Executives and Organizing Committee of the Fifth
International Symposium of IGCP 608
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 Fifth International Symposium of IGCP 608
Prof. Daekyo, Cheong
Department of Geology, Kangwon National University, Korea
Prof. Min Huh
The President of Geological Society of Korea
Department of Geology, Chunnam National University, Korea
Prof. Yongil Lee
Department of Geology, Seoul National University, Korea
Prof. Insung Paik
Department of Earth and Environmental Sciences, Pukyong National University, Korea
Prof. Hyoun Soo Lim
Department of Geology, Pusan National University, Korea
Prof. Taejin Choi
Department of Mineral Resources Engineering, Chosun University, Korea
Daewoo Kim (Secretary General)
Department of Geology, Kangwon National University, Korea- i -Sponsors
UNESCOThe Korean Federation of Science and Technology Societies
Kangwon National University
BK21 Plus Project of the Graduate School of Earth Environmental Hazard System,
Pukyong National University
INPEX Corporation Co., Ltd. (Japan)
Japan Petroleum Exploration Co., Ltd. (Japan)
JX Nippon Oil and Energy Corporation Co., Ltd. (Japan)
Mitsui Oil Exploration Co., Ltd. (Japan)
Mitsubishi Corporation Exploration Co., Ltd. (Japan)
Oyo Corporation Co., Ltd. (Japan)
DIA Consultants Co., Ltd. (Japan)
Chuo Kaihatsu Co., Ltd. (Japan)- ii -

Contents

1. Symposium Schedule ·
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3. Field Guidebook ·
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- iii -

Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Symposium Schedule

Symposium Schedule∙ Oral Session_IGCP 608※ The Plenary Session (09:10-09:55) is held together in the 7th presentation room.
※ The Closing Ceremony (18:00-18:10) is held together in the 7th presentation room.

October 26 (Tue)Plenary Session
09:00-09:10
09:10-09:35
09:35-09:55

Chairperson: Daekyo Cheong ❘ 7th presentation room (401)

Opening Ceremony & Group Photography
Dinosaur eggs and nests in South Korea and their contributions todinosaur research and conservation
Sequence stratigraphy and sedimentary history of the Upper Cretaceous Kuji Group:
forearc basin successions of fluvial to shallow-marine facies in north Honshu

Sedimentary Geology & Tectonics

Daekyo Cheong
Yuong-Nam Lee
Hisao Ando

Chairperson: Yong Il Lee ❘ 7th presentation room (401)

10:00-10:20

Marine elements in Lacustrine Intertrappean sediments of Deccan Flood
Basalt, India: Where did they come from?

Syeda Jafar

Stratigraphic constraints of Deccan volcano-sedimentary sequences,
their spatio-temporal correlation: implication for tracking terrestrial biotic
and environmental changes across K-Pg boundary in India

Dhananjay M. Mohabey

10:20-10:40
10:40-11:00

Coffee Break

11:00-11:20

U-Pb dating of zircons from gabbros of the Pujada Ophiolite, SE
Mindanao, Philippines

Valerie Shayne Olfindo

11:20-11:40

Well-preserved layered ultramafics in Palawan, Philippines: Implications
for the origin of the Palawan Ophiolite

Betchaida Payot

11:40-12:00

Petrography and geochemistry of Cretaceous sandstones in northeast
Catanduanes Island, Philippines: Implications for provenance and tectonic setting

Adrian RaymoundFernandez

12:00-13:20

Lunch

Chairperson: Kirillova Galina
13:20-13:40

Cretaceous tectono-stratigraphic systems of the sedimentary basinson the Russian southeastern continental margin

Kirillova Galina

13:40-14:00

Palaeoenvironmental and palaeoclimatic reconstruction of the Early
Cretaceous psittacosaur localities, Asia

Eugenia Bugdaeva

14:00-16:00

Poster & Coffee Break (Assembly of Geological Society of Korea)

Chairperson: Khien Nguyen Xuan
16:00-16:20

The Upper Cretaceous sediments in the Northwest of Vietnam: thedepositional paleoenvironments

Khien Nguyen Xuan

Shallow-water deposits and paleolandscapes on northwestern marginof Western Siberia at the Jurassic-Cretaceous boundary: data from theMaurynya section

Boris Shurygin

16:20-16:40
16:40-17:00

Balochisaurus malkani and Marisaurus jeffibalochisaurid titanosaurs ofPakistan: A review

M. Sadiq Malkani

Palynofloral changes in Late Cretaceous- Early Paleocene Deccan
volcanic associated sediments of Chhindwara area in Mandla lobe:
implications in assessing age and volcanism induced environmental changes

Deepali D. Thakre

17:00-17:20

3

Symposium Schedule
October 26 (Tue)
17:20-17:40
17:40-18:00

Correlation of palynofloras in the Tetori Province and consequences forthe angiosperm invasion in East Asia
Dinosaur Nesting Site of Salbardi-Ghorpend area, Betul District, Madhya
Pradesh, India: a unique Maastrichtian Megaloolithus oospecies

Plenary Session
18:00-18:10

10:20-10:40
10:40-11:00
11:00-11:20
11:20-11:40
11:40-12:00
12:00-13:20

Prabhakar Lakra

Chairperson: Daekyo Cheong ❘ 7th presentation room (401)

Closing Ceremony
Introduction : 6 th Symposium of 2018 IGCP 608 in Thailand by Mr. Naramase

Paleontology
10:00-10:20

Julien LegrandChairperson: Sunil Bajpai ❘ 8th presentation room (402B)

Dinosaur ecology and climate in Eastern Siberia during the Late
Cretaceous inferred from stable isotopes
Dinosaur Footprint Assemblage at the site Huai Dam Chum from the Lower
retaceous Khok Kruat Formation, Khorat Group, Northeastern Thailand

Romain Amiot
Shohei Kozu

Coffee BreakA review of new data on the belemnite family Cylindroteuthididae andbiostratigraphy of the Berriasian in Eurasia and North America
Diversity, extinction and evolutionary trend of palynoflora across CretaceousPaleogene in Deccan volcanic associated sediments of India

Oksana S. Dzyuba

Theropod dinosaurs and mesoeucrocodiles from Pakistan: A review

M. Sadiq Malkani

Bandana Samant

Lunch

Chairperson: Oksana S. Dzyuba
13:20-13:40
13:40-14:00
14:00-16:00

Calcareous nannofossil biostratigraphy of the Cretaceous Yop Formationin Catanduanes Island, Philippines
Microfossils along Kinabuan Creek, Sta. Ines, Tanay, Rizal Province,
Philippines: evidence of Cretaceous-Tertiary boundary

Mirko Alessandro C. UY
Maybellyn A. Zepeda

Poster & Coffee Break (Assembly of Geological Society of Korea)

Chairperson: Allan Gil Fernando
16:00-16:20

Tarbagatay dinosaur locality: flora, environments, and geological age

Eugenia Bugdaeva

New palynological data from infratrappean beds of Deccan Volcanic
Province, central Peninsular India: implications for late Cretaceous
paleogeography and early history of angiosperm diversification

Sunil Bajpai

16:20-16:40
16:40-17:00

Fossil liverworts from the Early Cretaceous in Inner Mongolia, China

Sun Bainian

Fossil vertebrate assemblages from the Late Cretaceous of Iwate
Prefecture, Japan
Palaeontological, Palaeoecological and Palaeobiogeographical studiesof the Cretaceous inter and infra-trappeans around Naskal, Gowripatnamand Devarapalli areas of Southern India - It’s significance in deciphering
the Cretaceous Ecosystem of Asia
New Progress in the study on the Cretaceous Micropalaeontology inSouthern Tibet, China

Ren Hirayama

17:00-17:20

17:20-17:40

17:40-18:00

4

Nidhi Misra

Guobiao Li

Symposium Schedule∙ Poster Session_IGCP 608

October 26 (Tue)1What is the origin of unusually long ‘Mega Cracks’ found in the Hasandong
Formation of the Cretaceous Gyeongsang Supergroup, Korea?

Shin Seung Won

2

Complex analysis of Early Cretaceous macrobenthos and palynomorphs
from southeastern margin of Western Siberia (Vostok-4 Well section)

Boris Shurygin

3

Lower Cretaceous Spore-Pollen from Brown Coal Deposit, Erdenetsogt
Govi, Southeast Mongolia

Ichinnorov Niiden

4

New ornithopod footprints from the Lower Cretaceous Kitadani Formation,
Fukui, Japan: Ichnotaxonomical implications

Yuta Tsukiji

5

Giant pterosaur remains from the upper-most Cretaceous in the Mongolian
Gobi Desert and their paleoecological implications

Takanobu Tsuihiji

6

Late Campanian-Early Maastrichtian megafossils from the Nakaminato
Group (central Honshu, Japan): an example of NW Pacific heteromorph
dominated ammonite fauna

Genya Masukawa

7

Quantification of skeletal pneumaticity in the pterosaur Anhanguera
piscator and comparison with the avian condition

Meg Wakui

8

Age of the Upper Cretaceous Himenoura Group on the KoshikishimaIslands, Kagoshima, Japan

Miyake Yuka

9

Clay mineralogy of the intertrapean beds near Dhar district of MP:
Implications for Cretaceous Paleogene paleoclimate

Neha Upreti

10

New Progress in the study on the Palaeogene Micropalaeontology inSouthern Tibet, China

Wenyuan Zhang

11

Non-marine Turga biota of the West-Urulunguy intermontane Basin(Transbaikal)

Nataliya Yadrishchenskaya

12

Preliminary report of Cretaceous radiolarite as raw material for stone tools
in the Zagros Mountains, Iran

Kenichiro Hisada

13

Updates on ongoing paleontological studies of Cretaceous units in thePhilippines

Allan Gil S. Fernando

14

Preliminary study on the provenance of the Cretaceous Neungju Basin,
Korea

Kwon Min Gyu

15

A review of Pakisaurustitanosaur: Associated skeletons of sauropod andtheropod dinosaurs and mesoeucrocodiles from Pakistan: Discussion ontitanosaurs of Indo-Pak subcontinent

M. Sadiq Malkani

5Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Symposium Sessions

Plenary Session

Keynote Speech 1

Dinosaur eggs and nests in South Korea and their contributions
to dinosaur research and conservation
Yuong-Nam Lee
School of Earth and Environmental Sciences, Seoul National University, Korea
ynlee@snu.ac.kr

It is notable that the high diversity and abundance of Korean dinosaurs are better represented by eggs and footprints
rather than skeletons. Since the first discovery of dinosaur eggshells in 1972, twelve dinosaur egg sites have beenreported in Korea. The temporal range of these egg-bearing formations is 50 million years from the Early Cretaceous(Aptian) to the Late Cretaceous (Campanian). They are located in Hwaseong, Buyeo, Buan, Mokpo, Gurye, Hadong,
Boseong, Sacheon, Goseong, Tongyoung, Busan, and Bongwha. Most of them are not yet well studied but a total of
577 dinosaur eggs with 90 clutches represent six different oofamilies. The size distribution of the eggs is extreme andthe egg shape is diverse as well. An egg nest found in the Mokpo City contains the largest eggs (Macroelongatoolithus)
ever found in South Korea which are average 41.17 cm long and 15.58 cm wide. On the other hand, a new oospecies ofPreprismatoolthusfound in the Wido Island is average 5.9 cm long and 4.2 cm wide. The Boseong and Hwaseong
dinosaur egg sites are the most important among all egg sites because they promoted educational facilities and dinosaur
research in Korea. The Boseong dinosaur egg site paved the way to build the Boseong Dinosaur Park whereas the
Hwaseong dinosaur egg site initiated a dinosaur research center. Moreover, two Korean dinosaur taxa (Koreanosaurus
boseongensisand Koreaceratops hwaseongensis) are associated with these two egg sites. Both were designated as the
National Monument and are protected by the law. Especially the Hwaseong egg site presents the first dinosaur colonial
nest ground in Asia. Over 200 dinosaur eggs with 29 clutches have been found in ten different egg horizons, showingsite fidelity.

9Plenary Session

Keynote Speech 2

Sequence stratigraphy and sedimentary history of the Upper Cretaceous
Kuji Group: forearc basin successions of fluvial to shallow-marine facies
in north Honshu✳

Hisao ANDO1, ․ Shunsuke MITSUZUKA2 ․ Ren HIRAYAMA3
1

Department of Earth Sciences, Faculty of Science, Ibaraki University, Mito, Japan
2
Graduate School in Science and Engineering, Ibaraki University, Mito, Japan(present: Shizuoka Office, Nagoya Branch, Nippon Koei, Co. Ltd., Shizuoka, Japan)
3
School of International Liberal Studies, Waseda University, Tokyo, Japanhisao.ando.sci@vc.ibaraki.ac.jp

The Upper Cretaceous Kuji Group distributed along the Pacific coast, north Honshu, represents the western
marginal siliciclastic deposits of the Paleo-Japan forearc basin. It records fluvial to shallow-marine sedimentary
successions 300 to 400 m thick, reflecting relative sea-level changes during Turonian to early Campanian．It also
shows the stratigraphical and geographical facies changes, depending upon developing history of the depositional
systems The Kuji Group unconformably covers the Jurassic accretionary complexes and the intruding early Cretaceous
granite basement, and is lithostratigraphically divided into three Tamagawa, Kunitan and Sawayama formations inascending order.
A total of 26 depositional facies are recognized on the basis of lithology, sedimentary structure and occurring fossils.
In terms of their stacking patterns, they are grouped into 7 facies associations 1) alluvial fan, 2) gravelly braid river, 3)
sandy meandering river, 4) inner bay-estuary, 5) upper shoreface, 6) lower shoreface and 7) inner shelf. Furthermore,judging from their stratigraphical and geographical distributions and their bounding surfaces, five depositionalsequences (DS1-DS5) can be recognized. Though DS5 is composed only of LST (Lowstand Systems Tract), other four
include LST, TST (Transgressive) and HST (Highstand). Considering the estimated chronostratigraphic ranges, these
are regarded as third-order sequences. TST1 of DS1 and TST4-HST4 of DS4 comprise four and six repetitiveparasequences (/fourth-order sequences), respectively, characterized by upward-coarsening/shallowing facies successions.
During early DS1 talus and dry lowland deposits unconformably covered the basement granite only in thesouthwestern part. Afterward, four transgressive fine sandy parasequences comprise thick TST1 of inner bay-estuary
facies associated with thick, large-sized Crassostreareef beds in the southwestern area.
In DS2, sandy and partly gravelly meandering river facies (LST2) and inner bay-estuary facies (TST2) are thick,compared with the overlying thin shoreface facies (HST2).
During DS3 stage, after thick facies of gravelly braid river and gravelly alluvial fan filled an incised valley in the
middle area, inner bay-estuary facies (TST3) were wide distributed over the whole area. In the northwestern area, smallcolonies of another ostreid bivalves Konbostrea konbowere developed within closed intertidal zone. Bone beds bearing

10Plenary Session

abundant non-marine turtles, crocodiles, and shark teeth, as well as some dinosaurs and other vertebrates are found intide-influenced back marsh facies, and has been excavated for this several years (Hirayama et al., 2010; Sato et al., 2012).
Due to the next long-ranging sea-level rise, thick TST4 and HST4 of DS4 were formed over the whole area.
Shallow marine facies constitute four and two parasequences of TST4 and HST4, respectively. The boundary between
TST4 and HST4 is regarded as a maximum flooding surface (MxFS), because inner shelf sandy siltstone facies are
dominant around the boundary horizon. These six parasequences can be lithostratigraphically easily assigned as theshallow marine Kunitan Formation, relatively offshore facies within the Kuji Group.
After a sea-level fall following HST4, LST5 of DS5 was formed as fluvial plain facies of meandering river distributed
over the whole area.
Paleocurrent directions measured mainly cross-stratification within sandstone and conglomerate, are generally
dominated by SW to NE, possibly reflecting fluvial down flows and shoreface rip currents, etc. Consideringanti-clockwise rotation of several tens degree by large sinistral strike-slip fault movements in Northeast Japan, orNortheast Japan plate motion during Miocene Japan Sea opening, paleogeography of the Kuji local basin ischaracterized a N-S trending and gently westward arcuate coastline, westerly hinterland with several easterly flowing
river systems and easterly wave-dominated shallow shelf. This paleogeographic configuration is generally concordant
with the paleogeographic reconstruction of paleo-Japan continental arc-trench system carried out by Ando (2003) andAndo and Takahashi (2017).
Therefore, the Kuji Group was deposited along the transitional area from paleo-Eurasina continent to paleo-Pacific,
composed of gravelly to sandy river, sand-dominated inner bay-estuary, and storm-dominated shallow shelf systems. It wasformed through five relative sea-level changes controlled by local tectonics and eustasy. As the group contains several
faunal and floral elements such as molluscs (ammonite and bivalves), vertebrate fragments (dinosaur, turtle, pterosaur,etc.), amber, plant leaves, pollen and spore, it is very important to reveal the Late Cretaceous ecosystems in East Asia.
References
ANDO, H., 2013, Stratigraphic correlation of Upper Cretaceous to Paleocene forearc basin sediments in Northeast
Japan: cyclic sedimentation and basin evolution. Journal of Asian Earth Science, 21 (8), 919-933.
ANDO, H. and TAKAHASHI, M., 2017, Reconstruction of the Cretaceous Paleo-Japan continental arc-trenchsystem reconsidered from Cretaceous geologic records in the Japanese Islands. Fossils (The PalaeontologicalSociety of Japan), 102.
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 City, Iwate Prefecture,northeastern Japan. Journal of Fossil Research, 42 (2), 74-82, Fossil Research Society of Japan.
SATO, T., Konishi, T., HIRAYAMA, R. and CALDWELL, M.W., 2012,A review of the Upper Cretaceous marine
reptiles from Japan. Cretaceous Research, 37, 319-340.

11

Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Oral Session● Presentation: 15 minutes● Discussion: 5 minutes

Oral Session

Sedimentary Geology & Tectonics 1

Marine elements in Lacustrine Intertrappean sediments of Deccan Flood
Basalt, India: Where did they come from?
Syed A. Jafar1,2
1

National Centre for Antarctic and Ocean Research, Headland Sada, Vasco-da-Gama, Goa 403804, India
2
Flat 5-B, Whispering Meadows, Haralur Road, Bangalore 560102, India
syeda_jafar@yahoo.com

Massive thermal anomalies in the mantle (= superplumes) over Réunion hot spot led to the outpouring ofvoluminous magma during a short period (ca.3Ma) straddling K/Pg boundary in India. Such Sub-aerial Large Igneous2

Province (LIP) covered over 500,000 Km area and attracted global attention for exquisite preservation of biota
straddling K/Pg boundary and their role in inducing Climate Change allegedly causing Mass Extinction. The First
phase of massive Lava and Gas emissions started at about 67.4 Ma (Magnetic Chron C30N - Late Maastrichtian); theSecond phase started ca. 200-100 Ka before K/Pg Boundary (Magnetic Chron C29R - Latest Maastrichtian) andcontributed about 80% of the entire Deccan Basalt eruptions; the Third and the final phase of eruption commenced in
Basal Danian (Magnetic Chron C29R) and may have lasted up to Magnetic Chron C28N, the K/Pg boundary lying
within Magnetic Chron C29R (Mohabey and Samant, 2016). During quiescent phases of eruptions, the Deccan Flood
Basalt terrain permitted the flourishing of endemic and adapted marine clade fauna and flora in Terrestrial/ Palustrian /Lacustrine and Marshy regions (Fig.1) and preserved in Intertrappean beds in an essentially Athallasic-ephemeral
Lakes and Ponds (Deckker,1981).
Ever since Hislop discovered fossil of mangrove plant Nypain intertrappeans of Central India 150 years ago,suggesting marine incursion via Krishna-Godavari lineament, subsequent researchers supported this uncritically andused phrases like: “Marine Influence”, “Marine Elements”, “Estuarine” and “Brackish”. Although observations werelargely correct, the interpretations were grossly erroneous as no sedimentologic-geologic evidence could be provided
for any deep entry of sea from coastal regions lying about 800 Km away (Jafar 2016a, b). It must be understood thatancient Lakes and Ponds possess all geomorphologic features of a “Miniature Sea” and are considered as evolutionary
hot spot promoting large number of endemic biota including a few well adapted coastal marine biota. However, theexact seeding mechanism bringing in clades of marine elements into fluvio-lacustrine set up continues to be rather
elusive (Patterson et al. 1997). Some of the fossil floral elements of marine coastal region are: Rhizophora(Wood),
Sonneratia (Wood), Barringtonia (Wood), Nypa (Fruit, root, leaves and pollen), Cocos (fruits, wood, pollen),Vivacorpon, Acrostichum (Root, stem, etc.) besides marine algae Pyssonnelia, Distichoplaxand Peridinoid
dinoflagellates. The Deccan Intertrappean bed (14 m) discovered in Jhilmili of Central India is somewhat unique in

15

Oral Session

containing a thin horizon (60 cm) with an assemblage of diminutive sized planktonic foraminifera of basal Danian (P1aZone) and the prospects of finding a similar horizon seembright in future. Other fossil fauna suggesting“Brackish-Marine” influence are the two Ostracodes: common Neocyprideis raoiand rare Buntoniasp. Noteworthy isthe absence of Calcareous Nannofossils and Benthic Foraminifera, which are otherwise present in coastal marine
intertrappean beds of Rajahmundry (Khosla, 2015). The presence of Calcareous Nannofossils assemblage is a key for
determining

marinesea

incursion.

Integrated

biostratigraphy/sedimentology/Mineralogy/magnetostratigraphy/chemostratigraphy was used to identify 5 distinct
lithounits and to erroneously speculate on marine incursion emanating along Narmada-Son lineament (Keller, 2009).
The term “Brackish” signifies

Fig.1. Schematic diagram depicting Ancient Lake biotic zones: Terrestrial-Palustrine-Marshy /Emergent-Floating-Submerged Plants and Open Water Body. Lake would contain Main Channel flow with several
Lateral flowing streams and Delta/Beach/Alluvial Fan and Fibrous Clay Mineral Palygorskiteat Lake margins during
Low Water Level. Benthic Zone contains sparse biota as evidenced by Ichnofossils.

Water that is somewhat salty but less salty than sea Water and does not imply marine / estuarine condition unlesssupported by sedimentologic-geologic data. Unit 3 containing planktonic foraminifera of basal Danian age displaying
spike of fibrous clay mineral Palygorskite, which can be formed at low water level of a Lake and does not suggest
marine condition (Colson et al.1998). Jhilmili intertrappeans can be interpreted to have been deposited in a typicalephemeral-athalassic fluvio-lacustrine system with enhanced salinity permitting flourishing of a few ancestral marine
clade adapting to non-marine conditions for a short spell (Schön and Martens,2004; Cristescu et al. 2010).
Songliao basin in northeast China is one of the largest Oil bearing continental deposit of Late Coniacian to16Oral Session

Santonian age. Like Jhilmili, the possibility of a sea incursion in this basin has been debated for about 40 years (Xi etal. 2011). “Brackish” water Fishes, Bivalves, Dinoflagellates, Calcareous Nannofossils and both Benthic and
Planktonic Foraminifera were documented in support of possible marine incursion. Calcareous Nannofossils
documented by Xi et al. (2016) are inorganic micritic carbonate crystals without any true Coccoliths, hence deserve tobe ignored. Other marine elements, especially dinoflagellates are common to abundant in fluvio-lacustrine deposits
including extremely rare monospecific bloom of coccolith in the world (Liu and Wang, 2013, Annenkova et al. 2015,
Smokotina, 2016). A similar case is known from Miocene of Colombia / Peru citing abundant Ammonia, Trochammina
and Elphidiumand dinocysts including mangrove pollen. The site is located 2000 Km inland from Caribbean portal and1000 Km from Atlantic coast. Favourable conditions in fluvio-lacustrine set up trigger the adaptation of most marine
derived lineages for a brief period in Amazonia without marine incursion (Boonstra et al. 2015). We might, therefore,
conclude that there are compelling evidences to suggest that certain marine clades could be adapted for a short spell in
fluvio-lacustrine wetland without any sea incursion. Also, it seems absurd to assume that Deccan volcanism andChicxulub impact induced environmental changes could have caused alleged global Mass Extinction at K/Pg boundary.
Keywords: Marine incursion, Marine biota, Fluvio-lacustrine intertrappeans, Deccan Flood Basalt.
References
Annenkova, N. V., Hansen, G., Moestrup, Ø and Rengefors, K. (2015): Recent radiation in a marine and freshwater
dinoflagellate species flock. The ISME Journal, 9, 1821-1834.
Boonstra, M., Ramos, M.I.F., et al. (2015): Marine connections of Amazonia: Evidence from foraminifera anddinoflagellate cyst (Early Middle Miocene, Colombia / Peru). Palaeogeog. Palaeoclimatol. Palaeoecolog. 417,
176-194.
Colson, J. et al. (1998): A hydrogeological model for Palygorskite formation in the Danian continental Facies of theProvence Basin (France). Clay Minerals, 33, 333-347.
Cristescu, M.E., et al. (2010): Ancient lakes revisited: from the ecology to the genetics of speciation. Molecular
Ecology, 19, 4837-4851.
Deckker, P.D. (1981): Ostracodes of athalassic saline lakes. Hydrobiol. 81, 131-144.
Jafar, S. A. (2016a): Terminal Maastrichtian-Danian marine incursion in Central India: Myth or reality? 4th.
International Symposium of IGCP Project 608, Short Papers, Novosibirsk, 43-45.
Jafar, S. A. (2016b): Episodes of subaerial Large Igneous Provinces (LIPs) linked to late Turonian / late
Maastrichtian deep incursion of sea on the Indian continental block. Global Geology, 19(4), 255-260, 276.
Keller, G., Adatte, T., et al.(2009): K-T transition in Deccan Traps and intertrappean beds in Central India mark17

Oral Session

major marine seaway across India. Earth and Planetary Science Letters, 282,10-23.
Khosla, A. (2015): Palaeoenvironmental, Palaeoecological and Palaeobiogeographical implications of mixed fresh
water and brackish marine assemblages from the Cretaceous-Palaeogene Deccan intertrappean beds at Jhilmili,
Chindwara District, Central India. Revista Mexicana de Cienciás Geológicas, 32(2), 344-357.
Liu, C and Wang, P. (2013): The role of algal blooms in the formation of lacustrine petroleum source rocks Evidence from Jiang depression, Bohai Gulf Rift Basin, eastern China. Palaeogeog. Palaeoclimatolog.
Palaeoecolog., 388, 15-22.
Mohabey, D. M. and Samant, B. (2016): Assessing effects of Deccan volcanism on biota and environments ofnon-marine Maastrichtian-Palaeogene sediments of Central India. The 4th International Symposium of IGCP
Project 608, Short Papers, Novosibirsk, 62-63.
Patterson, R. T., McKillop, W. B. et al. (1997): Evidence for rapid avian-mediated foraminiferal colonization of
Lake Winnipegosis, Manitoba, during Holocene Hypsithermal. J. Palaeolimnology, 18, 131-143.
Schön, I. and Martens, K. (2004): Adaptive, pre-adaptive and non-adaptive components of radiations in ancient
Lakes: a review. Organisms Diversity & Evolution Science Direct, Elsevier, 4(3), 137-156.
Smokotina, I. V. (2016): Upper Cretaceous Palynology (spores, pollen and dinoflagellate cysts) of theYakovlevyskaya-2 borehole, Ust-Yenisei region. The 4th International Symposium of IGCP Project 608, Short
Papers, 33-36.
Xi, D. P., Wan, X. et al. (2011): Discovery of Late Cretaceous foraminifera in the Songliao Basin: Evidence fromSK-1 and implications for identifying seawater incursions. Chinese Science Bulletin, 56(3), 253-256.
Xi, D., Cao, W. et al. (2016): Late Cretaceous marine fossils and sea water incursion events in the Songliao Basin,
NE China. Cret. Res., 62, 172-182.

18

Oral Session

Sedimentary Geology & Tectonics 2

Stratigraphic constraints of Deccan volcano-sedimentary sequences,
their spatio-temporal correlation: implication for tracking terrestrial biotic
and environmental changes across K-Pg boundary in India✳

Dhananjay M. Mohabey ․ Samant Bandana
Department of Geology, RTM Nagpur University, Law College Campus, Amravati Road, Nagpur-440001, India
dinomohabey@yahoo.com

Deccan volcanic province though one of the best studied large igneous provinces but still the knowledge generated
is under critical review. The terrestrial Maastrichtian-Palaeogene sediments associated with Deccan volcanism are
represented by the sediments representing ground-zero conditions, designated as 'infratrappean' (Lameta Fm)
depositing in different inland basins just before the advent of volcanism in the province and the interflow or'intertrappean' sediments deposited during the pause in the volcanic eruptions. The sediments are under investigationfor over last one and half century for study of biota, depositional environments and more in context to Late Cretaceous
palaeobiogeography of Indian subcontinent. Sediments associated with Deccan Volcanic Province (DVP) of central andwestern India has a long history of yielding dinosaur fossils, mammals and such as the first evidence of modern grasses
including rice in the Cretaceous and a snake that preyed upon hatchling dinosaurs.
Presently covering over 500,000 km2 the Deccan flood basalts are mainly exposed in central and western Indiain
geographically separated locales designated as Western Deccan Volcanic province (WDVP), Central Deccan Volcanic
province (CDVP), Eastern Deccan Volcanic province (EDVP) that includes Mandla Lobe and the Northern Deccan
Volcanic province (NDVP) of Malwa Plateau occurring to the north of Narmada River. There are in addition important
Deccan volcanic sequences of Kutch and Saurashtra Plateau in western India where the sequences are associated withmarked presence of alkaline and acidic flows. The stratigraphic completeness and temporal resolution of the volcanic
sequences in these provinces is currently not understood well. Each of these provinces has its own history of eruptions
and having separate sites and source of eruptions. So far the chronostratigraphic study mostly remained confined to
WDVP which lack any associated sedimentary excepting the Palaeocene intertrappean beds of Mumbai. Based on
chemostratigraphy the 3,000+ m succession of basalt flows of Sahyadri Group in the Western Ghats has been divided
into 11 formations. This chemostratigraphy was also attempted to be applied to the other provinces for possible
temporal correlation. However, it is observed that this is not tenable as the similar geochemical analogues appear atdifferent geomagnetic chrons in different provinces. Also the chronostratigraphic constraints of WDVP could not beapplied to the localities in the other provinces associated with multiple Maastrichtian-Palaeogene sedimentary beds.
The volcanic flows of the provinces other than the WDVP are associated with well developed multiple sedimentary

19Oral Session

and bole beds/palaeosols at different stratigraphic levels and offer opportunity for tracking biotic and abiotic changes.
However, it is unfortunate that chronostratigraphic studes in these provinces have been either lacking or very limited.
So far conducted palaeontological investigations on intertrappean sediments have been able to provide information
only in the taxonomic (coarse), environmental and palaeobogeographic context. But it has inadequate
chronostratigraphic and stratigraphic control on the horizons targeted for sampling. It gives a long check-list of faunaand flora but without any temporal constraint. It is important that any study for tracking biotic changes - is within thedefined time-frame with stratigraphic constraint. In this context we investigated over 150 localities in a number of fieldtransects in CDVP in Yaotmal sector (Sahyadri Group), EDVP including N-D basin (Sahyadri Group) and Mandla lobe
(Amarkantak Group); and NDVP (Malwa Group). The studies mainly focussed reptilian tetrapods, palynomorphs andenvironmental interpretations. We targeted study and sampling of intertrappean at different stratigraphic levels within
the DVS having well-established volcani-stratgraphy established by Geological Survey of India based on flow-to-flow
mapping (1:50,000 scale) of the lava piles. The studies were supplemented with limited palaomagnetic study mainly of
the lava flows bracketing the intertrappean at different levels- that provided chronostraphic constraint for intertrappean
sediments and associated lava flows. This clubbed with observed palynofloral changes/events at different stratigraphic
levels provided important tool for establishing temporal relationship of geographically separated lava flows andassociated interflow sedimentary beds in Deccan volcanic provinces (Mohabey and Samant, 2013; Samant andMohabey, 2016).
Based on chronostratigraphic constraints mainly in lava piles of Western Ghats in WDVP it is presently considered
to have spanned 68-62 Ma (Duncan and Pyle, 1988; Sheth and Pande, 2014). Knight et al, (2003), Baksi, (2005) and
Chenet, et al. (2008). It was suggested that Deccan eruptions were episodic in nature primarily in three phases of
eruptions with the earliest phase between 67-68 Ma, followed by the second and also the main phase of volcanism in
the Maastrichtian C29R and the third and the last phase in the early Paleocene C29R/C29N transition. Recently
Schoene et al. (2014) on the basis of U-Pb Zircon geochronology from the Decccan volcanic sequence of western Indiaof Maharashtra have indicated that the bulk of magma eruption has taken place in 750,000 years through the K-Pg
boundary which caused latest Cretaceous environmental changes resulting in the biotic turnover. Renne et al. 2015
based on the study in Western Ghat suggested that at least 70% of the total volume erupted post K-Pg after Chicxulub
impact. However, our current studies suggest that the different Deccan volcanic provinces having their own sites andsource of eruptions have different timing of their eruptions and durations. The chronostratographic constraints of
WDVP cannot be strictly applied to the other provinces. Our recent study in the eastern part of the CDVP (Samant andMohabey, 2016) in over 500m thick volcanic sequence of Sahyadri Group comprising 35 lava flows in
Yavatmal-Wardha sector, suggested that lava flows erupted through C30N (Maasthichtian) to at least C28R of
Palaeocene. Also the current study of lava flows exposed between 520m to 870m RL of Amarkantak Group (Thakre et20Oral Session

al. 2017) in Chhindawara sector of EDVP suggests main phase of eruptions as post K-Pg with the volcanism spanningmagnetochron C30N to C28R. Schobel et al. (2014) based on the transects in southern and western margin of the
Malwa Plateau suggested that volcanism was initiated in C30N thorough C29N. The unpublished study by Geological
Survey of India of over 700m thick (46 flows) Malwa Group and our ongoing investigation suggest that basal most pileof 18 lava flows exposed between 216m to 335m RL erupted in C30N. The intertrapppean are present only in thislower lava piles at least at seven stratigraphic levels and the upper flows are almost devoid of any associatedintertrappeaan. Our study suggests that main phase of eruptions are temporarily separated within the magnetochroan
C30N Maastrichian to C28N Palaeogene in different Deccan volcanic provinces.
References
Baksi, A. K., 2005. Comment on 40Ar/39Ar dating of Rajahmundry Traps, eastern India and their relations to the
Deccan Traps by Knight et al (Earth Planet Sci. Lett. 208 (2003) 85-99. Earth Planetary Science Letters 239,
368-373.
Chenet, A, L., Fluteau, F., Coutrillot, V., Gerard, M., Subbarao, K.V., 2008. Determination of rapid Deccan eruption
across the KTB using paleomagnetic secular variation: (I) Results from 1200 m thick section in the
Mahabaleshwar escarpment. Journal Geophysical Research 113, B04101.
Duncan, R. A., Pyle, D. B., 1988. Rapid eruption of the Deccan flood basalt at the Cretaceous/ Tertiary boundary.
Nature 333, 841-843
Jay, A. E., Widdowson, M., 2008. Stratigraphy, structure and volcanology of the SE Deccan continental flood basalt
province: implications for eruptive extent and volumes. Journal. Geological Society of London 165, 177-188.
Keller, K., Adatte, T., Bajpai, S., Mohabey, D. M., Widdowson, M., Khosla, A., Sharma, R., Khosla, S. C., Gertsch,
B., Fleitmann, D., Sahni, B., 2009. K-T transition in Deccan Traps of central India major marine Seaway acrossIndia. Earth Planetary Science Letters 282,10-23.
Knight, K. B., Renne, P. R., Halkett, A., 2003. White, N., 39Ar/40Ar dating of Rajahmundry traps, eastern India andtheir relationship to the Deccan traps. Earth Planetary Science Letters 208, 85-99
Mohabey, D.M. and Samant, B., 2013. Deccan continental flood basalt eruptions terminated Indian dinosaursbefore
Cretaceous-Paleogene boundary. Geological Society of India Special Publication 1, 260-267.
Renne, P.R. , Courtney J. Sprain, Mark A. Richards, Stephen Self, Loÿc Vanderkluysen, Kanchan Pande. 2015.
State shift in Deccan volcanism at the Cretaceous-Paleogene boundary, possibly induced by impact. Science,
350 (6256), 76-78.
Samant, B. and Mohabey, D.M., 2016. Tracking temporal palynoloral changes close to Cretaceous-Palaeogene
boundary in Deccan volcanic associated sediments of eastern part of Cenral Deccan Volcanic Province. Global

21Oral Session

Geology, 19 (4), 205-215.
Schoene, B., Samperton, K.M., Eddy, M.P., Keller, G., Adatte., T., Bowring, S.A., Khadri, S.F.R., Gertsch, B., 2014.
U-Th geochronology of the Deccan Traps and relation to the end-Cretaceous Mass extinction. Science Express,
aaa0118, 223-253.
Sheth, H.C. and Kanchan Pande., 2014. Geological and 40Ar/39Ar age constraints on late-stage Deccan rhyolitic
volcanism, inter-volcanic sedimentation, and the Panvel flexure from the Dongri area, Mumbai. Asian Journalof Earth Sciences 84, 167-175.
Thakre, Deepali, Bandana Samant, D.M.Mohabey, Satish Sangode, Pankaj Srivastava, D.K.Kapgate, Rasika
Mahajan, Neha Upreti and Steven R. Manchester. 2017. A new insight into age and environments ofintertrappean beds of Mohgaon Kalan, Chhindwara District, Madhya Pradesh using palynology, megaflora,magnetostratigraphy and clay mineralogy. Current Science. 112(10), 2193-2197.

