichtian) of India. Contrib. Mus. Pal., Uni.
Michigan, 31(1), pp.1-42.
Wilson, J. A., Mohabey D. M., Peter S. E. and Head J. J. (2010). Predation upon hatchling dinosaurs by a newsnake from the Late Cretaceous of India. PLoS Bio., v. 8(3), pp. 1-10.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Late Cretaceous paleogeography of the Deccan Volcanic Province,
peninsular India: palynological evidence
Vandana Prasad1 and Sunil Bajpai212

Birbal Sahni Institute of Palaeosciences, Lucknow 247667, India
Department of Earth Sciences, Indian Institute of Technology, Roorkee 226007, India

Abstract
The Late Cretaceous sedimentary sequences (Infra- and Intertrappean beds) of
Deccan Volcanic Province (DVP) of Central India is extremely rich in fossil flora and fauna.
Due to both terrestrial and marine nature of fossils present in these sequences, considerable
efforts were made over the last decade to delineate the marine and terrestrial ecosystems
within the volcanic province. Identification of marine facies in a few locations of the centralwestern part of the province have so far proved insufficient in providing a complete
perspective on the paleoenvironment, including the nature and extent of marine sea ways
during the Late Cretaceous in central India. In the present study sedimentary successions
from a number of Infra- and Intertrappean sections, namely, bore hole sediments from
Ashtona village, Yeotmal District (Infratrappean), Nand area (Infratrappean), Ninma river
section (Intertrappean), Dhaiwal (Intertrappean) were studied for their palynological content.
The presence of a large number of mangrove pollen Spinizonocolpites pollen (Nypa), in
these sediments indicate a brackish marine depositional setting due to the development oflarge scale shallow marine seaways in central India during the Late Cretaceous. The presenceof mangrove pollen and dinoflagellate cysts in the Yeotmal region, Wardha basin, during theLate Cretaceous adds to the previously described marine signatures from the Intertrappean
sediments from Rajamundary, Krishna-Godavari basin on the Southeastern margin ofpeninsular India. Subsequent investigations in the Wardha-Godavari basin have also provided
compelling evidence that suggest the presence of shallow seaways in central India, which
initiated from the east coast through the Godavari rift zone during the late Cretaceous, whileearlier reports of planktonic foraminifera from the intertrappean sediments at Jhilmili near
Nagpur suggested marine incursion through Narmada rift zone from the West Coast. It is thus
inferred that during the Late Cretaceous the central India was connected to both eastern
and western marine seaways rather than from the western corridor only.

40

Late Cretaceous Vertebrate Faunal Similarities between India andMadagascar: Palaeobiogeographic Scenarios
Guntupalli V.R. Prasad
Department of Geology, University of Delhi, Delhi – 110007, Indiae-mail: guntupalli.vrprasad@gmail.com

Abstract
India and Madagascar were integral parts of the southern supercontinent
Gondwanaland until the end of Late Jurassic and continued to stay as contiguous
landmasses even after successive break-ups from Africa, and Australia-Antarctica block. In the
Late Cretaceous (~88 Ma ago), the Marion hot spot volcanism led to the separation of India
and the Seychelles block from Madagascar. Following this break-up, India underwent rapid
northward drift ultimately leading to its collision with mainland Asia whereas Madagascar
remained in its southern position. The continental Upper Cretaceous deposits of India
represented by the Lameta Formation (=infratrappean beds), the Deccan volcanosedimentary sequences (=intertrappean beds) of central and western India and the Upper
Cretaceous (Maastrichtian) Kallamedu Formation, Caurvery Basin (South India) have been
extensively investigated in recent years for their vertebrate faunas. These studies revealed
the presence of many new taxa of amphibians, lizards, turtles, snakes, crocodiles, extensive
dinosaur nesting sites and some new dinosaur bone yielding horizons, and several
mammalian taxa. The Madagascan continental Upper Cretaceous (Maastrichtian) deposits are
known by the well studied Maevarano Formation of Mahajanga Basin, northwestern
Madagascar. A diverse vertebrate fauna comprising of fishes, amphibians, lizards, snakes,
turtles, crocodiles, dinosaurs and mammals has been described from the Maevarano
Formation by the palaeontologists of Stony Brook University, New York, USA. A comparisonof the Maastrichtian faunas from India and Madagascar reveals a close similarity between
them though these faunas come from rocks deposited 20-22 Ma after the break-up ofMadagascar from India-the Seychelles block. The faunal similarities, particularly between
some fish taxa, bothremydid turtles, simosuchid crocodiles, nigerophiid and madtsoiid
snakes, and abelisaurid dinosaurs, are observed. It is puzzling to find such close similarity
between faunas of two landmasses separated ~20 Ma ago. To explain this biogeographic
anomaly, one can offer two explanations: 1) vicariant evolution of once a single fauna into
disjunct faunas, or 2) there were some faunal dispersals between India and Madagascar at
the end of Cretaceous across the Mozambique Channel. The sister group relationships
established between bothremydid turtles, nigerophiid snakes, and abelisaurid dinosaurs
support the second biogeographic scenario. However, it is an enigma how these over sea
dispersals took place between India and Madagascar when a wide body of marine waters
separated India and Madagascar at the end of Cretaceous.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Late Jurassic – Early Cretaceous Belemnites in Gyangze,
Southern Tibet, China
Liping Hu1,2, Yuewei LI 1, 2, Qi LI1, 2 , Weiyuan ZHANG1, 2 , Guobiao LI 1, 2 *1State Key Laboratory of Environmental Geology and Biogeology, China University of Geosciences, Beijing 100083, China
2
School of Earth Sciences and Resources, China University of Geosciences, Beijing 100083, China*email: liguobiao@cugb.edu.cn

Abstract
The southern Tibet is rich in Belemnites. The output of the Belemnite is mainly
concentrated in the Late Jurassic to Early Cretaceous strata. The research of Belemnites insouthern Tibet originated in the early 20th century. In the 1980s, the Chinese Academy of
Sciences organized several large-scale comprehensive scientific investigations in the southern
Tibet region, collected and studied a large number of Belemnites, and since then, there havebeen few studies on Belemnites in southern Tibet.
As a kind of important fossil in the marine Jurassic and Cretaceous strata, thebelemnites is of great significance to determine the age of the strata and to analyze thesedimentary environment. The belemnites fossils described in this thesis were mainlycollected from the Jiabula Formation in the Cretaceous in Rilang, Gyangzi, and a small partof them were collected from the Zhela Formation in Wangdan, Bailang. The Cretaceous
Jiabula Formation is mainly composed of black shale. The Belemnites of the Jiabula
Formation are abundant and of positive significance for us to determining the age andexplore the environment of the Jiabula Formation. Based on the analysis of the fossils, it isconcluded that the collected belemnites should belong to two genera, one is the Late
Jurassic Belemnopsis, preserved in dark gray shale, which suggested an anoxic depositional
environment with deep water; the other is the early Cretaceous Hibolites, which alsosuggests a similar depositional environment.
Key words: Southern Tibet; Belemnites, Jiabula Formation, Zhela Formation

Acknowledgements
This research is supported by the Strategic Project of Science and Technology ofChinese Academy of Sciences (XDB050105003), the State Scholarship Fund of China(41272030), the National Basic Research Program of China (2012CB822001), and IGCP608.

42

Lithostratigraphy of the Berapit formation
along the Malaysia-Thailand border1

Mat Niza bin Abdul Rahman and 2Mohamad Hussein bin Jamaluddin

1

Technical Services Division, Department of Mineral and Geoscience Malaysia, Ipoh, Perak, Malaysia
e-mail: mniza@jmg.gov.my2
Department of Mineral and Geoscience Malaysia, State of Johor, Johor Bahru, Johor, Malaysia
e-mail: mhussein@jmg.gov.my

Abstract
The term Berapit formation had been introduced by the Malaysian Working Group of
the Malaysia-Thailand Border Joint Geological Survey for a sequence of continental deposits
exposed near Bukit Berapit checkpoint in Pengkalan Hulu area of northern Perak. The Berapit
formation comprises a sequence of well cemented conglomerate unit that unconformably
overlies the Silurian-Devonian Kroh formation. Previously it was considered as the lowermost
part of the Nenering beds that later was renamed as Nenering formation.
Lithologically, the Berapit formation consists of reddish brown, massive, poorly
sorted, matrix supported conglomerate. The clasts are subangular to rounded, ranging from 1
cm-10 cm in diameter, made up of sandstone, shale and minor limestone; cemented byreddish sandy matrix. It shows a fining upwards sequence and the clasts show an imbricationof about N-S direction with plunging towards north. Based on poorly sorted, subangular to
subrounded clasts which were well cemented by reddish argillaceous and arenaceous
materials, the conglomerate unit may be deposited in a channel of a continental
environment not far from the source.
Previous study revealed that the age of the Berapit formation is of late Early
Cretaceous based on the presence of few Caronatisporatelata and Spheripollertesscabratus(pollen) that characterize the Aptian-Albian age.
Keywords: Berapit formation, well-cemented conglomerate, Early Cretaceous

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Lower Cretaceous oysters from Mangyshlak peninsula (northwestern
Kazakhstan) and Crimea peninsula: taxonomical compositionand stratigraphic distribution (preliminary data)
Igor N. Kosenko1, 2, Egor K. Metelkin1
1

Novosibirsk State University, Novosibirsk, Russia
Trofimuk Institute of Petroleum Geology and Geophysics, Novosibirsk, Russia
email: kosenkoin@ipgg.sbras.ru

2

Abstract
Rich collections of Lower Cretaceous (Berriasian-Albian) oysters from Mangyshlak
peninsula (northeastern of Caspian Sea) collected by geologists from All Russia Research
Geological Institute (VSEGEI; Russia, St. Petersburg) as well as collection of BerriasianValanginian oysters from Crimea (north of Black Sea) collected by T.N. Bogdanova (VSEGEI)
have been studied.
Taxonomical composition of Berriasian oysters from Mangyshlak is similar to thosefrom Crimea (Figs. 1 and 2). Common taxa are represented by Rastellum rectangularis(Roemer), Amphidonte (Ceratostreon) minos (Coquand) and “Liostrea” germaini (Coquand).
Taxa from the subfamily Pycnodonteinae Stenzel, 1959 have been identified from bothregions: “Pycnodonte” weberae (Yanin in Tsceltsova) in Crimea and “Pycnodonte” miranda(Bogdanova) in Mangyshlak. Both species show typical character of Pycnodonteinae appearance of chomata. However, their taxonomic position within the Pycnodonteinae
should be clarified. Species Deltoideum delta (Smith) typical for Upper Jurassic of Europe
has been previously identified in Berriasian of Mangyshlak by Bogdanova (1988). This provesthat this species crossed the Jurassic/Cretaceous boundary. Aetostreon subsinuatum(Leymerie) appeared in Berriasian in Crimea and only in Valanginian in Mangyshlak.
Valanginian oysters associations from Mangyshlak are more diverse than in Crimea.
Common taxa are A. (C.) minos, “L.” germaini and Rastellum. In addition “P.” miranda,
Aetostreon subsinuatum and A. falciformis (Leymerie) have been identified in Mangyshlak.
Hauterivian oysters associations inherited taxonomic composition from Valanginian. In
Mangyshlak they are represented by “L.” germaini, A. (C.) minos, Aetostreon subsinuatum
and A. dorsatum (Leymerie).
In Barremian Amphidonte (Amphidonte) conicum (Sowerby) and Gyrostrea sp. nov.
appeared. The finding of Gyrostrea in Barremian of Mangyshlak is the oldest known.
Previously this genus was considered as typical for Upper cretaceous (Stenzel, 1971;
Mirkamalov, 1986).
Aptian is characterized by appearance of new species: “Ostrea” leymerii (Deshayes inLeymerie) and Gryphaeostrea canaliculata (Sowerby), Rastellum macroptera (Sowerby) and“Pycnodonte” sp. Only A. (A.) conicum, G. canaliculata and “Pycnodonte” sp. have been
identified in Albian of Mangyshlak.

Fig. 1. Stratigraphic distribution of oysters in Lower Cretaceous of Mangyshlak peninsula.

44

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Fig. 2. Stratigraphic distribution of oysters in Berriasian - Valanginian of Crimea peninsula.

46

References
Bogdanova, T.N., 1978. Berriasian and valanginian oysters from Mangyshlak. In: Second All Union
Symposium on morphology, system, phylogeny and ecogenesis of the Bivalvia. Abstracts. 8-10.
Tiraspol Pedagogic State Institute, Tiraspol (in Russian).
Bogdanova, T.N., 1980. New early Cretaceous oysters from Mangyshlak. In: New species of fossil plants andinvertebrates of USSR. Vol. 5, 26-28. Nauka, Moscow (in Russian).
Bogdanova, T.N., Lobacheva, S.V., Prozorovsky, V.A., and Favorskaya, T.A., 1981. Concerning the division of
the Berriasian of the Crimean mountains. Bulletin of Leningrad State University, Geology/Geography
6 (1), 5-14 (in Russian).
Bogdanova, T.N., 1983. Type Mollusca. Class Bivalvia. In: Valanginian of Mangyshlak. 72-87. Nauka, Moscow(in Russian).
Bogdanova, T.N., 1988. Type Mollusca. Class Bivalvia. In: Berriasian of Mangyshlak. 134-156. Nauka,
Leningrad (in Russian).
Mirkamalov, Kh.Kh., 1986. Stratigraphy and fauna of Cretaceous deposits of southwestern Gissar Ridge. 104
p. “FAN”, Tashkent (in Russian).
Stenzel, H.B., 1971. Oysters. In: R.C. Moore (ed.), Treatise of Invertabrate Palaeontology (N), Mollusca 6,
Bivalvia 3, N953-N1224. University of Kansas, Lawrence.

47

The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Non-marine Cretaceous turtles of Japan and its significancefor paleoenvironmental analysis
Ren Hirayama
School of International Liberal Studies, Waseda University

Abstract
Non-marine Cretaceous turtles are known from some dozen localities of Japan(Hirayama, 2006; Sonoda et al;, 2015 ). Although most of materials are disarticulated andfragmentary turtle shells, they are still useful for systematics based some features such as
sculptures and scute morphology remained on the shell surface (Hirayama et al., 2012).
Fossil turtles are especially abundant in two geological units, the Early Cretaceous Tetori
Group of Central Japan, and the Late Cretaceous Kuji Group of Iwate Prefecture of
Northeastern Japan (Hirayama 2010, 2017a, b; Hirayama et al., 2010).
In the Tetori Group distributed in Gifu, Ishikawa, and Fukui Prefectures around the
Mt. Hakusan, at least 13 different turtle taxa of 7 families are known (Hirayama, 2017b). Mostof turtles are classified as the group of Trionychia, such as the genus Adocus (Adocidae),Nanhsiungchelyidae, and Trionychidae in the uppermost Kitadani Formation (presumed as
the late Aptian), whereas more basal Trionychia is found from the older Okurodani andKuwajima Formations (presumed as the Hauterivian to Barremian; Hirayama, 2002; Sano,2018). Kappachelys okurai, an intermediate form between basal Trionychia and true
Trionychidae, was reported from the Akaiwa Formation (presumed as the early Aptian;Hirayama et al., 2012; Sano, 2018). Thus, turtles seem rather important as index fossils forcorrelating non-marine sediments of the Tetori Group.
Non-marine turtles from the Tamagawa Formation (dated as the Turonian) of Iwate
Prefecture are more developed as much bigger and diversified (Hirayama, 2017b). They are
identified as 5 different taxa, such as Adocus, Trionychidae, Carettochelyidae, andLindholmemydidae. Both Adocus and trionychids are more than twice the size of turtles
from the Tetori Group.
Non-marine Cretaceous turtles from China and Mongolia are classified as only few
taxa or families from one locality such as Sinemydidae or Trionychidae in the Early
Cretaceous, and Nanhsiungchelyidae, Trionychidae or Lindholmemydidae in the Late
Cretaceous (Hirayama, 2017a). Thus, taxonomic diversifications of the Cretaceous non-marine
turtles in Japan seem significantly larger than those of the inland area of Asian continent,
reflecting more humid and stable paleoclimate in the coastal area.