22

Oral Session

Sedimentary Geology & Tectonics 3

U-Pb dating of zircons from gabbros of the Pujada Ophiolite, SE Mindanao, Philippines✳

Valerie Shayne V. Olfindo 1, ․ Betchaida D. Payot1 ․ Kenichiro Tani2
1

Rushurgent Working Group, National Institute of Geological Sciences, University of the Philippines-Diliman,
Quezon City, Philippines
2
Department of Geology and Paleontology, National Museum of Nature and Science, Tsukuba-shi, Ibaraki, Japanvalolfindo@nigs.upd.edu.phIntroduction
The Pujada Ophiolite is one of the least studied ophiolitic complex in the Philippines. Located at the southeasternmost tip of the Philippines, the Pujada Ophiolite is believed to be the northernmost extension of the Molluca Sea
Collision Complex (Hamilton, 1979; Bader et al., 1999). However, its origin and geologic evolution is not yet wellconstrained due to lacking detailed petrographic, geochemical and geochronologic data. In this study, the radiometricages of the Pujada Ophiolite is reported for the first time using Laser Ablation Inductively Coupled Plasma Mass
Spectrometry (LA-ICPMS) U-Pb dating of zircons from the gabbroic section of the ophiolite.
Methodology
Six samples of gabbros from different localities were processed for U-Pb dating. The gabbros were fragmented into
individual mineral grains using the high voltage pulsed power selective fragmentation device (Selfrag-Lab) housed at
the National Museum of Nature and Science in Tsukuba, Japan. Traditional panning using a glass disk was done toconcentrate and separate heavier minerals such as zircon (SG= 4.7). Magnetic separation using the Neomag 8000 thenremoved magnetic minerals such as magnetite from the panned fractions. Heavy liquid separation using diiodomethane(Ch2I2) further isolated zircons from lighter minerals. Upon checking under the microscope with a UV light, threesamples yielded zircons (Figure 1). The zircons were mounted together with the standards TEMORA 2 (417 Ma; Blacket al., 2004), FC-1 (1099.9 Ma; Paces and Miller, 1993) and OD3 (33 Ma; Iwano et al., 2013). Cathodoluminescentimages were generated using a scanning electron microscope (SEM). U-Pb-Th isotope analysis was conducted using an
Electro Scientific Industries NWR213 laser ablation inductively coupled plasma mass spectrometry system and Agilent
Technologies 7700x Quadrupole ICP-MS. Data processing and reduction was adapted from Tsutsumi et al., 2012.
Results
The separated zircons are generally colorless to yellowish and are anhedral in shape. Most zircons obtained werefrom sample 04A. Cathodoluminescense imaging show weak zoning of the zircons (Figure 1). A few of the zircon

23Oral Session

grains are also highly fractured. The Th/U ratios of the analyzed spots were generally greater than 0.1 which indicatesa magmatic origin. The concordia plots show clustering of concordant ages at about 90 Ma (Figure 2). Sample 04A
showed tight cluster of ages with a weighted mean ²⁰⁷Pb-corrected ²⁰⁶Pb/²³⁸U age of 89.7 ± 2.0 Ma at the 95%
confidence level. The other two samples; 03 and 02B have the following mean ages respectively; 89.6 ± 6.7 and 90.6 ±4.2 Ma. The secondary standards (FC-1 and OD3) analyzed during the session were also consistent with theirpreviously reported ages and thus imply high accuracy of the ages determined for the three unknown samples.
Conclusion
U-Pb dating of the zircons from the gabbros of the Pujada Ophiolite using LA-ICPMS shows an accurate age of 90
Ma (Late Cretaceous, Cenomanian). The zircon U-Pb ages obtained from the gabbros of Pujada Ophiolite is older than
the reported age of the ophiolite based on radiolarian chert. his age may be correlated with other ophiolitic rocks within
the Molucca Sea Collision Complex which may help in constraining the origin of the Pujada Ophiolite.
References
Bader, A.G., Pubellier, M., Rangin, C., Deplus, C. and Louat, R., 1999. Active slivering of oceanic crust along the
Molucca ridge (Indonesia-Philippines): Implication for ophiolite incorporation in a subduction wedge. Tectonics
18 (4), 606-620.
Black, L.P., Kamo, S.L., Allen, C.M., davis, D.W., Aleinikoff, J.N., Valley, J.W., Mundil, R., Campbell, I.H.,
Korsch, R.J., Williams, I.S., Foudoulis, C., 2004. Improved 205Pb/238U microprobe geochronology by themonitoring of a trace element related
matrix effect; SHRIMP, ID-TIMS, ELA-ICP-MS and oxygen isotope documentation for a series of zircon standards.
Chemical Geology 205, 115-140.
Hamilton, W.B., 1979. Tectonics of the Indonesian region. United Stated Geological Survey Professional Paper
1078, 345.
Iwano, H., Orihashi, Y., Hirata, T., Ogasawara, M., Danhara, T., Horie, K., Hasebe, N., Sueoka, S., Tamura, A.,
Hasayaka, Y., Katsube, A., Ito, H., Tani, K., Kimura, J., Chang, Q., Kouchi, Y., Haruta, Y., Yamamoto, K.,
2013. An inter-laboratory evaluation of OD-3 zircon for use as a secondary U-Pb dating standard. The Island
Arc 22, 382-394.
Paces, J.B., Miller, J.D., 1993. Precise U-Pb age of Duluth Complex and related mafic intrusions, northern
Minnesota: geochronological insights to physical, petrogenetic, paleomagnetic, and tectonomagmatic processes
associated with the 1.1 Ga midcontinent rift system. Journal of Geophysical Research 98, 13997-14013.
Tsutsumi, Y., Horie, K., Sano, T., Miyawaki, R., Momma, K., Matsubara, S., Shigeoka, M., Yokoyama, K., 2012.

24

Oral Session

LA-ICP-MS and SHRIMP ages of zircons in chevkinite and monazite tuffs from the Boso Peninsula, Central
Japan. Bulletin of National Museum of Nature and Science 38, 15-32.

Fig. 1. Cathodoluminescent images of chosen analysis points. The zircons are generally anhedral with weak zoning.

Fig. 2. Concordia diagram for sample 04A. The weighted mean
was obtained at 95% confidence interval.

207

Pb-corrected

207

238

Pb/ U age of 89.7 ± 2.0 Ma

25

Oral Session

Sedimentary Geology & Tectonics 4

Well-preserved layered ultramafics in Palawan, Philippines: Implications
for the origin of the Palawan Ophiolite✳

Betchaida D. Payot ․ Jeanne Myrtia M. Macalalad ․ Gabriel Theophilus V. Valera ․Juan Miguel R. Guotana ․ Valerie Shayne V. Olfindo
National Institute of Geological Sciences, University of the Philippines-Diliman, Quezon City, Philippines
bdpayot@up.edu.ph, bdpayot@gmail.com

Introduction
Palawan and its neighboring islands bear the imprints of the arc-continent collision between the Philippine Mobile
Belt and the North Palawan Block. The Palawan island is roughly divided by the north-south trending Ulugan Bay
Fault into a continental northern block, and an oceanic central and southern block (Hamilton, 1979). The latter isdominantly comprised of lithologies belonging to the Palawan Ophiolite. The Palawan Ophiolite is composed of pillow
basalts, gabbros and ultramafic rocks dominantly exposed in central Palawan and near the vicinity of the Ulugan Bay
Fault (Raschka et al., 1985; Claveria and Fischer, 1991; Encarnacion et al., 1995). Paleontological dating of the pelagic
sediments intercalated with the pillow basalts indicate a Late Cretaceous age for the Palawan Ophiolite (Wolfart et al.,1986). The Palawan Ophiolite was emplaced during the Late Oligocene (~23 Ma; Aurelio et al., 2014).
Despite the numerous works conducted in Palawan, detailed petrological study of the lower crust and mantle
sections of the Palawan Ophiolite remains to be conducted. Our recent field mapping in Palawan revealed theoccurrence of an extensive and well-preserved sequence of layered ultramafics along the west coast of central Palawan.
As far as we know, this is the first report of the occurrence of the said lithologies in Palawan. The exposure iscomposed of olivine and pyroxene-rich lithologies including dunite, clinopyroxenites and websterites. The layers range
from 2 cm to 2 m in thickness and generally dip towards the NE.
Methodology
Samples representative of the different layers were collected. Thin sections were prepared and analyzed using apetrographic microscope. Point counting of at least 2000 grains was conducted to determine the modal abundances ofminerals comprising the rocks. The thin sections were then carbon coated using a Cressington carbon coater andanalyzed by a JEOL electron microprobe (JEOL JXA 8230) using the following analytical conditions: 15 kV
acceleration voltage, 20 nA beam current with beam diameter of 12-15 microns.

26Oral Session

Results
The layered ultramafics are composed of dunite, olivine websterite, clinopyroxenite and gabbronorite. The partly
serpentinized dunites are mainly composed of olivine and spinel with minor pyroxenes. The olivine websterite,
clinopyroxenite and gabbronorite show mesocumulate to adcumulate textures and are dominantly composed ofclinopyroxene, orthopyroxene and minor olivine (Figure 1). Plagioclase occurs as an interstitial phase only in thegabbronorite. Olivine and pyroxenes are the main cumulus phases and formed prior to the plagioclase. This
crystallization sequence is typical of an island arc setting (Debari and Coleman, 1989).
The olivine in the dunite shows high forsterite (=85-88) and low NiO wt% (<0.25 wt%). Spinel in the dunite havehigh Cr# (=0.55-0.65) and low TiO2 (<0.1 wt%). Both the clinopyroxene and orthopyroxene in the dunite, olivine
websterite and clinopyroxenite show high Mg# (88-93 for clinopyroxene; 85-88 for orthopyroxene) with Al2O3 content
below 2 wt %. Plagioclases in the gabbronorite have high An content (>An90) while the pyroxenes show slightly lower
Mg# (76-81 for clinopyroxene; 73-74 for orthopyroxene). These geochemical characteristics further imply an island
arc origin (Debari and Coleman, 1989; Arai, 1994; Greene et al., 2006).
Conclusion
Our initial data suggest that the layered ultramafics in western Palawan are cumulates possibly formed at the base of
an island arc. The crystallization sequence indicates suppression of plagioclase fractionation which is typical in an
island arc setting. The petrological characteristics of the layered ultramafics indicate an island arc origin. Furthermore,these also affirmthatthePalawanOphiolitewasgeneratedatasupra-subductionzone.
References
Aurelio, M.A., Forbes, M.T., Taguibao, K.J.L., Savella, R.B., Bacud, J.A., Franke, D., Pubellier, M., Savva, D.,
Meresse, F., Steuer, S., Carranza, C.D., 2014. Middle to Late Cenozoic tectonic events in south and central
Palawan (Philippines) and their implications to the evolution of the south-eastern margin of the South China
Sea: Evidence from onshore structural and offshore seismic data. Marine and Petroleum Geology 58, 658-673.
Claveria, R.J.R., Fischer, H.H., 1991. Characterization of the chromitite pods and lenses associated with the Ulugan
Bay peridotites, Palawan, Philippines. Journal of the Geological Society of the Philippines 46, 21-34.
Debari, S.M., Coleman, R.G., 1989. Examination of the deep levels of an island arc: Evidence from the Tonsina
ultramafic-mafic assemblage, Tonsina, Alaska. Journal of Geophysical Research 94, 4373-4391.
Encarnacion, J.P., Essene, E.J., Mukasa, S.B., Hall, C.B., 1995. High-pressure and temperature subophioltic
kyanite-garnet amphibolites generated during initiation of mid-tertiary subduction, Palawan, Philippines.
Journal of Petrology 36, 1481-1503.

27

Oral Session

Greene, A.R., Debari, S.M., Kelemen, P.B., Blusztajn, J., Clift, P.D., 2006. A detailed geochemical study of island
arc crust: the Talkeetna arc section, south-central Alaska. Journal of Petrology 47, 1051-1093.
Hamilton, W., 1979. Tectonics of the Indonesian Region. U.S. Geological Survey Prof. Paper 1078, 9, 338 pp.
Raschka, H., Nicario, E., Rammlmair, D., Samonte, C., Steiner, L., 1985. Geology of the ophiolite of central
Palawan island, Philippines. Ofioliti 10, 375-390.
Wolfart, R., Cepek, P., Graman, F., Kemper, E., Porth, H., 1986. Stratigraphy of Palawan island, Philippines.
Newslett. Stratigr. 16, 19e48.

Fig. 1. A-B) Mesocumulate texture in olivine websterite with pyroxene and olivine as the main cumulus phases.
A = plane polarized light, B = crossed polars.

28

Oral Session

Sedimentary Geology & Tectonics 5

Petrography and geochemistry of Cretaceous sandstones in northeast
Catanduanes Island, Philippines: Implications for provenance and tectonic setting✳

Adrian Raymund C. Fernandez1,2, ․ Allan Gil S. Fernando2 ․ Mirko Alessandro C. Uy2
1Partido State University, Goa, 4422 Camarines Sur
Nannoworks Laboratory, National Institute of Geological Sciences, University of the Philippines, Diliman, 1011 Quezon City
fernandez.adong@yahoo.com

2

Sandstone petrography, in conjunction with other sedimentological techniques, is an invaluable tool in basin
analysis and tectonic setting characterization because of the close correlation between the sandstone’s opticalcharacteristics (i.e., mineralogy and texture) and depositional setting/environment. The island of Catanduanes issituated offshore of southeast Luzon, Philippines, and is considered part of the Eastern Luzon Metamorphic Belt
(Karig, 1983). Geologic mapping done in 2014 by the Geology 215 (Advanced Field Geology) Class of the National
Institute of Geological Sciences, University of the Philippines (UP-NIGS) revealed the presence of previously
undocumented middle Cretaceous units in the northeast part of the island, consisting of limestones and interbedded
shales and sandstones. Fernando et al. (2016) suggested the possible association of middle Cretaceous units to the
Cenomanian-Turonian oceanic anoxic event (OAE2) based on lithology and calcareous nannofossil assemblages.
For the present study, fine- to coarse-grained sandstones will be investigated. Preliminary analysis suggests that thesandstones have low carbonate content and contains abundant lithic fragments. This study attempts to investigate themineralogical and textural variations, carbonate content and major oxide geochemistry of the sandstones. The possible
implications of the data to the provenance, tectonic setting, paleoceanography, as well as the geologic evolution of
Catanduanes Island during the Cretaceous will be discussed.
References
Fernando, A. G. S., Magtoto, C. Y., Guballa, J. D. S. and Peleo-Alampay, A. M., 2016. Calcareous nannofossils
from Cretaceous units in Catanduanes Island, Philippines. Bulletin of the National Museum of Nature and Science, Ser.
C., pp. 35-47.
Karig, D., 1983. Accreted Terranes in the Northern Part of the Philippine Archipelago. Tectonics, pp. 211-236.

29

Oral Session

Sedimentary Geology & Tectonics 6

Cretaceous tectono-stratigraphic systems of the sedimentary basinson the Russian southeastern continental margin
Kirillova G.L.
Yu.A. Kosygin Institute of Tectonics and Geophysics, Far East Branch, Russian Academy of Sciences, kirillova@itig.khb.ru

Tectono-stratgraphic systems (TSSs) approximate to megasequences. They characterize large stages of sedimentarybasins evolution and in general are separated by breaks or unconformities. Using TSS it is simpler and more logical todescribe the evolution of continental margins and sedimentary basins due to close stratigraphy-tectonics relations.
Cretaceous deposits usually occur conformably on Late Jurassic deposits. On he southeastern continental margin of
Russia within the troughs and uplifts of the Sikhote-Alin Foldbelt and Khanka Massif there are distinguished 10
structural-formational zones which differ in the composition of the deposits and section completeness (Fig.1). The
number of ESS is different in them (Fig.2). Breaks and unconformities of different duration are caused by major
geological events of regional and global scale.
The most complete Cretaceous sections are observed in the synclinal troughs of the Sikhote-Alin and Lower
Priamurye. On the Priokhotie continental margin, the Cretaceous TSSs accomplish the evolution of the Udaand Torombasins.
In the Amur-Zeya Basin, the Early Cretaceous represents a rift stage of the basin evolution, whereas the Late
Cretaceous reflects postrifting subsidence.
In summary, Cretaceous TSSs are present in a variety of basin types originated in different geodynamic conditions.
They are accretionary complexes and postaccretionary formations.

30Oral Session

Sedimentary Geology & Tectonics 7

Palaeoenvironmental and palaeoclimatic reconstruction of the Early
Cretaceous psittacosaur localities, Asia✳

E.V. Bugdaeva ․ V.S. Markevich ․ E.B. Volynets
Federal Scientific Center of the East Asia Terrestrial Biodiversity, Far Eastern Branch of Russian Academy of Sciences
bugdaeva@biosoil.ru

Psittacosaurus, whose name means "parrot lizard", is a genus of extinct ceratopsian dinosaurs, existed in the
mid-Cretaceous across Mongolia, Russia (Siberia), China, and possibly Thailand and Japan. Psittacosaurs wererelatively small in body size, ranging from one to two meters in body length. The psittacosaurs may also have had ahigh-fibre diet dominated by nuts and seeds, owing to the presence of many large stomach stones, according to thefindings (Sereno et al., 2010).
Shestakovo locality, Ilek Formation, Kiya River Basin
In Russia, the most numerous are burial places of psittacosaurus in the Kemerovo region in the locality near thevillage of Shestakovo. In the bone-bearing lens (its thickness is 60-70 cm) in the outcrop of the Ilek Formation on thebanks of the Kiya River, abundant remains of vertebrates Protosuchia (Tagarosuchus kulemziniAlifanov et al.),Lacertilia (Agamidae) and Ceratopsia (Psittacosaurus sibiricusVoronkevich and Averianov) were found.
During the post-symposium field excursion in 2016, E.B. Volynets selected samples for palynological analysis fromthe middle of the bone-bearing bed, as well as underlying gray sandstone. Their spectra are characterized by thesufficiently high taxonomic diversity. They are dominated by the bisaccate pollen close to Pinaceae (up to 35%). In thesecond position - spores of cyatheaceous and dicksoniaceous ferns (about 24%). They are accompanied by pollen
Ginkgocycadophytus (about 12%). The share of representatives of other groups of plants is rather low (about 5%),Cheirolepidiaceae is extremely rare.
The abundance of palynomorphs allowed us to draw conclusions about the geological age of sediments in thislocality. Such taxa as Taurocusporites reduncus, Osmundacidites wellmanii, Gleicheniidites senonicus, Pilosisporites
setiferusare characteristic of the Aptian palynofloras of Siberia and the Far East of Russia (Markevich, 1995,
Bolkhovitina, 1953, Verbitskaya, 1962). In the spectra there is no pollen of angiosperms, which suggests their
pre-Albian age. In the Albian palynofloras of the Northern Hemisphere, the flowering plants are an undoubtedlystablecomponent, although their number is usually small.

31Oral Session

Mogoito locality, Murtoy Formation, Gusinoozerskiy Basin
The Gusinoozerskiy Basin contains the sedimentary strata united into the Gusinoozyorskaya Group, which is
divided into Murtoy, Ubukun, Selenga, and Kholboldzhin formations (Skoblo et al., 2001). They overlay withstratigraphic unconformity the Upper Jurassic and older volcanic rocks.
Murtoy Formation consists mainly of conglomerates and sandstones. In the Mogoito localitythe remains of fossil
vertebrates (theropods, sauropods, ornithopods, and ceratopsians), as well as the abundant remains of limnetic fauna
occur (Skoblo et al., 2001; Nessov and Starkov, 1994; Averianov and Skutschas, 2009). The thickness of thisstratigraphic unit is 250-450 m.
The numerous remains of conifers Pityophyllumex gr. nordenskioldii (Heer) Nath. and Pityocladussp. were found.
The strobiles Scarburgia hilliiHarris are common in the burial with them. The horsetail stems, scale-leaved shoots
Cyparissidium gracileHeer and strobiles of conifers are rare. The flora of this formation also includes Coniopteris
onychioidesVassil. et K.-M., Cladophlebisaff. tongusorumPryn., Sphenopteris (Ruffordia)cf. goeppertii Dunk.,
Carpolithessp.
Palynological assemblage is dominated by Schizaeaceae (mainly Concavissimisporites), the share of the latter in thepollen spectra can reach 36%. A number of club-mosses is high, up to 24%. The percentage of cyatheaceous anddicksoniaceous ferns does not exceed 15%. Among gymnosperms the bisaccate pollen prevails (up to 36%); it isaccompanied by Ginkgocycadophytussp. (up to 18%). Only for palynological assemblage of this formation the pollenof unknown affinity, Pollenites sp., having elongated shape with longitudinal folds is characterized. Its amount may
reach 12% (Kotova, 1964).
Sihetun locality, Yixian Formation, Western Liaoning, China
The spore-pollen spectra were obtained from beds with findings of psittacosaurs, feathered dinosaurs, and birds at
the Sihetun locality (Li, Batten, 2007). In the palynological assemblage the gymnosperms dominate, mainly bisaccate
pollen (82.0-94.0%). Next in the significance is Ginkgocycadophytus(1.1% -10.8%). The content of spores of ferns
varies from 3.8 to 10.7%, their taxonomic composition is poor. Cyatheaceae, Schizaeaceae, Osmundaceae, and veryrare Gleicheniaceae were found. Pollen of angiosperms is not revealed. Li and Batten consider the age of strata at theSihetun locality "as Valanginian - Hauterivian or Barremian". According to our paleobotanical data, the age of the
Yixian Formation is the Barremian - Aptian (Bugdaeva, Markevich, 2012).
Conclusions
We palynologically characterized the beds with the remains of psittacosaurs occurred in the Shestakovo 3 locality(the Ilek Formation) and the Mogoito locality (Murtoy Formation).. A comparison with the palynospectra from the32

Oral Session

bone-bearing bed of the Sihetun locality (the Yixian Formation) has shown the similarity of their taxonomic
composition and the ratio of the main groups of plants. Every palynospectrum is dominated by bisaccate pollen having
affinity with Pinaceae, the next in importance - fern spores and monosulcate pollen Ginkgocycadophytus. Numerous
coniferous remains of plant megafossils have been found in the Murtoy Formation; the scale-leaved conifers arecommon, the ferns are rare. Based on our data, we can assume that the vegetation of habitats of psittacosaurs was
coniferous forests dominated by pine forests with a fern understory. A significant part of these forests were plants that
produced pollen Ginkgocycadophytus. These were not very highly productive forest ecosystems with small animals.
The age of the layers with the remains of psittacosaurs, in our opinion, is the Barremian-Aptian.. The climate, in all
likelihood, was warm (as evidenced by the existence of representatives of Araucariaceae) and moist (rather highparticipation of taxodialeans, club-mosses, and ferns). The lack of xerophytes, for example, gnetaleans andCheirolepidiaceae, may indicate the humid climate.
Acknowledgments
The authors are grateful 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, to N.K. Lebedeva(Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of the Russian Academy of Sciences) for a
discussion of the results of our work.. Our research was supported by Russian Foundation for Basic Research (grant17-04-01582).
References
Averianov, A.O., Skutschas, P.P., 2009. Additions to the Early Cretaceous Dinosaur Fauna of Transbaikalia, Eastern
Russia. Proc. Zoological Institute RAS, 313 (4), 363-378.
Bolkhovitina, N.A.,1953. Spore-pollen characteristic of the Cretaceous deposits of the central regions of U.S.S.R.
Proc. Institute of Geological Sciences AS of U.S.S.R 145 (61). Moscow: Izdatelstvo AS of U.S.S.R. [inRussian]Bugdaeva, E.V., Markevich, V.S., 2012. The age of Lycoptera beds (Jehol biota) in Transbaikalia (Russia) andcorrelation with Mongolia and China, in: Godefroit, P. (Ed.), Bernissart Dinosaurs and Early Cretaceous
Terrestrial Ecosystems. Indiana University Press, Bloomington, pp. 452-464.
The Dinosauria, 2004. /Eds.D.B. Weishampel, P. Dodson, H. Osmolska/ Berkeley and Los Angeles: University ofCalifornia Press.
Kotova, I.Z., 1964. The age of the continental deposits of the Gusinoozerskaya depression and features of the Early
Cretaceous floras of Transbaikalia. Izv. Akad. Nauk, Ser. Geol. (8), 84-93 [in Russian]33

Oral Session

Li, J.-G., Batten, D.J., 2007. Palynological evidence of an Early Cretaceous age for the Yixian
Formation at Sihetun, western Liaoning, China. Cretaceous Research, 28, 333-338.
Markevich, V.S., 1995. Cretaceous Palynoflora of the Northern East Asia. Vladivostok: Dalnauka. [in Russian]
Nessov, L.A., Starkov, A.I., 1992. The Cretaceous vertebrates from Gusinoozerskiy Basin of Transbaikalia and theirsignificance for age definition and conditions of formation of deposits. Geology and Geophysics (6), 10-18 [inRussian]
Sereno, P.C., Zhao X.J., Tan L., 2010. A new psittacosaur from Inner Mongolia and the parrot-like structure andfunction of the psittacosaur skull.. Proc. R. Soc. B, 277, 199-209.
Skoblo, V.M., Lyamina, N.A., Rudnev, A.F., Luzina, I.V., 2001. The Continental Upper Mesozoic of the Pribaikalia
and Transbaikalia (stratigraphy, depositional environments, correlation). Publishing House of the SB RAS,
Novosibirsk, [in Russian]Verbitskaya, Z.I., 1962. Palynological Evidence and Stratigraphical Subdivision of Cretaceous Deposits of the
Suchan Coal Basin, Moscow: Izdatelstvo AN SSSR. [in Russian]34

Oral Session

Sedimentary Geology & Tectonics 8

The UPPER Cretaceous Sediments in THE Northwest of Vietnam:
the depositional paleoenvironments✳

Nguyen Xuan Khien1, ․ NGUYEN THIMINHNGOC2
1

Vietnam Union of Geological Sciences (VUGS)
Faculty o fTechnology & Information Security, PSA. Hanoi
khien@vigmr.vn

2Stratigrapy
Stratigrafically, theUpperCretaceous sediments in the Northwest of Vietnam are described as the Yen Chau
Formation (K2yc) which stretches in the NW-SE direction and covers an area of about 250 km2 with thickness ranging
from 650 to 1400m. They are unconformably overlied Middle Triassic carbonate rocks of Dong Giao Formation or
Early Triassic terrigenous rocks ofCo Noi Formation. The complete cross-section have been described at Yenchau
basin, where they can be divided into 3 members:+) Member 1: basal conglomerate, with gravel aggregate mainly consisting of quartz, light browinish quartzitic
sandstone, carbonate and acidic/basic volcanic rocks, chert, cemented by reddish brown polymictic sandstone.
Sporadically the upper part of this member is seen with some interbeds of gravelstone or coarse-grained polymictic
sandstone. The thickness ranges from 30 to 65 m.
+) Member 2:polymictic sandstonewith some thin interbeds of oligomictic gravelstone and conglomeratewith
aggregate mainly consisting of quartz and chert, intercalated with reddish brown, thinly to moderately bedded silty
sandstone. The thickness of this member ranges from 70 to 115m.
+) Member 3: polymictic sandstoneintercalated with silty sandstone, thin mudstoneinterbeds, and reddish brown,
moderately to thick bedded claystone. At some places gypsumis found disseminated in finegrained sandstone, ormaking thin synsedimentation layers intercalated between layers of siltstone and claystone. The thickness ranges from
300 to 750 m.
Lithofacies Characteristics
Based on analyzing results of material composition and forming conditions,the Upper Cretaceous sediments in the
Northwest of Vietnam can be distinguished into the following main assemblages of lithofacies:
1. Assemblage of proluvial, proluvial-deluvial lithofacies, consisting mainly of breccia-conglomerate, gravel-bearing
conglomerate. The detritus poorly to moderately sorted andfraction consists mainly of massively structured, rounded
limestone, effusive rocks, quartz, quartzitic sandstone etc.,making from 60 to 75% of the rock mass. The rocks of thisgroup were formed during the early-forming stage of the sedimentary basin in the area.
2. Assemblage of fluviatile lithofacies, consisting of:+) Channel lithofaciescomposed mainly of poorly to moderately sorted, moderately to poorly rounded polymictic
gravelstone, with lenses of gravel-bearing coarse grained sandstone, at some places interbedded with sandstone and35

Oral Session

sandy siltstone of aluvial lithofacies. The main structure is unclear bedding and monoclinal cross-bedding.
+) Aluvial lithofaciescomposed mainly of medium to fine grained sandstone with horizontal ripple-mark bedding
structure or monoclinal cross-bedding, directly overlying the rocks of channel lithofacies.
3. Assemblage of lacustrine lithofaciescomposed of well rounded and wellsorted, fine grained sandstone, siltstone,
mudstone, gypsum. Their structure is gentle or nearly horizontal, with ripple-marks at some places.
Depositional Paleoenvironment
The results of paleoenvironmental studies show that Upper Cretaceous sediments in the northwestern part ofVietnam have been formed in the same hot and arid paleoenvironmental conditions, typically continental. The
following are some evidences:-The primary red, reddish brown, brownish red colors (red-beds) caused by the presence of hematite, goethite,limonite and lepidocrocite which are unevenly scattered in the sediments;-The presence of gypsium/anhydrite and salty trace. Gypsium/anhydrite exist in these sediments under 3 forms:+)Thin layers (thickness is ranging from 1 to 14cm), synsedimentation,+)Unevenly disseminated, authigenical existence in component of different rocks, such as claystones, silstones,
sandstones with content ranging from 3-5% to 10-15%, significantly to 30-35%,+)Secondary vein/nest type filled in rock fissure systems.
-The rare earth element (REE) content shows that ratio between Ce/La content is always <1.5 which is characterized
for rich of oxygen in continental environment (Wright et al.,1987).
- Many polygonal sand-filled shrinkage cracks have been found on the surface of claystone layers.
-The Cretaceous sediments are always very poor in organic material caused by dry and hot continental
paleoenvironment. The Pelecypod consist of species living in fresh and brackish water environment, such as
Hoffetrigonia kobayashi, Uniosp., Cardinioidessp.,..Plant fossils (Angiospermae, …) have leaf-shape with entire
margins which are typically for droughty climate.
Key-words: sediments, stratigraphy, lithofacies, ripple-mark, cross-bedding, paleoenvironment.
References
Andrew D. Miall, 2000. Principles of Sedimentary Basin Analysis. Springer.
Le Thanh Huu et al., 2004. Some characteristics of non-marine gypsum-bearing sediments in Yen Chau Formation.
The Geology and Minerals of Vietnam. The Northern Mapping Department, Gen. Dep. Geol. & Min. ofVietnam. Hanoi.
Nguyen Xuan Khien (ed.), 2003. Sedimentology and paleogeography of the Cretaceous-Jurassic red-beds andrelated mineral resources in North Vietnam. Dept. of Geology & Minerals of Vietnam. Hanoi, Vietnam.
Nguyen Xuan Khien, 2005. Stratigraphy of Cretaceous non-marine red-beds in the North Vietnam. Jour. The Earth
Sciences. Vietnam Acad. Sci. & Tech. Hanoi, Vietnam.