References
Hirayama, R. 2002. Preliminary report of the fossil turtles from the Kitadani Formation (Early Cretaceous)of the Tetori Group of Katsuyama, Fukui Prefecture, Central Japan. Memoir of the Fukui Prefectural
Dinosaur Museum, 1: 29-40, 6 figs. (in Japanese with English abstract).

48
Hirayama, R. 2006. Review of fossil turtles of Japan. Fossils (Palaeont. Soc. Japan) 80:47-59, 11 figs.,
1 tab. (in Japanese with English abstract)
Hirayama, R. 2010. Non-marine turtles from the Early Cretaceous Tetori Group of Kasekikabe of Hakusan
City, Ishikawa Prefecture, Central Japan. In, [Scientific report on fossils from the Kuwajima
Formation, Tetori Group, of Kuwajima "Kaseki-kabe", Hakusan City, Ishikawa, Japan], pp.19-24, 2 figs.
Hakusan City Board of Education, Ishikawa Prefecture, Japan. (in Japanese)
Hirayama, R. 2017a. Fossil turtles from the Tetori Group: their systematics and biostratigraphic
significance. Program and Abstracts of the 35th Annual Meeting of the Fossil Research, 9. (inJapanese)
Hirayama, R. 2017b. Fossil vertebrate assemblages from the Late Cretaceous Tamagawa Formation of
Kuji City, Iwate Prefecture, eastern Japan.Proceedings and Field guidebook for the 5th International
Symposium of International Geoscience Program IGCP Project 608, p. 77-78.
Hirayama, R., Brinkman, D.B. and Danilov, I.G. 2000. Distribution and biogeography of non-marine
Cretaceous turtles. Russian Journal of Herpetology, 7:181-198.
Hirayama, R., Isaji, S. and Hibino, T. 2012. Kappachelys okurai gen. et sp. nov., a new stem soft-shelledturtle from the Early Cretaceous of Japan. In: Brinkman, D.B., P. A. Holroyd, and J. D. Gardner (eds.),“Morphology and Evolution of Turtles: Origin and Early Diversification.”, pp. 179-185. Springer,
Dordrecht.
Hirayama, R., Kobayashi, Y., Sonoda, T., and Sasaki, K. 2010. Preliminary report of terrestrial vertebrates
from the Late Cretaceous Tamagawa Formation of the Kuji Group of Kuji, Iwate Prefecture, easternJapan. Journal of Fossil Research 42: 74-82, 10 figs. (in Japanese with English abstract)
Nakajima, Y., Danilov, I. G., Hirayama, R., Sonoda, T. and Scheyer, T. M. 2017. Origin of softshell turtles,
and their dispersal during the mid-Cretaceous supergreenhouse. Journal of Vertebrate Paleontology
37 (2).
Sano, S. 2018. Recent advances in the stratigraphy of the Upper Mesozoic Tetori Group in northern
Central Japan : beyond the paradigm of Maeda (1961). Journal of Fossil Research 51: 5-14. (inJapanese with English abstract)
Sonoda, T., Hirayama, R., Okazaki, Y. and Ando, H. 2015. A new species of the genus Adocus (Order
Testudines; Family Adocidae) from the Lower Cretaceous of Southwest Japan. Paleontologocal
Research 19:26-32.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Palaeoecology of a Maastrichtian lake during Deccan environmental
transition: evidences from Malwa Plateau
Dhobale Anup, Dhananjay M. Mohabey, Deepesh Yadav and Bandana Samant
Department of Geology, RTM Nagpur University, Law College Campus, Amravati road, Nagpur-440001, India.
email: anupdhobale@gmail.com

Abstract
Biotic and environmental impact of Deccan volcanism across the CretaceousPaleogene boundary (K-Pg B) has been a matter of debate. The Deccan volcanic sequencesof Malwa Plateau north of Narmada represent the northern most lava piles of Deccan
eruptions mainly in the state of Madhya Pradesh, India . The lava sequences are classifield as
Malwa Group of Deccan traps (Geological Survey of India, 1993). Presently occupying over
50,000 km2 the lava fields represent at least 46 basaltic lava flows having a cumulative
thickness of over 730m. The flows are associated with multiple intertrappean sedimentary
beds and red/green boles (weathered basalt profiles/palaeosols) at different strargraphic
levels. The sediments designated as 'intertrappean' are lake deposits formed over the lava
surface during the pause in the vocanic activity and record the history of contemporary
biota and environments.
In Malwa Group the lake sediments are present at 8 stratigraphic levels associatedwith lava flows of lower series of flows of Mandleshawar and Kalisindh formations. The
upper series of lava flows are not associated with any intertrappean sediments. Ourinvestigation showed that the lava piles of lower series were erupted during themagnetochron C30n (Schoebel et al, 2014, Mohabey et al, 2018). The lake sediments at
Bagvanya locality in the Bagh Valley in Dhar District are deposits between the two basal lava
flows. Outcrops of the sediments are spread over 4 km2 that may be the minimum size of
the Bagwanya lake that developed over the fresh lava surface. The lake sediments werestudied in eight geographically separated sections having thickness 120 cm to 240 cm. The
sediments are mainly yellow to cream finely laminated clayey siltstone to siltstone
representing a fine suspension deposits derived from the basin when the lake water level
was high. The limonitic bands in the siltstones indicate intermittent aerial exposure of thesediments and their oxidation. The intercalated carbonate band showing carst-weatheringfeatures and detachments represents the deposits during the dry spell developing alkalinity
with evaporative conditions. In the upper parts the sediments mainly comprise cream toyellow argillaceous bioturbated limestone with thin gray hard clay and black to gray chert
bands. Towards the top the intercalated argillaceous carbonate bands possibly represent
their deposition during the low water level strand along the margins of the lake. The lake
sediments show that they are smectite-quartz dominated in the lower parts whereas in theupper parts it is vermiculite dominated suggesting that they are derived products after theweathering of basalt flows. The quartz may be detritus derived from the basinal margins.
The capping 30-40 cm thick micritic limestone with thin chert stringers are full of float or50

debris-wash freshwater gastropods.Stable isotope analysis of few gastropods showed valueas δ13C -6.1 and δ18O -13.3.
Plants as represented by pollen-spores are dominantly aquatic to semiquatic mainly
Gabonosporis, Sparganiaceaepollenites and Azolla cretacae (Salvineaceae family)- the latersuggesting prevalence of temperature within 200-30°C and neutral to alkaline pH in the lakeat the time of deposition. These plants possibly colonised the lake floor with good light andoxygenated conditions and may be some shrubs and herbs growing along the lake margins.
Sizeable presence of charophyte gyrogonites suggests their growth in shallow water (1-3m)
may be having a slight alkalinity. Commonly present diatom frustules- pinnate and centric(Aulocoseira) also suggest alkaline lake conditions during low-water level strand during dry
phase of lake. Vertebrates are mainly represented by isolated teeth and dermal armour
fragments of Notosuchid crocodylimorphs, indeterminate lizards (Eolacertiia Litakis?),diversified fishes dominated by Lepisosteus and Lepidotes with scarce presence ofPycnodontidae, Clupeids and batoids.
Thus, based on the studies it is interpreted that the lake was developed on the freshlava surface of the earliest flow of C30n Maastrichtian. It was a small to medium sized(4km2), shallow water lake wherein the sediments under oxygenated conditions were
deposited during the wet and dry phase of the lake under semi-arid to arid conditions.
Exclusive aquatic to semi-aquatic plants colonised different parts of the lake inhabitated byaquatic reptiles- crocodylimorphs, lizards (semiaquatic?), frogs and fishes.

References
Geological Survey of India. (1993). Published Quadrangle Geological Map. Map Printing Division,
Geological Survey of India, Government of India Publications, Hyderebad.
Mohabey, D.M., Samant, B. , Deepesh Kumar, Dhobale A., Rudra, A. and Datta, S. (2018). Record of
charcoal from early Maastrichtian intertrapean lake sediments of Bagh valley of Madhya Pradesh:palaeofire proxy. Curr. Sci. , 114 (7), 1540-1544.
Stefan Schöbel Helga de Wall Morgan Ganerød Manoj K. Pandit Christian Rolf (2014). Magnetostratigraphy
and 40Ar–39Ar geochronology of the Malwa Plateau region (Northern Deccan Traps), central
western India: Significance and correlation with the main Deccan Large Igneous Province sequences.
J. Asian Ear. Sci., 89, 28-45.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Palynoflora and microfauna from Late Cretaceous Lameta sediments
and Intertrappean sediments of Nand-Dongargaon and
Salbardi-Belkher inland basins of central India: age andpaleoenvironment implications
1*Hemant Sonkusare, 1Bandana Samant and 1D.M. Mohabey

1Post Graduate Department of Geology, RTM Nagpur University, Nagpur- 440001 (INDIA)*e-mail: hemantsonkusare19@gmail.com

Abstract
Late Cretaceous-Early Paleocene Deccan Volcanic Flood Basalt occupying an
area of about 500,000 km2 in peninsular India. The Lameta sediments of Late Cretaceous
covered the six inland basins viz. Nand-Dongargaon (N-D); Jabalpur; Sagar; AmbikapurAmarkantak; Balasinor-Jhabua and Salbardi-Belkher in the states of Maharashtra, Madhya
Pradesh and Gujarat of Central India. The detail palynology and clay mineralogy is carried outof sediments of Nand-Dongargaon and Salbardi-Belkher inland basins during present study.
Lithologically, Lameta sediments comprises of limestone, red and green clay, marlite andcalcareous sandstone. The palynoflora from the Lameta sediments and sauropod dinosaur
coprolites is represented by gymnosperms (Araucariacites sp., Cycadopites sp.,
Podocarpidites sp., Classopollis sp., etc), angiosperms (Palmaepollenites sp., Longapertitessp., Graminidites sp., Compositoipollenites, Multiareolites, Tetracolporate and Polycolporate
pollen, etc.) and pteridophytes (Azolla massulae, Cyathidites, trilete spores, etc.). Presenceof good preservation of three genera of thecamoebians viz. Centropyxis, Difflugia andPontigulasia, grass phytoliths of Poaceae, starch cells, peltate hairs, fungi and other plantremains like leaf cuticles, starch cells and tracheal material. Other biota like fungal spore(Monocellate, Dicellate and Multicellate), algal (Botryococcus, Oedogonium) and bacterial
remains associated with diatom frustules (Aulacoseira), invertebrates like gastropods andbivalves have also been recovered.
However, many intertrappean beds have been studied from the study areaand lithologically they comprises mostly of cherty limestone with nodular structure, highly
fossiliferous dark green/ black grey chert, shales, shaly chert, tuffaceous breccias, green clay
and white clay, sandy shales and occasional calcareous sandstone. The biotic assemblage ofintertrappean beds consists of freshwater Maastrichtian age marker palynoflora viz.
Jiangsupollis, Farabeipollis, Aquilapollenites bengalensis, Gabonisporis vigaurouxii,
Gabonisporites, Azolla. Microfauna such as Foraminiferal linings, peridinium dinoflagellate
and other organic structures, Gastropods (Physa, Lymnia, Turittela and Viviforms) andOstracods (Mongolianella, Cypridopsis, Frambocythere and Paracypretta, etc) have also been
recovered. Apart from Palynoflora, megafloral remains represented by palm roots, fossil
woods of both dicots and monocots, well preserved fruits of angiosperm plants are alsopresent in intertrappean beds of the study area. Palynology from coprolites of N-D basin

52suggests sauropod dinosaurs preferred to ate soft tissues of angiosperms and gymnosperms.
The presence of phytoliths of Poaceae indicates diversity of grasses during the Maastrichtian
period. Sauropod dinosaurs ingested thecamoebians, burnt grasses, sponge spicules, diatoms,
fungal spores, mycorrhizal fungi and other plant tissues during intake of water.
Lithology, Palynoflora and Clay mineralogy from the study area suggests prevalenceof Arid to Semiarid climate with marked seasonality, lacustrine environments and prevailing
sub-humid condition at the time of deposition of the intertrappean beds. The study helped
in understanding the deposition and recording Palynoflora and microfauna, environmental
condition from the Lameta and Intertrappean sediments, floral changes with the volcanic
activity in the Nand-Dongargaon and Salbardi-Belkher inland basin as well as climate during
Late Cretaceous-Early Paleocene.
Keywords: Sauropod dinosaurs, coprolites, Palynoflora, Microfauna, Maastrichtian,Intertrappeans, Inland basins, Deccan Volcanic Flood Basalt, Central India.

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Palynology studies of the Talbulag coal deposit, Eastern Mongolia
Ichinnorov N.1 ,Tsolmon G. 1, Eviikhuu A. 2, Enerel G. 1, Odgerel N.3
1

Institute of Paleontology and Geology, Mongolian Academy of Sciences, S.Danzan street 3/1, 4th khoroo,Chingeltei district,Ulaanbaatar 15160 P.O. Box-46/650, Mongolia (E-mail: ichinnorov@ipg.mn)
2
Uyan Geo Resource LLC, Chingeltei duureg-4, Sambuu st 13/2, Global business center,703National University of Mongolia, Ulaanbaatar, Mongolia

Abstract
Palynology studies of the Early Cretaceous of the eastern part of Mongolia, Talbulag
coal deposit studied for the first time to improve geological dating and correlation of sporepollen assemblages. The assemblage described from open-pit Talbulag coal deposit, AptianAlbian age for the Tevshiingovi formation (Khukhteeg Formation) in this area. The quantitative
composition of the palynofloras is characterized by the dominance or abundance of pollen
produced by the non-saccate gymnosperm pollen such as Cycadopites, Ginkgocycadopites
and bisaccite coniferus Pinuspollenites, Podocarpidites, Quadraculina, Ginkgocycadopites,
Inaperturapollenites, Cycadopites, Piceapollenites. Spores are not numerous, but presenteddifferent species of Concavisporites, Cyathidites, Osmundacidites, Cycatricosisporites,
Laevigatosporites, Cyathidites, Lycopodiumsporites, Baculatisporites, Biretisporites.
This palynocomplex is different from the previous lower Cretaceous palynocomplex(Ichinnorov, 2005, 2009, Ichinnorov, et all, 2016, 2017). In the previous assemblages were
occurred many species of spores such as Pilosisporites trichopapillosus, Pilosisporites
notensis, Pilosisporites verus, Cooksonites variabilis, Trilobosporites microverrucatus, in thisassemblage not found these spores. Spores are represented by abundant species of
Cyathidites, Osmundacides.
According to occurrences of spores and pollen the stratigraphic distribution of
palynoassemblage is Aptian-Albian (correlated to the Khukhteeg) Formation.
The palynological evidence is consistent with a humid and warm paleoclimate.

References
Ichinnorov, N. 2005. Palynostratigraphic results of Shinekhudag and Khukhteeg Formations, Eastern
Mongolia. Mongolian Geoscientist. No. 27, p.12-14.
Ichinnorov,N. 2009. Palynocomplex of Mongolia. Paleontology of Mongolia, Fanerozoic Flora. 133-155.
Ichinnorov Niiden, Christa-Ch. Hofmann, Hasegawa Hitoshi, Uranbileg Luvsantseden. 2016. Lower
Cretaceous formations and palynology of the Matad area (Tamsag Basin), southeastern Mongolia.
The Fourth International Symposium of International Geoscience Programme IGCP Project 608,
Short Papers, Novosibirsk,p. 86-89.
Ichinnorov N., Eviikhuu A. , Gankhuyag Ch., Tsolmon G., Enkhtugs U. “Lower Cretaceous spore-pollen frombrown coal deposit, Erdenetsogt Govi, Southeast Mongolia”. Abstract, P.92-93.