36

Oral Session

Sedimentary Geology & Tectonics 9

Shallow-water deposits and palaeolandscapes on northwestern marginof Western Siberia at the Jurassic-Cretaceous boundary: new datafrom the Maurynya section✳

B.N. Shurygin1,2, ․ O.S. Dzyuba1 ․ E.B. Pestchevitskaya1 ․ O.S. Urman1 ․ A.S. Alifirov1,2 ․ A.E .Igolnikov1,2 ․ I.N. Kosenko1,2
1

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Novosibirsk, Russia,
shuryginbn@ipgg.sbras.ru
2
Novosibirsk State University, Novosibirsk, Russia

In the foothills of the Northern and Subpolar Urals on northwestern margin of Western Siberia, theJurassic-Cretaceous boundary deposits are exposed in bank escarpments of the streams belonging to the Severnaya
Sosva River basin. The accumulation of these deposits occurred in a marginal area of the epicontinental West Siberianmarine basin in which the transgression reached its maximum extent during Volgian (Tithonian-earliest Berriasian)time (Kontorovich et al., 2013).
The Maurynya section located in the foothills of the Northern Urals is one of few continuous sections of theJurassic-Cretaceous boundary deposits in Boreal regions. Simultaneously, this section can be considered as a key
section for the Volgian-Ryazanian transition beds formed in a shallow coastal area of the West Siberian marine basin.
We studied the upper part of the Fedorovskii Formation (Volgian to lowermost Ryazanian siltstones and sandstones)
exposed on the MaurynyaRiver. These sedimentary rocks are highly fossiliferous, yielding ammonites, belemnites,
bivalves, gastropods, brachiopods and palynomorphs (Dzyuba et al., in press). The C, O, and Sr isotope data were also
reported from the Maurynya section (Dzyuba et al., 2013; Kuznetsov et al., in press). Both palaeontological andisotopic data indicate that the section embraces the Upper Volgian and lowermost Ryazanian. The Jurassic-Cretaceous
boundary beds at Maurynya have not yet received palaeomagnetic characteristics. This boundary is located within the
middle part of the Upper Volgian regional substage, and we provisionally place it at the base of the Simobelus
compactusbelemnite beds (age analogue of the East Siberian Arctoteuthis tehamaensisbelemnite Zone), between two
13

positive δ C excursions but closer to upper one (ShuryginandDzyuba,2015;Dzyubaetal.,inpress).
Palaeoenvironmental reconstructions were made on the basis of palaeoecological group analysis and calculation of18

palaeoecological group analysis and calculation of palaeotemperature from belemnite and oyster δ O. Ammonites andbelemnites are remains of stenohaline organisms, and their occurrence in sedimentary rocks outlines existence periodof a sea basin with normal salinity. Morphological characteristics of cephalopods are informative for seawater depth
reconstructions (Mesezhnikov and Shulgina, 1975; Zakharov et al., 2014). The benthos catena analysis was used forthe reconstruction of bottom relief and depth; the available palaeoecological classifications and synecological analysis

37Oral Sessionof recurring associations were applied (Zakharov and Shurygin, 1985). The diversity curves of different mollusc
groups (ammonites, belemnites, and bivalves) have been reconstructed. Within an orictocoenosis, we took into
consideration the type of burial (accumulation or isolated finds), the orientation of shells, and the degree of theirsorting and preservation.
Facies characteristics of certain taxa of spores, pollen, microphytoplankton and their groups as well as existing
concepts on ecology of terrestrial and marine palynomorphs were considered for the reconstruction ofpalaeoenvironments on palynological data (e.g., Abbink, 1998; Pestchevitskaya et al., 2012). The relative percentagesof terrestrial and marine palynomorphs and microphytoplankton taxa were calculated from the total quantity of
palynomorphs (spores, pollen and microphytoplankton).
The estimated palaeotemperatures clearly indicate a warming trend through the Late Volgian and earliest Ryazanian(Chetaites sibiricusammonite Zone), with a short cooling episode at the Volgian-Ryazanian boundary. The warming is
also confirmed by percentage relations of certain taxa in palynological associations. Warmer climate resulted in thechanges of forest vegetation, the gradual crowding out of conifers that led to the formation of the forests dominated byginkgoaleans.
Among Maurynyamolluscs the most distinct correlation between biodiversity dynamics and climatic events isobserved at belemnites. Belemnite diversity increased during warming and decreased during the cooling episodes.
Ammonites show a more or less similar diversity dynamics. A response of bivalve fauna to climate change wassomewhat slow, but influence of temperature on their diversity is also obvious.
The established connection between biodiversity dynamics and climate fluctuations does not abolish influence oftransgressive-regressive events on development of mollusc communities. The sharp increase in a diversity of
cephalopods and benthic groups is observed in the second half of the Late Volgian. This event occurred approximately
in the beginning of the Cretaceous and was related to warming and, as we suppose, to transgression. The optimal
conditions (both climatic and bathymetric) for development of numerous, ecologically and taxonomically diverse
communities of molluscs existed here up to the beginning of the Ryazanian.
The data obtained from the studied site allows us to suppose frequent sea-level fluctuations which as a wholeoccurred against the background of tendency of the Maurynya sea area to deepening since the beginning of theCretaceous. We suppose that the decrease of diversity of belemnites and macrobenthos by the beginning of the
Ryazanian Hectoroceras kochiPhase was accompanied by the further deepening of the sea area near Maurynya, but canbe related to a climate cooling or a palaeoenvironment destabilization in principle.
Transgressive-regressive dynamic of palaeobasin were also consistent with the changes of nearshore landscapes andvegetation types. The conditions during the lowstands of the palaeobasin were favorable for moisture loving plants,
which occupied wet and partly waterlogged lowland near the shore in the beginning of the Late Volgian. The forests

38Oral Session

mainly represented by conifers were also widespread in the inshore land areas. In warm period, conifers were graduallyreplaced by ginkgoaleans in the forest vegetation. The near shore lowland areas were submerged during the sea-level
rise in the Early Cretaceous. It brought about the formation of more elevated inshore landscape. These territories were
mostly occupied by gleicheniaceous ferns adapted to drier localities and slopes.
This is a contribution to the IGCP608 and the SB RAS Complex Programme “Integration and Development”.
References
Abbink, O.A., 1998. Palynological investigations in the Jurassic of the North Sea region. LPPFoundation, Utrecht.
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.,
in press. Maurynya as the key section of the Jurassic-Cretaceous boundary deposits of shallow marine genesis
in Western Siberia. Russ. Geol. Geophys.
Kontorovich, A.E., Kontorovich, V.A., Ryzhkova, S.V., Shurygin, B.N., Vakulenko, L.G., Gaideburova, E.A.,
Danilova, V.P., Kazanenkov, V.A., Kim, N.S., Kostyreva, E.A., Moskvin, V.I., Yan, P.A., 2013. Jurassic
paleogeography of the West Siberian sedimentary basin. Russ. Geol. Geophys.54, 747-779.
Kuznetsov, A.B., Izokh, O.P., Dzyuba, O.S., Shurygin, B.N., in press. Sr isotopiccompositionof belemnitesfromthe
Jurassic-Cretaceous boundary deposits (MaurynyaRiver, Western Siberia). Dokl. EarthSci.
Mesezhnikov, M.S., Shulgina, N.I., 1975. Ecology of Late Jurassic and Neocomian boreal ammonites, in: The
palaeobiology of bottom invertebrates of marine coastal zones. FESC AS USSR, Vladivostok, pp. 66-82 (InRussian).
Pestchevitskaya, E.B., Smokotina, I.V., Baykalova, G.E., 2012. Lower Valanginian palynostratigraphy of southeasternregions of Siberia, palaeoenvironment and vegetation reconstructions. J. Stratigr. 36(2), 179-193.
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.
Zakharov, V.A., Shurygin, B.N., 1985. Method of the reconstruction of bottom relief and depths of marine
palaeobasins based on the analysis of benthos catena, in: Environments and life in ancient epochs. Palaeobasins
and their fauna. Nauka, Novosibirsk, pp. 97-107 (In Russian).
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 the Jurassic/Cretaceous
boundary in the Arctic realm: case study of the Nordvik section (north Siberia, Russia). Polar Res. 33, 19714.

39

Oral Session

Sedimentary Geology & Tectonics 10

Balochisaurus malkaniand Marisaurus jeffibalochisaurid titanosaursof Pakistan: A review
M. Sadiq Malkani
Geological Survey of Pakistan, Muzaffarabad, Pakistan. malkanims@yahoo.com

Review of Balochisaurus malkani: Its holotype includes seven caudal vertebrae including first biconvex caudal
vertebra. Associated fossils collected from holotypic site (with fitness of size and no duplication) added here as
lectotype (Fig.1a). Lectotype include presacral and caudal vertebrae, a sternal, a humerus, manus bones, an ilia, a
femur, a tibia, a fibula, ribs and neural spines (Fig.1a). Some bones from Kinwa PDL 4, two mid caudal vertebrae, a
mid scapula and armor bone from South Basti Nala (South Zubra, north of Nala) Gambrak PDL 7, and a caudal
vertebra, stocky distal tibia, coracoid and ulna from Grut Gambrak PDL 9 (Fig.1a) are attributed based on the typicalcharacteristic of mid caudal centrum as overlap and nonoverlap provides more information for diagnosis andcomparison. Cervical ribsare broad v shape. Dorsalcentraare opisthocoelous, slightly broad to tall, long, pneumatic andhave long and deep pleurocoel with thick lip. No hyposphene-hypantrum articulation. Dorsal neural spine is short andnot bifid. Proximal bifurcated process of rib join to form one wide rib strip which is pneumatic but at the distal ends it
becomes compact and width is slightly reduced. Caudal centrais procoelous, heavy, compact (not pneumatic/
cancellous), forward insertion of robust neural arch, its ventral length is also less than dorsal length, and its dorsal area
is greater than ventral area i.e., ratio of mid transverse width in dorsal face to ventral transverse width of mid caudal
centrum is about 2 (more than 1.7). Distalmost caudal may be trispinous. Sternal anterolateral edge seems to be
maximum thick. There are rugosities on the anterior, anterolateral, anteromedial of anterior sternal plate. Mid scapula
is not deflected laterodorsally i. e., it is straight or slightly deflected medially showing less wide gauge locomotion(while the member of pakisaurids host laterodorsally deflected scapula which shows more wide gauge locomotions).
Humerusis expanded at proximal and distal ends. Some proximal portion is damaged however preserved width is 25cm
while distal ends width is 33cm. Proximal ulnais gracile, rugose and has a prominent olecranon process. The proximal
ulna represents a triradiate structure. Metacarpalsare elongated and triangular and have rugose articular proximal
surfaces. Distal condyle shape is undivided and has no articular rugosities. Partial acetabulum includes the glenoid.
Ventrally the acetabulum is long and oval and bears parallel ridges. The acetabulum forms the embayment for the
reception and movement of femur heads. Femurhas thick head. Length of femur seems to be about 1.5m. Proximal
femora seem to be beveled one third medially. Tibial condyle is relatively more deep than fibular condyle while thefibular condyle is relatively more wide than tibial condyle. Tibial condyle is wheel like. Femoral shaft is elliptical.

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Head rises more than greater trochanter and also more thick than greater trochanter. There is no notch in between thehead and greater trochanter. Tibiais stocky and broad with thick proximal surface and oval shape distal surfaces. The
midshaft is circular. Tibia cnemial crest projects laterally. Tibial distal posteroventral process is broad transversely.
Proximal fibulahas arc shape morphology with well marked depression or medial scar for attachments of tibia which is
deepening anteriorly.
Review of Marisaurus jeffi: Its holotype is six caudal vertebrae (including one biconvex sent for preparation toMichigan University; other vertebrae are shown Fig.1b). Associated fossils collected from holotypic site show fitnessof size and no overlap, so added here as lectotype. Lectotype include caudal vertebrae, a scapula, a pubis, a distal
ischium/pubis and a femur (Fig.1b). Many localities produced referred associated fossils of Marisaurusshow exactly
same character as holotypic caudals (Fig.1b) as overlap for proof of referral and non overlap or some new elements
reveals fuller diagnosis of almost complete anatomical elements of skeletal body for phylogenetic analyses. Presacral
centraare opisthocoelous, broad, long and pneumatic. Cervical ribsare broad v shape. Dorsal centraare opisthocoelous
and slightly broad. Centra show lateral pleurocoel with bone intrusion on back. Pleurocoel is deep and has equal height
and length. No hyposphene-hypantrum articulation. Sacral vertebrae are coossified, broad and pneumatic. Neural spine
is single i.e. not bifid. Caudal centraare procoelous, heavy, compact (not pneumatic/cancellous), forward insertion ofrobust neural spine. Chevron is simple i.e. not boat type. Midcaudals of Top Kinwa show exactly same character as
Marisaurusholotypic midcaudals i.e. ratio of mid dorsal transverse width to mid ventral transverse width is about 1.5(1.3-1.6). Partial sternal plate expanded and represents the anteroventral crest. Distal scapular bladeis expanded andrepresents broadening and thickening at the distal end. Distal scapula is straight or slightly deflected medially and also
not expanded in the lateroventral side of mid scapular blade, while the scapula of pakisaurid Pakisaurusis deflected
laterodorsally. Distal scapula and coracoid seems to be separate. Proximalulnais rugose and bears a prominent
olecranon process. Proximal ulna represents a triradiate structure. Ulna is gracile. Partial ileumrepresented byacetabulum along with large pubic peduncle condyle (broken) and short and laminar ischium peduncle. Ventrally theacetabulum is long and oval and bears parallel ridges indicating calcified tendons. Proximal pubisbears a large glenoid
surface for femur head. Anterior side of pubis is broad, cylindrical to sub oval, and posterior side is platy and possibly
sigmoid. Proximal pubis has a ventral ridge. Distal ischium or pubisis platy having thick articular ridge and rugosities
at terminal distal bones for its fellow attachement. Proximal femurshows medial deflection, distal femur shows
laterally beveled knee condyles and femur shaft show transverse elliptical eccentricity. Tibial condyle (wheel like) is
more deep than fibular condyle while the fibular condyle is more wide than tibial condyle. Length of femur seems tobe about 1.5m and width at distal condyles is about 33-35cm. Stocky tibiahas a broad and thick proximal surface, oval
shape distal surfaces and circular in mid cross section. Shape of fibular proximal tibial scar is well marked anddeepening anteriorly. Osteodermsare mosaic type flat plate. Manus and pes shape is also solved by bone fossils and41

Oral Session

ichnofossils (Fig.1b). collected almost complete manus shows unguals are lost. Oval shape of manus print of
Pashtosaurus zhobiindicates no any claw/ungual. Pes print of Pashtosaurus zhobiis three digit and toed (thick, wide,
subparallel, slightly diverging forward or slightly converging backward) which show reduction of 5 toes into 3 toes.
Central digit is forward inserted and lateral digits are backward inserted created internal concavity on posterior face.

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43Oral Session

Sedimentary Geology & Tectonics 11

Palynofloral changes in Late Cretaceous-Early Paleocene Deccan volcanic
associated sediments of Chhindwara area in Mandla lobe: implications inassessing age and volcanism induced environmental changes✳

Thakre D. ․ Samant B. ․ Mohabey D.M.
Department of Geology, RTM Nagpur university, Nagpur, Maharashtra, India, 440001
thakredeepali1@gmail.com

The Deccan Continental Flood Basalt, Province covers 500,000 km2 area in central, western and southern part ofIndia. It is divided into four main sub-provinces namely, Mandla and Malwa in the North, Satpura Group in the central
and southern part to the south of Tapti lineament and Amarkantak Group in the eastern part, the volcanic flows ofnorth-western part are not formally categorised (Nair an Bhusari, 1991). The present study focuses on the DVP of
Amarkantak Group of Chhindwara area of Madhya Pradesh, India. The Deccan volcanic flows of Chhindwara area
comprises of 34 flows having total thickness of about 431m. The flows are classified as Amarkantak Group having
eight formations namely, Mandla, Dhuma, Pipardehi, Linga, Multai, Amarwara, Khampa and Kuleru Formations, inascending stratigraphic order (Geological Survey of India, 2001). The intertrappean sedimentary beds were deposited
between the lava flows during the period of quiescence in the volcanic activity. About 27 intertrappean beds werestudied for palynology, clay mineralogy and magnetic polarity studies in the study area.
Palynofloral changes and climatic conditions across Cretaceous -Paleogene
In Chhindwara area palynoflora bearing lowermost. Mohgaon Kalan Well Section (MKWS) and overlying megaand microflora rich Mohgaon Kalan Fossil Forest (MKFF) intertrappean deposits occur in between Mandla and Dhuma
Formations. The palynoflora from MKWS isrepresented by pteridophytes, gymnosperms, angiosperms, fungal spores,
fungal fruit bodies and algal remains. The recovered palynomorphs are assigned to 34 genera and 44 species. Important
palynomorphs from this intertrappean are Azolla cretacea, Ephedripites spp., Aquilapollenites bengalensis,
Jiangsupollis spp., Proxapertites spp., and Spinizonocolpitesspp.and fungal spore Dicellaesporitesspp. The presence of
epiphyllous fungi Microthyriaceae along with lignitic shales with pyrite indicates good rainfall and prevalence ofhumid climatic conditions at the time of deposition. Moreover, some dry spells in between are indicated by presence of
xeric shrub Ephedripites (Ephadraceae) and gypsum crystals in the lower shales. The clay mineral analysis of the
MKWS section shows dominance of Smectite and Smectite/Chlorite which suggests deposition in fluctuating
environment ranging from semiarid to humid. The overlaying megaflora rich MKFF intertrappean shows presence ofgood palynoassemblage represented by 20 genera and 23 species out of which Azolla cretacea, Cycadopites, Ephedripites
spp., Aquilapollenites bengalensis, Proxapertitesspp., and Spinizonocolpites spp.are the most dominating taxa. On the

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basis of palynotaxa, such as, Azolla cretacea, Cycadopites, Ephedripites, Farabeipollis minutesand Jiangsupollis spp. a
Maastrichtian age is assigned to MKWS and MKFF intertrappeans. Magnetic polarity study of the flow underlying
MKFF (MKF2) shows Normal polarity, whereas, flow capping (MKF3) it shows mixed/Reverse polarity. Due topresence of Maastrichtian palynotaxa in MKWS and MKFF Normal polarity is interpreted to represent C30N and flow
overly MKFF could be of C29R Maastrichtian or Danian. The intertrappean beds of Jhilmili-1 and Jhilmili-2 areexposed near Jhilmili village. It occurs at higher stratigraphic level in Dhuma Formation. The Jhilmili-1 section is richin diatoms (Aulacoseira) and sponge spicules, whereas, the Jhilmili-2 intertrappean has P1a Foraminifera whichindicate Early Palaeocene (Danian) age (Keller et al. 2009). Except some Glomuslike mycorrhizal fungi otherpalynomorphs are not recorded from these two intertrappean sections. Magnetic polarity studies of lower flow
(JHL-F1) shows Normal polarity, and the upper flow (JHL-F2) shows Reverse polarity signatures. The lower flow
(JHL-F1) is interpreted to represent C30N and upper flow (JHL-F2) as Danian C29R as the sediments in between theseflows have Palaeocene P1a foraminifera. Thus, in both the MKFF and Jhilmili intertrappean sections, the transition
from C30N-C29R is recorded (Thakre et al. 2017).
Stratigraphically, above this intertrappean are Palatwara, Singardip, Machagora, Bhutera/Lohara intertrappean beds
in between Pipardehi and Linga Formations and Ghat Parasia, Sonakhar, Imlikheda, Murmari and Umaria Israintertrappeans in Linga and Multai Formation. Clay mineral studies of Machagora intertrappean sediments showsnotable presence of Smectite, and Illite/Mica which suggests deposition under arid to semiarid conditions withaeolian/detritus input into the lake probably due to increasing aridity and, high amount of fine quartz indicate silica richsedimentation. The Bhutera intertrappean yielded biodegraded organic matter, Glomuslike mycorrhizal fungi(Paleomycites globatus) and fungal fruit bodies of Phragmothyrites. Ghat Parasia has good concentration of centric(Aulacoseira) and pennate diatoms as well as sponge spicules. Clay mineral investigation of Ghat Parasia intertrappean
suggests deposition is arid-semiarid climatic conditions. At higher stratigraphic level in Amarwara Formation is
Pindrai intertrap, which has yielded good palynoassemblage. Total 11 genera and 12 species were recorded from it.
Taxa such as Gabonisporis vigourouxii, Sparganiaceaepollenites spp., Incrotonipollis neyveliiand Palmaepollenitesspp.
are dominating taxa in it. The overlying Surli and Tenadi intertrappean section in Amarwara Formation also yieldedrich and diverse palynoassemblage represented by 25 genera and 31 species. Taxa such as Sparganiaceaepollenites
reticulatus, Incrotonipollis neyvelii, and Palmaepollenitesspp.are dominating in it. Maastrichtian age marker palynoassemblage
are not recorded from these two intertrappean. Due to presence of taxa, such as, Haloragacidites, Longapertites,
Mulleripollis and Palmaepollenites, higher stratigraphic position at 840 m RL, and above (P1a foraminifera bearing)
Jhilmili intertrappean, the Paleocene age is assigned to these intertrappean deposits. Magnetic polarity analysis offlows bracketing Pindrai (PIN F1 and PIN F2) and Surli intertrappean deposits (SUR-F1 and SUR-F2) indicate Normal
polarity and lower flow of Tenadi (TND-F1) show Reverse polarity. The polarity of these flows is interpreted to45

Oral Session

represent Paleocene C29N and C28R respectively.
Overall, analysis of palynoassemblage, clay mineralogy and magnetic polarity of the intertrappean beds andassociated flows of Amarkantak Group in Chhindwara area, shows presence of marker Maastrichtian palynoassemblage
in MKWS and MKFF intertrappean and Palaeocene palynoassemblage in Pindrai, Surli and Tenadi intertrappean
sediments. Clay mineral and palynomorphs indicate fluctuating climatic conditions from humid-arid-semiarid-humid
during deposition of intertrappean deposits occurring in between Mandla and Amarwara Formations. Magnetic polarity
analysis of flows bracketing intertrappean indicate N-R-N-R polarity which suggests deposition during C30N of
Maastrichtian, C29R of Maastrichtian-Danian, C29N and C28R of Danian.
References
GSI (2000) District Resource Map, Chhindwara district, Madhya Pradesh.
Keller, G., Adatte, T., Bajpai, S., Mohabey, D. M., Widdowson, M., Khosla, A., Sharma, R., Khosla, S. C., Getsch,
B., Fleitmann, D. & Sahni, A. (2009). K-T Transition in Deccan Traps of Central India marks major marine
seaway across India; Earth Planet. Sci. Letters 282: 10-23.
Nair, K.K.K. & Bhusari, B. (2001): Stratigraphy of Deccan Traps: A review, inrecent advances in the field of earthsciences and their implicationsin national development. Geological Survey of India Special Publication. 64:
477-491.
Smith, S. Y., Manchester, S. R., Samant, B., Mohabey, D. M., Wheeler, W., Baas, P., Kapgate, D., Srivastava, R. &Sheldon, N. (2015): Integrating paleobotanical, paleosol, and stratigraphic data to Study critical transitions: acase study from the Late Cretaceous-Paleocene of India. Earth-Life transition: Paleobiology in the context ofEarth system evolution. 21: 137-166.
Thakre, D., Samant, B., Mohabey, D.M., Sangode, S., Srivastava, P., Kapgate, D.K., Mahajan, R., Upreti, N. &Manchester, S. R. (2017). New insight into age of intertrappean beds of Mohgaon Kalan, Chhindwara district,
Madhya Pradesh using palynology, megaflora, magnetostratigraphy and clay mineralogy. Current Science
112(11): 2193-2197.

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Sedimentary Geology & Tectonics 12

Correlation of palynofloras in the Tetori Province and consequences
for the angiosperm invasion in East Asia✳

Julien Legrand1, ․ Toshihiro Yamada2 ․ Harufumi Nishida1,3
1Chuo University, Faculty of Science & Engineering, Tokyo, Japan, legrand@kc.chuo-u.ac.jp
Kanazawa University, Faculty of Natural Systems, Japan; 3Graduate School of Science, The University of Tokyo, Japan.

2

Mesozoic paleofloras have been widely studied in Japan and adjacent continental regions of eastern Asia chiefly
based on macrofossils, resulting in the proposal of the Siberianand Eurosinian phytogeographic provinces for theJurassic to Early Cretaceous period (Vakhrameev, 1987). In Japan, the Siberian-type flora is only reported from theLate Jurassic to Early Cretaceous parts of the Tetori Group, which is called “Tetori-type flora”. The Tetori Goupoutcrops in Hokushinetsu region of the Inner Zone of Japan and is divided into the Kuzuryu, Itoshiro and Akaiwa
subgroups in ascending order (Maeda, 1961; Fujita, 2002; see Sano, 2015 for a different opinion). The Tetori Basin
was originally located to the east of the Korean Peninsula, but sediments were moved to theirpresent position by
opening of the Sea of Japan.
Few palynological studies on Japanese Mesozoic strata, however, had been done until recently, and we are
performing a series of palynological surveys in accessible major Japanese fossil sites to clarify floristic andenvironmental changes of the period. Early Cretaceous is also a key period of angiosperm invasion in eastern Asia
where angiosperm pollen records come mostly from the Siberian phytogeographic province. We report here theHauterivian to early Aptian palynofloras of the Itoshiro Subgroup (Itsuki, Kuwajima and Okurodani formations) andthe Akaiwa Subgroup (Nochino and Kitadani formations) of the Tetori Group and compare them with coeval
palynofloras of the Gyeongsang Basin in Korea and Jehol Basin in China.
Only a limited number of palynomorphs (five genera of fern spores and one genus of gymnosperm pollen grains, but
no identifiable species) were previously reported from the Itoshiro and Akaiwa subgroups, most likely from theNochino Formation (Umetsu & Matsuoka, 2003). We already reported a rich and well-preserved palynologicalassemblage (45 genera and 41 species) from the “Dinosaur Quarry” locality of the Kitadani Formation (Legrand et al.,2013), which isdominated by spores of herbaceous plants, mostly Filicopsida (Schizaeales, Cyatheales, andOsmundales) and gymnosperm pollen, primarily of Coniferales and less amount of Bennettitales, Cycadales orPentoxylales. However, neither the macro- nor microfossil assemblages yielded any angiospermous remains. The
oldest angiospermous fossils for the Inner Zone were Maastrichtian leaves and pollen grains reported from the Asuwa
Group (Matsuo, 1962) and the Omichidani Formation (Matsuo, 1970; Nichols et al., 2010).
We collected new samples from the upper part of the Tetori Group and obtained a diversity of spores (26 species)and gymnosperm pollen grains (6 species) from the Itsuki, Nochino and Kuwajima formations. Moreover, one horizonof the upper part of the Kitadani Formation revealed for the first time the angiosperm pollen grain Clavatipollenites
hughesii, which represents the oldest angiosperm record for the Inner Zone of Japan. These new results enhance

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discussions on paleoclimatic and paleovegetational changes for this period confirming a correlation between Japanese,
Korean and Chinese deposits. In particular the palynoflora of the Nochino Formation is similar to those of the Myogog
and Jinju formations of the Gyeongsang Basin in species compositions. Moreover, paleofloras of the Kitadani andYixian formations (the Jehol Basin) were considered until this report as havingsimilar characteristics in terms ofcompositions excepting some elements as the presence of early angiosperms (Sun et al., 2001) and richness of
gnetalean fossils(Zhou et al., 2003; Rydin et al., 2006),but we could also observe a peak of gnetalean pollen
abundancein the horizon of the Kitadani Formationcontaining Clavatipollenites hughesii. This similarity would add asupport for the early Aptian age of the Yixian Formation.
References
Fujita, M., 2002: A new contribution to the stratigraphy of the Tetori Group, adjacent to Lake Kuzuryu, Fukui
Prefecture, central Japan. Memoir of the Fukui Prefectural Dinosaur Museum, no. 1, p. 41-53.
Legrand, J., Pons, D., Terada, K., Yabe, A., Nishida, H, 2013: Lower Cretaceous (upper Barremian-lower Aptian?)palynoflora from the Kitadani Formation (Tetori Group, Inner Zone of central Japan). Paleontolgical Research,
vol. 17, p. 201-229.
Maeda,S., 1961: On the geological history of the Mesozoic Tetori Group in Japan. Journal of College of Arts andSciences, Chiba University, Natural Sciences Series, vol. 3, p. 396-426. (in Japanese with English abstract)
Matsuo,H., 1962: A study on the Asuwa Flora (Late Cretaceous age) in the Hokuriku District, Central Japan.
Science Report of the Kanazawa University, vol. 8 (1), p. 177-250.
Matsuo,H., 1970: On the Omichidani Flora (Upper Cretaceous), inner side of Central Japan. Transactions andProceedings of the Paleontological Society of Japan. New Series, no. 80, p. 371-389.
Nichols,D.J., Matsukawa,M., Ito,M., 2010: The Geological Age and Phytogeographical Significance of some
Metamorphosed Palynomorphs from the Omichidani Formation of Japan. Palynology, vol. 34(2), p. 157-163.
Rydin,C., Wu,S.Q., Friis,E.M., 2006: LiaoxiaCao et S.Q. Wu (Gnetales): ephedroids from the Early Cretaceous
Yixian Formation in Liaoning, northeastern China. Plant Systematics and Evolution, vol. 262, p. 239-265.
Sano, S.,2015:New view of the stratigraphy of the Tetori Group in Central Japan. Memoir of the Fukui Prefectural
Dinosaur Museum, vol. 14, p. 25-61.
Sun, G., Zheng, S.L., Dilcher, D.L., Wang, Y.D., Mei, S.W., 2001:Early Angiosperms and their associated plantsfrom Western Liaoning, China. Shanghai Scientific and Technological Education Publishing House, Shanghai, 227 p.
Umetsu, K.,Matsuoka, A., 2003: Early Cretaceous fossil spores and pollen from the Tetori Group in the upper
reaches of the Kuzuryu river, Fukui Prefecture, central Japan. Journal of the Geological Society of Japan, vol.
109, p. 420-423 (in Japanese with English abstract).
Vakhrameev, V.A., 1987: Climates and the distribution of some gymnosperms in Asia during the Jurassic andCretaceous. Review of Palaeobotany and Palynology, vol. 51, p. 205-212.
Zhou, Z.-H., Barrett, P.M., Hilton, J., 2003:An exceptionally preserved Lower Cretaceous ecosystem. Nature, vol.
421, p. 807-814.

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Sedimentary Geology & Tectonics 13

Dinosaur Nesting Site of Salbardi-Ghorpend area, Betul District, Madhya
Pradesh, India: a unique Maastrichtian Megaloolithus oospecies✳

Prabhakar Lakra1, ․ VarshaA.Aglawe2
1

Geological Survey of India, CR, Nagpur, prabhakarlakra@gmail.com
2
Geological Survey of India, NR, Lucknow

The Late Cretaceous Lameta non-marine fluvial deposits comprising overbank, channel and back swamp deposit
occupies more than 5000 km2 area as detached outcrops in India (Mohabey et al., 1993), globally recognized for
hosting dinosaurian remains including skeletons, coprolites and eggs in central and western India. From various
nesting site a considerable progress has been made in recording diverse dinosaur eggs in India during the last thirty six
years. The majority of the oodiversity is recorded from the 6 inland basins namely, (i) Nand-Dongargaon(N-D), (ii)Jabalpur, (iii) Balasinor-Jhabua, (iv) Ambikapur-Amarkantak, (v) Sagar (Mohabey,1996) and (vi) Salbardi-Belkher(Srivastava and Mankar, 2015). Recent focus of research work in Salbardi-Belkher Inland basin has proven the area
paleontologically productive after discoveries of dinosaur eggs (Srivastava and Mankar, 2015)and bones(Srivastavaand Mankar, 2013; Aglawe and Bhadran, 2014; Bhadran and Aglawe, 2015). During the approved field season
programme (FSP) for 2015-16 of Geological Survey of India (GSI), 4 dinosaur nests comprising 27 spherical tosub-spherical eggs, one isolated egg and other eggshell fragments were recorded within an area of 0.5 km2 in
Salbardi-Ghorpend along the Maru River in Lameta strata. Nest (N) No. 1, 2, 3 and 4 comprises 6, 14, 4 and 3 eggs
respectively. Eggs within nest do not exhibit any specific pattern, however, N1 and N3 is roughly arranged in linear
and N2 in sub-circular fashion and positioned in shallow pit. All the dinosaur eggs/nests are embedded in calcretised
channel related sandstone in a single stratigraphic horizon. In general, the entire 4 nest are oriented along NW-SE
direction. The distance between N1-N4, N3-N4 and N2-N3 is approximately 60 m, 40 m and 10 m respectively. The
nest architecture indicates that lithounits exposed along Maru River has provided niche for laying of eggs. Within nest
the minimum and maximum inter-egg distance is 2 cm and 14 cm. The presence of insitu egg clutches within restricted
geographic and stratigraphic horizon supports to designate the area as “Dinosaur Nesting Site”. The nesting behaviour
suggests that the titanosaurus were gregarious and prefer in colonial nesting. Geological setup in Salbardi-Ghorpend
area show gneissic rock at the base which is unconformably overlain by the rocks of Gondwana Supergroup. Lameta
Formation comprising green sandstone, off-white yellowish calcareous sandstone, purple-green clay rich sandstone,cherty limestone, brecciated limestone and nodular limestone disconformably overlie the Gondwana sediments. The
rocks of Lameta Formation and Gondwana Supergroup are covered by thick pile of Deccan Traps in the SalbardiGhorpend area.

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Dinosaur eggs of Salbardi-Ghorpend area are spherical to sub-spherical with diameter ranging from 6.8-16.3cm.
The thickness of eggshells ranges from 1.50-2.70 mm with average thickness of 2.09 mm. The external surface
exhibits nodose ornamentation. These nodes are sub-circular to circular in shape and are closely spaced. Under
microscope, the diameter of the nodes varies from 0.28-1.61 mm. The inter- nodal spaces ranges from 71.45-363 µm.
In radial section, variability in nodal relief is observed due to non-uniformity in nodal size. In radial section,
spheroliths show moderately arch shaped growth lines following the contours of the external profile.The individual
spheroliths are elongated conical shaped (Fig.2A) with dome shape top which provides nodular appearance on theexternal surface. Microscopic studies of most of the samples show sweeping extinction. It was also observed that there
is variation in size and shape of shell units. Short sized spheroliths are also found with normal spheroliths. Shell units
are discrete although some degree of fusion may also occur between adjacent units. The individual spheroliths areobserved to have grown from single mammillae. The height of the shell unit’s varies from 1.35-2.70 mm. The width of
the shell unit’s ranges from 0.37-0.97 mm. The average height (H) to width (W) ratio comes to be 3.04:1. Pore canals
are straight, narrow and slightly inclined. Under Scanning Electron Microscope (SEM), pore canals are sub-circular to
sub-triangular shape. In radial section, widths of a pore canal varies from 12.42-37.28 µm. Basal caps are sub-circular
in shape and their diameter varies from 0.13-0.20 mm.Till date, due to excavation difficulties these fossil eggs andnests are still preserved in sandstone of Lameta Formation at Maru River section. However, thin sections of eggshells(Reg. No. 332/GSI/PAL/CR/2015/ N2E1, N2E3, N2E6, N2E7, N2E8, N2E13, N2E27; 333/GSI/PAL /CR/2015
N3E27, N3E23;334/GSI/PAL /CR/2015N4E1; 336/GSI/ PAL/CR/2016 N6E1,N6E2; 328/GSI/PAL/CR/2015-N1E5,
N1E3) collected so far for microscopic studies are registered and house at GSI, Palaeontology Division, CR, Nagpur.
The egg size of the Salbardi-Ghorpend egg (6.8-16.3cm) show similarity with M.cylindricus (12-20 cm),M.baghensis (14-20 cm), M.dhoridungriensis (14-18 cm), M.megadermus (13-18 cm) and M.jabalpurensis (14-16 cm).
Eggshell thickness of Salbardi-Ghorpend egg (1.50-2.70 mm) partially match with M.cylindricus (1.7-3.5 mm),M.baghensis(1-1.70 mm), M. khempuensis (2.26-2.36 mm), M.mohabeyi (1.88-1.90 mm), M.jabalpurensis (1.0-2.3)
and M.padiyalensis (1.47-1.75). The shell unit’s height to width ratio of Salbardi-Ghorpend egg (3.04:1) has close
similarity with M. dholiyaensis (2.94:1), M.mohabeyi (3.06:1) and M.dhoridungriensis (2.74:1). The Salbardi-Ghorpend
eggs have dinosauroid-spherulitic basic type eggshell organization, tubospherulitic morphotype, and compactituberculate
ornamentation.
The Salbardi-Ghorpend eggs are unique by means of its egg size which is ranging from 6.8-16.3cm . In the
N1(Fig.1B), 2 eggs (6.8-7.5cm and 8-10cm in diameter) and in N2, 1 egg (7.1-7.2cm in diameter) is smaller than other
Late Cretaceous (Maastrichtian) dinosaur eggs documented till date by the various workers. Large sized eggs ranges indiameter from 12-16.3cm. Macroscopic, microscopic and ultramicroscopic (SEM) characters of eggs and eggshellfragments of Salbardi-Ghorpend area were systematically studied and correlated with other Indian eggs and it was50Oral Session

concluded that present material belongs to oogenus: Megaloolithus (Vianey_Liaud et at.,1994) of oofamily:
Megaloolithidae (Zhao,1979). However, the eggs of Salbardi-Ghorpend resemble partially with 9 globally accepted
Late Cretaceous (Maastrichtian) oospecies of oogenus : Megaloolithus and hence it was found difficulty by the authors
to identify the oospecies for fossil eggs of Salbardi-Ghorpend area. For the establishment of the oofamily, oogenera
and oospecies distinct morphological characters of eggshell histostructure and macrostructure is required. Oospecies on
the other hand are based on (i) exact range of eggshell thickness, (ii) egg size, (iii) external pore pattern and (iv) detailsof sculpturing (Mikhailov et al., 1996).Presence of embryos in eggs is thought to be solid evidence for identification ofoospecies. However, associated embryos or hatchlings have not been found yet for this oospecies. At present, there isno data available which show small size eggs (6.8-10cm) in association with large size eggs in a single nest. Hence,
based on the peculiar features of eggs of the Salbardi-Ghorpend dinosaur nesting site, the authors of the present paper
suggests possibility of a new oospecies within Oofamily: Megaloolithidae.
References
Aglawe, V.A. & Bhadran, A. 2014. First report of turtle bones and occurrence of dinosaurian bones from Lameta
Formation, Ghorpend village, Salbuldi area, Betul district, Madhya Pradesh. News Geological Survey of India(Central region),30.
Bhadran, A. & Aglawe, V. A. 2015. First report of Theropod (Dinosauria) from Upper Cretaceous (Maastrichtian)
Lameta Formation of Salbardi basin, Betul district, Madhya Pradesh. Indian Journal of Geosciences, 69(2),421-424.
Mikhailov, K.E., Bray, E. S., & Hirsch, K.F. 1996. Parataxonomy of fossil egg remains(Veterovata): Principles and Applications. Journal of vertebrate paleontology, 16(4),763-769.
Mobabey, D.M., Udhoji, S.G., & Verma, K.K. 1993.Paleontological and sedimentological observations on
non-marine Lameta Formation (Upper Cretaceous) of Maharashtra, India: their palaeoecological andpalaeoenvironmental significance. Palaeo,105, 83-94.
Mohabey, D. M.1996. Depositional environment of Lameta Formation (Late Cretaceous) of Nand-Dongargaon
basin (Maharsahtra): the fossils and lithological evidences. Mem. Geological Society of India, 37, 363-386.
Srivastava, A., K., & Mankar, R.S.2015. Salbardi-Belkher inland basin: a new site of Lameta sedimentaion at theborder of districts Amravati, Maharastra and Betul, Madhya Pradesh, Central India. Current science, 109(7),1337-1344.
Srivastava, A., K., & Mankar, R.S.2015.Megaloolithus Dinosaur Nest from the Lameta Formation of Salbardi Area,
Districts Amravati, Maharashtra and Betul, Madhya Pradesh.Journal of Geological Society of India, 85,
457-462.