54

Plant Fossils from the Lower Cretaceous in Shandong Province, China
Sun Bainian, Jin Peihong, Hua Yifan,Huang Rehan
School of Earth Sciences, Lanzhou University, Lanzhou 730000, China
email: bnsun@lzu.edu.cn

Abstract
The Cretaceous is an important "greenhouse climate" period, and a series ofgeological tectonic and climatic activities happened in the time, which led to tremendous
changes in the global environment. The study on the Cretaceous plant fossils has aconstructive contribution for understanding palaeoclimate during this stage. The Laiyang area
is located in the central region of the Shandong Peninsula, China. A set of lacustrinedominated strata are developed in this area.
Plant fossils in this paper were collected from the Lower Cretaceous Laiyang
Formation of Shandong Province, eastern China, which provides an important fossil evidence
for analyzing paleoclimate, paleoecology and palaeogeography. Based on the morphologicalfeatures and microstructures of vegetative and reproductive organs, 21 species of 10 genus
from 5 families are identified, and Equisetites, Pararaucaria, Elatides, Brachyphyllum,
Pagiophyllum, Cupressinocladus, and Ephedra are discussed deeply. The dominate elementsof the Laiyang flora are the Coniferopsida, Cycadopsida, Bennettiopsida, Filicinae andPteridospermae. Otherwise, Ginkgopsida and Ephedraceae are rare. In additional, thepaleoatmospheric CO2 concentrations of the Early Cretaceous are reconstructed by using thestomatal parameters of Coniferopsida plant fossils from Laiyang Formation, which has
important guiding significance for predicting the trend of global climate change in future.
The paleoatmospheric CO2 concentration of the Early Cretaceous is reconstructedusing the stomatal ratio based on three species of Brachyphyllum, Pagiophyllum andCupressinocladus, with good indication of CO2 concentration. Furthermore, the lower paleo–
atmospheric CO2 concentration suggests a cooling trend of the palaeoclimate during the
Early Cretaceous (Hauterivian–Barremian) of the Shandong.
Keywords: Early Cretaceous, plant fossil, paleoclimate, Shandong Province

Acknowledgments
This work is supported by the National Basic Research Program of China (973 Program)(no. 2012CB822003), Specialized Research Fund for the Doctoral Program of Higher Education(Grant 20120211110022), the Fundamental Research Funds for the Central Universities (Grant
lzujbky-2015-610).

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References:
Aucour A.M., Gomez B., Sheppard S.M.F., et al., 2008. δ13C and stomatal number variability in the
Cretaceous conifer Frenelopsis [J]. Palaeogeography Palaeoclimatology Palaeoecology, 257: 462–
473.
Axsmith B.J., 2006. The vegetative structure of a Lower Cretaceous conifer from Arkansas: further
implications for morphospecies concepts in the Cheirolepidiaceae [J]. Cretaceous Research, 27:
309–317.
Berner R.A., 2006. GEOCARBSULF: a combined model for Phanerozoic atmospheric O2 and CO2 [J].
Geochimica et Cosmochimica Acta, 70: 5653–5664.
Channing A., Zamuner A., Edwards D., et al., 2011. Equisetum thermale sp. nov. (Equisetales) from theJurassic San Agustín hot spring deposit, Patagonia: anatomy, paleoecology, and inferredpaleoecophysiology [J]. American Journal of Botany, 98: 680–697.
Friis E.M., Pedersen K.R., Crane P.R., 2009. Early Cretaceous mesofossils from Portugal and eastern North
America related to the Bennettitales–Erdtmanithecales–Gnetales group [J]. American Journal of
Botany, 96: 252–283.
Haworth M., Heath J., McElwain J.C., 2010. Differences in the response sensitivity of stomatal index toatmospheric CO2 among four genera of Cupressaceae conifers [J]. Annals of Botany, 105: 411–418.
Tomlinson P.B., Takaso T., 2002. Seed cone structure in conifers in relation to development andpollination: a biological approach [J]. Canadian Journal of Botany, 80: 1250–1273.

56

Preliminary study on the growth of Fukuiraptor kitadaniensis(Dinosauria: Theropoda)
Soki Hattori1, Yoichi Azuma1,2, Soichiro Kawabe1, 2
1

2

Fukui Prefectural Dinosaur Museum, 5-11 Terao, Muroko, Katsuyama, Fukui 911-8601 Japan
Institute of Dinosaur Research, Fukui Prefectural University, 4-1-1 Kenjojima, Matsuoka, Eiheiji, Fukui 910-1195 Japan

Abstract
Fukuiraptor kitadaniensis is an allosauroid theropod known from the Lower Cretaceous
Kitadani Formation, Tetori Group cropping out in the Kitadani Dinosaur Quarry, Fukui, Japan. A
number of isolated bones of this taxon have been collected from the quarry including the
growth series of femora, most of which are much smaller than those of the holotype specimen(FPDM V97122; Currie & Azuma, 2006). Although such concentration of juvenile specimens may
indicate nesting or breeding (Currie & Azuma, 2006), a substantially-low growth rate could be
an alternative reason for such bias. To address this question, we examine the age composition
and reconstruct the growth curve of F. kitadaniensis based on the femoral growth series.
Currie & Azuma (2006) reports 18 femora of F. kitadaniensis in addition to theholotype specimen. Because this taxon is the only allosauroid species recognized in thisquarry, its identification was based on six characters synapomorphic to allosauroids. First, we
re-examined these femora and other theropod femora from the quarry based on eightcharacters, six from Currie & Azuma (2006) and additional two as follows; the mid-shaft ismediolaterally narrow and dorsoventrally elongated in the cross section, and the trochantericshelf does not reach the plantar margin of the shaft. Second, we analyzed thin sections of four
femora of Fukuiraptor including the holotype specimen to locate the best section to count
LAGs (lines of arrested growth), which are growth rings with an annual periodicity occurring in
the bones of tetrapods. There is a nutrient foramen on the dorsal aspect of the proximal shaft(Azuma & Currie, 2000) which probably suggests the position of the center of growth, where
the cortical bone possibly records the largest number of LAGs. The computed tomographic
images of the specimens revealed that the foramen penetrates the cortical bone nearly
perpendicular to the long axis of the shaft. This suggests that the center of growth of thefemur is possibly in this region of the shaft, just proximal to the fourth trochanter and distal to
the lesser trochanter. Because of these reasons, we made thin sections of this region, in
addition to the one at the mid-diaphysis region, which is a standard procedure in previous
histological studies on theropods. In this presentation, we report the result and discuss theimplication of our thin section analysis.

References
Azuma, Y., and P. J. Currie. 2000. A new carnosaur (Dinosauria: Theropoda) from the Lower Cretaceous ofJapan. Canadian Journal of Earth Sciences 37:1735–1753.
Currie, P. J., and Y. Azuma. 2006. New specimens, including a growth series, of Fukuiraptor (Dinosauria,
Theropoda) from the Lower Cretaceous Kitadani Quarry of Japan. Journal of Paleontological Society of
Korea 22:173–193.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Preliminary study on the provenance of the Hayang Groupsandstones in the Gyeongsang Basin, Korea using
detrital zircon geochronology
Taejin Choi1, Min Gyu Kwon1
1

Department of Energy and Resources Engineering, Chosun University, Gwangju 61452, Korea
e-mail address: tchoi@chosun.ac.kr

Abstract
Gyeongsang Basin is the largest Cretaceous nonmarine sedimentary basin in the
Korean Peninsula, formed by extension in an active continental margin setting. The basinfillof the Gyeongsang Basin is subdivided into the Sindong, Hayang and Yucheon groups withdecreasing age. The Hayang Group is divided into three subbasins: Yeongyang, Euiseong, andMilyang subbasins southward. Each subbasin has stratigraphically different basinfill eachother, which means their different evolution history. To characterize the sedimentary
provenance and basin drainage systems of the succession, 12 Hayang Group sandstones in
the Yeongyang subbasin were collected for U-Pb detrital zircon age dating using a laserablation-inductively-coupled-plasma mass spectrometry technique from each formation infour different parts of the subbasin.
Detrital zircons show a wide range of ages ranging from 3,560 Ma to 99 Ma withspatial and temporal variation of age population. The zircon grains from western part of thebasin are dominated by Jurassic and Paleoproterozoic ages, while those from the northernpart are dominated by Paleoproterozoic ages with minor Mesozoic ages. Based on thestatistical test, provenance of the Hayang Group sandstones in the Yeongyang subbasin canbe grouped into three groups according to their differences in the ratio between the
Mesozoic and Paleoproterozoic zircon age populations. These three groups may represent
the shared detrital drainage systems and their evolution during the deposition of the
Yeongyang subbasin sediments.

58

Provenance of the Cretaceous Neungju Basin, Korea
Min Gyu Kwon1*, Taejin Choi1, Seung Won Shin2
1

Department of Energy and Resources Engineering, Chosun University, 61452 Gwangju, South Korea
2
Department of Geological Sciences, Pusan National University, Korea
email: mingyu,Kwon@chosun.kr

Abstract
The Neungju Basin is a Cretaceous nonmarine basin located in the southwestern
Korean Peninsula. Basinfill of the Neungju Basin consists mainly of conglomerate, sandstone,siltstone, and tuff. The Neungju Basin is filled by the Neungju Group, which consists mainly ofsiliciclastic and pyroclastic rocks with volcanic rocks. The strata of the Neungju Group consistof Oyeri Fm., Manwolsan Tuff, Jangdong Fm., Yeonhwali Fm., Yeonsan Fm., Jeokbyeok Tuff,
Ongam Conglomerate. The Jangdong Tuff, one of the strata comprising the Neungju Group,
bears dinosaur track. Depositional environment of the Jangdong Tuff is interpreted to be alake margin. However, sedimentological characteristics of the whole Neungju Basin have notbeen studied yet. Thus, we carried out petrography and detrital zircon geochronology
analysis on the Neungju Basin sedimentary rocks to constrain their provenance.
Petrographic analysis on the Neungju Basin sediments reveals that the sandstones
and matrices of the conglomerate are comprised mainly by angular grains of quartz, feldspar,and metasedimentary and volcanic rock fragments. The conglomerate are generally matrixsupported and contain angular clasts such as quartzite, schist, granite, and tuff. The amountof rock fragments increase up sequence.
Zircon grains in tuffs in the Neungju Basin show ages of 96~88 Ma and indicate
depositional period of the basin. Conglomerates and sandstones mainly contain detrital
zircons of Jurassic(187 Ma) and Early Proterozoic age(1853 Ma), but no Cretaceous zircons.
Oyeri and Yeonsan Fm., located in northern part of the basin contain Jurassic(187 Ma) and
Early Proterozoic zircon grains(1,854 Ma). Jeokbyeok Tuff and Ongam Conglomerate, locatedin eastern of the basin contain only detrital zircons of Early Proterozoic(1,848~2,476 Ma).
Jandong Fm., located in southwestern of the basin mainly contains Jurassic zircons(187 Ma).
Deposition of the Neungju Basin was begun at about 96~94 Ma, earlier than theeruption time of the Mudeungsan Tuff (86~84 Ma). Sediments comprising clastic rocks of the
Neungju Basin were mainly supplied from nearby Jurassic granite, Paleozoic metasediments,
and Early Proterozoic gneiss. Considering that the clastic sedimentary rocks do not contain
Cretaceous zircons, the pyroclastic material was supplied intermittently from the southwestof the basin during the deposition of the Basin.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Refined chronostratigraphy of the late Mesozoic terrestrial strata
in South China and its tectono-stratigraphic evolution
Xianghui Li1, * Chaokai Zhang1 Yongxiang Li1 Yin Wang2 Ling Liu2
1

State Key Laboratory of Mineral Deposit Research, School of Earth Sciences and Engineering, Nanjing University, Nanjing,
210023, Jiangsu, China
2
East China Mineral Exploration and Development Bureau, Nanjing, 210007, Jiangsu, China

Abstract
The late Mesozoic terrestrial strata in numerous small basins in South China provide
important sedimentary archives to understand the tectonic evolution of South China andEast Asia. However, establishing regional stratigraphic framework within a basin and precisely
correlating strata among basins / regions remain challenging due to limited chronologicalconstraints. In this study, we report zircon U-Pb ages of 21 samples and a compilation of 132
reliable age data from 15 type sections of the volcanic-sedimentary basins in South China.
The synthesized geochronology allows us to establish a refined chronostratigraphy for thelate Mesozoic terrestrial strata. New calibrated results indicate most of lithostratigraphic units
are diachronic, laterally stacking, and / or interfingering in the Gan-Hang tectonic zone (backarc or rifting basins), South China. Particularly, the Cretaceous type sections, such as theZhoucun-Yanxia type section at Shouchang of Jiande and the Laozhu section of Lishui inwestern Zhejiang, were interpreted as two duplicates of the same stratigraphic sequences.
Six stacking styles are classified for the relationship of lithostratigraphic units. Analysis of therefined chronostratigraphy and the stratal stacking styles together with lithologicalcomposition reveals three episodes of tectono-stratigraphic evolution. Episode Ⅰ (~145-125
Ma) is featured by intense volcanism, as evidenced by widespread volcanic strata and (137120 Ma) A-type granites, and was probably related to the rollback of the subducting PaleoPacific plate; The strata deposited during Episode Ⅱ (~125-100 Ma) is composed ofvariegated sediments associated with/without volcanic intercalations in sedimentary faulteddepression basins, indicating the waning of volcanism and tectonism attributed to the endingof the Izanagi / Kula plate subduction; In Episode Ⅲ (<~100 Ma), red strata occurred along
the NE-SW strike-slipping sinistral faulting or failed rifting in small basins, which probably
resulted from the drastic directional change of the subduction of the Paleo-Pacific plate from
NW to SN.
Keywords: chronostratigraphy; stratigraphic stacking; tectono-stratigraphy; late
Mesozoic; South China

60

Review and Revision of the socalled "Khorat Group", NE, Thailand
Nares Sattayarak

Abstract
Non-marine Mesozoic red beds in the northeastern part of Thailand was firstmentioned in 1923 by Wallace Lee in his report on coal and petroleum exploration. Twenty
years later, Brown et al. (1953) named the Khorat Series to represent these strata and Triassic
limestone of northern Thailand. After measured 5 stratigraphic type sections, Ward andBunnag coined the new name “Khorat Group” in 1964. They divided the Group into 7
formations in ascended order namely as follow the Nam Phong, Phu Kradung, Phra Wihan,
Sao Khua, Phu Phan, Khok Kruat and Unnamed Formations. Iwai et al., (1966) proposed a
new formation “Huai Hin Lat” as the lowest formation, rested conformably under the Nam
Phong Formation and gave the Rhatian to Liassic ages from plant fossils found. On the other
hand, Gardner et al (1967) proposed the name Maha Sarakham Formation to replace theUnnamed, the uppermost formation of the Group. The age of these rock salt strata were
believed to be from Late Cretaceous to probably as late as Early Tertiary. In the following
decades, many formations found locally in various areas were mapped and placed as thelowest formation of the Khorat Group, e.g., Nam Pha, Sap Mai Daeng, Lom Sak. However,Chonglakmani and Sattayarak (1978) combined all those formations laid down below the
Nam Phong Formation into one formation, due to their equivalence in litho-stratigraphy. The
name Huai Hin Lat Formation was selected according to the rule of priority.
On the upper portion of the Group, Hite and Japakasetr (1979) described thesequence of the Maha Sarakham Formation into 6 units from bottom to top, as follow the
Basal Anhydrite, Lower Rock Salt, Lower Claystone (Lower Clastics), Middle Rock Salt, Middle
Claystone (Middle Clastics), Upper Rock Salt and Upper Claystone (Upper Clastics). In themeantime, Sattayarak and Suteethorn (1979) mapped the mountainous area located in thenortheastern part of the Khorat Plateau and presented the new rock strata called the Phu
Tok Formation which was believed to be mainly eolian sediments as probably equivalent to
the Upper Clastics of the Maha Sarakham Formation.
It had been almost 2 decades that Thai geologists accepted that the Mesozoic
monotonous redbeds Khorat Group composed of 9 formations in ascended order namely
the Huai Hin Lat , Nam Phong, Phu Kradung, Phra Wihan, Sao Khua, Phu Phan, Khok Kruat,
Maha Sarakham, and Phu Tok. All formations were accumulated in the same basin “theKhorat Basin”.
In 1989 Sattayarak et al, proposed a new Triassic sedimentary sequences found in
the west area of the Khorat Plateau. These sediments deposited mainly in half graben riftbasin. These rocks took place in various kinds of depositional environment. e.g., alluvial fan,river, swamp and lake. This rock sequence was comparable to the Huai Hin Lat Formation.
They further suggested that after rifting culminated and a mild deformation took place, thewhole area was subsided due to thermal cooling and formed a huge sagging basin, theKhorat Basin. Hence this rock formation should be separated from the Khorat Group.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Unfortunately, Sattayarak et al. did not coin this formation name but called it Triassic half garben sediments. Subsequently, geologists from foreign oil companies dubbed it as
Khuchinarai Formation and/or Group.
Later on, Sattayarak and Polachan (1990) demonstrated an unconformity between
the Khok Kruat and Maha Sarakham Formations and proposed to move the later and the
Phu Tok Formation out of the Khorat Group.
Up to now, study on various topics relating to the Khorat Group via different tools,
concepts, and methodologies have been carried. Such as geophysics, radioactive,
paleomagnetism, palynology, paleontology, stratigraphy and structural geology. Thesestudies resulted in many proposed revisions e.g., the proper nomenclature and subdivisions,the correct ages, paleogeography, as well as, basin configuration and evolution.
In conclusion, more studies and discussions on many topics related to the so-called
Khorat Group should be carried and published for better understanding and more benefits ofThai geologists.

62

Searching for the non-marine Jurassic/Cretaceous boundary
in northeastern China
Gang Li1, Atsushi Matsuoka2
1) State Key Laboratory of Palaeobiology and Stratigraphy, Nanjing Institute of Geology and Palaeontology, Chinese Academyof Sciences, Nanjing 210008, China. gangli@nigpas.ac.cn
2) Faculty of Science, Department of Geology, Niigata University, Niigata 950-2181, Japan. amatsuoka@geo.sc.niigata-u.ac.jp

Abstract
In northeastern China the well developed Jurassic and Cretaceous strata are mainlyof non-marine origin. The definition of a non-marine Jurassic/Cretaceous (J/K) boundary innortheastern China is mainly based on the age assignment of the well known non-marine
Jehol Biota of eastern Asia. Although the Eosestheria-Ephemeropsis-Lycoptera bearing strata
in China, Mongolia and Transbaikalia of Russia were originally assigned to Early Cretaceous in
1920s, the whole Jehol Group of western Liaoning of northeastern China, which contains theJehol Biota in the lower and the Fuxin Biota in the upper, was revised to Middle-Late Jurassic
since early 1960s. This age revision was further supported by the recoveries of an alleged
Bathonian (Middle Jurassic) Arctocephalites ammonite fauna and a Late Jurassic Buchia faunafrom eastern Heilongjiang Province in middle 1980s. Since early 1990s, through the revisionsof the above mentioned Jurassic marine faunas of eastern Heilongjiang to Early Cretaceous
ones, the Jehol Biota was re-assigned back to the Early Cretaceous by some authors. At thesame time the recoveries of feathered dinosaurs, early birds, mammals and angiosperms
from the Yixian and Jiufotang formations stimulated the interests to carry out preciseradiometric dating for the Jehol Group and its underlying strata in western Liaoning andnorthern Hebei. The new radiometric dating indicates that the non-marine J/K boundary innorthern China would be delineated within the contemporaneous Houcheng (in northernHebei) and Tuchengzi (in western Liaoning) formations, which are stratigraphically much
lower than the Jehol Group of western Liaoning.
Keywords: Non-marine, Jurassic/Cretaceous boundary, northeastern China

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Sedimentology and stratigraphy of Phuwiang Dinosaur excavationsites, Khon Kaen Province, northeastern Thailand
Pitaksit Ditbanjong1*, Kritsada Moonpa2, Nontawat Srisomporn3, Nuttawat Obaom4,
Kamonlak Wongko5 and Phornphen Chanthasit6
1,2,3,4

Department of Geological Sciences, Faculty of Science, Chiang Mai University, Chiang Mai, Thailand
Phu Wiang Fossil Research center and Dinosaur Museum, Department of Mineral Resources, Khonkaen, Thailand
6
Sirindhorn Museum, Department of Mineral Resources, Kalasin, Thailand*pitaksit.d@cmu.ac.th5

Abstract
Phuwiang Mountain Range, where first dinosaur bone of Thailand was discovered, islocated in the northeastern part of Thailand. Since 1977, Thai-French collaboration team had
researched continuously in the Early Cretaceous Phuwiang fossil sites and found 4 new
dinosaur species including Siamosaurus suteethorni, Phuwiangosaurus sirindhornae,
Siamtyrannus isanensis and Kinnareemimus khonkaenenis. However, few studies in
sedimentology and stratigraphy were reported. This work aims to study sedimentology andstratigraphy of 9 excavation sites in Phuwiang Moutain where bones and foot print were
found. According to field observation and facies analysis method, sedimentary successions
are composed of reddish to maroon siltstone and sandstone, conglomerate, calcrete layer
and limestone. Twelve lithofacies have been established and can be grouped into 4 facies
association interpreted as 1) channel fill deposit 2) crevasse splay deposit 3) lake and flood
plain deposit and 4) overbank deposit. Sedimentary logs from 9 excavation sites arecorrelated and can group into 3 units. The lowermost, unit A is white sandstone with crossbedding where dinosaur foot prints are present at site No.8. Unit B, overlying on Unit A, is
composed of medium to thick bedded sandstone interbedded with siltstone. Conglomerate
can be locally found with some bone fragments. The uppermost, unit C consists of reddish
siltstone, sandstone, limestone, conglomerate and calcrete layer. Bivalve and dinosaur bones
are common in this unit. After the previous works, unit A can correlated to upper Phra Wihan
Formation and unit B and C correlated to Sao Khua Formation of Khorat Group. The resultsof this study suggest that unit C have the most potential for future fossil exploration andresearch.
Key Word: Stratigraphy, Phuwiang, Dinosaur sites, Early Cretaceous, northeastern
Thailand64

Significance of Cretaceous strata in the Japanese Islands:
Cretaceous continental arc-trench system
Hisao Ando1 and Masaki Takahashi2
1

Department of Earth Sciences, Faculty of Science, Ibaraki University, Bunkyo 2-1-1, Mito, Ibaraki 310-8512, Japan;
hisao.ando.sci@vc.ibarki.ac.jp
2
Research Institute of Geology and Geoinformation, National Institute of Advanced Industrial Science and Technology (AIST),
Central 7, Higashi 1-1-1, Tsukuba, Ibaraki 305-8567, Japan

Abstract
The Japanese Islands are situated in an active convergent margin along the eastern
margin of Asian continent. Their geologic structure is therefore very complicated. The
distribution of Cretaceous strata reflects the tectonic settings of four arc-trench systems:
Kuril, Northeast (NE) Japan, Southwest (SW) Japan and Ryukyu (Takahashi and Ando, 2016).
The tectonic configurations of the two main systems (NE Japan and SW Japan) during theCretaceous have not yet been well resolved partly because of the heavy post-Cretaceous
tectonic influence. This is because the Cretaceous strata had been affected by postPaleogene tectonic movements such as the Japan Sea opening, the subduction ofPhilippines Sea Plate, the collision of the Izu-Ogasawara arc since the early Miocene. To
establish the paleogeographic and paleoenvironmental reconstruction of the Cretaceous, wemust thus pay attention carefully to the post-Cretaceous geologic settings.
We compiled spatiotemporal distributions of the Cretaceous rocks (plutonic andvolcanic rocks, sedimentary rocks, and accretionary complexes) in the SW Japan and NE
Japan arcs is based on the published geological maps as well as many current geologicalresearches. Their distributions were drawn on the straight paleogeographical map of the SW
Japan and NE Japan arcs prior to the opening of Japan Sea (25 Ma). Although the Cretaceousrock distributions apparently differ between the SW Japan and NE Japan arcs, their fourparallel zonal arrangements can be broadly recognized throughout both arcs: 1) mostly nonmarine sedimentary rocks in intra-arc basins, 2) granitic and volcanic rocks in the magmaticarc, 3) mainly marine and subordinately fluvial sedimentary rocks in forearc basins, and 4)
sedimentary rocks of turbidite and mélange facies in accretionary complexes.
We correlated a total of 48 Cretaceous successions in intra-arc and forearc basins,from Kyushu to north Honshu islands on a stratigraphic chart and compiled them as to major
sedimentary facies. This result shows the general similarity of major sedimentary facies andtrends between the NE Japan and SW Japan arcs, suggesting that the forearc basins had been
continued throughout the two arcs during the Cretaceous. Although surface exposures ofCretaceous strata are very scarce in NE Japan, the offshore forearc beneath the Pacific is
estimated to contain very potent subsurface Cretaceous forearc basin sediments, spread
more than a several tens of kilometers wide area. The conspicuous zonal distribution ofCretaceous forearc sediments along the southern half of SW Japan was possibly formed as
the result of post-early Miocene tectonics, such as the Japan Sea opening and related

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adjacent plate movements. Therefore, the conspicuous differences in geologic structure
between SW Japan and NE Japan arcs, resulted from their differentiated Neogene tectonic
histories.
Japanese Cretaceous strata record a wide variety of sedimentary facies and biofacies
changes from offshore to shallow-marine to continental, reflecting paleoenvironments andbasin tectonic settings such as backarc/intra arc, forearc and trench slope-trench basins along
the single continental arc-trench system between the Eurasian Plate and the subducting
Paleo-Pacific oceanic plate.

References
Ando, H. and Takahashi, M., 2017. Reconstruction of the Cretaceous Paleo-Japan continental arc-trenchsystem reconsidered from Cretaceous geologic records in the Japanese Islands. Fossil (Kaseki), 102,
43–62.
Takahashi, M. and Ando, H., 2016. Reconstruction of the Cretaceous continental arc of Japan on a
viewpoint of arc-trench system. Fossil (Kaseki), 100, 45–59.

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Stratigraphy and Structure of Jurassic – Cretaceous Rocks in theThong San Khan and Chat Trakan Areas, Northern Thailand.
Pongsathon Kanna, Weerapan Srichan*, Phisit Limtrakun, Boontarika Srithai, Pitaksit Ditbanjong
and Rattanaporn Fongngern
Department of Geological Sciences, Faculty of Science, Chiang Mai University*email: weerapan.s@cmu.ac.th

Abstract
Jurassic – Cretaceous rocks in the Thong San Khan and Chat Trakan areas can beclassified to 8 rock units from detail mapping. Unit A is composed of tuff interbedded with
tuffaceous sandstone, pyroclastic breccia and agglomerate. Unit B is white sandstoneinterbedded with thin bedded siltstone. Unit C is dominated by cross-bedded mediumgrained white sandstone. Unit D is mainly white and greenish grey sandstone. Unit E isconsisted of red fine-grained sandstone, red siltstone interbedded with medium-grainedsandstone. Unit F is composed of reddish purple fine-grained sandstone and reddish purple
siltstone. Fragments of fossil turtle shells and fossil fish scales were found in the middle partof unit F. Unit G is composed of grey sandstone and reddish purple siltstone. Unit H is mainly
white sandstone and conglomerate. Sedimentary strata (unit B to G) are mainly continental
deposit with corresponding to Khorat Group. Previously, unit A was interpreted to be Jpk,
unit B to D were grouped as JKpw whereas units E to H were grouped as Ksk with recently
found terrestrial fauna. In these areas, the geologic structures of Jurassic – Cretaceous rocks
are dominantly fold and thrust structures with closely N-S trending. NE-SW trending leftlateral strike slip faulting cross-cut the middle part of the area and is possibly associated to
the fold-thrust structure developing in the Cenozoic tectonic of SE Asia.
Key words: Stratigraphy, structure, Jurassic – Cretaceous, northern Thailand

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Terrestrial climates in East Asia during the Cretaceous inferredfrom the stable oxygen and carbon isotope compositionsof vertebrate apatites; Further results
Romain Amiot
Univ Lyon, Université Lyon 1, Ens de Lyon, CNRS, UMR 5276 LGL-TPE, 69622 Villeurbanne, France.
email: Romain.amiot@univ-lyon1.fr

Abstract
Past terrestrial climatic conditions in terms of local air temperatures andprecipitation amounts can be inferred from the oxygen and carbon isotope compositions ofvertebrate apatites preserved as fossilized skeletal remains (teeth, bones, scales). Using
existing phosphate-water oxygen isotope fractionation equations established for extant
crocodilians, turtles, mammals, dinosaurs and fish (Amiot et al., 2017, 2007, 2004; Barrick et al., 1999;
18
Lécuyer et al., 2013), the δ Ow value of Cretaceous local surface waters can been estimated fromvertebrate phosphate and, when possible, Mean Air Temperature (MAT) are calculated basedon the known relationship existing between local meteoric water δ18Omw value and MAT(Dansgaard, 1964). The mean amount of annual precipitation (MAP) can be estimated fromthe δ13Cplant value of C3 plants (Diefendorf et al., 2010; Kohn, 2010). In turn, the averagevalue of local Cretaceous C3 plants δ13Cplant value can be estimated either from the carbon
isotope composition of preserved organic matter in sediments, or the δ13Cc value of apatite
carbonate of plant-eating vertebrates such as sauropodomorph and ornithischian dinosaurs(Fricke et al., 2008; Fricke and Pearson, 2008; Tütken, 2011). Using published and newly acquired oxygenisotope composition of vertebrate apatite phosphate, as well as carbon isotope
compositions of sediment organic matter and dinosaur apatite carbonate, MAT and MAP
have been estimated for Early and Late Cretaceous localities of East Asia (China, Japan,
Thailand, Mongolia, Russia). The validity of these reconstructed climatic variables will be
discussed in the light of their paleolatitudinal, paleogeographic and paleontologic contexts,
and compared to other climate records.

References:
Amiot, R., Angst, D., Legendre, S., Buffetaut, E., Fourel, F., Adolfssen, J., André, A., Bojar, A.V., Canoville, A.,
Barral, A., Goedert, J., Halas, S., Kusuhashi, N., Pestchevitskaya, E., Rey, K., Royer, A., Saraiva, A.Á.F.,
Savary-Sismondini, B., Siméon, J.-L., Touzeau, A., Zhou, Z., Lécuyer, C., 2017. Oxygen isotope
fractionation between bird bone phosphate and drinking water. Sci. Nat. 104, 47.
https://doi.org/10.1007/s00114-017-1468-2
Amiot, R., Lécuyer, C., Buffetaut, E., Fluteau, F., Legendre, S., Martineau, F., 2004. Latitudinal temperature
gradient during the Cretaceous Upper Campanian-Middle Maastrichtian: δ18O record of continental
vertebrates. Earth Planet. Sci. Lett. 226, 255–272. https://doi.org/10.1016/j.epsl.2004.07.015

68
Amiot, R., Lécuyer, C., Escarguel, G., Billon-Bruyat, J.-P., Buffetaut, E., Langlois, C., Martin, S., Martineau, F.,
Mazin, J.-M., 2007. Oxygen isotope fractionation between crocodilian phosphate and water.
Palaeogeogr. Palaeoclimatol. Palaeoecol. 243, 412–420. https://doi.org/10.1016/j.palaeo.2006.08.013
Barrick, R.E., Fischer, A.G., Showers, W.J., 1999. Oxygen isotopes from turtle bone: applications for terrestrial
paleoclimates? Palaios 14, 186–191. https://doi.org/10.2307/3515374
Dansgaard, W., 1964. Stable isotopes in precipitation. Tellus 16, 436–468. https://doi.org/10.1111/j.21533490.1964.tb00181.x
Diefendorf, A.F., Mueller, K.E., Wing, S.L., Koch, P.L., Freeman, K.H., 2010. Global patterns in leaf 13C
discrimination and implications for studies of past and future climate. Proc. Natl. Acad. Sci. 107,
5738.
Fricke, H.C., Pearson, D.A., 2008. Stable isotope evidence for changes in dietary niche partitioning among
hadrosaurian and ceratopsian dinosaurs of the Hell Creek Formation, North Dakota. Paleobiology 34,
534–552.
Fricke, H.C., Rogers, R.R., Backlund, R., Dwyer, C.N., Echt, S., 2008. Preservation of primary stable isotope
signals in dinosaur remains, and environmental gradients of the Late Cretaceous of Montana andAlberta. Palaeogeogr. Palaeoclimatol. Palaeoecol. 266, 13–27.
Kohn, M.J., 2010. Carbon isotope compositions of terrestrial C3 plants as indicators of (paleo) ecology and(paleo) climate. Proc. Natl. Acad. Sci. 107, 19691–19695.
Lécuyer, C., Amiot, R., Touzeau, A., Trotter, J., 2013. Calibration of the phosphate δ18O thermometer withcarbonate–water oxygen isotope fractionation equations. Chem. Geol. 347, 217–226.
https://doi.org/10.1016/j.chemgeo.2013.03.008
Tütken, T., 2011. The diet of sauropod dinosaurs: implications from carbon isotope analysis of teeth,bones, and plants, in: Klein, N., Remes, K., Sander, M. (Eds.), Biology of the Sauropod Dinosaurs:
Understanding the Life of Giants. Indiana University Press, Bloomington, pp. 57–79.