51

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Vianey-Liaud, M., Mallan, P., Buscail, O., Montgelard, C.1994. Review of French dinosaur eggshells: morphology,
structure, mineral and organic composition. In K.Carpenter, K.F. Hirsch and J.R.Horner (Eds.), Dinosaur eggs
and Babies (pp.151-183).Cambridge University Press, Cambridge.
Zhao, Z. 1979. The advancement of researchers on the dinosaurian eggs in China. In Mesozoic and Cenozoic red
beds in Southern China (Eds.), IVPP and N.G.P. Science Press (pp.330-340), China.

Fig. 1. Eggs of Salbardi-Ghorpend dinosaur nesting site; (A) Large size dinosaur egg in nest no.4(N4) , (B) two
small size dinosaur eggs in nest no.1(N1).

Fig. 2. (A)Photomicrographs of eggshell showing conical shape spheroliths with sweeping extinction and narrow
pore canals(328/GSI/PAL/CR/2015 N1E5); (B) SEM image of outer surface of eggshell showing well developed
circular to sub-circular nodes (332/GSI/PAL/CR/2015 N2E8)52

Oral Session

Paleontology 1

Dinosaur ecology and climate in Eastern Siberia during the Late
Cretaceous inferred from stable isotopes✳

Romain Amiot1, ․ Lina B. Golovneva2 ․ Pascal Godefroit3 ․ Jean Goedert1 ․ Géraldine Garcia4 ․Christophe Lécuyer1 ․ Eugenia V. Bugdaeva5 ․ Alexei B.Herman6 ․ Robert spicer7
1

CNRS UMR 5276 LGL-TPE, Université Claude Bernard Lyon 1 and Ecole Normale Supérieure de Lyon, 2, Rue Raphaël
Dubois, 69622 Villeurbanne Cedex, France, Romain.amiot@univ-lyon1.fr
2
V.L. Komarov Botanical Institute, Russian Academy of Sciences, St. Petersburg, Russia
3
Directorate ‘Earth and History of Life’, Royal Belgian Institute of Natural Sciences, rue Vautier 29, B-1000 Brussels, Belgium
4
IPHEP, UMR CNRS 7262, Université de Poitiers, UFR SFA, Bat. B35, 6 rue M. Brunet, TSA 51106, 86073 Poitiers cedex
9, France
5
Institute of Biology and Soil Science, Far East Branch, Russian Academy of Sciences, Vladivostok 690022, Russia
6
Geological Institute,Russian Academy of Sciences,119017 Moscow, Russia
7
School of Environment, Earth and Ecosystem Sciences, The Open University, Milton Keynes, MK7 6AA, UK.

Dinosaur eggshells of two oofamilies (Spheroolithidae and Prismatoolithidae) recovered from the Late Cretaceous
Kakanaut Formation of Siberia constitute the northernmost record of dinosaur reproductive behavior (Godefroit et al.,2009). The high palaeolatitude of the locality (~70-75°N) as well as the cool climatic conditions inferred frompalaeobotanical data (Golovneva, 2000) raise questions about the reproductive strategies used by these dinosaurs inorder to successfully incubate their eggs and raise their hatchlings (Spicer et al., 2016). In order to investigate climaticand seasonal aspects of Kakanaut dinosaur reproductions, theropod, hadrosaur and ankylosaur dinosaur remains as wellas lepisosteid fish scales have been analysed for their oxygen and carbon isotope compositions of tooth and scale
phosphate (δ18Op), as well as of their tooth and eggshell carbonate (δ18Oc; δ13Cc). Based on the known oxygen isotope
fractionation established between environmental water and eggshell carbonate (Lazzerini et al., 2016) or apatite
18

phosphate (Amiot et al., 2017), δ Ow values of local waters ingested by the Kakanaut dinosaurs have been calculated.
18

Assuming that these ingested waters are derived from local precipitation, the mean δ Ow value of which is controlled
by mean air temperature (Dansgaard, 1964), then the average δ18Ow value derived from the δ18Op values of dinosaur
tooth apatites indicate a local mean air temperature of 9±7℃ (using the relationship of Lécuyer (2014). It isnoteworthy that this temperature matches the one of 10℃ estimated using CLAMP analysis (Golovneva, 2000), and is18

close to that of 7±13℃ calculated from fish scales δ Op values using the phosphate-water temperature scale18

established for fish (Lécuyer et al., 2013). The range in calculated δ Ow values (-7.2‰ to -13.4‰ V-SMOW) can beinterpreted as reflecting seasonal variations, lowest values corresponding to winter and highest ones to summer, andcompares well with the preliminary isotopic investigation of Goedert et al. (2016). Interestingly, the δ18Ow values
calculated from the eggshells δ18Oc values (-12.2‰ to -17.0‰ V-SMOW) are restricted to the lower part of the53

Oral Session

seasonal range, indicating that eggs have been produced by dinosaurs drinking winter waters. Because egg laying
during winter seems unlikely due to high latitude freezing temperatures, prolonged darkness and limited foodavailability, it is more plausible that the egg have been produced and laid during spring time and that the drinking waterof mother dinosaurs originated from the melting snow.
18

Despite a low number of available eggshell fragments (n = 5), their narrow range of δ Oc values indicate a laying
period restricted to the beginning of spring in order to benefit from mild temperatures and increasing food availability
until the next winter for both parents and the hatchlings.
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. doi:10.1007/s00114-017-1468-2
Dansgaard, W., 1964. Stable isotopes in precipitation. Tellus 16, 436-468. doi:10.1111/j.2153-3490.1964.tb00181.x
Godefroit, P., Golovneva, L., Shchepetov, S., Garcia, G., Alekseev, P., 2009. The last polar dinosaurs: high diversityof latest Cretaceous arctic dinosaurs in Russia. Naturwissenschaften 96, 495-501.
Goedert, J., Amiot, R., Boudad, L., Buffetaut, E., Fourel, F., Godefroit, P., Kusuhashi, N., Suteethom, V., Tong, H.,
Watanabe, M.E., Lécuyer, C., 2016. Preliminary investigation of seasonal patterns recorded in the oxygenisotope composition of theropod dinosaur tooth enamel. Palaios 31, 10-19.
Golovneva, L.B., 2000. The Maastrichtian (Late Cretaceous) climate in the Northern Hemisphere. Geol. Soc. Lond.
Spec. Publ. 181, 43-54.
Lazzerini, N., Lécuyer, C., Amiot, R., Angst, D., Buffetaut, E., Fourel, F., Daux, V., Betancort, J.F., Sánchez Marco,
A., Lomoschitz, A., 2016. Oxygen isotope fractionation between bird eggshell calcite and body water:
application to fossil eggs from Lanzarote (Canary Islands). Sci. Nat. 103, 81. doi:10.1007/s00114-016-1404-x
Lécuyer, C., 2014. Water on Earth: Physicochemical and Biological Properties. Wiley-ISTE, London.
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. doi:10.1016/j.chemgeo.
2013.03.008
Spicer, R.A., Herman, A.B., Amiot, R., Spicer, T.E.V., 2016. Environmental adaptations and constraints on latest
Cretaceous Arctic dinosaurs. Glob. Geol. 19, 241-254.

54

Oral Session

Paleontology 2

Dinosaur Footprint Assemblage at the site Huai Dam Chum from the Lower
Cretaceous Khok Kruat Formation, Khorat Group, Northeastern Thailand✳

Shohei KOZU1, ․ Apsorn SARDSUD2 ․ Doungrutai SAESAENGSEERUNG 2 ․Cherdchan POTHICHAIYA2 ․ Sachiko AGEMATSU1 ․ Katsuo SASHIDA1
1

Graduate School of Life and Environmental Sciences, University of Tsukuba, Japan, kouzu_0419@geol.tsukuba.ac.jp
2
Department of Mineral Resources, Ministry of Natural Resources and Environment, Thailand

The Upper Triassic to Lower Cretaceous non-marine sedimentary rocks exposed in northeastern Thailand arereferred to as the Khorat Group (Ward and Bunnag, 1964). Buffetaut et al. (1993)subdivided this group into eightformations, which are (from oldest to youngest) the Huai Hin Lat, Nam Phong, Phu Kradung, Phra Wihan, Sao Khua,
Phu Phan, Khok Kruat, and Maha Sarakham formations. Many fossils such as dinosaur bones, dinosaur footprints, fish,
crocodilians, turtles, bivalves, and palynomorphs have been recovered from the Khorat Group (Meesook, 2011). Many
dinosaur footprints have been known from the upper Lower Cretaceous (Aptian - Albian) Khok Kruat Formation
which is the upper part of the Khorat Group, at the Huai Dam Chum (Tha Uthen) dinosaur tracksite, northeastern
Thailand. Dinosaur footprints have previously been reported from this area (Buffetaut et al., 2005; Le Loeuff et al.,2003, 2005, 2009; Sato and Tumpeesuwan, 2005; Matsukawa et al., 2006; Kozu et al., in press). However, there has
been no previous study of the ichnotaxonomic classification or quantitative community analysis of the dinosaur
footprint assemblage. In this study, we systematically describe tracks and conduct quantitative analysis of theropod
track assemblage from the upper Lower Cretaceous Khok Kruat Formation.
The tracks described herein are preserved at the Huai Dam Chum site (N17°71'30.01", E104°38'15.76"), Ban Lao
Nat, Tha Uthen District, Nakhon Phanom Province, northeastern Thailand. The Khok Kruat Formation crops out at the
Huai Dam Chum site (e.g. Le Loeuff et al., 2003). The outcrop, which consists mainly of very-fine-grained sandstone,
is present along route 212. Approximately 600 tracks occur in thin mudstone layer of the northern part of the outcrop at
this site (Fig. 1). On the footprint-bearing thin mudstone layer, current-ripple marks that show a NW flow direction andmud cracks are overprinted by footprints. Two types of footprints, small-sized theropod and probably crocodylomorph
are imprinted with mud cracks and current-ripple marks on the thin mud layer. Most of footprints are referred to cf.
Asianopodusisp., and are imprinted by small-sized theropods, probably ornithomimosauria. Theropod tracks aremainly separated into two groups, Group A and Group B. From ichnological viewpoints, the small-sized theropod trackassemblage indicates the herd behaviour and its idiosyncratic group composition. In particular, the histogram ofsize-frequency measurements of Group A shows the anomalous bimodal distribution. We consider that there are two
hypotheses; the first one is due to the male-female difference, and the second is a result of the different growing stage.
References
Buffetaut, E., Suteethorn, V., Le Loeuff, J. L., Khansubha, S., Tong, H., and Wongko, K., 2005. The Dinosaur Fauna
from the Khok Kruat Formation (Early Cretaceous) of Thailand. In: Proc. of the International Conference on
Geology, Geotechnology and Mineral Resources of Indochina (GEOINDO 2005), Khon Kaen, 575-581.

55

Oral Session

Buffetaut, E., Suteethorn, V., Martin, V., Chaimanee, Y., and Tong-Buffetaut, H., 1993. Biostratigraphy of the
Mesozoic Khorat Group of northeastern Thailand: the contribution of vertebrate palaeontology. In: Proc. of theInternational Symposium on Biostratigraphy of Mainland Southeast Asia: Facies and Paleontology, Chiang Mai,
51-63.
Kozu, S., Sardsud, A., Saesaengseerung, D., Pothichaiya, C., Agematsu, S., and Sashida, K. Dinosaur Footprint
Assemblage from the Lower Cretaceous, Khorat Group, Northeastern Thailand. Geoscience Frontiers. (in press)
Le Loeuff, J., Saenyamoon, T., Suteethorn, V., Khansubha, S., Buffetaut, E., 2005. Vertebrate footprints of south
east Asia (Thailand and Laos): a review. In: Pro. of the International Conference on Geology, Geotechnology
and Mineral Resources of Indochina (GEOINDO 2005), Bangkok, 582-587.
Le Loeuff, J., Saenyamoon, T., Souillat, C., Suteethorn, V., and Buffetaut, E., 2009. Mesozoic vertebrate footprintsof Thailand and Laos. Geological Society, London, Special Publications,315,245-254.
Le Loeuff, J., Lauprasert, K., Suteethorn, S., Souillat, C., Suteethorn, V. and Buffetaut, E. 2010. Late Early
Cretaceous crocodyliform trackways from northeastern Thailand. New Mexico Museum of Natural History and
Science Bulletin, 51, 175-178.
Matsukawa, M., Lockley, M.G., and Jianjun, L., 2006. Cretaceous terrestrial biotas of East Asia, with specialreference to dinosaur-dominated ichnofaunas: towards a synthesis. Cretaceous Research, 27, 3-21.
Meesook, A., 2011. Cretaceous. In: Ridd, M. F., Barber, A. J., Crow, M. J. (Eds.), The Geology of Thailand.
Geological Society, London, 169-184.
Sato, Y. and Tumpeesuwan, S., 2005. Superexcellent preservation of dinosaur foot prints in Nakhon Phanom innortheast Thailand. In: Proc. of the International Conference on Geology, Geotechnology and Mineral
Resources of Indochina (GEOINDO 2005), Bangkok, 570-574.
Ward, D. E. and Bunnag, D., 1964. Stratigraphy of the Mesozoic Khorat Group in Northeast Thailand. Rep. Invest.
DMR 6, 1-95.

Fig. 1. Map of a part of the northern outcrop at the site Huai Dam Chum. Many consecutive theropod tracks anda few small-sized trackways of probably crocodylomorph are imprinted with mud crack and current-ripple markson the thin mud layer.

56

Oral Session

Paleontology 3

A review of new data on the belemnite family Cylindroteuthididae
and biostratigraphy of the Berriasian in Eurasia and North America
Oksana S. Dzyuba
Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Acad. Koptyug av. 3,
Novosibirsk 630090, Russia, dzyubaos@ipgg.sbras.ru

Belemnites of the family Cylindroteuthididae are widely used in the Middle Jurassic-Lower Cretaceous
biostratigraphy of Boreal regions. The investigation of this group of belemnites is especially urgent, taking into
account the revived interest to search of reliable markers for interregional correlation of the Jurassic-Cretaceous
boundary interval.
In northern and northeast Eurasia, there are several localities in which Berriasian cylindroteuthidids are studied to agreater or lesser extent. The key localities are situated in Svalbard (western Spitsbergen, Kong Karls Land), England(Yorkshire, Lincolnshire), Central Russia (Volga River near Kashpir, Pronya River near Nikitino), North European
Russia (Izhma River), Western Siberia (Maurynya, Tolya, Yany-Manya and Yatriya rivers), Eastern Siberia (Kheta
River basin, Nordvik Peninsula), Northeast Russia (Pekulneiskoe Lake area), and Central Japan (central Honshu). In
North America, some Berriasian cylindroteuthidids are known from western Canada (British Columbia), western USA(northern California), and Greenland.
The most detailed belemnite zonation of the Berriasian (uppermost Upper Volgian to Ryazanian) has been suggested
for Eastern Siberian sections (Dzyuba, 2012, 2013b). Two independent successions of biostratigraphic units based on
cylindroteuthidids are defined there: (1) Lagonibelus gustomesovi& Arctoteuthis porrectiformisbeds, and the Simobelus
curvulusZone; (2) the Arctoteuthis tehamaensisZone, the Cylindroteuthis knoxvillensisZone, and the Simobelus
curvulusZone. Some Californian belemnite taxa were recently found in Eastern Siberia for the first time, namely
Arctoteuthis tehamaensis, Cylindroteuthis knoxvillensis, Cylindroteuthiscf. newvillensis, and Cylindroteuthis ex gr.
occidentalis (Dzyuba, 2012, 2013b). These findings supplement the list of Cylindroteuthididae taxa in common with
the Californian belemnite assemblage, which also includes Arctoteuthis porrectiformisand Lagonibelus napaensis.
Boreioteuthis regularisrecently reported from the Boyarka River section (Kheta River basin) represents the first recordof this species from outside Svalbard (Dzyuba, 2013b).
The list of the most important recent findings in Western Siberiaincludes Arctoteuthis tehamaensis, Cylindroteuthis
newvillensis, Cylindroteuthis knoxvillensis (known in Eastern Siberia and northern California),Cylindroteuthis cf.
subobeliscoides (known in Eastern Siberia), Liobelus prolateralis (known in Russian Platform and Eastern Siberia),
and Pachyteuthis crassovalis (known in Svalbard). Furthermore, four new Berriasian species (Cylindroteuthis ornata,57

Oral Session

Acroteuthis pseudoconoides, Pachyteuthis eximia,and Simobelus compactus) have very recently been discovered in thisregion (Dzyuba, 2013a). In Western Siberia, the following cylindroteuthidid belemnite zones and beds are establishedin the Berriasian: (1) Lagonibelus gustomesovi& Arctoteuthis porrectiformisbeds, and the Simobelus curvulusZone; (2)Simobeluscompactusbeds, the Cylindroteuthis knoxvillensisZone, and the Simobelus curvulusZone; (3) Boreioteuthis
exploratabeds, and the Simobelus curvulusZone (Dzyuba, 2013a). Regional Simobeluscompactusbeds are considered
as an age analogue of the Eastern Siberian Arctoteuthis tehamaensisZone.
Available data from the Izhma River section (Sachs and Nalnjaeva, 1972; Nalnjaeva, 1984) show that Boreioteuthis
exploratabeds and Simobelus curvulusbeds can be recognised in North European Russia (Fig. 1). Some other
Berriasian belemnite zones of Siberia are traceable (in the beds’ rank) to northern California, namely Arctoteuthis
tehamaensisbeds, and Cylindroteuthis knoxvillensisbeds. Belemnite records from the Berriasian of northeast Asia are
still scant. Until recently, only a few cylindroteuthidids had been reported from a northeast part of the Koryak ridge(Pekulneiskoe Lake area), Northeast Russia (Vereshchagin et al., 1965). Therefore, the record of Cylindroteuthisaff.
knoxvillensisfrom the Mitarai Formation of Central Japan (Shokawa area) is of particular interest (Sano et al., 2015).
It is noteworthy that Berriasian belemnite scales of Siberia considerably differ from those of Central Russia and NWEurope. This situation is directly connected with peculiarities of belemnite biogeography during theJurassic-Cretaceous transition. In the terminal Volgian the seas of Central Russia and NW Europe, belonging to the
Boreal-Atlantic realm, became shallow basins with high-abundance but very low-diversity belemnite faunas. By theterminal Middle Volgian subfamilies Cylindroteuthidinae and Lagonibelinae disappeared in the Boreal-Atlantic realm.
In the Late Volgian-Ryazanian, mainly Acroteuthisand Liobeluswith robust dorsoventrally depressed rostrum occurredas the most adapted to shallow environment. In the Arctic realm, various taxa of cylindroteuthidids continued to exist
and generated a number of new species. Some Arctoteuthis, Cylindroteuthisand Lagonibeluspossessing slender
elongated rostrum could have migrated over long distances through the epicontinental seaways between the Arctic andthe Eastern Pacific, and between the Arctic and the Western Pacific.
In Central Russia, the position of regional belemnite beds, Liobelus russiensis& Acroteuthis mosquensisbeds,
Liobelus lateralisbeds, and Acroteuthis explanatoides beds, has been recently fixed in the Kashpir and Nikitino
sections (Dzyuba et al., 2015; Urman et al., 2016). All these biostratigraphic units are traceable to NWEurope (Fig. 1).
Acroteuthis subquadratoidesrecorded from the Ryazanian of Central Russia represents the first record of this species
from outside NWEurope (Dzyuba et al., 2015).
The Jurassic-Cretaceous boundary defined in Tethys at the base of the Calpionella alpinaSubzone cannot be strictlyrecognised in Boreal regions. This boundary falls in the pre-Brodno part of M19n, commonly in the middle part ofM19n.2n. Only one cylindroteuthidid marker, the base of the Arctoteuthis tehamaensisZone, is undoubtedly recorded
within M19n, close to the middle part of M19n.2n (Shurygin and Dzyuba, 2015). This marker has been recognised innorthern Eastern Siberia and northern California. In Western Siberia, the position of the Jurassic-Cretaceous boundary58

Oral Session

can be provisionally defined at the base of Simobelus compactus beds (age analogue of the Arctoteuthis
tehamaensisZone).
This is a contribution to the IGCP608 and the SB RAS Complex Programme “Integration and Development”.
References
Dzyuba, O.S., 2012. Belemnites and biostratigraphy of the Jurassic-Cretaceous boundary deposits of northern East
Siberia: New data on the Nordvik Peninsula. Stratigr. Geol. Correl. 20(1), 53-72.
Dzyuba, O.S., 2013a. 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., 2013b. Revision of belemnites from the Jurassic-Cretaceous boundary beds in the Boyarka River
Basin (northern East Siberia), in: Zakharov, V.A. (Ed.), Jurassic System of Russia: problems of stratigraphy andрaleogeography. Scientific materials. “ID “IzdatNaukaServis” LLC, Yekaterinburg, pp. 73-76.
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. (Eds.), The International Scientific Conference on theJurassic/Cretaceous boundary: Proceedings volume. Kassandra, Togliatti, pp. 36-41.
Nalnjaeva, T.I., 1984. Belemnites from the Jurassic-Cretaceous boundary beds of the Pechora River Basin, in:Boundary stages of Jurassic and Cretaceous systems. Nauka, Moscow, pp. 144-150.
Sachs, V.N., Nalnjaeva, T.I., 1972. Belemnites, in: Sachs, V.N. (Ed.), The Jurassic-Cretaceous Boundary and the
Berriasian Stage in the Boreal Belt. Nauka, Novosibirsk, pp. 204-215.
Sano, S., Iba, Y., Isaji, S., Asai, H., Dzyuba, O.S., 2015. Preliminary report of earliest Cretaceous belemnites fromJapan and their paleobiogeographic significance. J. Geol. Soc. Japan121(2), 71-79.
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., 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 рaleogeography. Proceedings.Chernomorpress, Simferopol, pp. 279-281.
Vereshchagin, V.N., Kinasov, V.P., Paraketsov, K.V., Terekhova, G.P., 1965. Field atlas of Cretaceous fauna ofNortheast USSR. Magadan (in Russian).
Figure Caption
Fig. 1. Panboreal correlation of the Jurassic-Cretaceous boundary interval based on cylindroteuthidid belemnites.

59

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Paleontology 4

Diversity, extinction and evolutionary trend of palynoflora acrossCretaceous-Paleogene in Deccan volcanic associated sediments of India✳

Samant Bandana ․ Mohabey Dhananjay
Department of Geology, RTM Nagpur University, Law College Campus, Amrawati Road, Nagpur, 440001, India
bandanabhu@gmail.com

Deccan flood basalt eruptions are considered as one of the main causes for the mass extinction of biota at theCretaceous-Paleogene (K-Pg) boundary. The age and duration of the Deccan basalt eruptions are a matter of debate,
however, based on radiometric dating it is presently considered to have spanned 68-62 Ma (Sheth and Pande, 2014).
Earlier studies have indicated that these eruptions were episodic in nature and took place primarily in three phases.
Recently Rene et al (2015) based on their study on Deccan volcanic eruptions of Western Ghat suggested that the
Deccan volcanic eruptive mechanism was affected by the Chicxulub impact at K-Pg boundary after which over 70% of
the total volume of eruption was extruded. This voluminous eruption caused environmental changes resulting in thebiotic turnover. The studies have indicated with Deccan volcanism was initiated in the northwest (Nasik and Narmada
regions including the Saurashtra Plateau) and the terminal phase of eruptions occurred in the south near Belgaum with
the northward drifting of the Indian plate (Jay and Widdowson, 2008). The Deccan volcanic province which covers
vast area in western, central and southern part of India is divided into four groups namely Malwa Group towards thenorth of Narmada river, Satpura Group to the south of Narmada river to the Tapti river and Sahyadri Group to the southof Tapti river in the central and southern part and Amarkantak Group in Mandla lobe. The volcanic flows in thenorth-western part are still unclassified (Nair and Bhusari, 1991).
Palynological study of the Late Cretaceous-Early Paleocene Deccan volcanic associated sediments of western,
central, eastern and southern part was carried out to understand the biodiversity, evolutionary trend, extinction pattern
and paleoecological conditionsat the time of deposition. The study helped in recovery of rich palynoassemblage fromthese sediments. The recovered palynotaxa are grouped into five major groups 1) Palynotaxa characteristic of Late
Cretaceous (Maastrichtian) and could not cross the K-Pg boundary such forms are Azolla cretacea (Salviniaceae),
Ariadnaesporites (Salviniaceae), Crybelosporites (Regnellidium), Triporoletes reticulatus, Cranwellia, Farabeipollis
spp., Proxapertites sulcatus, Scollardia conferta, Scabrostephanocolpites spp., Racemonocolpites maximus, andEchtricolpites sp.2) Taxa remained unaffected during Cretaceous- Paleogene transition and continued in Paleocene
sediments such forms are Ephedripites (Ephedraceae), Spinizonocolpites echinatus (Nypa, Arecaceae), Proxapertites
spp. (Araceae), Ericipites (Ericaceae), Incrotonipollis (Euphorbiaceae),, Echiperiporites (Malvaceae), Sparganiaceaepollenites(Sparganiaceae/ Typhaceae).), Dipterocarpuspollenites (Dipterocarpaceae), Psilodiporites, Proteacidites reticulatus

60Oral Session(Proteaceae), Matanomahiasulcites maximus,Aquilapollenitesbengalensis and Normapolles Group pollen. 3) Taxa
which appeared in Danian and continues in Paleogene are Neocouperipollis, Haloragacidites (Haloragaceae),
Intrareticulites brevis (?Gunneraceae), Palmaepollenites eocenicus, Longapertites vaneendenburgii (Arecaceae), Striatricolporites
striatus, ,4) Taxa exclusively confined to Paleocene (Danian) are Gabonisporis intertrappean, Mulleripollis
bolpurensis, Rhombipollis sp.5) Taxa which became extinct after Danian are Gabonisporis vigourouxii (?Marseliaceae),
Aquilapollenites spp., and Normapolles Group pollen. Overall palynological data from Deccan volcanic associatedshows that palynofloral changes in the terrestrial sequence across Cretaceous- Paleogene were gradual andcommensurate with advent of Deccan volcanism. Many floral elements survived the K-Pg event. Palynological datafrom the marine sections of Krishna-Godavari and Cauvery Basins also shows that extinction was gradual and selectiveat different stratigraphic levels (Prasad and Pundeer 2002).
Herngreen et al (1996) proposed six palynofloristic province namely Aquilapollenites, Normapolles, Palmae,
Proteacidies, Schizaeoisporites and Khatanga-Lena provinces in Late Cretaceous based on distinctive flora and theIndian subcontinent was broadly placed in Palmae province having Normapolles and Aquilapollenites pollen also. The
present study shows that Aquilapollenites pollen grains in overall morphological characters are distinctly different fromthat of the pollen recorded from the Aquilapollenites Province. Although Indian subcontinent is placed in the Palmae
province but overall palm pollen record from the late Cretaceous sediments is very limited. Palm pollen such as
Andreisporis and Constantinisporis are only recorded from the Early Senonian and rarely from the Maastrichtian of
Cauvery Basin and Victorisporis from Senonian-late Cretaceous of Cauvery and Bengal basins. The pollen grains of
Spinizonocolpites (Arecaceae) are widely known from the Senonian to Paleogene sediments of the Indian subcontinent
whereas other palms such as Palmaepollenites spp., Longapertites spp., Neocouperipollis are mostly recorded from theDanian onwards. Overall palynofloral record from the Indian subcontinent is unique having distinct floral composition.
Late Cretaceous evolution and out of India migration of families namely Poaceae, recorded from Nand-Dongargaon
Basin (Prasad et al 2005, 2011), Vitaceae, from intertrappean sediments of Central India (Manchester et al, 2014),
Cocos recorded from the Ghansor, Mandla area (Srivastava and Srivastava, 2014) and Phyllanthaceae from Singpur
intertrappean (Kapgate et al 2017) have already been reported. The present study recorded pollen grains of the families
such as Ericaceae (Ericipites), Euphorbiaceae (Incrotonipollis), Malvaceae (Echiperiporites), Dipterocarpaceae(Clavatricolpites), Sparganiaceae (Sparganiaceaepollenites) and Caryophyllaceae (Periporopollenites)from the Late
Cretaceous (Maastrichtian) intertrappean sediments of central India. This is the oldest record of palynomorphs
associated with these families and suggests out of India migration of these families. The data shows that Deccan
volcanic associated Late Cretaceous-Early Paleocene was significant period in the evolution and extinction ofangiosperm flora. Changing climatic and environmental conditions owing to latitudinal change as well as volcanism
caused evolution and extinction of many angiosperm families on the Indian subcontinent.

61

Oral Session

References
Herngreen G.F.W, Kedves, M., Rovnina, L.V., Smirnova, S.B., (1996) Cretaceous palynofloral provinces: a review
In: Jansonius, J. McGregor, D.C. (Eds), Palynology: Principles and Application volume 3. American
Association of Stratigraphic Palynologist Foundation, Salt Lake City, pp.1157-1188.
Jay, A. E., Widdowson, M., (2008). Stratigraphy, structure and volcanology of the SE Deccan continental floodbasalt province: implications for eruptive extent and volumes. Journal.
Manchester, S. R., D. K. Kapgate, and J. Wen. (2013). Oldest fruits of the grape family (Vitaceae) from the late
Cretaceous Deccan cherts of India. American Journal of
Nair K K K and Bhusari B (1991) Stratigraphy of Deccan Traps: A review; Geol. Surv. India Spec. Publ. 64,
477-491.
Prasad, B. and Pundeer B. S. (2002) Palynological events and zones in Cretaceous-Tertiaryboundary sediments ofKrishna-Godavari and Cauvery basin, India. Palaeontographica Abt. B. 262, 39-70.
Prasad, V., Caroline, A.E., Stromberg, C.A.E., Alimohammadian, H. and Sahni, A. (2005) Dinosaur Coprolites andthe Early Evolution of Grasses and Grazers; Science, 310, 1177-1180.
Prasad, V., Stromberg, C.A.E., Leache, A.D., Samant, B., Patnaik, R., Tang, L., Mohabey, D.M., Ge, S. and Sahni,
A. (2011) Late Cretaceous origin of the rice tribe provides evidence for early diversification in Poaceae. Nature
Communication,v.2, 480/DOI:10.1038/ncomms1482.
Renne, P,R, Sprain, C.J., Richards, M.A., Self, S., Vanderkluysen, L., Pande, K., (2015) State shift in Deccan
volcanism at the Cretaceous-Paleogene boundary, possibly induced by impact. 350,(6256),76-78.
Sheth, H.C. and Kanchan Pande., (2014) Geological and 40Ar/39Ar age constraints on late-stage Deccan rhyolitic
volcanism, inter-volcanic sedimentation, and the Panvel flexure from the Dongri area, Mumbai. Asian Journalof Earth Sciences 84, 167-175.
Srivastava R., and Srivastava, G. (2014).Fossil fruit of Cocos L. (Arecaceae) from Maastrichtian-Danian sedimentsof central India and its phytogeographical significance. Acta Palaeobotanica 54(1), 67-75.
Kapgate, D.K., Manchester, S.R., Wolfgang, (2017). Oldest fruit of Phyllanthaceae from the Deccan Intertrappean
Beds of Singpur, Madhya Pradesh, India. Acta Palaeobotanica 57(1),33-38.

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Paleontology 5

Theropod dinosaurs and mesoeucrocodiles from Pakistan: A review
M. Sadiq Malkani
Geological Survey of Pakistan, Muzaffarabad, Pakistan. E. Mail; malkanims@yahoo.com

Theropod dinosaurs from Pakistan
Vitakridrinda sulaimaniand Vitakrisaurus saraikitheropods (and Saraikisaurus minhuia flying pterosaur, Fig.1) arefound from terrestrial Latest Cretaceous Vitakri Formation of Sulaiman Basin.
Review of Vitakridrinda sulaimani: It is based on a pair of proximal femora, a tooth (embedded in specimen
MSM-61-19) and braincase. More than nine teeth with a few cranial remains embedded in holotypic specimen(MSM-61-19) and tooth and cranial material (un-number), a distal femur and two centra are being added here as
lectotype (Fig.1) because of same site occurrence, same formation and size matching. A pair of proximal femorashow
hollow in the core and stout thick walled bone on the periphery. It shows evidence of inturned head with a distinct
neck. Greater trochanter is well developed and lesser trochanter may be missing or may be lower. Anteroposterior andtransverse diameter of the hollow is about 5 and 5.5 cm. Thickness of peripheral bone is 1cm on the ventral side and2.5cm just below the inturned head. The femoral cross section just below the inturned head is slightly
eccentric/elliptical having the anteroposterior and transverse maximum width as 7.5 and 9.5cm respectively. Distal
femur has hollow cavity in the core with thick peripheral bone on one side but on the other side/ventral side fibrousbone network in the hollow, representing close approach to fibular and tibial condyles. Basioccipital condylelength is
8cm, width is 7.6cm and height is 6.6cm. Anterior view of preserved braincase shows paroccipital process going to be
down on the edges and basipterygoid processes/rami are close to each other forming high angles from the vertical line
forming close v shape. Approximate length of paroccipital process is about 4.8cm and depth is about 3cm.
Ventrodorsal height of basipterygoid processes is about 4 cm. Matrix of its braincase and basioccipitalresemble withthe matrix of holotypic materials of Maojandino alami found close to few meters westward/upward. Mickey Mortimer(personal communication in 2012) conveyed the basioccipital condyle and posterior most part of braincase showsdecurved and much taller paroccipital processes match with titanosaur braincase while the anterior view of paroccipital
processes and basipterygoid processes which is similar in rough outline to Abelisaurus(assuming the supposedbasipterygoid processes are basal tubera instead). Its massive and thick braincase parietal/ dorsal cover matches with
Carnotaurus sastreiand Indosaurus matleyi,its basipterygoid process is high angle while in Indosuchus raptoriusis low
angle (Mickey Mortimer, personal communication in 2012). One D shape toothfound is slightly asymmetrical, laterallycompressed, having low crown (significant character) and extremely low ratio of crown height and rostro-caudal width.

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Tooth anteroposterior breadth is 2.2 cm, labial to lingual depth is about 1.3 cm. Tooth is found embedded in matrix so
possible length seems to be low like 2.2 cm as broad. Nine other teeth with a few cranial remainsare embedded inholotypic specimen (Fig.1). These teeth are heterodont, mostly D shape to some oval, in most of teeth one side isalmost flat and relatively thick cavity and thin bone cover/enamel (significant character) as compared tomesoeucrocodile Induszalim balawhich show relatively thin hollow with thick bone cover. Most of the teeth arelaterally compressed. In most of teeth, the anterior and posterior margins are sharp, lingual side is flat to slightly
convex (asymmetric) outward and labial side is relatively more convex (asymmetric). A few cranial bones like eye
peripheral bone/lacrymal and other trirays star like bone are also found. Centraare cylindrical and articular surfaces areamphicoelous (not platy coelous). Central core of centrum may have sub circular hollow and peripheral thick bone.
Referred three vertebrae(Fig.1) are cylindrical to sub cylindrical, amphicoelous (not platycoelous), horizontal toslightly waisted and lack pleurocoel. Neural arch is located on the anterior part of centrum. Articular surfaces are
expanded, while the mid centra are slightly reduced. Neural canal is subrounded. Prezygapophyses are subcircular.
Referred whiplash type amphicoelouscaudal centrumis long and slender. It is 11 cm long and 3-4cm wide. Limbboneshows central hollow and thick peripheral bone (Fig.1).
Review ofVitakrisaurussaraiki: It is based on isolated hand/ manus collected Bor locality. The other materials foundin Bor locality being included as lectotype like four vertebrae and leg bones (Fig.1). The relative size of lectotype isalso fit with holotypic hand (previously diagnosed as pes). Previously lectotype material was referred to Vitakridrinda.
The manus seems to be tridactyl. Phalanges are robust. There are three preserved digits. The digit II has partial
metacarpal II (robust and elongate), phalanx II-1, phalanx II-2, hand toe II. The digit III has preserved partial
metacarpal, possibly three phalanges and one toe shown by some bone remains with impressions, extended ahead justbelow the end of digit I. The digit IV may have 4 phalanges and one toe but only 1 phalange is preserved in therelevant row while other phalanges and toe may be found in the matrix just below these 3 digits. Many smaller boneand phalanges of digit IV are found just below the digit II. The phalanges are elongated having well developed
expanded articular surfaces/ condyle. In general the width of phalanges is about 7mm while length is about 21mm(modified after Mickey Mortimer, personal communication in 2012).The holotypic manus and lectotypic fossils
revealed large abelisaurian theropod. Many smaller bone and phalanges are found just below the claw, which may be
the bones of left hand of Vitakrisaurusor may belong to birds or other flying reptiles like pterosaur. The vertebraeare
tall, thin, amphicoelous (not platycoelous but slightly inward concave), waisted and lack pleurocoel. Articular surfaces
are highly expanded, while the mid centrum width and height are reduced. Neural arches are found on the anterior of
caudal centra. Prezygapophyses process seems to be thin and slender while the postzygapophysis is robust and short.
The prezygapophyses process is oval to subcircular shape in cross sections. On the posterolateral side it has articular
facet for the relevant prezygapophysis. Neural canal cross sectional shape is diverse variable from rectangle to64Oral Session

suboval/subcircular. The rectangle shape neural canal base transverse width is more than dorsal anteroposterior width.
The transverse base of neural canal is convex upward in the middle i.e. concavity in the ventral view. The ventrodorsal
width of neural canal is equal with each other and converging upward due to relatively less upper width. In somevertebrae the neural canal is large and subcircular. The leg bones show thick peripheral bone and central hollow/cavity(Fig.1).
Mesoeucrocodiles from Pakistan
The Cretaceous fresh waterPabwehshi pakistanensis, Sulaimanisuchus kinwai and Induszalim bala, and marine
Khuzdarcroco zahri, andOligocene Asifcroco retraicrocodiles found in Pakistan. Review of Sulaimanisuchus kinwai: It
is first described by Malkani in 2010. It is afresh water mesoeucrocodilebased on holotypic anterior dentary withsplenial found from Kinwa. Tibia (Fig.1) is being added here as lectotype because found on the same horizon, samesite and same locality.
Review of Induszalim bala: It is first described by Malkani in 2014 and formally published by Malkani in 2015.
ItisInduszalimine Induszalimid Mesoeucrocodile based on rostrum. Two vertebrae, one proximal humerus and one
distal humerus are being added here as lectotype (Fig.1) due to finding in the same site and same formation. The
relative size is also fit. Further one vertebra is being referred. This crocodile was a big terrible, terrestrial fresh water(river) predator and scavenger. The holotypic rostrum shows anteriorly and anterodorsally directed external nares, very
high and deep and narrow rostrum, ziphodont type laterally compressed teeth (oval to D shape, heterodont in size), andthick rostral elements. Lectotypic vertebra has amphicoelous articular surfaces. Its centrum is long and slightly tall.
The anterior and posterior articular surfaces are not equal. It is strongly waisted and shows ventral longitudinal groove.
This vertebra has anterior prezygapophyses. Some parts of postzygapophysis and neural spine are preserved. Neural
canal is subcircular. Its centrum width is 1.3cm, height is 1.5cm and length is 2.3cm. Distal humerus/femur showspreserved distal length 7cm, distal condyles width 3.5cm and depth 2.5cm. One condyle is greater in size than other.
The greater condyle width is 2.6cm and depth is about 2cm while smaller condyle width is 1.8cm and depth is 1.5cm.
Cross section of shaft is elliptical and maximum on the distal condylar part and decreasing toward the proximal centreof shaft. The shaft is curved/sigmoid. The referredvertebra may be dorsal because big in size than lectotypic vertebra.
Its centrum is long, slightly tall, waisted and amphicoelous. Its width is 1.7cm, height is 1.9cm and length is 2.9cm.

65Oral Session

66Oral Session

Paleontology 6

Calcareous Nannofossil Biostratigraphy of the Cretaceous Yop Formationin Catanduanes Island, Philippines✳

Mirko Alessandro C. Uy1, ․ Allan Gil S. Fernando1 ․ Adrian Raymund C. Fernandez2
1

Nannoworks Laboratory, National Institute of Geological Sciences, University of the Philippines,
Diliman, Quezon City, Philippines 1101, mcuy2@up.edu.ph2
Partido State University, Goa, Camarines Sur, Philippines 4422

Catanduanes is one of the provinces in the Philippines with identified Cretaceous rock units. Its stratigraphy iscomposed of Cretaceous to Neogene sedimentary sequences and an Oligocene intrusive unit. Recent geologic mappingin the northeastern part of the island recognized a previously undocumented outcrop of dark sandstone and mudstoneinterbeds which was tentatively assigned to the Yop Formation based on its Cretaceous age (Guballa et al., 2014). Yop
Formation, a sequence of volcanic and volcaniclastic rocks intercalated with clastic rocks, is considered the basementof the island. Calcareous nannofossil investigation of several samples collected from the outcrop assigned thesandstone-mudstone interbeds within the middle Cretaceous (Fernando et al., 2016). To further refine the age of theinterbeds, higher resolution sampling was conducted for a more detailed nannofossil biostratigraphic study.
Preliminary analysis of the high resolution samples revealed moderate to poorly-preserved nannofossils. The
samples, in addition, contain few to common nannofossils dominated by Watznaueria, Eprolithus, Rhagodiscus, andZeugrhabdotus. Based on the presence of Helenea chiastiaand Rhagodiscus asper, the UC5 zone (latest Cenomanian toearliest Turonian) is recognized, similar to the result of a previous study in the area (Fernando et al., 2016). Other
nannofossil taxa observed in the samples includeRetecapsa spp., Rhagodiscus achlyostaurion, Rhagodiscus asper,
Tranolithus gabalus, and Zeugrhabdotus diplogrammus.The nannofossil data will be used to infer the paleoceanographic
and paleoclimatic conditions of the section during the Cretaceous.
References
Guballa, J. D. S., Callejo, G. P., Castro, A. L., Crisologo, I. A., Geronia, M. M., Grajo, M. P. A., Lagura, M. L. H.,
Llanes, F. V., Magtoto, C. Y., Marquez-Ardiente, D. J. D., Nogot, J. R. C. P., Pena, M. A. Z., Rosario, D. J. G.,
Sabado, J. M. J., Supnet, K. M., Tupaz, C. A. J., Peleo-Alampay, A. M. and Fernando, A. G. S. (2014). The
geology of Catanduanes: Revisited. Abstract volume of the 2014 Geological Convention of the GeologicalSociety of the Philippines, Makati City, Philippines, 31.
Fernando, A. G. S., Magtoto, C. Y., Guballa, J. D. S., Peleo-Alampay, A. M. (2016). Calcareous nannofossils from
Cretaceous units in Catanduanes Island, Philippines. Bulletin of the National Museum of Nature and Science,
Ser. C., 42, 1-13.

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Paleontology 7

Microfossils along Kinabuan Creek, Sta. Ines, Tanay, Rizal Province,
Philippines: evidence of Cretaceous-Tertiary boundary✳

Maybellyn A. Zepeda1, ․ Elsa Y. Mula1 ․ Kevin Bien D. Tee1 ․ Nilo Lemuel J. Dolojan2 ․ Byron V. Baldivicio2 ․ Fidel R. Zepeda2
1

Lands Geological Survey Division, Mines and Geosciences Bureau, North Avenue,
Diliman, Quezon City, PHILIPPINES, mazepeda1014@yahoo.com
2
Geosciences Division, Mines and Geosciences Bureau Region IV- CALABARZON,
1515 DENR Bldg., Roxas Blvd. Manila, PHILIPPINES

Extended Abstract
Recent studies on the microfossils of the lithologic sequences exposed along Kinabuan Creek, a tributary of Lenatin
River in Sta. Ines, Tanay, Rizal Province, revealed the occurrence of planktonic foraminifera spanning the Late
Cretaceous to early Cenozoic (Paleocene-Eocene) interval.
The Late Cretaceous is marked by the identification of the planktonic foraminiferal Abathomphalus
mayaroensisZone representing the end of the Cretaceous Period (latest Maastrichtian stage). The Zone is characterized
by the presence of Abathomphalus mayaroensis, the marker species, Gobotruncanita stuartiand Racemiguembelina
fructicosa. The early Cenozoic interval is recognized based on the planktonic foraminiferal assemblages assigned with
Paleocene-Eocene age.
The recognition of some species of Heterohelixin lithologic sequence of early Cenozoic age could possibly establish
the Cretaceous-Tertiary boundary (KTB) in the area since numerous studies have shown that KTB are characterized by
the presence of heterohelicid groups which occur during the Late Cretaceous and appear to have survived into the early
Cenozoic (Danian stage).
The KTB in the Philippines are oftentimes missing probably due to tectonic and/or erosional processes thus, therecent findings will proved to be the first established evidence of KTB in the Philippines that will provide new insights
and great implications in the geotectonic development of the region.
Introduction
The present study aims to refine the stratigraphy of the area and determine possible Cretaceous-Cenozoic
boundaries which were not yet fully established in the Philippines due to lack of good exposures and in-depth studies.
The Cretaceous-Cenozoic (also known as K/T) boundary refers to the transition between the Cretaceous and Cenozoic
periods of geologic time characterized by mass extinction of many forms of life (nearly three-quarters of plant andanimal species on Earth including the dinosaurs) occurring over a geologically short period of time, 66 million years

68Oral Sessionago. It marked the end of the Cretaceous period and with it, the entire Mesozoic Era, commencing the Cenozoic Era
that continues today.
The lithologic sequences in southern Sierra Madre within the Rizal Province presents an ideal study area sinceCretaceous and Cenozoic rocks are prominently distributed in the region. The Cretaceous rocks characterized by the
Barenas-Baito and Kinabuan formations constitute the oldest rocks in Rizal Province. They are considered to be thevolcanic carapace and sedimentary cover, respectively of the incomplete ophiolitic sequence called Angat Ophiolite.
On the other hand, Cenozoic sequences are represented by the Maybangain, Binangonan, Angat, Madlum andGuadalupe formations and Quaternary Alluvium. Specifically, exposures along Kinabuan Creek in Brgy.Sta. Ines
makes it a good section for K/T boundary studies since earlier works reported the occurrence of Cretaceous andPaleogene microfossils in these areas.
The study areas are situated in southern Sierra Madre within the Province of Rizal covering Kinabuan Creek andLenatin River in Barangay Sta. Ines (14°45’35.6”N/121°19’05.4”E). Specifically, Kinabuan Creek (Figure 1) is locatedon the lower portion of Mt. Irid Quadrangle. Sampling points were plotted down on topographic maps of 1:50,000
scale and observations were noted especially the descriptions, orientations and locations of the outcrops as well as the
structures found in the field.

Fig. 1. Locality of map of the study area.

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References
Bureau of Mines and Geoscience, 1981, Geology and Mineral Resources of the Philippines, vol. 1 (Geology), BMG,
Ministry of Natural Resources, Manila, 406 p.
Duyanen, J.P, 1988, Stratigraphy and sedimentology of the Upper Cretaceous to Middle Tertiary Sequences ofNortheastern Tanay, Rizal Province, MS Thesis, UP-NIGS, 51 p.
Haeck, G.D., 1987, The geological and tectonic history of the central portion of the southern Sierra Madre, Luzon,
Philippines, PhD Thesis, Cornell University, Ithaca, 311 p.
Hashimoto, W., Ariate, E., Aoaki, N., Balce, G.,Ishibashi, T., Kitamura, N., Matsumoto, T., Tamura, M., andYanagida, J., 1977, Cretaceous System of Southeast Asia, Journal of the Geological Society of the Philippines,
vol. 61, nos. 1-4, p. 14-18.
____________, Kitamura, N., Balce, G.R., Matsumaru, K.,Kurihara, K., and Ariate, E., 1979, Larger Foraminiferafrom the Philippines, Pt. X. Stratigraphic and faunal breaks between the Maybangain and Kinabuan Formationsin the Tanay Region, Rizal, Philippines, In: T. kobayashi, R. Toriyama and W. Hashimoto, (eds), Geology andPaleontology of Southeast Asia, vol. 20 p.p 143-157.
ndMines and Geosciences Bureau, 2010, Geology of the Philippines, 2 edition(Aurelio,M.A.andPeña,R.E.,eds),532p.
Peña, R.E., 2008, Lexicon of Philippine Stratigraphy, The Geological Society of the Philippines, 364p.
Revilla, G.P., 1988, Geology of Southern Sierra Madre, Phil. Bureau of Mines and Geosciences, unpublished, 25-29 p.
Reyes, M.V. and Ordoñes, E. P., 1970, E.P., Philippine Cretaceous smaller foraminifera, Journal of the GeologicalSociety of the Philippines, 24 (2), 1-13.
Santiago, P., 1982, Paleocene Planktonic Foraminifera (Reworked) in Maysawa Creek, Lenatin, Tanay, Rizal, BMG,
unpublished report.
Ringenbach, J.C., 1992, La Faille Philippine et les châines en décrochement associés (centre et nord de Luzon):
Evolution cénozoique et cinématique des déformations quaternaire. (Doctoral Thesis; Univ. de Nice, 316 p.

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Paleontology 8

Tarbagatay dinosaur locality: flora, environments, and geological age✳

E.V. Bugdaeva ․ V.S. MarkevichFederal Scientific Center of the East Asia Terrestrial Biodiversity, Far Eastern Branch of Russian Academy of Sciences,bugdaeva@biosoil.ru

Introduction
The Tarbagatay Basin is located in the west of the Transbaikalian Region in the valley of the Khilok River, between
the ridges of Tsagan-Khurtei and Yablonovy. This basin is filled with sedimentary strata, united in the Doronino andTignya formations. The Doronino Formation is composed of siltstones and mudstones with thin sandstone interlayers.
Its thickness is 400-500 m. The Tignya Formation conformably lies on the former stratigraphical unit and ischaracterized by a variety of facies and lithological composition. Sandstones, siltstones, gravelites prevail,conglomerates, argillites, carbonaceous argillites and coals (often having industrial thickness) are less common. The
thickness of the Tignya Formation is from 860 to 950 m. The abundant remains of mollusks, conchostracans,ostracods, insects, and fish occur here. This limnetic fauna evidences the lacustrine environments.
In 1912 the mining engineer K.F. Egorov found in the Tarbagatay coal mine and delivered to the GeologicalMuseum of the Imperial Academy of Sciences the fragments of fish and dinosaur bones. I.P. Tolmachev passed thesefossils for study to the Russian vertebrate paleontologist A.N. Riabinin. According to this researcher, the sample fromthe roof of the first coal seam is the vertebra of a fish of indeterminable affinity, the specimen from the roof of thesecond coal seam is the "hollow bone of the dinosaur's posterior limb" (Riabinin, 1915, p. 133). He described it as
Allosaurus(?) sibiricusRiabinin and compared to the dinosaurs of North America, coming to the conclusion about theLate Jurassic age of the Transbaikalian find.
The age of the Tignya Formation at the present time is considered as the beginning (?) or the middle (?)
Aptian-Albian (Decisions ..., 1994).
Material And Method
The vertebrate paleontologist Yu.L. Bolotsky (Institute of Geology and Nature Management FEBRAS) sent us thepiece of sandy siltstone with fish remains collected from the roof of coal seam of the Tarbagatay coal quarry. The local
geologist of the Open Joint Stock Company “Tugnuy Coal Mine” sampled for us the specimens of coals from the same
quarry.
We used these samples for spore-pollen analysis and for revealing of dispersed cuticles from the coals. The

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Oral Session

palynological samples were processed using a standard method. For the purpose of floral analysis, spores and pollen
were united into the main groups: (1) Bryopsida and Lycopsida; (2) Dicksoniaceae and Cyatheaceae; (3) Schizaeaceae;(4) Ginkgocycadophytus; (5) bisaccate pollen of conifers close to Pinaceae; (6) Araucariaceae; (7) Taxodiaceae; (8)others, including representatives of other groups of ferns, as well as Podozamitaceae, Cheirolepidiaceae, andangiosperms.
The coals were treated with nitric acid and alkali and further washed out with distilled water to extract thephytoleims. The mounts with disperse cuticles were prepared for study under an Axioscop 40 optical microscope
equipped with an Axiocam HRc camera and on an EVO 40 SEM (Carl Zeiss).
The coal-forming plants were revealed directly from the coal beds. We consider that they grew at the place of thepeat deposition and supplied phytomass to unambiguously hypoautochtonic burial at mostly biogenic rather thanterrigenous sedimentation. Because the clastic rocks represent the transported material from the runoff areas, the mixed
composition of thetaphocenoses includes the remains of both depression and slope plants.
Results
It was revealed very representative palynospectrum from the sandy siltstone, collected from the roof of a coal seam..
It is dominated by bisaccate pollen (Vitreisporites oncodes, Podocarpidites multesimus, Abiespollenites sp.,Alisporites
aequalis, A. similis, Rugubivesiculites aralicus, Piceapollenites mesophyticus, Cedruspollenites parvisaccatus,
Protocedrus cenomanicus, and indeterminable pollen grains). Its percentage is 52.62%. In the second position Araucariaceae (8.62%), on the third - Ginkgocycadophytus(6.77%). Next in significance - pollen of Taxodiaceae(4.31%).
The content of spores of ferns in this palynospectrum reaches 18.16%. They are represented by Osmundacidites
nicanicus, O. wellmanii, Impardecispora variverrucatus, Concavissimisporites asper, Pilosisporites setiferus,
Laevigatosporites ovatus, Leiotriletesspp., Tripartina variabilis. Spores of the lycophytes (Leptolepidites verrucatus,
Densoisporites vellatus, Taurosporites reduncus) form an insignificant part of the spectrum - 4.62%.
The group "Others" includes representatives of Osmundaceae, Laevigatosporites, Cheirolepidiaceae,
Podozamitaceae, and angiosperms.
A feature of the spectrum is the abundance of spores of freshwater green algae (Schizosporis reticulatusCookson etDettman) and phytoplankton Scatula baccataChlonova.
Previously, from the deposits of the Tarbagatay coal mine, such fossil plants as Sphenopteris tenuissimaPrynada,
Scleropteris tarbagataicaPrynada, S. dahuricaPrynada, Czekanowskia vachrameevii Kiritch et Samyl., Podozamites
eichwaldiif. minorSchimp. were described (Prynada, 1962; Kiritchkova, Samylina, 1984). Dispersed cuticles, revealed72Oral Session

from the coals of this quarry, are well preserved, which makes it possible to study them using light and scanningmicroscopes. It was recognized: Pseudotorelliasp. (abundant), Anomozamitessp. (rare), Czekanowskiales sp.ind. (rare),Ginkgocf. insolita Samylina (common), G. cf. coriaceaFlorin (common), Pityophyllumsp.1. (common),
Pagiophyllumsp. (rare).
geological age
The abundance of palynomorphs allows us to draw conclusions about the age. Such taxa as Taurocusporites
reduncus, Osmundacidites wellmanii, Pilosisporites setiferusare characteristic of the Aptian palynofloras of Siberia andthe Far East of Russia (Markevich, 1995, Bolkhovitina, 1953, Verbitskaya, 1962). The single pollen of angiosperms
Tricolpitessp. was identified in palynospectrum. The similarity of this obtained spectrum with the palynologicalassemblage from the Baisa locality (Zaza Formation, the Barremian-Aptian) is expressed in common dominants, aswell as in the presenceof single angiosperm pollen. In the deposits of the Tarbagatay coal mine, Czekanowskia
vachrameeviiwas also found, this taxon is characteristic of the Zaza Formation of Central Transbaikalia.
In our opinion, the age of the bone-bearing beds of the Tarbagatay coal mine is the Aptian.
Paleoreconstructions
Based on the data of palynological analysis, it can be assumed that the territory of the Tarbagatay Basin was
occupied with the lake with marshy banks surrounded by a ginkgo-coniferous forest having an understory consisted oflycophytes, ferns, and cycadophytes. On higher places, perhaps, araucariaceous and cheirolepidiaceous plants grew. It
is possible that in the mouths of the rivers flowing into the lake the taxodialeans inhabited. The water of this lake wasoverfilled with phytoplankton and green algae.
Acknowledgments
Our study was supported by the Russian Foundation for Basic Research (grant 17-04-01582).
References
Averianov, A.O., Skutschas, P.P., 2009. Additions to the Early Cretaceous Dinosaur Fauna of Transbaikalia, Eastern
Russia. Proc. Zoological Institute RAS 313 (4), 363-378.
Bolkhovitina, N.A.,1953. Spore-pollen characteristic of the Cretaceous deposits of the central regions of U.S.S.R.
Proc. Institute of Geological Sciences AS of U.S.S.R 145 (61). Moscow: Izdatelstvo AS of U.S.S.R, 183 p. [inRussian]Prynada, V.D., 1962. Mesozoic flora of Eastern Siberia and Transbaikalia. Moscow: Gosgeoltekhizdat. [in Russian]73

Oral Session

Decisions of IVth Interdepartment Regional Stratigraphic Conference on Precambrian and Phanerozoic of the SouthFar East and Eastern Baikal Region (Khabarovsk, 1990): Explanatory Note to Stratigraphic Schemes(Khabarovsk, KhGGGP, 1994). [in Russian]Riabinin, A.N., 1915. Note about a dinosaur from Transbaikalia. Proceedings of the Peter the Great GeologicalMuseum of the Imperial Academy of Sciences. 8 (5). Geological series (# 61). Petrograd: A.F. Dresler'sPrinting House, 133-140. [in Russian]Verbitskaya, Z.I., 1962. Palynological Evidence and Stratigraphical Subdivision of Cretaceous Deposits of the
Suchan Coal Basin, Moscow: Izdatelstvo AN SSSR. [in Russian]
Kiritchkova A.I., Samylina, V.A., 1984. A new species of the genus Czekanowskiafrom the Lower Cretaceous ofTransbaikalia. Botanicheskiy Zhurnal (Botanical Journal). 69 (1), 99-100. [in Russian]
Kotova, I.Z., 1964. The age of the continental deposits of the Gusinoozerskaya depression and features of the Early
Cretaceous floras of Transbaikalia. Izv. Akad. Nauk, Ser. Geol. (8), 84-93 [in Russian]Markevich, V.S., 1995. Cretaceous Palynoflora of the Northern East Asia. Vladivostok: Dalnauka, 200p.[inRussian].
Nessov, L.A., Starkov, A.I., 1992. The Cretaceous vertebrates from Gusinoozerskiy Basin of Transbaikalia and theirsignificance for age definition and conditions of formation of deposits. Geology and Geophysics (6), 10-18 [inRussian]Skoblo, V.M. Lyamina, N.A. Rudnev, A.F., Luzina, I.V., 2001. The Continental Upper Mesozoic of the Pribaikalia
and Transbaikalia (stratigraphy, depositional environments, correlation). Novosibirsk: Publishing House of the
SB RAS, [in Russian]74

Oral Session

Paleontology 9

New palynological data from infratrappean beds of Deccan Volcanic Province,
central Peninsular India: implications for late Cretaceous paleogeographyof and early history of angiosperm diversification✳

Sunil Bajpai ․ Vandana Prasad ․ Anjum Farooqui ․ Srikanta Murthy ․ O.S. Sarate
Birbal Sahni Institute of Palaeosciences
Lucknow, INDIA

Recent palynological investigations of infratrappean sediments from a borehole succession located in the Ashtona
village, Yeotmal District, Wardha basin in the Maharashtra state of western India, have provided important insights into the early history of angiosperm diversification relative to the Cretaceous-Paleogene (K-Pg), transition, as well as on
the late Cretaceous paleogeography of peninsular India. The study revealed a Maastrichtian palynological assemblage
consisting of several species of triprojectate pollen (Aquillapollenites, Jigansupollis), Azolla cretacea, Gabonisporissp., Scollardia conferta together with the marine dinoflagellate Pierceitessp. A rich and diverse assemblage ofangiosperm pollen of tropical nature was recovered. Numerical abundance of the mangrove pollen Spinizonocolpites
pollen (Nypa), and a large number of dinoflagellate cysts (Pierceites sp.) indicate a brackish marine depositionalsetting close to low-lying coastal rain forests in central India during the late Cretaceous. Furthermore, the new
evidence strongly suggests the existence of a shallow marine embayment in central India during the late Cretaceous,which extended from the east coast through the Godavari rift zone, thus adding significantly to the previously
described marine signatures from the late Cretaceous sequence of Rajamundary area on the south-eastern coast of
peninsular India. Additionally, the recovered assemblage includes fossil palynomorphs of the family Dipterocarpaceae.
Together with the arecaeous palm Pigafetta, the late Cretaceous fossil pollen of Dipterocarpaceae provides compelling
evidence for the evolution of these tropical rain forest elements in peninsular India and their dispersal to SE Asia after
the initiation of India-Asia collision, consistent with the Out of India hypothesis. Furthermore, the new palynomorph
assemblage has important implications for our understanding of floral response to the initiation of Deccan volcanism.

75Oral Session

Paleontology 10

Fossil liverworts from the Lower Cretaceous in Inner Mongolia, China✳

SUN Bainian1, ․ LIRuiyun1,2 ․ JIN Peihong1 ․ MA Fujun1 ․ YANDefei11School of Earth Sciences, Lanzhou University, Lanzhou 730000, China
Northwest University Museum, Northwest University, Xi’an 710069, China

2

Bryophyte is the second largest group in the plant kingdom. The simple plant lacks lignified tissue and has no or avery thin cuticle. Bryophyte is spore-producing, rather than seed-producing. In addition, the plant exhibits analternation of generations between the independent gametophyte generation and the dependent sporophyte generation.
Bryophyte contains three linkages: liverworts, mosses and hornworts. The liverwort is considered one of the earliest
divergent land plants. Fossil liverwort is important in shaping the paleoecosystem in earth’s history, and is significant
in understanding the origin and evolutionary history of land plants and terrestrial ecosystems. However, liverworts areherbaceous and delicate in texture. They are presumably susceptible to mechanical damage and biological degradationcompared to the vascular plants.
Fossil liverworts in this paper were collected from the Lower Cretaceous Huolinhe Formation of Huolinhe Basin,
Inner Mongolia, northeastern China. The fossil liverworts were classified and identified according to the generalmorphology and the anatomical features. Blasiites, Marchantites, Rebouliothallus and Ricciopsis are the main genera
from the Huolinhe Formation.
Stable carbon isotope composition (δ13C)ofMarchantites huolinhensiswas measured. The paleoatmospheric CO2
concentration of the early Early Cretaceous was reconstructed using the BRYOCARB model. According to the
distribution of the related living species of the fossil liverworts, the paleoclimate of Huolinhe Basin in Inner Mongolia
at the early Early Cretaceous is humid and warm. The fossil liverwort can be considered as a proxy of paleoclimate.
The rare fossil liverwort records in the Early Cretaceous floras of China may be the result of taphonomic bias.
Key words: fossil liverwort, paleoclimate, Early Cretaceous, Inner Mongolia
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), and the National Natural Science Foundation ofChina (Grants 41172022).

76Oral Session

Paleontology 11

Fossil vertebrate assemblages from the Late Cretaceous Tamagawa Formationof Kuji City, Iwate Prefecture, eastern JapanRen Hirayama
School of International Liberal Studies, Waseda University, Tokyo, JapanThe Tamagawa Formation in Kuji Group of Kuji City, Iwate Prefecture of northeastern Japan is the richest
geological unit bearing the Late Cretaceous terrestrial vertebrates as wellas numerous ambersin this country. More than
one thousand vertebrate fossils have been found from about the 20 cm thick coaly mudstone layer and overlying 1 m
thick marine sandstone bed of the Tamagawa Formation since 2005. Fission track dating carried about the volcanic tuff
layer inter-bedded between the mudstone and marine sandstone units indicates the Turonian age of Late Cretaceous (Y.
Tsutsumi, in preparation).
Sharks (Elasmobranchs) are known by 150 isolated teeth of Scapanorhynchus,Cretolamna, Cretodus, Protolamna,
and Schlerorhynchidae, as well as vertebrae and presumed coprolites from the sandstone bed.
Turtles (Order Testudines) are the most abundant vertebrates (514 specimens in total), identified as the genus
Adocus (Adocidae), Trionychidae, Nanhsiungchelyidae, Lindholmemydidae, and Carettochelyidae. Most of turtle
remains are isolated shell elements, whereas few cranial and appendicular materials were collected. Adocusfrom theTamagawa Formation seems the most derived species of this genus in the possession of extremely wide marginal scales
and the loss of cervical scale of carapace. Largest specimen of Adocusin this locality suggests an individual with 70 cm
long shell. Crocodiles (Order Crocodyliformes) are next abundant group (116 specimens in total). Its amphicoelous
vertebrae, osteoderms and dental morphology suggest they were the member of neosuchian grade, possibly close to thegenus Paralligator. Twenty six isolated almost cylindrical teeth of sauropods (Order Saurischia) have been collected,
whereas other dinosaurs (Theropoda and Ornithischia) are known by few limb bones and isolated teeth. A wing digitalbone of medium size pterosaur (Order Pterosauria) was found in 2010. Two isolated vertebrae from the sandstone bed
are identified as the first known Choristodera from Asia during the Late Cretaceous.
All terrestrial vertebrate fossils from bone bed inter-bedded by marine sandstone layers except three partiallyarticulated turtle shell of Adocusare isolated and fragmentary. This occurrence suggests they were transported by river
stream near the mouth. Abundance of sauropod teeth seems unique as the Late Cretaceous biota.
Fauna and flora of the Kuji Group is one of the most expectable examples of both non-marine and marinevertebrates of the Late Cretaceous in Japan. This excavation will continue for coming years for more plentiful results.
Many people helped me for this paleontological research of the Tamagawa Formation. I would like to especially

77Oral Session

thank to the following people: Toshio Takisawa (Kuji Amber Museum, Kuji, Japan), Kazuhisa Sasaki (Kuji City
Office, Kuji, Japan), Teppei Sonoda (Fukui Prefectural Dinosaur Museum, Katsuyama, Japan), Masataka Yoshida(Graduate School of Science, the University of Tokyo, Tokyo, Japan), Ai Ito (Graduate School of Science, theUniversity of Tokyo, Tokyo, Japan), Shunsuke Mitsuzuka (Nippon Koei Co., Ltd., Shizuoka, Japan), Yoshitsugu
Kobayashi (Faculty of Science, Hokkaido University, Sapporo, Japan), Takanobu Tsuihiji (Faculty of Science, theUniversity of Tokyo, Tokyo, Japan), Ryoko Matsumoto (Kanagawa Prefectural Museum of Natural History, Odawara,
Japan), Mariko Kurosu (China University of Geosciences, Beijing, China), Yuji Takakuwa (Gunma Museum of Natural
History, Tomioka, Japan), Shinya Miyata (Josai University, Tokyo, Japan), and Yukiyasu Tsutsumi (National Museumof Nature and Science, Tsukuba, Japan).