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The depositional environments of the Late Jurassic-Early Cretaceous
Phu Noi dinosaur site, Phu Kradung Formation,
Kalasin, northeastern Thailand
Rattanaphorn Hanta1, Phornphen Chanthasit2, Kajeepan Sorndech1, Jiraporn Promthong1
1School of Geotechnology, Institute of Engineering, Suranaree University of Technology, 111 University Ave.,
Suranaree, Muang, Nakhon Ratchasima, 30000, Thailand
2
Sirindhorn Museum, Department of Mineral Resources, Kalasin, 46140, Thailand
Corresponding author: hantar@sut.ac.th, hantarch@gmail.com

Abstract
Phu Noi is a small rounded and marginal erosional remnant hill of the NW-SE
aligned Phu Phan Range. Phu Noi has gently southwestward dipping beds of the lower part of the
Phu Kradung Formation. The area is covered by sparse trees and shrub of the dry dipterocarp
forest. The discovery of the Phu Noi fossil site was from the fish scales and bone fragment findingby the villagers. A further excavation and research activities have been proceeded by thecollaboration between Department of Mineral Resources, Mahasarakham University and Frenchpaleontologists. A great number of dinosaur remains comprising of mamenchisaurid sauropods,
sinraptorid theropods, small theropod and ornithopod found associated with pterosaurs, hybodont
sharks, bony fishes, turtles, temnospondyls, teleosaurid crocodilians, bivalve and plants werecollected in situ. The fossil assemblage suggests the Late Jurassic and likely a latest Jurassic toearliest Cretaceous in age to the site. This study aims to provide information on the sedimentarydepositional environment and to elucidate the accumulation of these fauna by using field data,
petrography and geochemical analysis. The studied section was approximately 10 meters thick. It
comprises mainly of the lower greenish gray clastic facies and the upper grayish red purple finer
grained deposits. The lower greenish gray facies was composed primarily of the lowermost
conglomerate with vertebrate fragments and the overlying moderately to well sorted very fine tofine grained calcareous sandstone. According to petrography and geochemical analysis, sandstone
is composed of quartz, feldspar and other minerals such as biotite, muscovite and chlorite. Thesesandstone beds show planar cross lamination and ribbon structure which evidenced the crevasse
channel deposit. This lower facies forms gradational contact to the overlying grayish red purple finegrained sandstone to mudstone deposits. This upper fine grained facies comprises of the welldeveloped ripple lamination, pedogenic slickensides, mica-rich mottling mudstone to very finegrained sandstone in which the majority of fossil and dinosaurs were found. The fossil bearing bed
is successively overlaid by the strongly mottling mudstone and the horizontal thin beds of fissile
mudstone to very fine grained sandstone representing crevasse splay deposit with a lowering
current energy to stagnant shallow water. In summary, the Phu Noi dinosaurs was accumulated in
the crevasse splay deposits of the meandering river system.

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The Early Cretaceous angiosperm pollen of Transbaikalia andPrimorye region (Russia)
E.V. Bugdaeva, V.S. MarkevichFederal Scientific Center of the East Asia Terrestrial Biodiversity, Far Eastern Branch of Russian Academy of Sciences,
Vladivostok, bugdaeva@biosoil.ru

Abstract
We revealed in recent years the angiosperm pollen in the Lower Cretaceous depositsof the Transbaikalia and Primorye region.
In the Porechye quarry of the Ilyichevka coal field of the Razdolnaya River Basin(Southern Primorye region), which outcrops the Lipovtsy Formation of the Aptian age, pollenof the Clavatipollenites hughesii Coup., Tricolpites micromunus Burger, T. vulgaris Pierce, T.
variabilis Burger, Tricolpites spp., Quercites sparsus (Mark.) Samoil., Retitricolpites georgensis
Brenn. was found. The percentage of this pollen in the palynospectra is extremely low. In
the sequence of this formation, the aforementioned palynomorphs appear above the acidic
tuffs, widely distributed in the upper part of the thick rhabdopissite-humic coal seam. In thisterritory, after the termination of coal accumulation, the extensive river valleys developed.
Such environments are favorable for angiosperm colonization.
In the palynospectra of coeval sediments, outcropping in the Aleksei-Nikolsky quarry
in this basin, Tricolpites spp. (0.9%) and Clavatipollenites hughesii (0.3%) were obtained. The
acidic tuff bed in the thick rhabdopissite-humic coal seam is almost not expressed, alluvial
deposits are not found. Perhaps the existence of marsh conditions was unfavorable forflowering plants, so they are extremely rare here.
In 2015, we visited Dongning coal mine in the north-western margin of the
Razdolnaya River Basin in China, where the coeval coal-bearing deposits are developed. Herein palynospectra of the Dongning Formation we identified the following species ofangiosperms: Tricolpites sp., Quercites sparsus, Retitricolpites vulgaris, R. georgensis,
Clavatipollenites hughesii, Fraxiniopollenites variabilis Stanl. The percentage of this pollen isvery low - most often a fraction of a percent, sometimes 1-2%, maximum 2.9%.
The early angiosperms of Transbaikalia were first discovered by paleoentomologistsof the Paleontological Institute (Moscow) in the Baisa locality in Central Transbaikalia, where
the Zaza Formation of the Barremian-Aptian age is distributed. V.A. Vakhrameev and Z.I.
Kotova (1977) described Dicotylophyllum pussilum Vachr. and pollen Asteropollis asteroides
Hedl. et Norr. In the same article Kotova pointed to the findings of pollen, in addition to theabove, as well as Clavatipollenites hughesii in the Lower Cretaceous deposits of theTransbaikalian basins, such as Konda, Beklemishevo, Chita-Ingoda, Arbagar, and East
Urulungui.
We studied more abundant palynospectra from Baisa locality. They include
Asteropollis asteroides, Clavatipollenites hughesii, C. incisus Chlon., and Tricolpites sp. The

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lacustrine deposits of this locality were formed in semi-arid environments, which areindicated by the presence of marl and black "paper shale" layers.
Recently, in the palynospectra of the coal-bearing beds of the Tarbagatay coal mineof the Khilok River Basin and the Olon-Shibir coal mine of the Tugnuy Basin of Transbaikalia,
we found single tricolpate pollen and monosulcate Clavatipollenites incisus. These findings
are confined to the marsh facies. Besides angiosperms, the costate spores having affinity with
Schizaeaceae (Cicatricosisporites sp., Impardecispora apiveruccata, Concavissimisporites
asperus, Pilosisporites setiferus), characteristic of the Early Cretaceous, were found in these
spectra. Based on these data, we believe that the age of these coal-bearing deposits is theBarremian-Aptian.
Thus, the first angiosperms of the Barremian-Aptian age of the Transbaikalia andPrimorye region included plants that produced tricolpate and monosulcate pollen.
The pollen Clavatipollenites constitutes early elements in angiosperm pollen records
from the western North Atlantic (Hochuli and Kelts, 1980) as well as in deposits from theNorth American Potomac Group (Brenner, 1963; Doyle and Robbins, 1977) and Portugal(Heimhofer et al., 2007). The oldest finding of this pollen type, according to Brenner (1996),
was in sediments from Israel, dated as old as the late Hauterivian.
We have an interesting fact that the early angiosperms of the Transbaikalia andPrimorye region certainly include very rare tricolpate pollen, while in pre-Albian palynofloras
of Portugal and North America it is absent. It should be taken into account that theformation of these coeval floras took place in different paleoenvironments. The palynofloras
we described existed in the inland continental basins of the Asian continent, whereas thefloras of the Lusitanian Basin (the Cresmina section) and the Algarve Basin (the Luz section),and the Potomac Group of the Atlantic coasts - in the coastal lowlands. The European andNorth American sites from palaeolatitudes between ~10°S and ~60°N were mostly situatedalong the margins of the Tethys Ocean (Heimhofer et al., 2007, see references in this paper).
Two forms of Clavatipollenites are found in the Barremian sediments of the Cresmina
section, in the lower Aptian - several forms of Retimonocolpites, Asteropollis and Pennipollis.
The same palynomorphs are found throughout the entire section. After a break insedimentation, more diverse pollen was found in the sediments of the lower Albian,including also Dichastopollenites, Stellatopollis and Racemonocolpites. Here, the firsttricolpate pollen of the groups Tricolpites, Artiopollis and Striatopollis appears. Further along
the section in the sediments of the middle and upper Albian, the number and diversity ofangiosperms increases (Heimhofer et al., 2007).
In the Barremian and lower Aptian of the Cresmina section, the pollen ofangiosperms in the assemblage is extremely small - less than 2%, the diversity varies from 2
forms in the Barremian to 4 in the lower Aptian. Above the unconformity in the lower Albian,the percentage of angiosperm pollen increases (5-8%), while the diversity increases to 17
taxa per sample (Heimhofer et al., 2007).
The pollen Clavatipollenites, Retimonocolpites, Asteropollis, as well as Pennipollis
and Stellatopollis are found in the lower part of the lower Aptian of the Luz section. Thesepalynomorphs are relatively common and distributed throughout the sequence (the upper
part of the lower Aptian Asteropollis is not found). The early Albian assemblage is

72characterized by the appearance of new forms of monosulcate pollen (including
Dichastopollenites) and tricolpate (Tricolpites, Artiopollis, Virgo spp., Rousea spp.,
Phimopollenites spp.).
The amount of angiosperm pollen in the early Aptian assemblage is less than 2%(total 5 taxa), in the late Aptian - less than 5% (5-10 taxa). From the end of the Aptian
angiosperm pollen becomes an important element (5% and 10%). Diversity ranges from 10
to 15 (maximum 17) taxa in the early Albian.
The development of angiosperms at an early stage in the Asian continent has similarfeatures to that of the coast of the Tethys Ocean - a trend of a gradual increase in theamount and taxonomic diversity from the Barremian to the Albian, the presence of such
palynomorphs as Clavatipollenites, Asteropollis, and Tricolpites. But there are also thedifferences - in the North American and West European palynofloras Pennipollis,
Dichastopollenites, Stellatopollis, Racemonocolpites, Artiopollis and Striatopollis occured,and this pollen absent in the East Asian palynofloras. One of the most significant is theappearance of the tricolpate pollen in the early Albian, while in Asia it took place in the
Barremian-Aptian palynofloras. Heimhofer et al. (2007) believe that the time of appearanceof the eudicotyledons producing tricolpate pollen is the early Albian. But, note that from theAptian deposits of the Potomac Group of the USA, the eudicot Potomacapnos apeleutheron(Jud, Hickey, 2013), similar to the representatives of modern Fumarioideae (Papaveraceae),
was described. These authors, discussing the absence of co-occurring tricolpate pollen inlocality, suggested that the tricolpate pollen may not have been preserved in these plantbearing beds due to its entomophilous nature; it is also possible that low preservation
probability indicates that some leaf features of extant eudicots appeared before the origin oftricolpate pollen.
According to E.-M. Friis et al. (2017), the eudicotyledons, producing tricolpate pollen,
appeared at the Barremian-Aptian boundary and constituted an insignificant part of thoseplant communities. In the Albian these plants become more diverse and the common
components of vegetation. These authors also assumed that the rarity of pre-Albian finds ofeudicotyledons can be explained by their predominantly herbaceous or shrubby life forms.
The formation of the Early Cretaceous palynofloras of North America, Western Europe
and East Asia underwent in different paleoenvironments. We can assume that the existenceof a more humid climate on the Asian continent, confirmed by the extensive developmentof coal-bearing facies, was more favorable for the growth of plants producing tricolpate
pollen. Perhaps the Albian humidization of climate in Portugal caused appearance of plants
produced this pollen. The plants produced such palynomorphs as Pennipollis,
Dichastopollenites, Stellatopollis, Racemonocolpites, Artiopollis and Striatopollis, absent in
Asian palynofloras, probably existed under arid and semi-arid conditions.
With a difference in the taxonomic composition, the trend of quantitative
participation of angiosperm pollen in the palynofloras of the Northern Hemisphere is very
similar - from the share of one percent in the Barremian, 1-4% in the Aptian (at the end of
the Aptian even 5-10%), more than 8% in the Albian. The taxonomical diversity ofangiosperm pollen in the palynofloras also increases from 1-2 taxa in Barremian, 1-7 in the
Aptian and more than 7 in the Albian.

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Acknowledgments
The authors are grateful to V.N. Kulezky and G.D. Chimitov (the Open Joint Stock
Company “Tugnuy Coal Mine”, the Buryat Republic) for sending of the palynologicalsamples, N.P. Domra (Federal Scientific Center of the East Asia Terrestrial Biodiversity, Far
Eastern Branch of Russian Academy of Sciences, Vladivostok) for the processing of thepalynological samples.
Our study was supported by the Russian Foundation for Basic Research (grants 16-0401411 and 17-04-01582).

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and Water Resources Bulletin. 1963. Vol. 27. Department of Geology, Mines and Water Resources,
Baltimore. P. 1-215.
Brenner G.J. Evidence for the earliest stage of angiosperm pollen evolution: a paleoequatorial section from
Israel // Taylor D.W., Hickey L.J. (Eds.). Flowering Plant Origin, Evolution and Phylogeny. London:
Chapman & Hall, 1996. P. 91–115.
Doyle J.A., Robbins E.I. Angiosperm pollen zonation of the continental Cretaceous of the Atlantic coastal
plain and its application to deep wells in the Salisbury Embayment // Palynology. 1977. Vol. 1. P.
43–78.
Friis E.M., Pedersen K.R., Crane P.R. Kenilanthus, a new eudicot flower with tricolpate pollen from the Early
Cretaceous (early-middle Albian) of eastern North America // Grana. 2017. Vol. 56, No. 3. P. 161–
173.
Heimhofer U., Hochuli P.A., Burla S., Weissert H. New records of Early Cretaceous angiosperm pollen from
Portuguese coastal deposits: Implications for the timing of the early angiosperm radiation // Review
of Palaeobotany and Palynology. 2007. Vol. 144. P. 39–76.
Hochuli P., Kelts K. Palynology of Middle Cretaceous black clay facies from Deep Sea Drilling Project sites
417 and 418 of the western North Atlantic // Initial Reports of the Deep Sea Drilling Project. V. 51,
52, 53. Washington: U.S. Government Printing Office. 1980. P. 897–935.
Jud N.A., Hickey L.J. Potomacapnos apeleutheron gen. et sp. nov., a new Early Cretaceous angiospermfrom the Potomac Group and its implications for the evolution of eudicot leaf architecture //American Journal of Botany. 2013. Vol. 100. № 12. P. 2437–2449.
Vakhrameev V.A., Kotova I.Z. Early Angiosperms and Associated Plants from the Lower
Cretaceous of Transbaikalia // Paleontol. Zhurn., 1977. No. 4. P. 101–109.