78

Oral Session

Paleontology 12

Palaeontological, Palaeoecological and Palaeobiogeographical studies of
the Cretaceous inter and infra-trappeans around Naskal, Gowripatnamand Devarapalli areas of Southern India - It’s significance in deciphering
the Cretaceous Ecosystem of Asia✳

Nidhi Misra1, ․ Ch. Venugopal Rao2 ․ V. Chakravarthy3
1

Senior Geologist, Geological Survey of India Training Institute, Hyderabad, India, nidhimisra5@gmail.com
2
Dy. Director General (Retd.), Geological Survey of India, Hyderabad, India
3
Senior Mineralogist, Geological Survey of India, Hyderabad, India

India has several Cretaceous geological records containing well-preserved signatures of environment and ecosystemof the past. Palaeontological, palaeoecological and palaeobiogeographical studies were carried out to decipher thevariations and evolution of Cretaceous terrestrial and marine environments in inter and infra-trappean horizons ofDeccan volcanism episode around Naskal in Telangana state and in Gowripatnam and Devarapalli in Andhra Pradesh
state of Southern India. The objective of the research investigation was to collect the fossil assemblage; study the age,environment and stratigraphic significance of the individual forms as well as the assemblage; carry out stratigraphic
correlation and to work out the Cretaceous-Tertiary boundary.
Geological studies, section measurements, systematic collection of sediment samples and fossils yielded rich anddiverse marine and non-marine invertebrate fauna and micro-fossils from the study area. These include Turitellassp.
(Fig. 1), Cerithiumsp., Physassp. (Fig. 2), (including silicified internal cast from mould) Lymnaeasp. (Fig. 3),
Viviparussp., Carditasp., other Gastropods and Bivalves along with some carbonaceous vegetative imprints. Processingof the collected sediment samples yielded micro fossils like Ostracodes (Podocopan Ostracodes, Paracypretta jonesi,etc), Chara ssp., juvenile forms of Gastropods and Bivalves, etc. Detailed analyses of the micro fossils were carried out
with the aid of SEM studies.
The inter-trappean sediments in Naskal and adjoining areas yielded silicified internal cast from mould of Physa ssp.;
Lymnaeasp.; other juvenile forms of gastropods and bivalves; Ostracodes (Fig. 4-5); Chara ssp, (Fig. 6);vegetation
debris imprints, etc. These findings coupled with the earlier reported occurrences of Gondwanatherium (Das Sarma,et.al., 1995), Deccanolestes (Prasad and Sahni, 1988), Dinosaur bones (Rao and Yadagiri (1981), etc. suggest an Upper
Cretaceous age for these sediments (probably Campanian-Maastrichtian).
Physassp. have good tolerance towards environmental toxicity and can withstand a wide variety of aqueousconditions. They are therefore geographically widespread. Benthic community structure is a reflection of theenvironment. Lymnaeasp. are in scanty numbers due to their intolerance of elevated temperature conditions of79

Oral Sessioninter-trap horizons of uppermost Cretaceous (warmest period of Phanerozoic) times.Presence of Pulmonates (lungbearing gastropods adapted to wider ecological tolerances) and absence of Prosobranchs (gill bearing forms which
require more stable perennial lake conditions) - is suggestive of intermittent periods of desiccation.The existing
members of Charophyceae are ecologically sensitive and grow submerged in fresh standing water upon a muddy or
sandy bottom. In most fresh water lake environments - the sediments to a large extent are composed of Charophyte andOstracodes. The species of Ostracoda (Paracypretta jonesi)are fresh water having wide distribution in standing waterrich in rooted vegetation, algal mats, mud and sand.Taphonomic study of the SEM photomicrographs suggests
attritional accumulation of fauna. The assemblage has possibly resulted from instantaneous death of the animals due todesiccation of lakes during drought condition. The fresh water lacustrine fauna suggests deposition in low lying,shallow, wind sheltered,alkaline lakeswith moderate to heavy vegetation cover. The area also had muddy and marlyflats at some places which were subjected to sub aerial exposure and drought conditions intermittently.
Basaltic flows equivalent to Deccan Traps are exposed in patches in the Krishna-Godavari basin between Pangidi
and Kateru over a distance of 50 km. In Gowripatnam and adjoining areas inter-trappean sediments exhibit weatheredsoil profiles (palaeosols) with limestone beds denoting a distinct time gap during various phases of lava eruption(Keller, 2014). The fossils collected from Gowripatnam, Devarapalli and adjoining areas during the present fieldworkinclude Molluscs (both Bivalves and Gastropods) and marine microfossils. Gastropods are represented by
Cerithiumsp., Turitellassp., etc. and Bivalves by Ostreasp., Carditasp, etc.
Oysters (Fig. 7) are one of the most common fossils in the late Cretaceous sediment horizons. They are fairly wellpreserved which indicates that they were an important fauna in the Late Cretaceous marine biota. The changes in oyster
shells (in form, shell-mass and stability) are useful for palaeo-geographic reconstruction (Ivanov, 2000). They indicate
shallow water, high energy conditions, sandy substrates and near shore conditions as the depositional environments(Badve and Ghare, 1978).The osteriids are suggestive of the transgressive nature of the deposition of sediment andoccupy the new environmental niche created by the incursion of sea on to land. Oysters are known to be marine
shallow water inhabitants in the present. Oyster shells indicate the beginning of marine sedimentation in the area,
probably inundation of the palaeo-shoreline. The absence of fossil shells in presumed live position indicates sometransportation before burial. Worn out shells indicate transportation before burial in gritty horizon.
One of the criteria used to deciphering the base of upper Maastrichtian is the extinction of the majority of
inoceramids and rudist reefs (Govindan, 2000). Ammonites and Inoceramushave not been reported from infra andinter-trappean sediments from Gowripatnam and Devarapalli while these are present in good numbers in Jhilmil area
and Bagh beds. The Fossiliferous Limestone (Fig. 8) exposed near Devarapalli is dominated by the occurrence ofTurritellassp. in addition to several Gastropods and Bivalves. However, no Ammonites could be found. The detailed
studies indicate that Gowripatnam and Devarapalli have both Tertiary and Cretaceous sediments of brackish water and80Oral Session

marine environment with intercalations of fresh water sediments locally.
The period between 65-45 Ma (Palaeocene to Early Eocene?) is important as it spans the interval from the terminal
phase of India’s northward movement as an isolated landmass till its collision with Asia. Endemism among fresh water
ostracodes around Cretaceous-Tertiary Boundary (KTB) 65 m. y. ago, co-existence of Laurasian taxa in Late
Cretaceous Deccan inter-trappeans including eutherian mammals and several Gondwanian taxa-mammals andabeliscurid dinosaurs with affinity to Madagascar and South America are explained in terms of trans-oceanic(sweepstakes) dispersal (eg. Gingerich et. al.,1997, Ali and Aitchison, 2008;). Major sea way existed across India
during K-T transition having implications for palaeogeography, evolution and biotic diversity during K-T transition
probably along Narmada-Tapti rift zone. “Out of India” dispersal hypothesis assumes that some living Asiatic biotic
elements originated on former Gondwanaland and arrived in Asia by rafting the Indian plate which served as a biotic
ferry. The dawn of Tertiary was marked by extensive volcanism which was a manifestation of the tectonism that was
responsible for shaping of the western coast of India and the formation of the Arabian Sea. Deccan volcanism is amajor cause of faunal extinction including that of the dinosaurs at KTB (Keller et. al., 2009). The present researchfindings substantiate the above models pertaining to the Late Cretaceous-Early Tertiary palaeogeographic set up of
Peninsular India.

Fig. 1. Turritellasp(Devarapalli)Fig. 2. Physasp.
(Naskal)Fig. 3. Lymnaeasp.
(Naskal)Fig. 4. Paracyprettasp(Naskal)Fig. 5. Cyclocyprissp.
(Naskal)Fig. 6. Charasp.
(Naskal)Fig. 7. Ostreasp.
(Gowripatnam)

Fig. 8. Fossiliferous
Limestone (Devarapalli)(Figs.1 to 8) Photographs of some of the fossil samples collected from the study area81Oral Session

References
Ali, J. R. and Aitchison, J. C. (2008): Gondwana to Asia: Plate tectonics, paleogeography and the biologicalconnectivity of the Indian sub-continent; Earth Sci. Rev. 88, (3-4), pp. 145-166.
Badve, R. M. and Ghare, M. A., (1978): Jurassic ichnofauna of Kutch-I. Biovigyanam, v. 4, p 125.
Das Sarma, D.C., Anantharaman, S., Vijayasarathi, G., Nath, T.T. and Rao, C.V. (1995): Palaeontological studies forthe search of micromammals in the infra and inter-trappean horizons of Andhra Pradesh. Rec. Geol. Surv. India,
v.128.
Gingerich, P. D. and Arif, M. (1997): Early Eocene Ouettacyon parachai (Condylarthra) from the Ghazij Formationof Baluchistan (Pakistan): J. Vert. Paleon. 17, pp. 629-637.
Govindan, A. (2000): Cretaceous Stage Boundaries: Review of Current Definitions and Relevance to Sections inIndia. Memoir Geological Society of India, No. 46, pp. 39-64.
Ivanov, Alex V. (2000): Late Cretaceous Pycnodont Oysters from the South-East of the Esat European Platform.
Memoir Geological Society of India, No. 46, pp. 131-138.
Keller, G., Khosla, S.C., Sharma, R., Khosla, A., Bajpai, S., and Adatte, T., (2009): Early Danian planktic
foraminifera from Cretaceous-Tertiary intertrappean beds at Jhilmili, Chhindwara District, Madhya Pradesh,
India: Journal of Foraminiferal Research, v. 39, no. 1, pp. 40-55.
Keller G. (2014): Deccan volcanism, the Chicxulub impact, and the end-Cretaceous mass extinction: Coincidence?
Cause and effect? The Geol. Soc. Of America, Spl. Paper, pp. 505.
Prasad, G. and Sahni, A. (1988): First Cretaceous Mammal from India. Nature, v. 332, pp. 638-640.
Rao, B.R.J. and Yadagiri, P. (1981): Cretaceous intertrappean beds from Andhra Pradesh and their stratigraphic
significance. Geol. Soc. India, Mem.,v. 3, pp. 287-291.

82

Oral Session

Paleontology 13

New Progress in the study on the Cretaceous Micropalaeontology
in Southern Tibet, China
Guobiao Li
China University of China

Will be provided it later.

83

Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Poster Session

Poster Session

Poster 1

What is the origin of unusually long ‘Mega Cracks’ found in the Hasandong
Formation of the Cretaceous Gyeongsang Supergroup, Korea?
✳

✳

Seungwon Shin1, ․ Daekyo Cheong1, ․ Taejin Choi2 ․ Hyun-Soo Lim3
1

Department of Geology, Kangwon National University, Korea, dkcheong@kangwon.ac.kr
2
Departmentof Energy Resources Engineering, Chosun University, Korea
3
Department of Geological Sciences, Pusan National University, Korea

Twenty ‘Mega Crack’ sedimentary structures, which are 1m long and 5cm thick, are found from the Hasandong
Formation, the Cretaceous Gyeongsang Supergroup in Euisung, Korea. Each crack is situated within purple siltstonebeds, and is filled with coarse or medium sandstones probably supplied from the overlying sandstone beds. Cracks arevertical plane-shaped showing at least 10 cm width, and some are even branched.
Through preliminary studies several origins have been suggested by Korean sedimentologists.
One of them is a large-scaled mud crack. Long and severe drought after subaerial exposure could form big and deep
desiccation crack within a thick mud layer. Some vertically wrinkled cracks also would be caused by diagenetic
compaction after burial. Previous many studies already suggested the depositional environments of the Hasandong
Formation were fluvial systems including floodplains.
Second suggestion is an ice-wedge or soil wedge origin under cold weather. However, ice wedges which are formed
in soil horizons during a glacial period are usually filled with fine-grained sediments unlike coarse sands in thesecracks. And it is difficult to imagine a very cold weather in the mid Cretaceous time.
The last idea is that the origin of the cracks is a neptunian sandstone dyke. Many neptunian clastic dykes are often
initiated by large earthquakes. But it is doubt that deep and large branched cracks were formed by shaking andcrevassing solely by earthquakes for consolidated mudstone beds and thereafter were filled with inflowing coarse
sands.
In conclusion the cracks are most probable to have been formed as in origin of mud cracks in a floodplain setting ofa fluvial system. But they are still waiting further detailed researches

87Poster Session

Poster 2

Complex analysis of Early Cretaceous macrobenthos and palynomorphs
from southeastern margin of Western Siberia (Vostok-4 Well section)
Pestchevitskaya E.B.1 ․ Urman O.S.1 ․ Shurygin B.N.1,2,✳

1

Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of RAS, Novosibirsk, Russia, Pescheviс
kayaEB@ipgg.sbras.ru
2
Novosibirsk State University, Novosibirsk, Russia

Valanginian benthos and palynomorphs are studied in the Vostok-4 well, which is situated in south-eastern region ofWestern Siberia, in the upper reaches of the River Ket. In this region, the Kulomsino and Tarskaya Formations of theLower Cretaceous overlap Upper Jurassic deposits with significant stratigraphic unconformity. Lower Cretaceous
deposits in the Vostok-4 well contain shell accumulations of macro- and microfauna as well as abundant palynologicalassemblages. Previous palynological data obtained from the Lower Cretaceous of south-eastern regions of Western
Siberia allow the definition of stratigraphic extend of the deposits within the Stage only (Markova, 1971; Nesterov,
1991; etc.). Macro- and microbenthos are here represented by specific taxa providing the age definition within the
Substage interval. New material from the Vostok-4 well gave the data for more detail dating and reconstruction oftransgressive-regressive (T-R) events in the marginal zone of West Siberian marine palaeobasin.
Biostratigraphic successions on mollusks and palynomorphs developed for the Boreal regions of Siberia were usedas the base for biostratigraphic subdivision of the section in the Vostok-4 well (Pestchevitskaya, 2007; Nikitenko et al.,2013; etc.). The analysis of benthos catena and palaeoecological features of macrobenthos and palynomorphs took into
consideration for the reconstruction of palaeoenvironments (Zakharov, Shurygin, 1978, 1985; Abbink, 1998; Van
Konijnenburg-Van Cittert, 2002; etc.).
The studied interval of the section from the Vostok-4 well is characterized by macro- and microbenthos
assemblages, which are typical for the Lower Cretaceous of Siberia. The bivalves are represented by Early Valanginian
Gryphaea borealis,Hartwellia superjrensis (abundant) and juvenile Buchia keyserlingi, which is the index species of
Buchia-zone of the Lower Valanginian. Other taxa are: Proveniella ovalis, Lopatinia arctica, Grammatodonex gr.
schourovskii, Astarte veneriformis (its abundance is typical for the Lower Valanginian), Hiatellahatangensis,Liostrea
ex gr. anabarensis,Arctotisex gr. anabarensis, Anomiasp., etc. Macrobenthos also includes abundant gastropods:
Calliomphalus elegans (typical for the Lower Valanginian), Sulcoactaeonex gr. canalicularis,Khetellaex gr. ventrosa,
Euspira gerassimovi. Gastropods as well as ostracodes sometimes form single-species accumulations interchanging
with phyllopoda accumulations. The Valanginian is confirmed by palynological data. Two local palynological zones
are defined: the Hepatiacea, Selaginella granata Zone and Foraminisporis asymmetricus, Laevigatosporites sp. Zone.

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The presence of Foraminisporis asymmetricus is important for the stratigraphy, it provides the correlation withpalynological succession of northern Siberia, while, in general, palynological assemblages from the Vostok-4 welldiffer in high percentage of gymnosperm pollen, especially Classopollis and Taxodiaceae.
The characteristic features of studied associations of fossils are: specific taxonomic composition of bivalves(Anomia, Gryphaea, Liostrea, Proveniella, Hartwellia) and gastropods (Calliomphalus, Sulcoactaeon, Euspira,
Khetella), single-species accumulations of ostracodes and phyllopodes, more abundant prasinophytes (3-9%,
Leiosphaeridia) among microphytoplankton and the presence of fresh water forms (1-3%; Schizosporis, Ovoidites).
These features show that the deposits were formed in marginal zone of marine palaeobasin with alternation of thefollowing facies: the marginal shallow water facies, the lagoons, the facies of offshore bar. Two stages can be defined
based on specific taxonomic composition of fauna and microphytoplankton: 1) regressive stage with two phases (firstone is characterized by more stable marine conditions), and 2) transgressive stage. During the regressive stage, theshort-termed transgressive events are associated with specific fauna associations including arcticids, gastropods andostracodes typical for lagoons. During the regressions, the interconnections of the lagoon and open marine basin wererestricted resulting in the change of salt regime that is evidenced by abundant accumulations of phyllopodes.
Transgressive events are consistent with diverse macrofauna with abundant Anomia, Gryphaea, Liostrea. Sometimes
the representatives of the genus Arctotis are abundant (especially in the upper part of the section), which are commonly
prosperous in well-aerated conditions with active hydrodynamic and rather high water temperature. Transgressive
episodes in both stages are associated with the presence of dinocysts in microphytoplankton associations.
The analysis of spore-pollen associations allow the reconstruction of climatic conditions. It shows hot, arid and,possibly seasonal climate with alternation of wet and dry periods. It is evidenced by high percentage of lycopods andferns together with abundant cycads, bennettites, taxodialeans and other gymnosperms having adaptations to withstanddry seasons. In the beginning of the first stage, the near-shore wet lowland and marshy land were favorable formoisture-loving plants, which spores and pollen are abundant in palynological associations. The landscape wasmonotonous that is consistent with low diversity of terrestrial plants: palynological associations are mostly represented
by cyatheaceous/dipteridaceous ferns and pteridosperms. Further T-R events resulted in the changes of near-shore
landscapes that is evidenced by frequent changes of quantitative relations of main components in palynologicalassociations. In general, landscapes become less monotonous providing more diverse floral communities: palynologicalassociations are enriched by spores of schizaeaceous, osmundaceous, gleicheniaceous ferns and different lycopods.
During the transgression in the second stage, the near-shore lowland was mostly submerged. The landscape was moreelevated, and occupied by drought-resistant plants.
The reconstruction of detailed T-R succession confirm the biostratigraphic results. Frequent T-R changes arereconstructed for the lower part of the section, and more stable transgressive period is reconstructed for the upper part89

Poster Sessionof the section. Similar T-R succession is defined in northern regions of Siberia: in the upper part of the SP2
palynological Zone (correlated with the Hepatiacea, Selaginella granata Zone in the Vostok-4 well) and in the SP3
palynological Zone (correlated with Foraminisporis asymmetricus, Laevigatosporites sp. Zone) (Pestchevitskaya,
2016). It allows more detailed correlation with palynological succession of northern Siberia calibrated against
ammonite zones, and more accurate definition of stratigraphic extend of the Kulomsino and Tarskaya Formations instudied section: upper part of the Lower Valanginian, the Euryptichites quadrifidus - Siberites ramulicosta ammonite
Zones. Note that the detailed reconstruction of lateral succession of benthos associations in the marginal part of marine
Siberian palaeobasin shows that, in this region, the deposits were formed in specific lagoon-marine facies. It differsfrom the traditional point of view on the formation the Kulomsino and Tarskaya Formations.
Programs RAS РАНII.2П/IX.126-1, II.2П/IX.126-4 and Project IGCP608.
References
Abbink, O.A., 1998. Palynological investigations in the Jurassic of the North Sea region.Utrecht, LPP Foundation.
192 p.
Markova, L.G. 1971. The history of the development of Early Cretaceous flora of West-Siberian lowland (onpalynological data). Moscow, Nedra. 100 p. (in Russian)th

Nesterov, I.I. (Ed.), 1991. Solution of 5 interdepartmental stratigraphic meeting on the Mesozoic deposits ofWest-Siberian plain (Tyumen, 1990). Tyumen, 54 p. (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 (8),808-837.
Pestchevitskaya, E.B., 2007. Lower Cretaceous biostratigraphy of Northern Siberia: palynological units and theircorrelation significance// Russ. Geol. Geophys.48 (11), 941-959.
Pestchevitskaya, E.B., 2016. Environmental changes in Early Cretaceous palaeobasin of Western Siberia based on
marine and terrestrial palynomorphs, in Cretaceous ecosystems and their responses to palaeoenvironmental
changes in Asia and the Western Pacific. Short papers for the Fourth International Symposium of International
Geoscience Programme IGCP 608, August 15-20, 2016, Novosibirsk, Russia. Novosibirsk, IPGG SB RAS,
pp.64-67.
Van Konijnenburg-Van Cittert, J.H.A., 2002. Ecology of some Late Triassic to Early Cretaceous ferns in Eurasia.
Rev. Palaeobot.Palynol. 119, 113-124.
Zakharov, V.A., Shurygin, B.N. 1978. Middle Jurassic biogeography, facies and stratigraphy of Soviet Arctic

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regions (on bivalves).Novosibirsk, Nauka, 206 p.
Zakharov, V.A., Shurygin, B.N. 1985. Method of the reconstruction of bottom relief and depths of marine
palaeobasins based on the analysis of benthos catena, in Environments and life in ancient epochs. Palaeobasins
and their fauna.Novosibirsk, Nauka, pp. 97-107.(in Russian)91

Poster Session

Poster 3

Lower Cretaceous Spore-Pollen From Brown Coal Deposit, Erdenetsogt
Govi, Southeast Mongolia✳

Ichinnorov N.1, ․ Eviikhuu A.2 ․ Gankhuyag Ch.2 ․ Tsolmon G.1 ․ Enkhtugs U.3
1

Institute of Paleontology and Geology, Mongolian Academy of Sciences. Ulaanbaatar, Mongolia. iichka@yahoo.com
2
UyanGeoLLC,Mongolia
3
Tsakhiurt Khuder LLC, Mongolia

Palynology studies in Mongolia very important to clarify the stratigraphy of some sediments hosting coal, shale andpetroleum. Within the framework of this study, the Erdenetsogt Govi Brown Coal Deposit that located in AltanshireeSoum, Dornogovi Province has been included into this study; and the preliminary new data of Lower Cretaceous
palynology study that identified in some samples taken from exploration drill holes are presented in this abstract.
The Erdenetsogt Govi Brown Coal Deposit is located at NE end of Valley Erdentsogt Govi, in territory of
Altanshiree Soum, Dornogovi province, and within frame of contour map sheet L-49-78. The deposit locates in 130
km to the North from Sainshand Town (the capital of Dornogovi province), in 50 km to the North from Altanshiree
soum center and in 465 km to SE from Ulaanbaatar City.
The Erdenetsogt Valley is represented by a depression trending to NE; its length takes 18 to 20 km, and width is 5 to
6 km. Lower Cretaceous sediments of Shinekhudag Formation found in small area on northern and northwestern partof the depression. These sediments are represented by greycolored shale, greenish clay and mudstone, siltstone, papery
shale, marl and sandstones; thickness of them reaches 150 m.
The Lower Cretaceous coal-bearing sediments of Khukhteeg Formation (K1ht) has the largest distribution within the
Erdenetsogt Valley; and the sediments consist mainly of sandstone, mudstone, and gray, dark gray, bluish gray andgreenish gray colored coal-bearing mudstone and siltstone containing coal seams and plies having various thickness.
Thickness of the unit is 250 to 300 m.
At Erdenetsogt Govi Coal Deposit, the seam-V is being the most important coal seam, having 25.4 m thickness,
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moisture (W -9.62%), ash (A -16.37%), volatile (V -34.32%), carbon content (C -34.19%), sulfur (S -1.44%) anddcalorific value (Q -4782kCal/kg). Basically, the quality characteristics of the coal seams are very similar to each other.
Judging on average values of moisture and volatile matter, the brown coal of Erdenetsogt Govi Deposit belongs to“B2” type by Mongolian standard and into class of “high volatile sub bituminous coal” by Australian and Canadianstandards.
The spores and pollen first time recovered from the Erdenetsogt Govi coal deposit (drilling holes SK-32, SK-46,
SK-48). The palynology assemblage of Erdenetsogt Govi coal deposit is composed of Pteridophyta spores 68 % and of92

Poster Session

Gymnosperm pollen 32%. Spores are represented mostly by Cicatricosisporites australiensis, Cicatricosisporites
ludbrooki, Appendidporites sp., Lygodiumsporites subsimplex, Concavissimisporites verrucatus, Trilobosporites
microverrucatur, Concavisporites punctatus, Pilosisporites notensis, Cyathidites australis and Aequitriradites
spinulosus. Non-saccate gymnosperm pollen is presented by Cycadopitessp., Inaperturapollenitessp. Monosulcitessp.
In thisassemblages specimens of bisaccate conifer pollen, most assignable to the genus Podocarpidites,Piceapollenites,
PinuspollenitesandProtopicea.
There are many different species of spores, and similarity with second assemblage of the Shivee Ovoo and Matadassemblages. Thus, the age of the strata is probably Aptian-Albian (Ichinnorov, 2003; Ichinnorov & Hofmann, 2012).
The keywords:spore and pollen, assemblage, Cretaceous
References
Ichinnorov.N., 2003. Palynocomplex of the Lower Cretaceous sediments of the Easthern Mongolia. Mongolian
Geoscientist. N.22, p. 12-16.
Ichinnorov Niiden,Christa-Ch. Hofmann. 2012. Palynology studies of the Matadartea (Tamsag Basin), South-eastern Mongolia. Journal of Geoscience. №21. p. 63-84.

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Poster 4

New ornithopod footprints from the Lower Cretaceous Kitadani Formation,
Fukui, Japan: Ichnotaxonomical implications.
✳

Yuta Tsukiji ․ Yoichi Azuma ․ Fumito Shiraishi ․ Masateru Shibata
Department of Earth and Planetary Systems Science, Graduate School of Science, Hiroshima University
1-3-1 Kagamiyama, Higashihiroshima, Hiroshima, 739-8526 Japan. m145115@hiroshima-u.ac.jp

Large-sized ornithopod footprints, which are more than 25 cm in size (senseThulborn, 1990), have been discoveredfrom all continents, except for Antarctica (Diaz-Martinez et al., 2015). In Japan, numerous large-sized ornithopod
footprints have been reported from several sites (Matsukawa et al., 2005). Especially, the largest number of specimens
has been discovered from the Lower Cretaceous Kitadani Formation (Akaiwa subgroup, Tetori Group) in Katsuyama
City, Fukui Prefecture, central Japan (Azuma, 2003). More than 50 large-sized ornithopod footprints have been foundfrom several layers so far. Tsukiji et al. (2016) suggested that these footprints can be divided into two ichnospecies.
We observed the large-sized ornithopod footprints found from the Kitadani Formation by utilizing the 3D imaging
device. Furthermore, a bivariate analysis of AT versus FL/FW was carried out to compare the mesaxony and FL/FW
variation (Lockley et al., 2009). We recognize at least two morphotypes of new large-sized ornithopod footprints.
Ichnotype A is characterized by longer than its width with a strong mesaxony. Track is formed by three digital pads
and a single heel pad. Ichnotype A shows different features fromC. magnifyicum (Leonardi, 1984) and C. liucixini(Xing et al., 2016); a narrow heel pad and larger digital pad III than other digital pads. Ichnotype A has no bilobed heelmark seen in C. leonardiiand C. kyoungsookimi (Lim et al., 2012). Outline of digits and heel mark in Ichnotype A are
quite different from C. protohadrosaurichnos (Lee, 1997).
Ichnotype Bis characterized by wider than its length with a weak mesaxony. Several ichnotaxa, including
Amblydactylus (Sternberg, 1932), Ornithopodichnus (Kim et al., 2009), and Hadrosauropodus (Lockley et al., 2003),
are also wider than long with weak mesaxony. Especially, the outline of Ichnotype B is quite similar to that of A.
kortmeyeri (Currie and Sarjeant, 1979). Therefore, Ichnotype Bcan be assigned to the same ichnogenus. On the other
hand, Ichnotype B has no interdigital-webs and sharp pointed toe mark seen in A. kortmeyeri. Ichnotype B is quite
different from Ornithopodichnus in outline of digits. Outline of digits in Ichnotype B is similar to Hadrosauropodus,
whereas Ichnotype B has no bilobed heel mark seen in Hadrosauropodus. Therefore, it is suggested that Ichnotype B is
also a new ichnospecies.
The bivariate analysis indicates different trends between that of Ichnotype A and Ichnotype B. In addition, trends ofother ichnospecies, including Caririchniumand Amblydactylus are also different.
Two genus of iguanodontians, a non-hadrosauroid Fukuisaurusand a basal hadrosauroid Koshisaurus, had been

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reported from the Kitadani formation (Kobayashi and Azuma, 2003; Shibata and Azuma, 2015). Coexistence ofprimitive and derived iguanodontians in the same formation implies that morphological variations of large-sized
ornithopod footprints might represent a taxonomical differences of trackmakers.
Moreover, Ichnotype A-type footprints have been reported from pre-Barremian-Aptian strata, whereas Ichnotype
B-type footprints have been known from post-Barremian-Aptian in northern hemisphere (Diaz-Martinez et al., 2015).
This tendency is accordant with the temporal and geographical distributions of iguanodontians; non-hadrosauroid
iguanodontia are reported from pre-Barremian-Aptian, and hadrosauroid iguanodontia are reported frompost-Barremian-Aptian (McDonald, 2012). As a result, it can be proposed that the trackmaker of Ichnotype A was a
non-hadrosauroid iguanodontian and that ofIchnotype B was a hadrosauroid.
References
Azuma, Y., 2003. Early Cretaceous vertebrate remains from Katsuyama City, Fukui Prefecture, Japan. Memo. Fukui
Prefect. Dino. Mus.2, 17-21.
Currie, P.J., Sarjeant, W.A.S., 1979. Lower Cretaceous dinosaur footprints from the Peace River Canyon, British
Columbia, Canada. Palaeogeogr., Palaeoclimatol.. Palaeocol. 28, 103-115.
Díaz-Martínez, I., Pereda-Suberbiola, X., Pérez-Lorente, F., Canudo, J.I., 2015. Ichnotaxonomic review of large
ornithopod dinosaur tracks: Temporal and geographic implications. PLoS One 10, e0115477.
Kobayashi, Y., and Azuma, Y., 2003. A new iguanodontian (Dinosauria: Ornithopoda) from the Lower Cretaceous
Kitadani Formation of Fukui Prefecture, Japan. J. Vertebr. Paleontol.23, 166-175.
Kim, J.Y., Lockley, M.G., Kim, H.M., Lim, J,D., Kim, K.S., 2009. New dinosaur tracks from Korea,
Ornithopodichnusmasanensisichnogen. et ichnosp. nov. (Jindong Formation, Lower Cretaceous). implications
for polarities in ornithopod foot morphology. Cretaceous Res.30, 1387-1397.
Lee, Y.N., 1997. Bird and dinosaur footprints in the Woodbine Formation (Cenomanian) Texas. Cretaceous Res. 18,
849-864.
Leonardi, G., 1984. Le impronte fossili di dinosauri. In: Bonaparte, J.F., Colbert, E.H., Currie, P.J., de Rocles, A.,
Kielan-Jaworowska, Z., Leonardi, G., Morello, N., Taquet, P. (Eds.), Sulle ormi de dinosauri. Editio Editrice,
Venice, pp. 165-186.
Lim, J.D., Lockley, M.G., Kong, D.Y., 2012. The Trackway of a Quadrupedal Ornithopod from the Jindong
Formation (Cretaceous) of Korea. Ichnos19, 101-104.
Lockley, M.G., 1987. Dinosaur footprints from the Dakota Group of Eastern Colorado. Mt. Geologist24, 107-122.
Lockley, M.G., 2009. New perspectives on morphological variation in tridactyl footprints: clues to widespread
convergence in developmental dynamica. Geol. Q.53, 415-432.

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Lockley, M.G., Nadon, G., Currie, P.J., 2003. A diverse dinosaur-bird footprint assemblage from the Lance
Formation, Upper Cretaceous, Eastern Wyoming: implications for ichnotaxonomy. Ichnos11, 229-249.
McDonald, A.T., 2012. Phylogeny of Basal Iguanodonts (Dinosauria: Ornithischia): An Update. PLoS One7,
e36745.
Matsukawa, M., Shibata, K., Kithara, R., Koarai, K., Lockley, M.G., 2005. Review of Japanese Dinosaur Track
Localities: Implications for Ichnotaxonomy, Paleogeography and Stratigraphic Correlation. Ichnos12, 201-222.
Shibata, M., Azuma, Y., 2015. New basal hadrosauroid (Dinosauria: Ornithopoda) from the Lower Cretaceous
Kitadani Formation, Fukui, central Japan. Zootaxa3914, 421-440.
Sternberg, C.M., 1932. Dinosaur tracks from Peace River, British Columbia. Annu. Rep. Natl. Mus. Canada 1930,59-85.
Thulborn, T. 1990. Dinosaur Tracks. Chapman and Hall.
Tsukiji, Y., Azuma, Y., Shiraishi, F. 2016. Ornithopods footprints from the Kitadani Formation, Tetori Group,
Katsuyama City, Fukui. Abstract with programs of the 2016 annual meeting of the Palaeontological Society ofJapan, pp. 27.
Xing, L., Lockley, M.G., Marty, D., Klein, H., Yang, G., Zhang, J., Peng, G., Ye, Y., Persons, W.S.IV., Yin, X., Xu,
T., 2016. A diverse saurischian (theropod-sauropod) dominated footprint assemblage from the Lower
Cretaceous Jiaguan Formation in the Sichuan Basin, southwestern China: A new ornithischian ichnotaxon,
pterosaur tracks and an unusual sauropod walking pattern. Cretaceous Res. 60, 176-193.
Xing, L., Wang, F., Pan, S., Chen, W., 2007. The discovery of dinosaur footprints in the middle Cretaceous Jianguan
Formation of Qijiang County, Chongqing City. Acta Geol. Sinica81, 1591-160.

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Poster 5

Giant pterosaur remains from the upper-most Cretaceous in the Mongolian
Gobi Desert and their paleoecological implications✳

Takanobu Tsuihiji1, ․ Brian Andres2 ․ Patrick M. O’Connor3 ․ Mahito Watabe4 ․ Khishigjav Tsogtbaatar5 ․BuuveiMainbayar5
1

Department of Earth and Planetary Science, The University of Tokyo, Tokyo, Japan, ttsuihiji@eps.s.u-tokyo.ac.jp
Department of Earth and Environmental Science, University of Pennsylvania, Philadelphia, Pennsylvania, U.S.A.
3
Ohio Center for Ecology and Evolutionary Studies and Department of Biomedical Sciences,
Heritage College of Osteopathic Medicine, Ohio University, Athens, Ohio, U.S.A.
4
School of International Liberal Studies, Waseda University, Tokyo, Japan
5
Institute of Paleontology and Geology, Mongolian Academy of Sciences, Ulaanbaatar, Mongolia

2

Pterosaurian remains are very scarce in Mongolia despite a long history of extensive paleontological survey inMesozoic strata in the Gobi Desert. This is especially true for Upper Cretaceous strata, from which only two specimens
have been reported as definitively pterosaurian, both being cervical vertebrae of azhdarchids from the CenomanianSantonian Bayn Shire Formation (Watabe et al., 2009). We herein report pterosaur remains collected from the upper
Campanian-Maastrichtian Nemegt Formation at Gurilin Tsav, Southern Gobi Desert, during the Hayashibara Museumof Natural Sciences‐Mongolian Paleontological Center Joint Expedition in the western Gobi Desert in 2006. The
material consists of three fragments of posterior cervical vertebrae and represents the first discovery of pterosaurian
remains from this formation. Pterosaurian affinities of these specimens are indicated by the presence of the postexapophyses
on a centrum and the highly pneumatic nature and very thin cortical bone in the all preserved elements. The estimatedwidth of the preserved centrum across the postexapophyses is 198 mm, indicating that these specimens belong to agigantic pterosaur, of which size is comparable to such taxa as Quetzalcoatlus northropi, Arambourgiania philadelphiaeand Hatzegopteryx thambema(e.g., Witton and Habib, 2010).These gigantic species all belong to Azhdarchidae and arefound from the Maastrichtian. The present specimen thus adds to further evidence that gigantic pterosaurs were widelydistributed in Eurasia and North America during the latest Cretaceous. It has been suggested that gigantic pterosaurs
were the largest carnivores in some ecosystems (Witton and Naish, 2015). However, remains of the large tyrannosaurid
theropod Tarbosaurus baatar have been found at the Gurilin Tsav locality and are also abundant at nearby Bugin Tsav,suggesting that T. baatar most likely coexisted with the present pterosaur. Similarly, remains of Tyrannosaurus rex
occurred in the Javelina Formation in Texas, U.S.A., which also yields remains of Quetzalcoatlus northropi and
Quetzalcoatlus sp. (Lawson, 1976). Accordingly, if giant pterosaurs were indeed terrestrial carnivores, they would
likely have had competed with large theropods for food resources and would thus not have been sole, top carnivores.

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References
Lawson, D. A. 1976. Tyrannosaurusand Torosaurus, Maastrichtian dinosaurs from Trans-Pecos, Texas. Journal of
Paleontology 50: 158-164.
Watabe, M., T. Tsuihiji, S. Suzuki, and K. Tsogtbaatar. 2009. The first discovery of pterosaurs from the Upper
Cretaceous of Mongolia. Acta Palaeontologica Polonica 54: 231-242.
Witton, M. P., and M. B. Habib. 2010. On the size and flight diversity of giant pterosaurs, the use of birds aspterosaur analogues and comments on pterosaur flightlessness. PLoS ONE 5: e13982.
Witton, M. P., and D. Naish. 2015. Azhdarchid pterosaurs: water-trawling pelican mimics or “terrestrial stalkers”?
Acta Palaeontologica Polonica 60: 651-660.

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Poster 6

LATE CAMPANIAN-EARLY MAASTRICHTIAN MEGAFOSSILS FROM THE
NAKAMINATO GROUP (CENTRAL HONSHU, JAPAN): AN EXAMPLE OF NWPACIFIC HETEROMORPH-DOMINATED AMMONITE FAUNA✳

Genya MASUKAWA1, ․ Hisao ANDO2
1

Graduate School in Science and Engineering, Ibaraki University, Mito, Japan, 16nm312h@vc.ibaraki.ac.jp
2
Department of Earth Sciences, Faculty of Science, Ibaraki University, Mito, Japan

Campanian to Maastrichtian marine strata have been known as several groups represented by the Nemuro, Yezo,
Nakaminato, Izumi and Sotoizumi groups commonly bearing mega fossils distributed along the Japanese Islands in the
Northwestern Pacific region. Though continuously stratigraphic successions are limited to be observed due to exposure
conditions, the Nakaminato Group is suitable to demonstrate the stratigraphic succession of heteromorph-dominatedammonite fauna as well as other molluscan species, on 4 km-long wave-cut benches north-southward along the Pacificcoast in Hitachinaka City, Ibaraki Prefecture, central Honshu. We report the faunal components and their succession in
addition to the lithostratigraphy and sedimentary environments of the Nakaminato Group as basic information forreconstructing their habitat and ecological significance.
The Nakaminato Group, homoclinally inclined (30 to 40˚ NE) strata, provides a continuous lithostratigraphic
succession of the Upper Campanian to the Lower Maastrichtian about 1,900 m thick. The group is subdivided into theoffshore mudstone-dominated Hiraiso, and sandstone- and sandy turbidite-dominated Isoai formations in ascending order.
The lower part of the Hiraiso Formation, inferred as basin-plain to lower submarine-fan muddy deposits, contains
various ammonoids, bivalves (including several inoceramid species), gastropods, and echinodermates such as
Niponaster nakaminatoensis. Heteromorph ammonites and inoceramid bivalves include biostratigraphically important
index species in Japan. Didymoceras sp. occurred from massive mudstone of the lowermost part of the Hiraiso
Formation. Rather common Didymoceras awajiense co-occurred with rare Diplomoceras sp., the largest molluscan
species in the Late Campanian NW Pacific area, from siltstone frequently intercalated with thin, fine to very finesandstone of the lower part of the Hiraiso Formation. D. awajiense shows a wide range of variation in modes of coilingand shell ornamentation. This species commonly occurs also from other Upper Campanian strata in Japan: Izumi
Group and Toyajo Formation of Sotoizumi Group in Southwest Japan. However, the co-occurrence with Diplomoceras
has not been known in other areas in Japan at all. In having broad and high ribs on the retroversal hook, Didymoceras
sp. morphologically differs from previously named species of Didymoceras of the NW Pacific region. This shellornamentation cannot be observed in the “Bostrychoceras sp.-Didymoceras awajiense-Pravitoceras sigmoidale
evolutionally lineage” recently proposed by Misaki and Tsujino (2017). Three inoceramids, Inoceramus

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Poster Session(Platyceramus) cf. ezoensis, I. (Endocostea) balticus and I. (E.) shikotanensis occurred from the lower part of theHiraiso Formation in ascending order. Only fragmentary specimen of Diplomoceras sp. and some bivalves have been
known from sandy siltstone of the upper part of the Hiraiso Formation, inferred as lower to mid submarine-fan
deposits. Parvitoceras sigmoidale known from the horizon above D. awajiense Zone in the Izumi, Sotoizumi and Yezo
groups, has not discovered yet from the upper Hiraiso and the lowermost Isoai formations.
The lower part of the Isoai Formation, inferred as middle to upper submarine-fan deposits, contains some isolated
vertebrate bones such as mosasaur, trionychid and nyctosaurid pterosaur in debris flow and high-density turbidite beds
(Kato et al., 2016). Shell fragments of ostreid and inoceramid bivalves have been also rarely occurred from thishorizon. A small fragment of nostoceratid, which may represent the lowermost Maastrichtian index species
Nostocerashetonaiense, occurred also from the debris flow bed.
The upper part of the Isoai Formation, inferred as middle submarine-fan deposits, contains many fragments of
Baculitesspp.from debris flow beds and siltstone frequently intercalated with thin, fine to very fine sandstone. Some
bivalves (including “Inoceramus” kusiroensis, Lower Maastrichtian index species), gastropods and echinodermateshave been also occurred from these horizons. An indeterminate long-spined large nostoceratid occurred from mudstoneof the upper part of the Isoai Formation shows similar shell ornamentation to Nostocerassp., which was recently
reported from the middle part of the “Etanpakku” Formation (Lower Maastrichtian) of the Yezo Group by Shigeta etal.(2017).The U-Pb age of detrital zircons recently measured by our collaborators also indicates Early Maastrichtian
for the upper part of the Isoai Formation.
As described above, the Upper Campanian to Lower Maastrichtian Nakaminato Group contains valuable records of
nostoceratid heteromorphs, major components of the heteromorph ammonoid fauna of late Cretaceous in the NW
Pacific region. It is expected that the group provides the important information connecting the contemporaneous
Nemuro, Yezo, Izumi and Sotoizumi groups to reconstruct the Campanian and Maastrichtian ecosystems in the NW
Pacific Region.
References
KATO, T., KODA, Y., ANDO, H. and SONODA, T., 2016. Late Cretaceous reptile fossils from Nakaminato Group,
Hitachinaka, Ibaraki (in Japanese). Abstracts with Programs the 2016 Annual Meeting the PalaeontologicalSociety of Japan, 47 (P33).
MISAKI, A. and TSUJINO, Y., 2017. Nostoceratid ammonoids from the Upper Cretaceous Izumi Group in
northeastern Shikoku, Japan and their evolutionary implications (in Japanese). Abstracts with Programs the2017 Annual Meeting the Palaeontological Society of Japan, 42 (P13).
SHIGETA, Y., IZUKURA, M. and TSUTSUMI, Y., 2017. An early Maastrichtian (latest Cretaceous) ammonoid
fauna from the Soya Hill area, Hokkaido, northern Japan. Bulletin of the Hobetsu Museum, 32, 7-41.

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Figure Captions
Selected heteromorph ammonoids succession in Nakaminato Group. A: Didymocerassp.; B: Didymoceras
awajiense; C: Diplomocerassp.; D: indeterminate nostoceratid; E: Baculitessp.

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Poster 7

Quantification of skeletal pneumaticity in the pterosaur Anhanguera
piscator and comparison with the avian condition✳

Meg Wakui ․ Takanobu Tsuihiji
Department of Earth and Planetary Science, Graduate School of Science, The University of Tokyo, Tokyo, Japan
megwakui@eps.s.u-tokyo.ac.jp

In birds, parts of the axial and appendicular skeletons are hollowed out by air sacs emerging from the lung,producing pneumatic bone. Evidence of similar postcranial skeletal pneumaticity (PSP) is also observed in pterosaursof the Mesozoic Era (O’Connor & Claessens, 2005).The degree of PSP is correlated with the body size both in birds
and pterosaurs, suggesting its significance in reducing the skeletal and body mass associated with flight (Claessens et al, 2009).
Only a few past studies quantitatively examined the degree of PSP or air space proportion (ASP) in pterosaurs.
Furthermore, most of such studies focused on measuring only a single cross-section of each sampled bone. Martin &Palmer (2014) is an exception, measuring the change in ASP along the long axis of bones and revealing that ASP
varies within each bone based on computer tomography (CT) scan data on ornithocheirid wing phalanges. The numberof the analyzed samples, however, was limited. Furthermore, the variation of ASP among different skeletal elements ina single individual has never been analyzed in pterosaurs, and it thus remains unknown whether ASP obtained from thewing phalanges by Martin & Palmer (2014) is applicable to other bones.
In this study, we obtained ASP in several bones of the holotype specimen of Anhanguera piscator (NSM-PV 19892)
in order to clarify a possible variation in ASP among skeletal elements in a single individual. For each image slice, theempty or medullary space (now filled with calcite or sediment) and the surrounding bone wall were selected using the3D imaging software Amira and were converted into colored pixels (Fig. 1). The pixels were then counted using thesoftware ImageJ. ASP was calculated as the ratio of the empty or air-filled area to total area.ASP values in the humeri
of extant birds, Diomedea immutablis (albatross) and Aptenodytes patagonicus (king penguin), were also analyzed for comparison.

Fig. 1. An example of cross section used to determine ASP where bone and air space are segmented in black andwhite, respectively. A, left ulna; B, left radius. Scale bar = 10mm.

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As a result, we found that ASP values varied among forelimb bones in Anhanguera piscator(Fig. 2). The range of
ASP values were 0.70-0.95 in all the examined forelimb bones. The fourth cervical vertebra was more highly
pneumatized than the forelimb bones. The humeri of both albatross and penguin had average ASP values lower thanthose in the forelimb bones in A. piscator, and also showed wider ranges than the latter (Fig. 3).

Fig. 2. Plot of ASP along the long axis (length measured from the proximal end) in forelimb bones of Anhanguera
piscator.

Fig. 3. Plot of ASP along the long axis (length measured from the proximal end) in the humeri of albatross and penguin.

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Although variations of ASP within individual bones within Anhanguera piscatordid not show a common pattern,
the range of ASP in each bone found in this pterosaur was much smaller than those in the humeri of the examinedextant birds, suggesting that the way air sacs invaded the bone might have been different between pterosaurs and birds.
Further quantitative analyses of the pneumatic volume of the entire skeleton will contribute to realistic estimations of
the skeletal and body mass in pterosaurs and abetterunderstandingoftheirflightcapacity.
References
Claessens LP, O'Connor PM, Unwin DM (2009) Respiratory evolution facilitated the origin of pterosaur flight andaerial gigantism. PloS one, 4(2), e4497.
Martin EG, Palmer C (2014) Air space proportion in pterosaur limb bones using computed tomography and its
implications for previous estimates of pneumaticity. PloS one, 9(5), e97159.
O'Connor PM, Claessens LP (2005) Basic avian pulmonary design and flow-through ventilation in non-avian
theropod dinosaurs. Nature, 436(7048), 253-256.

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Poster 8

Age of the Upper Cretaceous Himenoura Group on the KoshikishimaIslands, Kagoshima, Japan✳

Miyake Y.1, ․ Aramaki M.1 ․ Tsutsumi Y.2 ․ Manabe M.2 ․ Misaki A.3 ․ Komatsu T.4
1

Graduate School of Science and Technology, Kumamoto University, Kumamoto 860-8555, Japan,
121d9010@st.kumamoto-u.ac.jp
2
Department of Geology and Paleontology, National Museum of Nature and Science, 4-1-1 Amakubo, Tsukuba, Ibaraki
305-0005, Japan3
Kitakyushu Museum of Natural History & Human History, 2-4-1 Higashida, Yahatahigashi-ku, Fukuoka 805-0071
4
Faculty of Advanced Science and Technology, Kumamoto University, Kumamoto 860-8555, JapanThe Upper Cretaceous Himenoura Group is widely distributed in western Kyushu, Japan, and is composed mainlyof non-marine to marine fossiliferous siliciclastics on the Koshikishima Islands, Kagoshima Prefecture. The
successions of this group are important for understanding regional correlations, coastal paleo-environments, andterrestrial and marine faunas during the Upper Cretaceous in the East Asia.
In the study area of northern Koshikishima Islands, Tanaka and Teraoka (1973) divided the Himenoura Group into
B, C, D, E, F and G formations in ascending order. The D Formation is subdivided into the D1, D2, D3 and D4
members, and the E is E1, E2 and E3 members. The C Formation composed mainly of shallow marine sandstone andmudstone contains the upper Santonian to lower Campanian Eupachydiscus haradai (ammonoid), lower Campanian
Sphenoceramus orientalisand middle Campanian Sphenoceramus schmidti (inoceramids). Furthermore, Upper
Cretaceous radiolarians are commonly found in the C and E formations. The C Formation yields middle Campanianradiolarian Amphipyndax pseudoconulus. The E1 Member contains Santonian to middle Campanian radiolarianassemblages consisting mainly of Amphipyndax stocki, Dictyomitra koslovae and Dictyomitra multicostata.
Zircon U-Pb ages were investigated using laser ablation inductively coupled plasma mass spectrometry(LA-ICP-MS) for acidic tuff samples from the C and F formations and for a sandy tuff sample from the F Formation.
Although the three samples contain some accidental zircons, the samples have definite youngest age clusters. The
weighted mean zircon U-Pb ages from the acidic tuff samples of the C and F formations are 82.5 ±1.0 Ma (lower
Campanian) and 70.0 ±0.5 Ma (Lower Maastrichtian), respectively (errors are 95% confidence interval). The age ofyoungest peak separated by multi-peak gauss fitting from the sandy tuff sample of the F Formation indicates 67.3 ±2.3
Ma (Upper Maastrichtian).
In this study area, the Himenoura Group had been accumulated during the lower Campanian to Upper Maastrichtian.
The boundary between lower and middle Campanian is intercalated within the C Formation. The Campanian and
Maastrichtian boundary seems to be embedded in the F Formation.
References
Tanaka and Teraoka, 1973. Bulletin of the Geological Survey of Japan, 24, 157-184.

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Poster 9

Clay mineralogy of the intertrapean beds near Dhar district of MP: I
mplications for Cretaceous Paleogene paleoclimate✳

Neha Upreti1, ․ PankajSrivastava1 ․ BandanaSamant2
1

Department of Geology, University of Delhi, New Delhi, India 110 007, nehageo89@gmail.com
2
Department of Geology, Rashtrasant Tukadoji Maharaj, Nagpur University, India 440 001

The Deccan Continental Flood Basalt (DCFB) Province is one of the largest and best studied continental floodbasalt provinces in the world. The present study focuses on the sedimentary beds associated with the DCFB sequences
exposed in the Dhar district of MP. It occurs in the Malwa Group of rocks. In this study we have studied 3 sections
exposed along Bagwania, NH3, and Gujrimaan. Eighteen samples studied for have provided details of clay mineralformation and their transformation during Cretaceous Paleogene boundary. Field characters, macro-morphology,
micromorphology, grain size of the intertrapean sediments suggests deposition predominantly in arid-semiarid
environmental conditions. The X-Ray Diffraction (XRD) of total clay (<2µm) and fine clay (<0.2 µm) shows
dominance of smectite and small amounts of feldspar and quartz. Some of smectite show chloritization. Dominance ofsmectite indicates deposition under arid-semiarid conditions whereas formation of Smectite/chlorite suggests atransition from arid to humid conditionsduring the deposition of the marly sediments during Cretaceous-Paleogenetime.
Key words: Deccan Continental Flood Basalt (DCFB), Clay Minerals, Paleoclimate

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Poster 10

New Progress in the study on the Palaeigene Micropalaeontology
in Southern Tibet, China
Wenyuan Zhang
China University of China

Will be provided it later.

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Poster 11

Non-marine Turga biota of the West-Urulunguy intermontane Basin (Transbaikal)✳

Natalya G. Yadrishchenskaya ․ Alena V. Kurilenko
Public corporation «Chitageologorazvedka», 672000, Amurskaya St., 91, Chita, Russia
Alena_Kurilenko@mail.ru

The Lower Cretaceous of Transbaikal is represented only by continental deposits. They are widely distributed inintermontane rift basins. The LowerCretaceous sedimentsof the Turga-Ingoda facial zone of Transbaikal (fig. 1) are
united into the Turga Formation, characterized by very numerous faunistic and floristic remains and known as
Lycoptera Beds (Bugdaeva & Markevich 2012; Kurilenko & Yadrishchenskaya 2014, and others). The most complete
section of the Turga Formation is located in the West-Urulunguy Basin (fig. 1) and is represented by terrigenous andtuffaceous-terrigenous deposits, rocks with carbonate cement and layers of limestones. The zeolite deposit is located in
the Shivertuy graben, which complicates the basin.
The Cretaceous rocks overlie the Jurassic deposits with discordance in the West-Urulunguy Basin. The lower part ofthe section of the Turga Formation here (Lower Turga Subformation) consists of cyclic interbedded breccias,
conglomerates, gravelstones, inequigranular sandstones, rare tuffstones, siltstones and tuffaceous siltstones, tuffs, andtrachyandesite-basalt lava flows (fig. 2). The thickness of the tuffs and tuffites reaches 85 m, their zeolitized
differences - a few metres. The thickness of the Lower Turga Subformation in the basin is 270-530 m. The number ofcoarse clastic rocks increases towards the margins of the basin.
Organic remains are rare (fig. 2) and consist of conchostracans Bairdestheria middendorfii(Jones), mollusks Valvata
transbaicalensis Martinson, plants Archaeolarix argunensis Teslenko, Pseudolarix sp., Brachyphyllum sp.,palynological assemblage Neoraistrickia truncata (Cooks.) Potonie, Leiotriletes pallescens Bolchovitina,
Camptotriletes cerebriformis Naumova et Iljina, Vitreisporites pallidus (Reissinger) Nilsson, and others. The Lower
Turga Subformation is composed mainly of deposits of proluvial-alluvial origin and to a lesser degree volcanic rocks.
The upper part of the section (400-1200 m) of the Turga Formation (Upper Turga Subformation) is characterized byfiner granulometric composition and represented by siltstones, mudstones with layers of sandstones, tuffstones andtuffaceous siltstones, tuffs, zeolites (fig. 2). The number of tuffaceous rocks increases up the section. Thin layers ofrocks with carbonate cement, limestones, and marls are located here. All rocks are zeolitized and montmorillonitized.
In the base of this part of the section, thin layers of conglomerates, tuffaceous conglomerates, and gravelstones occur.
Sediments of this part contain numerous organic remains of freshwater fauna and terrestrial flora. The assemblageof fossils is as follows (fig. 2): fishes Stichopterus sp., Irenichthys sp., Lycoptera sp.; insects Ephemeropsis trisetalis

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Eichwald, Chironomaptera gregaria (Grabau), Coptoclava longipora Ping, Clypostemma sp., Orthoptera sp.,
Terrindusia (T.) cf. minuta Vialov et Sukatsheva, Folindusia (Profolindusia) sp.; conchostracans Bairdestheria
middendorfii (Jones), B. variabilis Novojilov, B. chii (Kobayashi et Kusumi), B. takechenensis (Kobayashi et Kusumi),
B. oblonga Oleynikov, B. sinensis (Chi), B. jeholnensis (Kobayashi et Kusumi), B. turgaensis Oleynikov, B. elongata(Kobayashi et Kusumi), Estherites dahuricus (Tshernyschev); mollusks Limnocyrena wangshihensis (Grabau), L. tanii(Grabau), L. sibirica (Rammelmeyer), Probaicalia elongata Martinson, Sphaericoncha amgensis (Martinson),Arguniella ovalis Ch. Kolesnikov, Corbicula altiformis (Grabau), Daurinia marginata Ch. Kolesnikov, Valvata
transbaicalensis Martinson, Viviparussp.; ostracodes Cypridea zagustaica Mandelshtam, Darwinulacf. nimia Sinitsa,
D. cf. contracta Mandelshtam; plants Archaeolarix argunensis Teslenko, Pityospermum sp., Pseudolarix sp.,
Pseudolarixerensis Krassilov, Otozamites lacustris Krassilov, Baisia hirsuta Krassilov, Kutiella transbaicalica
Srebrodolskaya, Equisetum cf. semenenses Srebrodolskaya, Schizolepis sp., Phoenicopsis sp., Cladophlebis sp.,
Pityophyllum? sp.
In the Shevertuy graben, the Upper Subformation has the greatest thickness (to 1200 m) and is characterized thestratified siltstones, mudstones, and sandstones, rare gravelstones, and tuffaceous rocks: crystal-vitric tuffs, tuffites,
carbonate-tuffaceous rocks. Zeolitizated tuffs and tuffites occupy up to 40 % of the deposit’s volume. The deposits ofUpper Turga Subformation of the Shevertuy graben are characterized by a very rich and varied association of organic
remains. Most species listed above were found in this structure.
This part of the section is dominated by interbedded beds of small lakes and oxbow-lake facies. The presence ofcharacteristic associations of fauna and flora and often of guide forms makes it possible to trace the Turga Formation to
the territory of northeastern China (the Jehol Biota) and Mongolia. E. V. Bugdaeva considered the paleofloras from theYixian Formation in northeastern China, from Bon-Tsagan, Manlaj, and Gurvan-Eren localities of Mongolia and Upper
Turga Subsuite, to be of the same age. She and V. A. Krassilov dated these fossil plants as Barremian-Aptian(Krassilov 1982; Bugdaeva & Markevich 2012). The geochronological age of the basalt covers in the upper part of theLower Turga Subsuite are defined using the K-Ar method in the Torey Basin (fig. 1) is 129+4 in the lower part of thebasalt cover and 119+3 Ma - in its upper part (Yadrishchenskaya et al. 2010). These dates correspond well to thoseobtained for the Yixian Formation. The age of the basaltic lava from the bottom of this Formation is 129.7+5 Ma andthe age of the tuff from the lowermost part of the overlying Jiufotang Formation is 122.1+0.3 (Chang et al. 2009). We
also have new data on the age of the Lower Turga Subformation from the Chita-Ingoda Basin of the Turga-Ingoda
facial zone of Transbaikal (fig. 1). The geochronological age of the basalt covers of the Lower Turga Subsuite aredefined using the Ar-Ar method from 143+2 to 136+5.
The upper Subformation lies with concordance on the Lower Turga Subformation and with discordance is overlain
by the Kutya Formation (400 m), which includes poor coal-bearing deposits (fig. 2). They are confined to small

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troughs in the internal part of the basin. The basal part is characterized by conglomerate-breccias, gravelstone-breccias
changing up the section to gravel sandstones, sandstones, sandy siltstones, interbedding siltstones, mudstones, andcoaly mudstones, which prevail. These strata include new species of conchostracans: Bairdestheria memolabilis
Trussova, B. chinchudukensis Trussova, Esterites sp. nov., Paleochirocephalus vialoviTrussova. The age of the Kutya
Formation is considered as Aptian-Albian (Kurilenko et al. 2002). Thus, the age of the Upper Turga Subformation is
confirmed as Barremian-Aptian, but the dating of the basaltic flows of the Lower Turga Formation does not exclude anolder, Berriasian-Hauterivian age.
Our research was supported by IGCP 608.
References
BUGDAEVA, E.V. & MARKEVICH, V.S. 2012. Chapter 25. The age of Lycoptera Beds (Jehol biota) in
Transbaikalia (Russia) and Correlation with Mongolia and China. In GodefroitP. (ed.) Bernissart Dinosaurs and
Early Cretaceous Terrestrial Ecosystems. pp. 452-464. Bloomington: Indiana University Press.
CHANG, S.C., ZHANG, H.C., RENNE, P.R. & FANG, Y. 2009. High-precision40

Ar-39Ar age for Jehol Biota.

Paleogeography, Paleoclimatology, Paleoecology, 280, 94-104.
KRASSILOV, V.A. 1982. Early Cretaceous flora of Mongolia. Paleontographica, B181, pp. 1-43.
KURILENKO,A.V., KOTLYAR, G.V. KULKOV, N.P.et al.2002. Atlas of Fauna and Flora of Paleozoic-Mesozoic
in the Transbaikal.Nauka, Novosibirsk (in Russian).
KURILENKO, A.V. & YADRISHCHENSKAYA, N.G. 2014. The Lower Cretaceous deposits of southeastern
Transbaikal. In Hisao Ando, Hiromichi Hirano, Takashi Hasegawa et al. (eds.) Land-Ocean Linkages and Biotic
Evolution during the Cretaceous: Contribution from Asia and Western Pacific.The Material of the Second
International Symposium of International Geoscience Programme (IGCP) Project 608, pp. 123-126.
YADRISCHENSKAYA, N.G., KURILENKO, A.V., KOROSTOVSKY, R.A., RAITINA,N.I.2010. New data instudying of the Torey Basin (Eastern Transbaikal). In Baraboshkin E.Yu. and Blagoveschensky I.V. (eds.) The
Cretaceous of Russia and the nearest Abroad: the problems of Stratigraphy and Paleogeography,pp.356-360.
Publishing house Ulyanovsk State University, Ulyanovsk, (in Russian).

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Poster 12

Preliminary report of Cretaceous radiolarite as raw material for stone tools
in the Zagros Mountains, Iran
Kenichiro Hisada1 ․ AyumiI karashi2 ․ Yoshihito Kamata1 ․ Monireh Poshtkoohi3
1Division of Earth Evolution Sciences, Graduate School of Life and Environmental Sciences, University of Tsukuba, Tsukuba,
Ibraki 305-8572, Japan, hisadak@geol.tsukuba.ac.jp
2
Master’s Program in Education, University of Tsukuba, Tsukuba, Ibraki 305-8572, Japan3
Department of Petrology, Geological Survey of Iran, Tehran-Iran

The Zagros Mountains in Iran formed along the convergent boundary between the colliding Arabia and Eurasia
plates during late Miocene to early Pliocene time. The range consists almost entirely of limestone. Recently, the Zagros
Mountains have yielded key evidence of the expansion from Africa of Homo sapiens, which originated in East Africa
200,000 to 100,000 years ago. There are two main routes from Africa to Eurasia, a northern route from the Sinai
Peninsula to the Levant and a southern route around the Arabian Peninsula. Because recent research in Iran has
documented Paleolithic remains from before 50,000 years ago at Arsenjan, northeast of Shiraz, the southern Zagros
Mountains have received attention for their role in the southern route of early human migration.
The bedrock of Arsenjan consists of thick-bedded limestone, radiolarite, and muddy limestone. The thick-bedded
limestone belongs to the Salvak Formation, of middle Cretaceous age, and hosts caves in which early human remains
have been found. The radiolarite underlies the lower flat areas. Although the radiolarite has previously been considered
to be of Jurassic age, the present study showed that it dates from the latest Jurassic to Early Cretaceous. The muddy
limestone, of Triassic to Jurassic age, composes higher-standing platforms and is fossiliferous, yielding stromatolites
and other remains.
To the east of Arsenjan, the Neyriz ophiolite crops out in the vicinity of Abadeh-e-tashk. The ophiolite is a large
fragment of former ocean crust, obducted onto the Eurasian continent along with its overlying deep-sea sediments. The
former ocean crust contains a sequence of serpentinite (altered peridotite) overlain successively by pillow basalt andbedded chert. The bedded chert has been considered to represent Cretaceous deep-sea sediments; however, the present
study showed that it contains radiolarians of Middle to Late Jurassic age. The Neyriz ophiolite was also observed tothrust southward over the Salvak Formation near Abadeh-e-tashk. This means that the limestones and radiolarite wereoriginally deposited on the shallow continental shelf of the ancient Arabian continent and that the bedded chert was
originally deep-sea sediment in the Neotethys ocean. This ophiolite occurs at Kermanshah in the Zagros Mountains andradiolarite is also exposed there.
Radiolarite would have been preferable to the bedded chert as stone tools. Bedded chert consists of chert beds no112

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more than 10 cm thick separated by mudstone films a few millimeters thick. This chert would not have yielded piecesof stone large enough to manufacture a full range of tools. However, radiolarite beds are thick enough to yield pieces
suitable for flake production using the Levallois technique.
During the Jurassic, the continents of Laurasia and Gondwana were separated by the shallow Neotethys ocean.
Present-day western Asia was located at the innermost part of the Neotethys near the paleo-equator at a favorable
location for upwelling currents, resulting in high faunal productivity. Thus, an extensive carbonate platform developedon the Arabian continental margin. After the Arabia plate separated from the Africa plate and collided with the Eurasia
plate, the limestone-radiolarite association was folded and uplifted to form the Zagros Mountains. Here came to be aland replete with limestone caves and widespread radiolarite that welcomed ancient Homo sapiens.

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Poster 13

Updates on ongoing paleontological studies of Cretaceous units
in the Philippines
Allan Gil S. Fernando
National Institute of Geological Sciences, University of the Philippines, Diliman, Quezon City 1101 Philippines;
agsfernando@yahoo.com, asfernando@up.edu.ph

The paper presents results of ongoing biostratigraphic and/or paleontological analysis of Cretaceous marine sectionsin the Philippines. These studies aim to update and supplement data from previous studies, as well as to further
elucidate the paleoenvironment and paleoclimatic conditions of the investigated sections during the Cretaceous. New
calcareous nannofossil biostratigraphic data is presented for Catanduanes, Camarines Sur and Rizal Provinces in Luzon
Island, while additional sedimentological and paleontological data is reported for Palawan Island.

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Poster 14

Preliminary study on the provenance of the Cretaceous Neungju B asin, Korea
Min Kyu Kwon ․ Taejin Choi✳

Department of Mineral and Resources Engineering, Chosun University, 61452 Gwangju, South Korea
tchoi@chosun.ac.kr

The Neungju Basin is a Cretaceous nonmarine basin including dinosaur track-bearing deposits, located in thesouthwestern Korean Peninsula. The Neungju Basin is filled by the Neungju Group, which consists mainly ofsiliciclastic and pyroclastic sedimentary rocks with volcanic rocks. However, sedimentological characteristics of the
Neungju Basin have not been studied yet except for the Jangdong Tuff, which includes the dinosaur tracks. The
depositional environment of the dinosaur track-bearing strata (Jangdong Tuff) is known to be a lake margin. Thus, weare carrying out petrography and detrital zircon geochronology analyses on the Neungju Basin sedimentary rocks toconstrain their provenance.
Basinfill of the Neungju Basin consists mainly of conglomerate, sandstone, siltstone, and tuff. Tuff content increases
southwards. The conglomerates are generally matrix-supported and contain angular clasts such as quartzite, schist,granite, and tuff. Sandstones and matrix of the conglomerates are comprised mainly by angular grains of quartz,
feldspar, and metasedimentary and volcanic rock fragments. The amount of rock fragments increase up sequence.
Modal composition of the Neungju Basin indicates that siliciclastic sediments were supplied from the adjacentbasement rocks such as Paleozoic sedimentary rocks and Jurassic granites in the northern part, while the southern partwere mainly provided volcanic material. Volcanic activity and exposure of the basement rocks in the source region
increased with time. Further study by detrital zircon U-Pb analysis will reveal more detailed information about thesource rocks of the Neungju Basin.

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Poster 15

A review of Pakisaurus titanosaur: Associated skeletons of sauropod
and theropod dinosaurs and mesoeucrocodiles from Pakistan:
Discussion on titanosaurs of Indo-Pak subcontinent
M. Sadiq Malkani
Geological Survey of Pakistan, Muzaffarabad, Pakistan. E. Mail; malkanims@yahoo.com

Review of Pakisaurus balochistani-a pakisaurid titanosaurian sauropod dinosaur:Its holotype includes four tallcaudal centra. The vertebrae, ribs, sternal, scapulae, humerai, radius, ulnae, ilia, femora, tibia, fibula, manus and footbones and osteoderms found from holotype locality are added here as lectotype (Fig.1). Some associated bones arefound from West Bor PDL 2, North Alam PDL 19n, Top Kinwa PDL 16, Shalghara PDL 3 and Basti Nala/ Zubra peakPDL 7 (Fig.1). Based on the morphology of holotypic caudal vertebrae as overlap and used the non-overlapping
portion of the skeleton to broaden the diagnosis of the species and its distinction from the other Cretaceous titanosaurs.
The cervicalcentra are broad, long, opisthocoelous, pneumatic and host pleurocoel. The opisthotic dorsal vertebrae
represent 3 morphs like short and broad centra, short and circular centra, tall and relatively long. The neural spine isundivided. There is no hyposphene-hypantrum articulation. The sacralvertebrae are broad with ventral keel. Anteriorcaudal centraare broad while the mid caudals are strong to moderately tall while posterior caudals are slightly tall.
Along with other features, its main characters are mid caudal tallness and ratio 1 of mid transverse width of dorsal face
to mid transverse width of ventral face of mid caudal centrum i.e., mid caudal centrum dorsal and ventral faces andareas are almost equal. All the caudal vertebrae are strongly procoelous (except anteriormost caudals). Neural arch issituated on the anterior half of the caudal centra. One caudal cone with horizontal groove (Fig.1) show unique featurein pakititanosaurs. Distalmost caudal centrum is trispinous. Anterolateral edge of sternum is maximum thick and hasanteroventral crest and becoming gradually thin as proceeding posterior and medial directions. Dorsal/outer surface ofscapularepresents dominant convexing curvature and ventral/inner surface is concave, forming asymmetric D shapecross section. Distal scapula is deflected laterodorsally and expanded in the lateroventral side of mid scapular blade(while the distal scapula of balochisauridsis not deflected laterodorsally i. e., it is straight or slightly deflected mediallyand also not expanded in the lateroventral side of mid scapular blade). Distal scapula and coracoid are separate.
Coracoidplate is maximum thick at the glenoid area and become thin abruptly in the other areas except toward therugose articular area for the attachment of scapula. Proximal humerusis slightly rugose while distal humerus has
intense rugosities. Humeral midshaft cross section shape is elliptical, with long axis oriented transversely. Proximaland distal ends of radiusare expanding well. Proximal end is elongated sub oval type, while the distal end is sub116

Poster Session

rectangle type. Radius shaft is nearly circular, only oval when attaching with the distal ends. Proximal ulnais rugosewith a prominent olecranon process. Proximal ulna is gracile and represents a triradiate structure with three faces.
Ulnar proximal condylar processes are unequal. Metacarpalcross section is triangular. Proximal surface of shaft isrugose. Distal end is undivided and has no rugosities showing absence of phalanges and claw. Broken part ofiliarepresents parallel spongy/pneumatic texture with large open internal cells. Preacetabular process is thick and platy.
Ventrally the acetabulumis long and circular and bears parallel ridges indicating calcified tendons. Femorarepresent
proximal one third medially deflected and elliptical mid shaft. The constricted part of femur seems to be relatively
high. Slender tibiarepresents elongate and thin/narrow proximal surface observed on proximal view and lunate distal
surface observing on distal view. The mid tibia is oval shape in cross section. The slender and stocky nature of tibia is
one of the differentiating features between pakisaurids and balochisaurids respectively. Fibularproximal tibial scar iswell marked and deepening anteriorly. Distal fibula is oval shape. Fibular distal condyle size is more than twice
midshaft breadth. Multitypes armor boneslike ellipsoid with median cut, false jaw ramus with false teeth/spikes andfalse jaw arc type with false teeth/spikes are assigned to Pakisaurus balochistani (Fig.1).
Associated partial skeletons of sauropod and theropod dinosaurs and mesoeucrocodiles from the Terminal
Cretaceous of Pakistan: More than a dozen associated skeletons are collected from the red muds of Latest Cretaceous
Vitakri Formation (67-66 Ma). First associated skeleton of Sulaimanisaurus gingerichiis collected from Sangiali PDL(Pakistan Dinosaur Locality) 1, second associated skeleton of Maojandino alamicollected from central Alam PDL 19,
third associated skeleton of Nicksaurus razashahicollected from North Kinwa PDL 4, fourth associated skeleton of
Balochisaurus malkani(named on Malkani tribe inhabitant of Indo-Pak subcontinent but not on author name M. Sadiq)
from central site of Mari Bohri PDL 15, fifth associated skeleton of Marisaurus jeffifrom northernmost site of Mari
Bohri PDL 15, sixth associated skeleton of South Bor PDL 2 exemplar of Marisaurus jeffi, seventh associated skeletonof Top Kinwa (PDL 4) exemplar of Marisaurus jeffi, eighth associated skeleton of Pakisaurus balochistanifrom SouthKinwa PDL 4, ninth associated skeleton of West Bor (PDL 2) exemplar of Pakisaurus balochistani, tenth associatedskeleton of Top Kinwa (PDL 16) exemplar of Pakisaurus balochistani, eleventh associated skeleton of North Alam
(PDL 19n) exemplar of Pakisaurus balochistani,twelfth articulated and associated skull bones of Gspsaurus
pakistanicollected from Alam PDL 19, thirteenth articulated almost complete skull of Saraikimasoom vitakri collected(partly excavated) from South Kinwa PDL 4, fourteenth associated skeleton of Sulaimanisaurus gingerichi found fromSouth Kinwa PDL 4, fifteenth associated skeleton includes rostrum, vertebral and limb bones of Induszalim balafoundfrom central Alam PDL 19c, sixteenth associated skeleton of Vitakrisaurus saraikicollected from Bor PDL 2.
Discussion on titanosaurs of Indo-Pak subcontinent: About ten titanosaurian sauropods are known from the Latest
Cretaceous of South America, six from India and nine from Pakistan. Wilson and others in 2011 interpreted twosauropod genera (Isisaurusand Jainosaurus) of India the mirror image of Pakisauridae and Balochisauridae but they117

Poster Session

ignored the third genus hosting stocky tibia (with almost circular midshaft) and dorsal and ventral width of midcaudal
centrum ratio about 2 like Balochisaurus because both of these Indian genera show caudal ratio1 (close to 1).Wilson
and others in 2011 assigned caudal centrum (like Pakisaurus) to Jainosaurus. Isisaurus also have square shaped caudal
with caudal ratio almost 1.So the Jainosaurus and Isisaurusof India both these belong to Pakisauridae (ratio of midtransverse width of dorsal face to mid transverse width of ventral face of mid caudal centrum is about 1). So thequestion arises for the stocky tibia hosting taxa which are common in Pakistan and also show mid dorsal face width tomid ventral face width of mid caudal centrum ratio more than 1 (vary from 1.3 to 2). It means atleast the third species
Balochisaurusmalkani (a member of Balochisauridae) exist in Pakistan which host stocky tibia and caudal ratio about
2. Nicksaurusand Saraikimasoommay be close to Balochisaurus. Khetranisaurusfossils are distinct but very rare. If theslender tibia for Jainosaurusand stocky tibia for Isisaurus is assumed, but both show mid caudal ratio 1, which
revealed the presence of third genus having mid caudal ratio more than 1 which commonly exist in Pakistan.
Conclusively the third genera hosting stocky tibia and caudal ratio 2 will be Balochisaurus (or its closerNicksaurus
orSaraikimasoom) balochisaurids which host the stocky tibia and caudal ratio about 2 of mid transverse dorsal width toventral transverse width of mid caudal centra. If I follow Wilson and others report of 2011 to reduce the richness ofsauropod taxa in Indo-Pak subcontinent, then at least three valid genera of titanosaurian sauropods are found in
Indo-Pak subcontinent in any above cases. The first genus is Isisaurus colbertifrom India and Sulaimanisaurus
gingerichi (square, mid caudal ratio 1, slender tibia) from Pakistan, the second genus is Pakisaurus balochistanifrom
Pakistan (tall, mid caudal ratio 1, slender tibia) and Jainosaurus septentrionalisfrom India, and third genus is
Balochisaurus malkani (or its closerNicksaurus razashahi orSaraikimasoom vitakri) from Pakistan. Pakistan has
dominant bones of Balochisauridae than Pakisauridae while India has common fossils of Pakisauridae. India has
dominant fossils of theropod while Pakistan has dominant fossils of mesoeucrocodiles. India is rich in egg clutches ofdinosaurs while Pakistan is rich in footprints and trackways of dinosaurs.