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The Early Cretaceous Birds from the Kitadani Formation, Katsuyama,
Fukui, Japan: a Unique Window to the Extinct Avifauna in the Far East
Imai, T.1,2, Azuma, Y.1,3, Shibata, M.1,3, Kawabe, S.1,3, Miyata, K.1,3, and Tsukiji, Y.4
1

Fukui Prefectural Dinosaur Museum, 51-11 Terao, Muroko, Katsuyama, Fukui 911-8601, Japan
Graduate School of Natural Science and Technology, Kanazawa University, Kakuma, Kanazawa, Ishikawa 920-1192, Japan
3
Institute of Dinosaur Research, Fukui Prefectural University, 4-1-1 Kenjojima, Matsuoka, Eiheiji, Fukui, 910-1195, Japan
4
Department of Earth and Planetary Systems Science, Graduate School of Science, Hiroshima University, 1-3-1 Kagamiyama,
Higashihiroshima, Hiroshima 739-8526, Japanemail: t-imai@dinosaur.pref.fukui.jp
2

Abstract
Abundant skeletal and trace fossils of the Early Cretaceous birds have been collectedfrom northeastern China and the Korean Peninsula, facilitating our understanding of diversity,
ecology, and evolution of birds during the time. In contrast, the Early Cretaceous avian fossils
had been very poorly known from Japan. Here, we present avian fossils from the Lower
Cretaceous Kitadani Formation, the Tetori Group. They comprise a single partial skeleton,
seven separate tracks (Azuma, 1993), and a single eggshell fragment (Imai & Azuma, 2015), allcollected from the Kitadani Dinosaur Quarry, Katsuyama, Fukui, Japan. The avian-fossil recordof the Kitadani Formation is notable in that both skeletal and trace fossils occur, and that it
can be compared to the avian-fossil record in other parts of East Asia.
The Kitadani Formation (Aptian) is the uppermost part of the Tetori Group croppingout in the central Japan and represents a temperate inland meandering fluvial systemsituated in the eastern continental margin of Asia (Sano & Yabe, 2016, and references
therein). The formation is well-exposed in the Kitadani Dinosaur Quarry which yields various
vertebrates including dinosaurs.
The partial skeleton (FPDM-V-9769) of a bird (Fig. 1A) comes from greenish siltstone,
which is interpreted as an overbank deposit. High-resolution X-ray micro-computedtomography at SPring-8 (RIKEN/JASRI, Hyogo, Japan) reveals that the skeleton is disarticulated
and composed of fragmentary skull, several vertebrae with a pygostyle, furcula, coracoids,
several ribs, partial ilium, and most of forelimbs and hindlimbs lacking pes. FPDM-V-9769
exhibits several primitive features including pygostyle with reminiscent individual caudal
vertebrae, boomerang-shaped robust furcula, triangular-shaped and unfused ilium, unfused
metacarpals and manual digits with manual craws, and unfused metatarsals, possibly
suggesting its basal position in the clade Pygostilia. Histological and phylogenetic analyses arebeing conducted to assess its ontogenetic stage and phylogenetic position within class Aves.
The avian tracks occur in an alternating sequence of mudstone and fine sandstone.
Among the seven avian tracks initially described by Azuma (1993), with aid of portable 3D
imaging devices (Artec Spider and Artec Eva, Artec 3D), we present detailed description andtaxonomic assessment of two specimens, FPDM-F-74 and FPDM-F-75 (Fig. 1B). FPDM-F-74 islarge with slender digits with pointy ends and lacks hallux and webbing traces. FPDM-F-75 issmaller than FPDM-F-74, and exhibits webbing traces between digits II and III, and III and IV.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

FPDM-F-75 is larger than most semi-palmate avian ichnotaxa. These avian tracks indicate thepresence of at least two different avian taxa in the Kitadani Formation, one of them possibly
being a shorebird with webbed pes.
Avian eggshell from the Kitadani Formation is represented by a single specimen,
FPDM-V-9175 (Fig. 1C), coming from pale structureless siltstone rich in reworked calcareous
nodules and small gastropods, interpreted as an overbank deposit. The specimen is assigned
to its own oogenus and oospecies Plagioolithus fukuiensis (Imai & Azuma, 2015). The
specimen exhibits a combination of characters that is comparable to extinct and extant avian
eggshells including thin shell (0.44 mm), smooth external surface, non-branching and narrow
pore canals with relatively constant width, and three structural layers. Imai & Azuma (2015)
argues that FPDM-V-9175 most likely belongs to a bird, while additional specimens withassociated skeletons are required to test this interpretation. It is noteworthy that, in contrast
to other avian-fossil-bearing Lower Cretaceous deposits, the Kitadani Formation yields bothskeletal fossils and hard-shelled eggshells. This is probably because the lacustrine andshallow marine deposits favor fossilization of delicate avian skeletons (e.g., the Jehol Group,
northeastern China, and the Calizas de La Huérgina Formation, Las Hoyas, Spain), but not
eggshells, while fluvial overbank deposits observed in the Kitadani Formation can adequately
preserve both skeletons and eggshells.
In northeastern China and South Korea, the regions that are rich in avian fossils,
occurrence avian skeletons, tracks, and eggshell from a single locality had not beenreported. In this regard, the Kitadani Formation is notable where avian skeletons, tracks, andeggshells are all preserved, providing a variety of avian fossils. The Kitadani Formation andother avian-fossil-bearing horizons in Japan provide unique windows to the avifauna in the
Far East during the Early Cretaceous.

References
Azuma, Y. 1993. The Early Cretaceous dinosaur ichnofauna and its paleoenvironmental development in
the Tetori Group, Japan. Ph. D. dissertation, University of Tokyo, Tokyo, 155 pp.
Imai, T., and Azuma, Y. 2015. The oldest known avian eggshell, Plagioolithus fukuiensis, from the Lower
Cretaceous (upper Barremian) Kitadani Formation, Fukui, Japan. Historical Biology 27: 1090–1097.
Sano, S., and Yabe, A. 2016. Fauna and flora of Early Cretaceous Tetori Group in Central Japan: The clues
to revealing the evolution of Cretaceous terrestrial ecosystem in East Asia. Palaeoworld 26 (2): 253–
267.

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Figure 1. Avian fossils from the Kitadani Formation. (A) Partial skeleton of a pygostylian bird, FPDM-V-9769;(B) Tracks, FPDM-F-74 (top left) and FPDM-F-75 (top right) with corresponding topographic images(bottom) for each specimen; and (C) eggshell, FPDM-V-9175.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

The Facies Analysis of Sedimentology of the Phu Tok Noi architecture,
Phu Tok Formation, Khorat Plateau, Northeast Thailand.
Kiattisak Sonpirom1, PeangtaSatarugsa1, and Natthawiroj Silaratana1,
Department of Geotechnology ,Faculty of Technology, KhonKaen University, Thailand

Abstract
This study aimed to detail the vertical succession of Phu Tok Noi, Phu Tok Formation
exposed in the Khorat Plateua, Northeast Thailand with a facies analysis. From the bottomto-top succession of the Phu Tok Formation at the PhuTok Noi area can be grouped into
three facies that included ephemeral channel facies, eolian dune facies, and marginallacustrine facies. The ephemeral channel faciesat the base is characterized by planar
bedding and cross planar bedding of clast-supported intra formational conglomerate, and by
grading up to massive sandstone, planar horizontal bedded sandstone and trough crosslaminated sandstoneat the top. This facies indicates fluvial deposits. The eolian dune facies
consists of thick to massive beds of large tangential cross bedding sandstone. In general,
bedding of the eolian dune facies is truncated at the top surface with large cross bedding ofhigh dip at the top with the dip angle decreasing to horizontal at the bottom of thesuccession. In addition, at the top of sequence, this eolian dune facies is interbedded withthe marginal lacustrine facies. The marginal lacustrine facies consists of planar horizontal
stratified sandstone at the base and fining upward to wavy ripple sandstone at the top withthickness up to 5 m.The wavy ripple sandstone is interstratified with lenses of coarsegrainded sandstone. The planar horizontally stratified sandstone is well sorted lying on an
erosional surface of the underlying eolian dune remnant. The erosional surface indicates
sheet flood flew rapidly over the sand dune into a lake basin. The wavy ripple sandstone
with lenses of coarse grain sands is represented to wave-ripple deposit at shallow lakemargin. These bed sets are up to 5 meters thick indicate a continued flow of subsurface
water into a lake basin after sheet flood ceased.
Key words: PhuTokNoi, PhuTok Formation, eolian deposits

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The Skull of Pelecanimimus Polyyodon (Theropoda,
Lower Cretaceous, Spain): Comparative Approachto Asian Ornithomimosauria.
Elena Cuesta1; Francisco Ortega2; José Luis Sanz3.
1

Institute of Dinosaur Research, Fukui Prefectural University, Matsuokakenjojima 4-1-1, Yoshida-gun Eiheijicho, Fukui, 9101195 Japan. Email: elena.cuestaf@gmail.com
2
Grupo de Biología Evolutiva, Facultad de Ciencias, Universidad Nacional de Educación a Distancia, Paseo Senda del Rey 9,28040 Madrid, Spain.
3
Unidad de Paleontología, Facultad de Ciencias, Universidad Autónoma de Madrid, Cantoblanco, 28049 Madrid, Spain.

Extended Abstract
Introduction
Pelecanimimus polyodon Pérez-Moreno et al. (1994) was discovered in the Spanish
fossil site of Las Hoyas (Barremian, Lower Cretaceous). The holotype of Pelecanimimus iscomposed by the anterior half of an articulated skeleton that preserves evidence of softtissues as a soft occipital crest and a gular structure. Pelecanimimus was defined as a basal
ornithomimosaurian (Pérez-Moreno et al., 1999), being the first ornithomimosaurian describedin Europe.
Ornithomimosauria is widely distributed throughout the world. However, the Asian
record contains a huge number of taxa that represents almost its lineage. There are primitive
representatives such as Shenzhousaurus from China or Harpymimus from Mongolia. The
more derived representatives are Beishalong and Sinornithomimus from China; andGarudimimus, Deinocheirus, Anserimimus and Gallimimus from Mongolia.
One of the most striking features of Ornithomimosauria is its dentition and therelation with its biomechanical and diet behaviour. A partial or complete edentulism and adevelopment of keratinous beaks are specializations related to a most herbivorous dietarybehaviour (e.g. Barret, 2005; Cuff and Rayfield, 2015). Most of the members ofOrnithomimosauria are edentulous, especially the derived taxa as Gallimimus, Garudimimus,
Sinornithomimus or Deinocheirus. However, Pelecanimimus polyodon has over 200
premaxillary, maxillary and dentary teeth. Pérez-Moreno et al. (1994) explained this condition
as an alternative functional counterpart of the cutting edge of a beak. This function would
become an exaptation with a slicing effect, eventually leading to the cutting edge observedin most derived ornithomimosaurs.
A detailed osteological description of the skull of Pelecanimimus is required previous
to a functional study comparing the its biomechanics with those of the Asian edentulous
derived ornithomimosaurian. Here, we perform an osteological description of thePelecanimimus skull, whose features have been compared with those of other Asianornithomimosaurian. A CT scan and 3D reconstruction have allowed to decipher somefeatures not previously available.

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Material and methods
The holotype of Pelecanimimus polyodon (MCCM-LH 7777) is the anterior half of anarticulated skeleton. Both side of the skull was subjected to a delicate transfer preparation inorder to eliminate the matrix around the fossil and allowing to observe both lateral views of
the skull. This process was performed before its first publication in Pérez-Moreno et al., 1994.
In the left side of the skull, the facial bones are almost perfectly preserved but the occipitalpart of the skull is crushed and disarticulated. The right side is also almost completely
visible, only the snout is hidden. As the left part, the occipital area is disarticulated but more
complete than that of the left one.
Pelecanimimus skull was CT scanned. The slices obtained were imported to asegmentation software for visualization, segmentation, identification and isolation of eachsingle bone of the skull. This have allowed to decipher some osteological features, which are
not visible in the fossil to the naked eye. For instance, identifying bones at medial side as
splenial and prearticular or the right snout, which is obscured by sediments.
The osteological features of the skull of Pelecanimimus was compared with othermembers of Ornithomimosauria, whose information was gathered from the literature.

Results
Both premaxillary process in both premaxilla are in contact with the nasal and do notreach the antorbital fossa. Pelecanimimus presents 14 premaxillary teeth and a subnarial
foramen on the lateral surface, over the teeth row. In the maxilla, there are two fenestra
additional to the antorbital fenestra in the antorbital fossa, and the maxillary body is large,
triangular, acute and posterodorsal inclined as in the basal ornithomimosaurian
Nqwebasaurus (Choiniere et al., 2012). The maxillary teeth row only extends to the anterior
end of the antorbital fossa. Posterior to the teeth row, the buccal edge is a sharp ridge as inderived ornithomimosaurian such as Gallimimus (Osmólska, 1972) or Garudimimus (Kobayashi
and Barsbold, 2005a). The palatal process has a jugal ramus well developed. The lacrimalpresents a well-projected posterior and anterior processes, a ventral process perpendicular
to the anterior one and a medial recess separated by a vertical lamina. The prefrontal is
hypertrophied, occupying almost half width of the orbital edge, and developing along theventral process of the lacrimal. A peculiar feature in the jugal is the presence of a pneumatic
recess between the lacrimal and maxillary processes, a primitive feature not observed inother ornithomimosaurian. The frontal is triangular in dorsal view and it have a dome on its
posterodorsal surface. It is well-developed, occupying more than the half width of orbitaledge. The dentaries have more than 100 teeth between both side and their anterior end is
not anteroventrally deflected. The surangular has two posterior foramina and an
anteroposteriorly oriented lateral ridge. The mandibular fenestra is reduced.

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Discussion
Pelecanimimus shares with other ornithomimosaurs an elongated premaxilla, theseparation between the maxilla and external naris, the domed surface of frontal, a sharp
posterior margin of the maxilla, a well-developed jugal ramus of palatal, and a hypertrophied
prefrontal. However, Pelecanimimus also retains several primitive features such as apremaxillary process not reaching the antorbital fossa or a pneumatic recess in the anteriorramus of jugal. Undoubtedly, the most striking feature of Pelecanimimus is the presence ofapproximately 200 premaxillary, maxillary and dentary teeth. Another autapomorphy
associated to the dentition is the absence of a symphysis deflection of the dentary, which ispresent in all members of the group with known dentary, including those with dentary teeth
as Harpymimus (Kobayashi and Barsbold, 2005b) and Shenzousaurus (Ji et al., 2003).

Acknowledgments
We acknowledge to S. Langreo (MUPA) for providing access to Pelecanimimus
polyodon. We also thank to the palaeontologist of the Fukui Prefectural Dinosaur Museum
for the scan of the skull. EC research is financed by a Postdoctoral Grant of Japan Society for
the Promotion of Science (Ref: PE18034).

References
Barrett, P. M., 2005. The diet of ostrich dinosaurs (Theropoda: Ornithomimosauria). Palaeontology 48(2),347-358.
Choiniere, J. N., Forster, C. A., de Klerk, W. J., 2012. New information on Nqwebasaurus thwazi, acoelurosaurian theropod from the Early Cretaceous Kirkwood Formation in South Africa. Journal of
African Earth Sciences 71, 1-17.
Cuff, A. R., Rayfield, E. J., 2015. Retrodeformation and muscular reconstruction of ornithomimosaurian
dinosaur crania. PeerJ 3, e1093.
Ji, Q., Norell, M. A., Makovicky, P. J., Gao, K. Q., Ji, S. A., Yuan, C., 2003. An early ostrich dinosaur andimplications for ornithomimosaur phylogeny. American Museum Novitates, 1-19.
Kobayashi, Y., Barsbold, R., 2005a. Reexamination of a primitive ornithomimosaur, Garudimimus brevipes
Barsbold, 1981 (Dinosauria: Theropoda), from the Late Cretaceous of Mongolia. Canadian Journal of
Earth Sciences 42(9), 1501-1521.
Kobayashi, Y., Barsbold, R., 2005b. Anatomy of Harpymimus okladnikovi Barsbold and Perle 1984
(Dinosauria; Theropoda) of Mongolia. In: The Carnivorous Dinosaurs. Indiana University Press,
Bloomington 97-126.
Osmólska, H., Roniewicz, E., Barsbold, R., 1972. A new dinosaur, Gallimimus bullatus n. gen., n. sp.
(Ornithomimidae) from the Upper Cretaceous of Mongolia. Palaeontologica Polonica 27, 103-143.
Pérez-Moreno, B. P., Sanz, J. L., Buscalioni, A. D., Moratalla, J. J., Ortega, F., Rasskin-Gutman, D., 1994. A
unique multitoothed ornithomimosaur dinosaur from the Lower Cretaceous of Spain. Nature 370,
363.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Through The Looking Glass: Insights From Radiolarian Researchin Elucidating The Geologic Evolution of The Philippines
Edanjarlo J. Marquez1, Karlo L. Queaño2, and Carla B. Dimalanta3
1

GAEA Research Laboratory, Department of Physical Sciences and Mathematics University of the Philippines Manila,
Padre Faura St., Manila, Philippines
2
Apex Mining Co. Inc., Pasig City, Philippines
3
National Institute of Geological Sciences, University of the Philippines, Diliman, Quezon City Philippines
email: ejmarquez@post.upm.edu.phAbstract
The Philippines is one of the areas in the world where ophiolite and ophiolitic
complexes have been studied. Available paleontologic and isotopic data have indicated thatthese sequences are pre-Cenozoic. In the last 30 years or so, radiolarian research has
contributed in deciphering and understanding the geologic evolution of the Philippines. Mostof these investigations are concentrated in Luzon with very few studies done in Visayas andin Mindanao. Figure 1 shows the location of areas discussed in this work.
Southern Sierra Madre, Rizal: The Kinabuan Formation, the sedimentary cover of theMontalban Ophiolite Complex, is composed of clastic and calcareous rocks. Reported ages
varies from Turonian (Arcilla, 1991) and Campanian (Tumanda, 1994). Ringenbach (1992)
opined that the depositional environment of the limestones as bathyal based on thepresence of radiolarians.
Northern Sierra Madre, Rizal: Cherts associated with the Casiguran Ophiolite exposed
along the eastern coast of the Northern Sierra Madre were investigated. The cherts and thelimestone interbeds conformably overlie the ophiolite. The radiolarian assemblages from thecherts constrain the stratigraphic range of the cherts to the Lower Cretaceous (upper
Barremian–lower Aptian to Albian)(Queaño et al., 2013). This new biostratigraphic result is incontrast with the Upper Cretaceous stratigraphic range previously reported in the region.
Zambales: The Zambales Ophiolite Complex (ZOC) is one of the most studied
ophiolites in the region. Several massifs comprise the ZOC, one of which is the Coto Blockoverlain by clastic sedimentary units previously dated as Eocene. This resulted to tectonic
models grounded on the assumption that the entire ZOC is Eocene. However, a recent study(Ishida et al., 2011, Queaño et al., 2011, Queaño et al., 2017a) showed the presence of chert
blocks within the Early to Middle Miocene clastic formation overlying the Acoje Block in thenorthern part of the ophiolite complex. Radiolarians extracted from the cherts yielded a
stratigraphic range that suggests a Late Jurassic to Early Cretaceous age. As such, a reexamination of ZOC is warranted.
Northwest Ilocos Norte: Radiolarian biostratigraphic investigation of the cherts thatwere incorporated withinthe tectonic mélange from the northwestern Ilocos Norte indicate
an Upper Jurassic to Lower Cretaceous stratigraphic range (Queaño et al, 2017b). These chert
units are incorporated within the Dos Hermanos Mélange which also includes metamorphic
and serpentinized peridotite fragments that are set in a highly sheared, sandy matrix. The

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radiolarianbiostratigraphic data provide evidence for the existence of a Mesozoic basinal
source fromwhich the cherts and associated rocks were derived.
These research works have provided either new age information or refinement in thecalibration of ages. It has also given additional evidence for the existence of a Mesozoic
oceanic substratum as well as confirmation of the localities block affinity.

References
Arcilla, C.A., 1991. Lithologic, age, and structural study of the Angat Ophiolite, Luzon, Philippines. M.Sc.
Thesis, University of Illinois, Chicago, 107 pp.
Ishida, K., Suzuki, S., Dimalanta, C.B., Yumul, G.P. Jr., 2011. Radiolarian dating of ophiolites and theoverlying tur- bidites in the Philippine Mobile Belt, Northern Luzon Island. Geocon 2011”Geology
working for a resilient society”, Dec. 8-9, 2011, Quezon City, 20-21.
Queaño, K.L., Marquez, E.J., Dimalanta, C.B., Salapare, R.C., Guotana, J.M., Casulla, M., Paringit, M.A.,
Tumulak, M.L., Sanchez, M.P., Yumul, G.P. Jr., 2011. Mesozoic piece of oceanic lithosphere inWestern Luzon: From the rocks of Northwestern Ilocos Norte to the Zambales Ohio- lite Complex.
Geocon 2011”Geology working for a resilient society”, Dec. 8-9, 2011, Quezon City, 75.
Queaño, K.L., Marquez, E.J., Aitchison, J.C. and Ali, J.R., 2013. Radiolarian biostratigraphic data from theCasiguran Ophiolite, Northern Sierra Madre, Luzon, Philippines: Stratigraphic and tectonic
implications. Journal of Asian Earth Sciences, v. 65, 131-142.
Queaño, K.L., Dimalanta, C.B., Yumul, G.P. Jr., Marquez, E.J., Faustino-Eslava, D.V., Suzuki, S. and Ishida, K.
2017a. Stratigraphic units overlying the Zambales Ophiolite Complex (ZOC) in Luzon, (Philippines):
Tectonostratigraphic significance and regional implications. Journal of Asian Earth Sciences, Volume
142, 20-31.
Queaño, K.L., Marquez, E.J., Dimalanta, C.B., Aitchison, J.C., Ali, J.R. and Yumul, G.P. Jr., 2017. Mesozoic
radiolarian faunas from the northwest Ilocos Region, Luzon, Philippines and their tectonic
significance. Island Arc, e12195. doi:10.1111/iar.12195.
Ringenbach, J.C., 1992. La faille Philippine et les chaines en decrochement associees (centre-nord Luzon)
evolution cenozoique et cinematique des deformations quaternaries. These de doctoral delUniversite de Nice-Sophia Antipolis. Documents et Travaux, 16, 316 pp.

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The Sixth International Symposium of International Geoscience Programme IGCP Project 608

Turtles from the Lower Cretaceous Khok Kruat Formation of Nakhon
Ratchasima, Northeastern Thailand: New data
Wilailuck Naksri1*, Teppei Sonoda2, Duangsuda Chokchaloemwong1, Masateru Shibata2,3,
Yoichi Azuma2,3, Pratueng Jintasakul1
1

Northeastern Research Institute of Petrified Wood and Mineral Resources, Nakhon
Ratchasima Rajabhat University, 184 Moo 7 Suranaree Subdistrict, Mueang, Nakhon Ratchasima 30000, Thailand
2
Fukui Prefectural Dinosaur Museum, 51-11 Terao, Muroko, Katsuyama, Fukui 911-8601, Japan
3
Dinosaur Research Institute, Fukui Prefectural University, 4-1-1 Kenjojima, Matsuoka,
Eiheiji, Fukui 910-1195, Japan*Corresponding author: wilailuck.naksri@yahoo.com

Abstract
Two pan-trionychian turtles have been reported from the Khok Kruat Formation in
Nakhon Ratchasima, Northeastern Thailand including a carrettochelyid, Kizylkumemys
khoratensis and an adocid, Shachemys sp., based on shell materials (Tong et al., 2005;2009). Since 2007, new turtle materials have been discovered by the Thailand-Japan
Dinosaur Excavation Project at Suranaree and Khok Kruat subdistricts, Nakhon Ratchasima
Province. The material consists mainly of shells of both Shachemys and Kizylkumemys, butalso a nearly complete skull which probably belongs to K. khoratensis (Sonoda et al., 2015).
The different shell characters in carrettochelyid may suggest sexual dimorphism or different
taxon. In 2017, a skull and shell fragments have been discovered in a new locality, Ban Krok
Duean Ha, Suranaree subdistrict. The taxonomic composition of the turtle fauna from the
new locality is similar to that from Ban Saphan Hin. The comparisons of the skull of K.
khoratensis with that of other carettochelyids will provide information on the cranial
morphology and early evolution of the Carettochelyidae.
Keywords: turtle, Khok Kruat Formation, Nakhon Ratchasima, Thailand

References
Sonoda, T., Naksri, W., Shibata, M., Songtham, W., Jintasakul, P., and Azuma Y. 2015. New
Materials of Pan-Trionychian Turtles from the Lower Cretaceous Khok Kruat Formation in Northeastern
Thailand. Program and abstracts of the 2nd International Symposium on Asian Dinosaurs in
Thailand 2015. Bangkok, Thailand. 19th-20th November 2015. p.49-50. (Oral presentation)Tong, H., Claude, J., Suteethorn, V., Naksri, W., and Buffetaut, E. 2009. Turtle assemblagesof the Khorat Group (Late Jurassic-Early Cretaceous) of NE Thailand and their palaeobiogeographicalsignificance. In: Buffetaut, E., Cuny, G., Loeuff, J., & Suteethorn, V. (eds.) Late Palaeozoic andMesozoic Ecosystems in SE Asia. London, Geological Society, Special Publication, 315, 141-152.
Tong, H., Suteethorn, V., Claude, J., Buffetaut, E., and Jintasakul, P. 2005. The turtle faunafrom the Khok Kruat Formation (Early Cretaceous) of Thailand. In: Wanakao, L., Youngme, W., Srisuk, K.,
and Lertsirivorakul, R.(eds) Proceedings of the International Conference on Geology, Geotechnology
and Mineral Resources of Indochina (GEOINDO 2005). Khon Kaen University, Khon Kaen, 610–614.

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Upper Cretaceous palynofloras from the Himenoura Group (SouthWest Japan) and consequences for the Normapolles andAquilapollenites palynological provinces in eastern Asia
Julien Legrand1, Toshifumi Komatsu2, Yuka Miyake3, Takanobu Tsuihiji4, Makoto Manabe5
1Chuo University, Tokyo, Japan – e-mail: legrand@kc.chuo-u.ac.jp;
2
Kumamoto University, Japan;
3
Satsumasendai City, Japan;
4
Tokyo University, Japan; 5 National Museum of Nature and Science, Tokyo, Japan

Abstract
The Himenoura Group consisting of non-marine to marine siliciclastics is widelydistributed in the western part of Kyushu Island, where it outcrops sporadically on
Koshikishima Islands (Kamikoshikishima, Nakakoshikishima and Shimokoshikishima islands
from North to South) and the Amakusa Archipelago (Kamishima and Shimoshima islands from
North to South). The group, divided into Hinoshima and Amura formations on eastern
Kamishima Island was assigned to the Santonian to middle Campanian, and strata of western
Shimoshima Island to the Campanian to Maastrichtian on the basis of rich bivalve andammonoid records. In the past few years, many vertebrate fossils, including dinosaurs, were
newly discovered from the lower to middle Campanian strata of Shimokoshikishima Islandand Maastrichtian strata of Kamikoshikishima Island. However, there exists no report aboutplant fossils from these strata and the paleovegetation still remains unclear. Recently, wellpreserved palynomorphs were recovered from the Mitsuse Formation in Nagasaki area, whichis stratigraphically equivalent to the Himenoura Group of Shimoshima Island.
We report here for the first time palyno-assemblages of the Himenoura Group,
obtained from the Koshikishima Islands and the Amakusa Archipelago, and propose
paleovegetation and paleoenvironment reconstructions for these areas. We could identify
spores with affinities to the Bryophyta (Marchantiaceae), Lycophyta (Selaginellaceae,
Lycopodiaceae) and Monilophyta (dominated by Cyatheaceae, Osmundaceae, Anemiaceae).
Concerning Gymnosperm pollen, grains with affinities to the Coniferales (Cheirolepidiaceae,
Podocarpaceae, Pinaceae) were most diversified. Some Angiosperm pollen of genera
Liliacidites (Liliales) and Aquilapollenites were observed from Koshikishima Islands, andScollardia was also obtained from the Amakusa Archipelago, among others. It represents thefirst report of index genera Scollardia and Aquilapollenites in South Japan. Scollardia
trapaformis obtained from the Amura Formation has been previously reported only from theMaastrichtian of Canada, Sakhalin and China, and the present report from middle Campanianstrata thus becomes the first occurrence of the species. Composition of the assemblage
indicates a vegetation including a mangrove, with similar environmental conditions as the
Mitsuse Formation. Moreover, Normapolles pollen was previously obtained from the later,
and the presence of Aquilapollenites in the Koshikishima Islands permits to discuss about
the geographical distribution and limit of these two provinces.

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Vertebrate remains from the Early Cretaceous fluvial deposits of Phu
Wiang Valley, Khon Kaen Province, Northeastern Thailand
Kamonlak Wongko1, Phornphen Chanthasit2 and Chompoonoot Chanwicha1
1

Phu Wiang Fossil Research center and Dinosaur Museum, Department of Mineral Resources, Khonkaen, Thailand.
2
Sirindhorn Museum, Department of Mineral Resources, Kalasin, Thailand.

Abstract
Remains of dinosaurs and other vertebrates including sharks, bony fish, turtle,
crocodilians and footprints were reported from the Sao Khua Formation and Phra Wihan
Formation of Phu Wiang Valley, Khon Kaen Province in northeastern Thailand. These twoformations of the Khorat Group are Early Cretaceous continental deposit. Most of dinosaurbones and teeth are found in reddish siltstone and sandstone from crevasse splay and flood
plain deposits of a low-energy meandering river system. The most prominent dinosaur fossils
discovered at Phu Wiang valley is a new species of a sauropod dinosaur later named as
Phuwiangosaurus sirindhornae after the name of Her Royal Highness Princess Maha Chakri
Sirindhorn who pay a great attention in the dinosaur research. Moreover, Thai and Frenchpaleontologists erected other three new dinosaur species comprising of a large theropod
Siamotyrannus isanensis together with a spinosaurid, Siamosaurus suteethorni and an
ostrich-mimic dinosaur, Kinnareemimus khonkaenensis. Due to low-energy current, thepreservation of dinosaur bones and teeth, notably the partial skeleton of a Phuwiangosaurus
is particularly good. The other vertebrate fossils transported under high energy condition anddeposited in the low- energy current are fragmentary. The presence of caliche pebble
conglomerate indicates arid – semiaridity in subtropic climate.
Keyword: Vertebrate remains; Cretaceous; Phu Wiang Valley; Khon Kaen Province;
Thailand86

Diversity of Mesozoic crocodiles in the northeastern Thailand
Komsorn Laupraserta and Jérémy MartinbaDepartment of Biology, Faculty of Sciences, Mahasarakham University, Mahasarakham, 44150,
Thailand.
b
Laboratoire de Géologie de Lyon: Terre, Planète, Environnement, UMR CNRS 5276 (CNRS, ENS,
Université Lyon1), Ecole Normale Supérieure de Lyon, 69364 Lyon cedex 07, France

Abstract
Three formations of the Khorat Plateau, northeastern Thailand, were investigatedand excavated the vertebrate fossils, including the Phu Kradung Formation which is dated
as Late Jurassic-Early Cretaceous; whereas the Sao Khua and Khok Kruat Formations aredated as Early Cretaceous (Racey et al., 1996; Carter & Bristow, 2003). All material were
described and compared with well-known specimens from the European and RussianMuseums to assess their taxonomic identification at the lowest possible level. The resultshows that the Phu Kradung Formation consists of three families: Pholidosauridae,“Chalawan thailandicus (Buffetaut and Ingavat 1980), Atoposauridae (based on the typicalteeth morphology) and Teleosauridae (based on a complete skull with mandibles). The
Sao Khua Formation also consists of two Families. The first one is Goniopholididae which
consist of two genera, i.e., “Goniopholis” phuwiengensis Buffetaut and Ingavat 1983 andSiamosuchus phuphokensis Lauprasert et al., 2007. The second family is Atoposauridae,
Theriosuchus gradinaris Lauprasert, et al., 2010. The youngest formation of the Khorat
Group, the Khok Kruat Formation comprises three families: Goniopholididae (KPS 1, fromthe Khorat Fossil Museum, Nakhon Ratchasima Province) and Atoposauridae (based onteeth morphology) from Ubon Ratchathani Province. Furthermore, this formation alsopresents a primitive neosuchian crocodile, Khoratosuchus jintasakulii Lauprasert et al.,2009 from Nakhon Ratchasima Province, which is considered as Family incertae sedis.
The crocodilian diversity of the Khorat Plateau is much more increasing from theprevious study from one family and two genera (before 2006) to five families and at least
six genera. The crocodile faunas from the Khorat Plateau are rather different from North
America, Europe and China which indicates that Thai crocodiles are mostly endemic
animals.
Keywords: Diversity, Mesozoic, Crocodilian, northeastern Thailand

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Academic Values of Mudeungsan UNESCO Global Geopark
Min HUH1,2,3, Yeon WOO2 & Jong-Sun KIM3
1

Faculty of Earth Systems and Environmental Sciences & Korea Dinosaur Research Center,
Chonnam National University, KOREA. minhuh@jnu.ac.kr
2
Green City Office, Gwangju Metropolitan City, Republic of KOREA. wy0923@korea.kr
3
Geoconvergence Research Center, Chonnam National University, KOREA. petrology@hanmail.net

Abstract
The Mudeungsan UNESCO Global Geopark is located in the southern part of the
Korean peninsula near the large regional city of Gwangju. Administration is shared between
Gwangju City and two counties of Jeollanam Province. The Mudeungsan UGG gets its namefrom Mount Mudeung which rises about 1,178 m above the lowlands. The core area of 75
km2 is within Mudeungsan National Park. In and around the area there are many villages
and cultural features closely connected to Mt Mudeung. Twenty geosites have been
identified in the 1,051 km2 mountainous UGG area. Seven geological periods are
represented. The geological sites range from five large colonnades of polygonally jointed
tuff columns recording at least three phases of Cretaceous volcanic activity, extensive
periglacially-produced block streams and cryoplanation surfaces, unusual microclimatic
environments within talus accumulations, very unique dinosaur footprints and trackways,
and a variety of other geological and geomorphological features such as lengthy scenic
cliff-lines and waterfalls. Among them, outstanding universal value sites are colunnadesof Mudeung Mt., Unjusa stratified tuff, Hwasun Dolmen site, Seoyuri dinosaur fossil site
and Climatic change in Quaternary
Moreover, one of the greatest features of the Mudeungsan Global Geopark is
its unique culture stemming from geological features. Unjusa temple (Unjusa stratifiedtuff), the UNESCO World heritage list, is well-developed tuff stratifications by the volcanic
activities of the Cretaceous era. The Buddha statues and pagodas in this temple were
subdivided into their own cultures by stratified tuff. The Hwasun Dolmen Site is supposedthat they used the giant rocks separated in layers and naturally weather-flowed along thesoil and built the dolmens in place. Chunghyodong clay mineral site is the place where
the porcelain which was called ‘Buncheongsagi’. This porcelain is highly related to thecharacteristics of the Mt. Mudeung’s soil. The soil for making ceramic material occur fromthe weathered soil in the adjacent area by applying the kaolin in the Mt. Mudeung.

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Among the various projects promoted in the Mudeungsan Glabal Geopark, thegeoeducation program is the most outstanding and interesting. The program is developed
to combine indoor and outdoor classes in conjunction with geosites.

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Dinosaurs, Birds and Pterosaurs of Korea: A Paradise of Mesozoic
Vertebrates
1

MIN HUH1 and JEONG YUL KIM2

Faculty of Earth Systems and Environmental Sciences & Korea Dinosaur Research Center,
Chonnam National University, Gwangju 61186, Republic of Korea<minhuh@jnu.ac.kr>
2
Department of Earth Science Education, Korea National University of Education, Cheongju 28173,
Republic of Korea

Abstract
Korea is one of the best known regions in the world for the Cretaceous vertebrate
ichnology. Abundance of diverse vertebrate tracks with very good quality of preservationand high density of occurrence of tracks and track-bearing stratigraphic beds in the
Cretaceous of Korea represent the Mesozoic paradise of vertebrates and the UNESCOWorld Heritage candidate and Global Geopark.
Bird tracks named in Korea are much more diverse than those of any othercountries in the world. The smallest theropod tracks (Minisauripus), raptor tracks with only
two digits impressions (Dromaeosauripus), new ornithopod tracks with three clover leafshape (Ornithpodichnus), a new ichnospecies of Brontopodus (B. pentadactylus), newquadrupedal ornithopod tracks (Caririchnium kyoungsookimi and C. yeongdongensis), thelargest pterosaur tracks (Haenamichnus gainensis), the second named bird tracks(Koreanaornis), the oldest web-footed bird tracks (Ignotornis yangi), and diverse dinosaur
eggshells including Macroelongatoolithus goseongensis, as well as new dinosaur bones(Koreanosaurus and Koreaceratops) first named in the Cretaceous of Korea have verysignificant scientific values for understanding the history of the Mesozoic vertebrates.
Several new dinosaur tracks recently named in Korea are as follows:
Hamanosauripus ungulates (Kim, 1986), Koreanosauripus cheongi (Kim, 1986), Brontopodus
ichnosp. (Lockley et al. 2006), Dromaeosauripus hamanensis (Kim et al. 2008), Minisauripus
zhenshounani (Lockley et al. 2008), Ornithopodichnus masanensis (Kim et al. 2009),
Brontopodus birdi (Kim et al. 2012), Ornithopodichnus (Lockley et al. 2012), Caririchnium
kyoungsookimi (Lim et al. 2012), Brontopodus pentadactylus (Kim and Lockley, 2012),
Dromaeosauripus jinjuensis (Kim et al. 2012), Caririchnium yeongdongensis (Kim et al.
2016). Several new dinosaur tracks recently named in Korea are also important for

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understanding gait, stance, and behavior of dinosaurs. They are Brontopodus
pentadactylus (Kim and Lockley, 2012), Caririchnium kyoungsookimi (Lim et al. 2012), C.
yeongdongensis (Kim et al. 2016), Dromaeosauripus hamanensis (Kim et al. 2008), D.
jinjuensis (Kim et al. 2012), Minisauripus (Kim et al. 2012), and Ornithopodichnus
masanensis (Kim et al. 2009).
How vertebrate tracks are abundant in Korea can be estimated on the basis ofcomparison of counting data of tracks and trackways, and tracksites. The world largest
tracksite in terms of exposed surface was the Upper Cretaceous dinosaur tracksite at Cal
Orckó of Bolivia. The tracksite was the most spectacular in the world exposing more than
5,000 tracks. However, unfortunately the track-bearing surface was collapsed in 2010.
Eleven tracksites of Spain and Portugal for nomination of the World Heritage inscription
contain about 13,640 tracks. Recent study showed that about 1,370 trackways and 14,280
tracks of dinosaurs have been reported from the Cretaceous at ~90 tracksites in Korea. It
was known that Spain has about 150 tracksites and High plains of eastern Colorado and
New Mexico have about 70 dinosaur tracksites. Therefore, Korea is a region with one of
the most abundant and highly dense occurrence of dinosaur tracks and trackways.
Compared with dinosaur tracks and eggshells, dinosaur bones have been rarely
reported from the Cretaceous of Korea. In this regard, a new basal ornithopod dinosaur
described as Koreanosaurus boseongnesis (Huh et al. 2010), the first ceratopsian dinosaur
described as Koreacertops hwaseongensis (Lee et al. 2011) and Pukyongosaurus
millenniumi (Dong et al. 2001) are paleontologically important.
The most diverse and abundant bird tracks from the Cretaceous of Korea areremarkable compared with those of any other countries. To date, there are 26 Cretaceous
avian ichnospecies assigned to 20 ichnogenera, if Archaeornithipus meijida andMagnoavipes lowei are interpreted as dinosaurian-like, and Moguiornis robusta,
Dongyangornis sinensis, Ignotornis gajinensis, Gyeongsangornis lockleyi and Paxavipes
babcockensis are included. Thus, six ichnogenera among the 20 ichnogenera of Cretaceous
avian tracks were formally named in Korea. They are Koreanaornis (Kim, 1969),
Jindongornipes (Lockley et al. 1992), Hwangsanipes (Yang et al. 1995), Uhangrichnus (Yanget al. 1995), Goseongornipes (Lockley et al. 2006) and Gyeongsangornipes (Kim et al. 2013).
Eight avian ichnospecies among 26 ichnospecies of Cretaceous were also named in Korea,
among which Ignotornis gajinenisis (Kim et al. 2012) are included. Therefore, about one
third of Cretaceous avian ichnogenera and ichnospecies has been formally named in

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Korea, which means the most diverse record in the world and much more diversity thanthose of any other countries. In this regard, the Gajin tracksite is notable. At the Gagin
tracksite, more than 2500 well-preserved bird tracks associated with theropod andsauropod tracks were recorded from the Early Cretaceous Haman Formation of the Gajinarea, Jinju, Korea. Bird tracks were described as Koreanaornis hamanensis, Goseongornipes
markjonesi, ? Aquatilavipes, and Ignotornis gajinensis which is a semi-palmate bird track
associated with arcuate to semi-circular, double-grooved impressions resulting fromspoonbill-like feeding behavior. The Gajin tracksite represents a record of the world’s
richest and most diverse Cretaceous bird assemblage, which was dubbed “A paradise of
Mesozoic birds”.
The record of pterosaur ichnotaxa named in eight countries in the world. Although
ichnotaxonomy of pterosaur tracks has been debated, three ichnogenera including
Haenamichnus, Pteraichnus, and Pubeckopus and nine ichnospecies are regarded to bevalid. Several Spanish ichnogenera and ichnospecies of pterosaurs as well as Pteraichnus
koreanensis (Lee et al. 2008) are regarded as invalid ichnotaxa. If we follow these,
Haenamichnus, one of three ichnogenera of pterosaurs, and Haenamichnus uhangriensis(Hwang et al. 2002) and H. gainensis (Kim et al. 2012), two of nine ichnospecies ofpterosaurs, have been named from the Cretaceous of Korea. To date, nine valid
ichnospecies belonging to three ichnogenera of pterosaur tracks have been known in theworld. They are Pteraichnus saltwashensis (Stokes, 1957), P. stokesi (Lockley et al. 1995),
P. longipodus (Fuentes Vidarte et al. 2004). P. parvus (Meijide Calvo et al. 2001), P.
nipponensis (Lee et al. 2010), P. palacieisaenzi (Pascual Arribas et al. 2015), Purbeckopus
pentadactylus (Wright et al. 1997), Haenamichnus uhangriensis (Hwang et al. 2002), and H.
gainensis (Kim et al. 2012). Therefore, two of nine pterosaur ichnospecies and one of threeichnogenera of pterosaur tracks were formally named in Korea. Especially, Haenamichnus
gainensis shows the longest trackway and it is the largest pterosaur tracks. In addition,
Haenamichnus gainensis is the only one pterosaur tracks attributable to bipedal, fully
erect, and digitgrade stance and gait. The other six ichnospecies have generally accepted
as having been made by quadrupedal, semi-erect, and plantigrade pterosaurs. Therefore,
Haenamichnus gainensis support Bennett (1990), who documented that at least somelarge pterodactyloids could have been primarily plantigrade bipeds.
Korean dinosaur eggs were named as Spheroolithus sp. (Huh and Zelenitsky, 2002),
Faveoloolithus sp. (Huh and Zelenitsky, 2002), Dictyoolithus neixiangensis (Kim et al. 2011),

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Macroelongatoolithus goseongensis (Kim et al. 2011) and Macroelongatoolithus xixiaensis(Huh et al. 2014). Dinosaur teeth also recognized as named Chiayüsaurus asianensis (Leeet al. 1997) and Chiayüsaurus sp. (Park et al. 2000), and turtle tracks (Chelonipus ichnosp.
Kim and Lockley, 2016) and mammaliform tracks (Koreasaltipes jinuensis Kim et al. 2017)
included. Especially, lizard skeleton (Asprosaurus bibongriensis Park et al. 2015) has very
important scientific valve related to dinosaur fossils in Korea and Asia.
Among the various projects promoted in the Mudeungsan Glabal Geopark, thegeoeducation program is the most outstanding and interesting. The program is developed
to combine indoor and outdoor classes in conjunction with geosites.

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Sedimentary Environments of the Lower Formations of theCretaceous Yeongyang Subbasin of the Gyeongsang Sedimentary
Basin in Bonghwa-gun, Gyeongsangbuk-do, Korea
Eun-Hye Kong and Daekyo Cheong
Department of Geology
Graduate School, Kangwon National University, Korea

Abstract
The Yeongyang Subbasin is separated from the Uiseong subbasin by the
Cheongsong Ridge, which is connected to the Andong Fault in the west, and is bounded
by a thrust in the north. The Myogog Formation is the lowest sedimentary sequence in
the Yeongyang Subbasin, which has been known as a post-Daedong Group and preGyeongsang Supergroup. This is an important stratigraphic unit connecting the Jurassic
Daedong Group to the Cretaceous Gyeongsang Supergroup The Myogog Formation is
distributed in a small wedge at the northwestern part of the Yeongyang Subbasin. The
entire outcrops were measured as detailed columnar sections and were described fromthe lower Myogog Formation to the Ullyeonsan Formation and Donghwachi Formation.
The sedimentary formations consists of five conglomerate facies, four sandstone facies,
two siltstone and a mudstone facies(Ccs : clast-supported, stratified conglomerate. Ccd :clast-supported, disorganized conglomerate. Cms : matrix-supported, stratified
conglomerate. Cmd : matrix-supported, disorganized conglomerate. tCmd : matrixsupported, disorganized tuffaceous conglomerate. Sgc : cross-stratified gravelly sandstone.
Sm : massive sandstone. St : trough cross-stratified sandstone. tSm : massive tuffaceous
sandstone. Ss : crudely stratified siltstone. Ml : laminated mudstone). The sedimentary
sequences can be grouped into six facies associations on the basis of constituent
sedimentary facies: swamp or lacustrine deposits(FA I: St-Ml / Sm-Ml), alluvial fan deposits
along a fault scarp(FA II: Cmd-Ccd), pyoclastic-rich debris flow deposits(FA III: tCmd, Cmd),
gravelly braided-stream deposits (FA IV: Cms-Ss /Cmd-Ss), sandy braided-stream
deposits(FA V: Sgc-Ss), pyoclastic-rich mud flow deposits (FA VI: tSm). The sedimentary
environment of the Mogog Formation was a swamp or lacustrine setting, and those of the
Ullyeonsan Formation and Donghwachi Formation evolved from an alluvial fan to a
braided stream nearby a very active volcano.

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Keywords : Yeongyang Subbasin, Myogog Formation, Ullyeonsan Formation,
Donghwachi Formation, facies, facies associations, swamp or lacustrine, alluvial fan,pyoclastic, debris flow, mud flow

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Radiolarian assemblage of Barremian to Aptian interval in the
Tethys and the influence of the oceanic anoxic event (OAE) 1a
Li Xina, Matsuoka Atsushib, Bertinelli Angelac, Chiari Marcod, and Wang ChengshaneaState Key Laboratory of Palaeobiology and Stratigraphy, Nanjing Institute of Geology andPalaeontology and Center for Excellence in Life and Paleoenvironment, Chinese Academy of
Sciences, Nanjing, 210008, China. xinli@nigpas.ac.cnbFaculty of Science, Niigata University, Niigata, 950-2181, Japanc
Dipartimento di Fisica e Geologia, Università degli Studi di Perugia, Via A. Pascoli snc,
Perugia, 06123, Italyd
C.N.R., Istituto di Geoscienze e Georisorse, Sezione di Firenze, via G. La Pira 4, Firenze, 50121, Italye
Department of Earth Science and Resources, China University of Geosciences, Beijing, 100083, China

Abstract
Comparison of radiolarian assemblages from marls in the Gorgo a Cerbara sectionin the Umbria–Marche Basin in central Italy and from a siliceous sequence (section BB1)
near Babazhadong in southern Tibet indicates similar faunas comparable to those in the
Aurisaturnalis carinatus Zone and the Turbocapsula costata Zone. Comparison with theGorgo a Cerbara section provides an accurate age constraint for the siliceous succession
in southern Tibet, which contains no fossils other than radiolarians. The siliceous
succession in section BB1 encompasses the Early Aptian Oceanic Anoxic Event 1a (OAE
1a). The Early Aptian OAE 1a is located in the upper part of the Aurisaturnalis carinatusperforatus subzone. The first occurrence biohorizon of the genus Turbocapsula and theevolutionary first appearance biohorizon of T. costata (Wu) multicostata Li & Matsuoka
are useful criteria for constraining the OAE 1a. Common species of these two zones inboth sections are: Stichomitra communis Squinabol, Hiscocapsa grutterinki (Tan Sin Hok),
Squinabollum asseni (Tan Sin Hok), Pseudoeucyrtis hanni (Tan Sin Hok), Mictyoditra
columbarium (Renz), Acastea sp., Suna sp., Archaeospongoprunum patricki Jud, andHalesium sp. Important and typical Early Cretaceous taxa, like Archaeodictyomitra
lacrimula (Foreman), A. excellens (Tan Sin Hok), Dictyomitra communis (Squinabol),
Pantanellium sp., and A. carinatus perforates Dumitrica and Dumitrica–Jud occurring inolder strata show their last occurrence after the OAE 1a.