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119Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Field Guidebook

Field Guidebook∙ SCHEDULE

Oct. 23. 2017 (Mon)
08:30-11:30

Ramada Songdo Hotel, Incheon ➡ Buan, Jeollabuk-do

11:30-12:00[Stop 1] Observe the Gyeokpori Formation : Jurassic Granite

12:00-13:00

Lunch

13:00-14:30[Stop 2] Observe the Gyeokpori Formation : Delta lobe system and Soft-sediment
deformation structure

14:30-16:00[Stop 3] Observe an exposure of the Jeokbyeokgang peperite

16:00-18:00

Buan, Jeollabuk-do ➡ Fontana Beach Hotel, Mokpo

18:30-20:00

DinnerOct. 24. 2017 (Tue)08:00-09:00
09:00-11:00
11:00-12:00
12:00-13:00
13:00-15:00
15:00-17:00
17:00-19:00
19:00-20:30

Fontana Beach Hotel, Mokpo ➡ Dinosaur Museum, Haenam[Stop 4] Observe the Uhang-ri Formation : Dinosaur tracks
Dinosaur Museum, Haenam ➡ Boseong, Jeollanam-do
Lunch
Boseong, Jeolla-Namdo ➡ Goseong, Gyeongsangnam-do[Stop 5]Observe the Jindong Formation : Sangjokam section
Goseong ➡ Busan Beach Hotel, Busan
DinnerOct. 25. 2017 (Wed)08:30-09:00
09:00-12:00
12:00-13:00
13:00-14:00
15:35-16:35
16:35-17:35
18:30-20:00

Busan Beach Hotel, Busan ➡ Songdo Peninsula Geosite, Busan[Stop 6] Observe the Dadaepo Formation : Dadaepo basin
Lunch
Songdo, Busan ➡ Gimhae International Airport
Gimhae International Airport ➡ Jeju International Airport
Jeju International Airport ➡ Accomodation
Dinner

Accomodation
Contact
Information

Ramada Songdo Hotel, Incheon : +82-32-832-2000
Fontana Beach Hotel, Mokpo : +82-61-288-7000
Busan Beach Hotel, Busan : +82-51-231-0750

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Field Guidebook∙ Field Guide Map

124Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

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Oct. 23. 2017 (Monday)

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Introduction
During the Cretaceous, the northeastern margin of the Eurasian Plate was subjected to sinistral crustal deformationand continental arc volcanism by oblique subduction of the Izanagi Oceanic Plate beneath the Eurasian Plate (Klimetz,
1983; Engebretson et al., 1984; Watson et al., 1987; Kim et al., 1997; Taira, 2001; Chough and Sohn, 2010; Liu et al.,2014)(Fig. 1). As a result, non-marine volcanic and sedimentary successions and plutonic rocks formed on the Korean
Peninsula along NE-SW- and NNE-SSW-trending fault systems (Kim et al., 2012; Chough, 2013,and references
therein). A number of detailed studies have been conducted on the crustal evolution and tectonic history of theCretaceous Korean Peninsula and nearby areas (Chun and Chough, 1992; Rhee and Chough, 1993a,b; Rhee et al.,
1993; Chun and Kim, 1995; Kim et al., 1995, 2003; Jo et al., 1997; Kim et al., 1997; Rhee et al., 1998; Lee andChough, 1999; Ryang and Chough, 1997, 1999; Jo and Chough, 2001; Paik et al., 2001; Jo, 2003; Ryang, 2003; Kim etal., 2009; Chough and Sohn, 2010; Kwon et al., 2013; Ghim and Hwang, 2014).
Recent mapping results in the southwestern part of the Korean Peninsula showed that Cretaceous volcanic rocks
occur along a NE-SE-trending, sinistral strike-slip fault (Hamyeol Fault)(Figs. 2 and 3). Based on their spatial
distribution, the volcanic rocks are classified into three lithostratigraphic units: the Buan, the Seonunsan, and theBeopseongpo Volcanics (Kwon et al., 2017)(Fig. 2). These volcanics are composed of various types of pyroclastic,
sedimentary, and lavas/intrusive rocks (Koh et al., 2013; Kwon et al., 2015, 2017)(Fig. 3). These observations indicatethat each volcanics had been formed by deposition of the intrusive/lava flows and primary/secondary pyroclastic
materials of various independent volcanic eruptions and sedimentation events. The shape of the craters and nested
cauldron structures are not currently observable, due to denudation after volcano formation. However, since thevolcanoes exhibit distinct and large topographic characteristics and contain a wide variety of volcanic rock, they are
determined to be calderas formed from the depositions of numerous volcanic eruptions (Cas and Wright, 1987;
Gottsmann and Marti, 2008). In other words, each tuff found in these volcanics is interpreted as a product of acaldera-forming eruption, and it can then be inferred from the diverse rock composition of each volcanics, that the
volcanics were formed from complex volcanic evolutionary processes. For further understanding of the eruption,
sedimentation, and spatiotemporal evolutionary processes of calderas, additional in-depth studies on each volcanic rockare needed.
Conformable stacking (> 1 km thick) of the volcanic rocks in the Buan, Seonunsan, and Beopseongpo Volcanics, aswell as the SHRIMP zircon U-Pb age (87-85 Ma), suggests that intense explosive volcanic activity occurred in thesouthwest of the Korean Peninsula (Kwon et al., 2017)(Fig. 4). This is consistent with the Late Cretaceous volcanic
rocks in the southern part of the Korean Peninsula that formed by regional crustal extension. This interpretation is also
supported by recent geological mapping results that indicate a wide distribution of Late Cretaceous volcanic rocks
along the southwestern to southern part of the Korean Peninsula (Choi and Hwang, 2013; Koh et al., 2013; Song, et al.,127

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2013; Kihm et al., 2014; Kim et al., 2014; Kwon et al., 2015). In addition, geochronology data of Late Cretaceous
volcanic rocks in the Korean Peninsula are comparable to laser ablation inductively coupled plasma-mass spectrometry(LA-ICP-MS) U-Pb age data of the volcanic rocks in the Aioi and Arima groups in the central part of the JapaneseIslands (approximately 86-81 Ma; Sato et al., 2016). The distribution and comparable ages of the Late Cretaceous
volcanic rocks reflects that, during the Late Cretaceous, regional volcanic activity (from the Japanese Islands to thesouthwestern Korean Peninsula) occurred on the eastern edge of the Eurasian Plate, presumably resulting from thedevelopment of a magma plumbing system by upwelling of hot asthenosphere coupled with regional crustal extension
during slab rollback. Furthermore, the spatial distribution of the Buan, Seonunsan, and Beopseongpo Volcanics along
the Hamyeol Fault indicate that volcanic activity occurred along the fault, suggesting that this fault acted as a favorable
pathway for rising magma toward the surface, in a similar manner to Andean continental arc volcanism (Acocella,2014).

Figure 1. A paleogeographic plate reconstruction of the Japanese Arc relative to the Korean Peninsula during theCretaceous (modified from Chough and Sohn, 2010). The distribution of intrusive-extrusive-non-marine deposits
represents a volcanic arc associated with subduction of the Izanagi Plate under the Asian continent.

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Figure 2. Satellite image (data from Google Earth) and distribution of Cretaceous rocks in the southwestern partof the Korean Peninsula. Cretaceous volcanic rock groups (Buan, Seonunsan, and Beopseongpo Volcanics) are distributed along the NE-SW trending Hamyeol Fault. NHF = Northern Hamyeol Fault; SHF = Southern Hamyeol
Fault.

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Figure 3. (Former page). Geologic map of Buan and Seonunsan Volcanics (modified after Koh et al., 2013). Eachvolcanic unit is divided into many lithological subunits (formations). Each unit has a unique distribution and lithological composition, indicating independent volcanic systems. See Figure 2 for location.

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Figure 4. Distribution of Cretaceous plutonic, volcanic, and sedimentary rocks in the Korean Peninsula, showing
previous and present SHRIMP zircon U-Pb age data.

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Geologic setting: characteristics of the Cretaceous volcano-sedimentary basin system in the Korean Peninsula
During the Cretaceous, the Korean Peninsula was situated on the northeastern edge of the Eurasian Plate and was
subjected to broad sinistral deformation due to oblique subduction of the oceanic Izanagi Plate beneath the Eurasian
Plate (Fig. 1). NE-SW- and NNE-SSW-trending sinistral strike-slip fault systems developed on the Korean Peninsula(from north to south, these were the Chugaryeong, Kongju, Hamyeol, and Gwangju Fault Systems; Fig. 1). Small-scale2(< 50 × 50 km ), non-marine sedimentary basins formed along these fault systems along with the Gyeongsang Basin,
which is the largest sedimentary basin (~20,000 km2) in the Korean Peninsula (Fig.1). The Chugaryeong Fault Systemcomprised many N-S- and NNE-SSW-trending sinistral strike-slip faults, along which the Cheolwon, Namyang (orSihwa), Tando, and Chunsuman Basins formed (Fig.1). The basin-fill sediment is composed largely of siliciclastic
deposits that accumulated in alluvial-fluvial-delta-to-lacustrine environments and is frequently intercalated withbasaltic to rhyolitic volcanic rocks (Kee, et al., 2006a&b; Kim, et al., 2009; Kwon, et al., 2013). SHRIMP zircon U-Pb
age dating on the volcanic rocks has revealed ages of approximately 115-109 Ma (Hwang, et al., 2011; Kee, et al.,2006b; Kim, et al., 2012), indicating that these sedimentary basins were formed during the Early Cretaceous (Fig. 4).
In the south-central region of the Korean Peninsula, the Gongju, Gwangju, and Hamyeol Fault Systems trend in a
NE-SW direction (Fig. 1). Non-marine sedimentary basins (Eumseong, Gongju, Buyeo, Pungam, Kyokpo, Yongdong,
Jinan, Neungju, and Haenam Basins) developed along the fault systems, and the basin-fill sediments were deposited inalluvial fan and fluvio-lacustrine environments. Basaltic to rhyolitic volcanic rocks are also intercalated with thebasin-fill sediments (Chough, 2013, and references therein). In the case of the Gongju Basin, K-Ar ages of basaltic
andesites covering the basin-fill sediments were estimated at approximately 77 Ma (Cheong, 2002), while SHRIMP
zircon U-Pb ages of the volcanic rocks in the northeast of the basin were dated at approximately 108 Ma (rhyolitic tuff)
and 84 Ma (quartz feldspar porphyry) (Kim et al., 2010). These ages indicate that basin formation and volcanism in the
Gongju Fault System was continuous from the Early to Late Cretaceous (Fig. 4).
The Gyeongsang Basin, which is the largest non-marine sedimentary basin on the Korean Peninsula, contains
deposits up to 9 km thick, non-marine sedimentary rocks (Sindong and Hayang Groups), volcanic rocks (Yucheon
Group), and plutonic rocks (Bulguksa granites), which formed from the Early to Late Cretaceous (Chang et al., 1997).
The Sindong and Hayang Groups are mostly comprised of conglomerates, pebbly sandstones, sandstones, mudstones,
shales, and carbonate rocks, with intercalated layers (< 100 m thick) of basaltic to rhyolitic volcanic rocks. Zircon fromthe Gusandong Tuff exposed in the upper part of the Hayang Group was LA-ICP-MS age dated to approximately
96-97 Ma (Jwa et al., 2009). The Yucheon Group, which overlies the aforementioned groups, is comprised mostly ofrhyolitic to andesitic volcanic rocks and volcanogenic sedimentary rocks (Chang, 1975; Chang, et al., 1997). Recently,
Chough and Sohn (2010) interpreted the sedimentary (Sindong and Hayang Groups) and volcanic rocks (Yucheon
Group) of the Gyeongsang Basin as the Gyeongsang back-arc basin and the Gyeongsang arc system, respectively,
which formed as a result of crustal extension and coeval continental arc volcanism due to subduction of the Izanagi
Oceanic Plate.

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Lithological characteristics of the Buan Volcanics
The Buan Volcanics are located at the southern end of the NHF. The unit is oval-shaped and has currently amaximum diameter of approximately 20 km in the NE-SW direction. Recently, Koh et al. (2013) classified thevolcanics into the Cheonmasan, the Yeondong, the Udongje, the Yujeongje, and the Seokpo Tuffs, the Gyeokpori
Formation, the Gomso Rhyolite, the Byeonsan Tuff, and the Samyebong Rhyolite, from bottom to top (Figs. 3 and 5).
The tuffs trend in ENE-WSW or WNW-ESE directions, and are inclined toward the north (Fig. 3). They are typicallymassive and very thick bedded (< 50 m). Locally the tuffs show a welded texture, defined by flattened pumices andbended vitric ash around the lithic clasts, and stratification defined by alternating lithic-rich and lithic-poor layers (Fig.
5). These tuffs are poorly sorted mixtures of ash-, lapilli-, and block-sized lithic clasts, pumices, and crystal fragments
supported within a fine volcanic ash matrix. The lithic fragments are purple mudstone, tuff, rhyolite, granite, gneiss,
and andesite. The crystal fragments are composed of, in descending order of abundance, quartz, plagioclase,
orthoclase, biotite, tachylite, and opaque minerals. Quartz crystal fragments are dominant within the Cheonmasan, theUdongje, and the Yujeongje tuff, while orthoclase and plagioclase crystal fragments are dominant in the Yeondong,
Seokpo, and Byeonsan tuff, with virtually no quartz fragments (Fig. 5). The Gyeokpori Formation, underlain andoverlain by the Seokpo Tuff and the Gomso Rhyolite, respectively, is composed of mudstone, sandstone, pebbly
sandstone, and conglomerate rock deposited in a lacustrine fan-delta, intercalated with rhyolitic tuff and volcanogenic
sediment horizons (Kim et al., 2003). In the uppermost part, peperites are present along the boundaries of the
Gyeokpori Formation and the Gomso Rhyolite. These volcanic and sedimentary rocks were intruded by the final stageof the Samyebong Rhyolite.

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Figure 5. Schematic diagram of the Buan Volcanics with brief descriptions and inferred thicknesses of the lithologicalunits.

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Sedimentological studies of the Gyeokpori Formation
The Gyeokpori Formation, about 300 m in thickness, occurred between the underlying Seokpo Tuff and overlying
Gomso Rhyolite (Fig. 5). It consists mainly of conglomerate, gravelly sandstone, sandstone, and mudstone, andrhyolitic (lapilli) tuffs are minorly interlayer at variable stratigraphic levels (Kim et al., 2003). Based on the constituent
sedimentary facies, their interbedding relationships and bedset-scale geometries, Kim et al. (2003) classified theformation into eight facies associations (FA) that represent distinctive depositional environments: subaqueous talus (FAI), delta plain (FA II), steep-gradient large-scale delta slope (FA III), base of delta slope to prodelta (FA IV),
small-scale nested Gilbert-type delta (FA V), small-scale delta-lobe system (FA VI), subaqueous fan (FA VII) andbasin plain (FA VIII). Two depositional sequences are identified from the formation: the lower coarsening- tofining-upward succession (up to 215 m thick) and the upper fining-upward succession (up to 75 m thick)(Fig. 6). Kim
et al. (2003) suggested three-stage depositional model of the Gyeokpori Formation, aggradation of subaqueous talus
and coarse-grained delta systems developed on the steep-gradient basin margin (stage 1), basinwide transgression
marked by black shale deposits (stage 2), and small-scale gravelly delta-lobe systems (stage 2), that strike-slip
movements on the basin-bounding faults were prevalent in the basin evolution (Fig. 7). However, recent detail geologic
mapping (Koh et al., 2013) shows that basin-bounding faults cannot be recognized in the vicinity of the formation, as
contacts with the basement rocks are mostly unconformable, and thus the previous basin configuration (pull-apart basinbounded by NE-SW-trending strike-slip faults) and controlling tectonics have to reconsider.

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Figure 6. Composite columar logs and stratigraphic correlation of the Gyeokpori Formation (Kim et al., 2003). The
formation comprises two depositional sequences. The lower succession show either a prograding to retrograding,coarsening- to fining-upward trending. The upper succession shows a retrograding fining-upward trend.

Figure 7. Basin-filling model of the Gyeokpori Formation (Kim et al., 2003).

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SHRIMP zircon U-Pb dating
To constrain the eruption/sedimentation period of volcanogenic sequences, we performed SHRIMP U-Pb age datingon zircon crystals separated from the Cheonmasan Tuff (CT), Udongje Tuff (UT), Seokpo Tuff (KP-2), and Yujeongje
Tuff (YUT) of the Buan Volcanics. The weighted mean of 206Pb/238U zircon ages from the Cheonmasan and Udongje
Tuffs are 87.23±0.92 Ma (n=18, 2σ, MSWD=2.2) and 86.79±0.71Ma (n=19, 2σ, MSWD=1.3), respectively (Figs.
8b,c). The zircon ages from the Seokpo and Yujeongje Tuffs are 87.30±0.99 Ma (n=15, 2σ, MSWD=2.0) and86.66±0.93 Ma (n=20, 2σ, MSWD=2.8), respectively (Figs. 8d,f). Zircon U-Pb ages of the four Buan Volcanic tuffs
are equal within the error range.

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Figure 8. Cathodoluminescence (CL) images of zircons and Tera-Wasserburg diagrams of the Buan Volcanics. CL
images of zircons with analysis spots and 206Pb/238U ages for (a) Cheonmasan and (e) Yujeongje Tuffs.
Tera-Wasserburg diagrams of analyzed U-Pb isotope ratios of zircons separated from (b) Cheonmasan, © Udongje,(d) Seokpo, and (f) Yujeongje Tuffs. Gray dotted ellipsoid is excluded from the weighted mean calculation.

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Stop locations

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Stop 1- Unconformable contact with the basement rock (Jurassic granite)

Figure 9. Unconformable and high-angle contact with the basement.

The Gyeokpori Formation rests on a basement of Precambrian gneiss and Jurassic granite (or quartz monzonite;
Lambiase & Bosworth, 1995)(Fig. 9). The granite is exposed as a small mass in the Gyeokpo beach and is recoveredfrom nearshore boreholes. A K-Ar age of the quartz monzonite (128±3.0 Ma) defined the lower sedimentation age ofthe formation (Lambiase & Bosworth, 1995). Recent SHRIMP zircon U-Pb age of the monzonite (or granite),
however, is ca. 170 Ma. SHRIMP zircon U-Pb age of the underlying Seokpo Tuff is 87.3±0.99 Ma (Kwon et al., 2017),
which indicating the lower limit of the formation. The formation consists mainly of graded or bedded
conglomerate/sandstone couplets in the lower part, where it abuts the basement (granite), and thin- to thick-bedded
sandstones in the upper part. Kim et al. (2003) interpreted these strata as a small-scale delta-lobe system.

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Stop 2- Delta lobe system and Soft-sediment deformation (SSD) structure▪ Stop 2-1: Delta lobe system

Figure 10. Mound-shaped gravelly sandstone and conglomerate strata within sandy black-shale strata. Note theoutward dipping of individual beds.

Along the coastal cliffs and wave-cut terraces of the Gyeokpo harbor, sedimentary sequence is well exposed (Fig.
10). This section consists mainly of sandy black-shale sequence interlayered bedded gravelly sandstones andconglomerates, having a mound-shaped or lobate bodies. Each body is a few meters high (up to 9 m) and a few tens ofmetres wide (up to 30 m). They are conformably underlain and overlain by sandy black shale deposits, forming an
isolated or coalesced package. Individual beds dip outward toward both lateral margins, abruptly downlapping onto theunderlying strata.

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▪ Stop 2-2: Soft-sediment deformation (SSD) structure

Figure 11. Exposure of SSD structures show a well lateral continuity. Each SSD structure distinguished by undeformed mudstone layer between them.

The SSD structures (up to 2m-thick) occurred continuously (>200 m-wide) within the black mudstone andconglomerate strata along the coastal cliff of the Gyeokpo harbor (Fig. 11). The highly deformed black mudstones
indicate that the deformation is generated by gravity-driven slumping on a basin plain environment with low gradientless than <1°. The SSD, consisting of fold, thrust and normal fault, shows different geometric characteristics at threesites (site 1 to 3 from east to west)(Figs 12~14). The folding at site 1 predominantly occurs in the middle to upper part(from 1 to 2m-high) of the deformed layer together with syn-deformational faults (thrust and normal fault), whereas
folding observed in the whole layer (up to 2 m-thick) at site 2 and 3 without the faults. Fold vergence at site 1 and 2 istoward east, but is variable at site 3. Scattered directions of the fold hinge and axial plane of the folds together withdiverse vergence directions of the folds indicate that the folds can be classified into a non-cylinderical fold. The
inferred paleoslope direction on the basis of the Fold Hinge Azimuth and Interlimb Angle Method (HIM) is ESE (120˚)(Fig. 15), and it is toward the Buan Volcanics locating the east side of the Gyeokpo Basin and is inconsistent withpaleoflow direction inferred from a previous study (north- to northwest-ward; Kim et al., 2003). This envisages that thetriggering mechanism of the SSD is closely related to volcanogenic-slumping, which was caused by volcanic-ward
tilting of the basin floor during and/or shortly after volcanic eruptions.

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Figure 12. Characteristics of fold geometry at site 1. Outcrop photographs showing east-verging (a) and west-verging(b) folds. It is noteworthy that the east-verging folds are mainly occurred in the middle to upper part of the deformed
layer, while the west-verging folds at the bottom. Stereographic projection (lower hemisphere, equal area) of foldhinges (c) and axial planes (d).

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Figure 13. Characteristics of fold geometry at site 2. (a) An outcrop photograph showing recumbent, asymmetricfold verging toward ESE-direction on a detachment. Z-, M-, S-shaped parasitic folds are well developed. (b) An
enlarged photograph of hinge zone of the asymmetric fold. It is notable that higher order crenulation fold is cogenetically occurred parallel to the first order asymmetric fold. Stereographic projection (lower hemisphere, equal area)of fold hinges (c) and axial planes (d).

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Figure 14. Characteristics of fold geometry at site 3. (a) An outcrop photograph showing various directions of foldverging well observed compared with other sites. (b) An outcrop photograph showing gently curved fold hinge-line
is well exposed. Stereographic projection (lower hemisphere, equal area) of fold hinges (c) and axial planes (d).

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Figure 15. Hinge Interlimb Method (HIM) plot of fold hinge azimuth and interlimb angle data, suggesting a preferredslope direction of 120°.

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Stop 3- Jeokbyeokgang peperite

Figure 16. Photograph of peperites along interface between rhyolite and host sediment (hammer is 28 m in length).

The peperites occur along the coastline in the western part of the Buan Volcanics where the Gyeokpori Formation is
conformably overlain by < 30 m thick, rhyolite (lava flow, Kim, 2000)(Fig. 16). In this area, the Gyeokpori Formationconsists mostly of laterally continuous, laminated to bedded couplets of dark-gray mudstones and sandstones(basin-plain deposits of a lacustrine fan-delta system (Kim et al., 2003)). At the contact with the Gomso Rhyolite, thehost sediment is distorted with the development of a series of load and flame structures. The peperites area are
generally thinner (<0.5 m) in load zones and thicker (≤3 m) in flame zones. In addition, based on the position of
peperites on the load and flame structures, the peperites show vertical and lateral textural variations, and, thus weclassified the peperites into two species (Type-1 and Type-2).
Type-1 peperites are common in the load zones, whereas Type-2 peperites only occur above the flame zones. Type-1
peperites are composed of rounded to blocky varieties. The rounded juvenile clasts (rhyolite fragments) have gently
curved margins and commonly present near to the sediment-rhyolite contact (Fig. 17a). The blocky juvenile clasts havewell-defined, sharp planar margins. The blocky ones are closely packed and show a jigsaw-crack texture (Fig. 17b).
Type-2 peperites occur above the flame zones and are surrounded by rhyolite (Fig. 18a). They decrease in thickness
laterally away from the flame zones together with lateral textural variations, which can be used to delimit a proximal
zone composed of poorly sorted mixtures of juvenile clasts, a middle zone showing a jigsaw-crack texture, and a distal

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zone characterized by reticular fracture networks (Fig. 18).
The peperites are interpreted to form by flowing of lava flow over the wet substrate (the Gyeokpori Formation). The
disruption of the host sediment indicate that it underwent fluidization owing to heat transfer from the overlying rhyolite(Busby-Spera and White, 1987). In addition, loading of the 30-m thick rhyolite to the fluidized host sediment gave riseto the development of load and flame structures. Rounded juvenile clasts in Type-1 peperites are inferred to be formedby abrasion of initially angular juvenile clasts by continued motion of the overlying lava flow, after brittle
fragmentation occurred. The blocky juvenile clasts were produced by in situ quenching fragmentation caused bythermal contraction of rhyolite, resulting in the development of the jigsaw-crack texture (Hanson and Wilson, 1993).
The platy, angular to polyhedral juvenile clasts present in Type-2 peperites also indicate brittle fragmentation. The
lateral tapering of Type-2 peperites and a decrease in abundance of fine-grained juvenile clasts away from the flamezones suggest that the efficient of responsible fragmentation processes propagated from flame zones towards theinterior of the rhyolite (Fig. 19). Because of the development of the load and flame structures, the fluidized hostsediment and pore water was concentrated toward the flame zone, and pressure would have increased towards theoverlying lava flow at each of the flame zones (Hurst et al., 2011). As a result, the sediment-laden pore water has been
vertically injected into hot interior of the rhyolite and undergone volume expansion. When the increased pore pressure
exceeded the loading pressure, internal steam explosions would have taken place within the rhyolite, resulting in a
rapid release of mechanical energy (e.g., a shock wave) and brecciation of the surrounding featureless rhyolite. Lateraltapering of Type-2 peperites within the rhyolite and absence of widely dispersed juvenile clasts in the host sediment(Skilling et al., 2002) indicate that the mechanical energy was transferred laterally, resulting in lateral variations intextures of Type-2 peperites.

Figure 17. Photographs of Type-1 peperites. (a) Photographs of rounded juvenile clasts with gently curved margins(arrows and inset). The rounded juvenile clasts tend to occur near to the boundary with the host sediment. (b)Jigsaw-crack texture in the polyhedral, coarse-grained juvenile clasts.

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Figure 18. Photographs of Type-2 peperites. (a) Type-2 peperites only occur above the flame zones and laterally
penetrate into the interior of the featureless rhyolite. (b) The proximal zone of Type-2 peperites. (c) Photographsof the middle zone, which consists mostly of tetragonal to polyhedral, coarse-grained juvenile clasts that commonly
contain jigsaw-crack textures. (d) Interconnected, reticular, and mud-filled fractures, and tabular to wedge-shaped,
coarse-grained juvenile clasts in the distal zone, which gradually transitions into featureless rhyolite by the lateraltapering, merging, and disappearance of fractures

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Figure 19. Schematic models for the formation processes of Type-1 and Type-2 peperites (not to scale). See section
5.2 in the main text for detailed interpretation (Abbreviations: P= proximal zone, M= middle zone, D= distal zone).

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Jo, H. R., Rhee, C. W., and Chough, S. K., 1997, Distinctive characteristics of a streamflow-dominated alluvial fan
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Jwa, Y. J., Lee, Y. I., and Orihashi, Y., 2009, Eruption age of the Kusandong Tuff in the Cretaceous Gyeongsang
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Kee, W.S., Cho, D.R., Kim, B.C., and Jin, K.M., 2006b, Geological report of the Pocheon sheet (1: 50, 000). Korea
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Kihm, Y.H., Choi, P., Hwang, J.H., Kim, H., Ko, K and Chun, H.Y., 2014, Geological report of the Mokpo sheet(1:50,000). Korea Institute of Geoscience and Mineral Resources, Daejeon, 93p, (in Korean with English
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PhD Thesis, Seoul National University, Seoul, Korea.
Kim, S.B., Chough, S. K., and Chun, S. S., 1995, Bouldery deposits in the lowermost part of the Cretaceous
Kyokpori Formation, SW Korea: cohesionless debris flows and debris falls on a steep-gradient delta slope:
Sedimentary Geology. 98, 97-119.
Kim, S.B., Chough, S.K., and Chun, S.S., 2003, Tectonic controls on spatio-temporal development of depositional152

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systems and generation of fining-upward basin fills in a strike-slip setting: Kyokpori Formation (Cretaceous),
south-west Korea: Sedimentology 50, 639-665.
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Kyokpo Pull-Apart Basin, South Korea and tectonic implication for inverted extensional basins: Journal of
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Kim, S.B., Kim, Y. G., Jo, H. R., Jeong, K. S., and Chough, S. K., 2009, Depositional facies, architecture andenvironments of the Sihwa Formation (Lower Cretaceous), mid-west Korea with special reference to dinosaur
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Kim, S.W., Kwon, S., Ryu, I. C., Jeong, Y. J., Choi, S. J., Kee, W. S., Yi, K., Lee, Y. S., Kim, B. C., and Park, D.
W., 2012, Characteristics of the early cretaceous igneous activity in the Korean Peninsula and tectonic
implications: Journal of Geology 120, 625-646.
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Geoscience and Mineral Resources, Daejeon, 76p, (in Korean with English abstract).
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Koh, H. J., Kwon, C.W., Park, S.I., Park, J., and Kee, W.-S., 2013, Geological report of the Julpo andWido-Hawangdeungdo sheets (1: 50,000). Korea Institute of Geoscience and Mineral Resources, 81p, (inKorean with English abstract).
Kwon, C.W., Choi, S.J., Lee. Y.N., Chwae, U.C., Kee, W.S., and Kim, B.C., 2013, Depositional environment andbasin development of the Cretaceous Tando Basin, mid-west Korea. Journal of the Geological Society of Korea
49, 47-71, (in Korean with English abstract).
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Bunamgundo· Imjado sheets (1:50,000). Korea Institute of Geoscience and Mineral Resources, 65p, (in Korean
with English abstract).
Kwon, C.W., Ko, K., Gihm, Y.S., Koh, H.J. and Kim H., 2017, Late Cretaceous volcanic arc system in thesouthwestern Korea: Distribution, lithology, age, and tectonic implications. Cretaceous Research, 75, 125-140.
Lee, S. H., and Chough, S. K., 1999, Progressive changes in sedimentary facies and stratal patterns along the
strike-slip margin, northeastern Jinan Basin (Cretaceous), southwest Korea: implications for differential
subsidence. Sedimentary Geology 123, 81-102.
Liu, L., Xu, X., and Xia, Y., 2014, Cretaceous Pacific plate movement beneath SE China: Evidence from episodic
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Paik, I. S., Kim, H. J., and Lee, Y. I., 2001, Dinosaur track-bearing deposits in the Cretaceous Jindong Formation,
Korea: occurrence, palaeoenvironments and preservation: Cretaceous Research 22, 79-92.
Rhee, C. W., and Chough, S. K., 1993a, The Cretaceous Pyonghae Basin, southeast Korea: sequential developmentof crevasse splay and avulsion in a terminal alluvial fan: Sedimentary Geology 83, 37-52.
Rhee, C. W., and Chough, S. K., 1993b, The Cretaceous Pyonghae sequence, southeast Korea: Terminal fan facies:
Palaeogeography, Palaeoclimatology, Palaeoecology 105, 139-156.
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deposits in Cretaceous alluvial successions, Korea: Sedimentary Geology 85, 401-410.
Ryang, W. H., 2003, Contrasting basin fills in a strike-slip setting, Eumsung Basin (Cretaceous), Korea:
Geosciences Journal 7, 263-275.
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basin (Cretaceous), Korea: Journal of Sedimentary Research 67, 274-285.
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margin of the Eurasian Plate: New zircon U-Pb ages from the Aioi-Arima-Koto region of SW Japan. Journal ofVolcanology and Geothermal Research 310, 89-97.
Skilling, I.P., White, J.D.L., McPhie, J., 2002. Peperite: a review of magma-sediment mingling. In: Skilling, I.P.,
White, J.D.L., McPhie, J. (Eds.), Peperite: Processes and Products of Magma-Sediment Mingling. J. Volcanol.
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crystal-rich, and pumice-free ignimbrite (the Cretaceous Kusandong Tuff, Korea): Sedimentary Geology 220,141-154.
Song, K.-Y, Kim, S.W., Ko, K. and Kim, B.c, 2013, Geological report of the Jeongup sheet (1: 50,000), Korea.
Korea Institute of Geoscience and Mineral Resources, Daejeon, 67p, (in Korean with English abstract).
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154

Proceedings and Field Guidebook for

The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Stop 4 & 5
Oct. 24. 2017 (Tuesday)

Stop 4 & 5

Stop 4. Uhang-ri section, Haenam County, Jeollanam-do
Introduction of Site 4 and Outcrop photos
At Stop 4 we will observe outcrops of the Cretaceous Uhangri Formation, big dinosaur tracks and the Dinosaur
Museum in Haenam, Southwest Korea. The outcrops of this formation are well exposed along the coastline before
reclamation.

Figure 4-1. An outcrop of the Uhangri Formation, Haenam shows well-laminated mudrocks interbedded with thinsandstones.

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Figure 4-2. Many bird tracks are well printed on a bedding plane of the Uhangri Formation.

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Figure 4-3. The first dinosaur footprints found in the Uhangri Formation, Haenam (above) and well-preserved dinosaurs tracks inside the roof building (below).

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Stop 4 & 5Geological Setting
The Haenam Basin in southwestern Korea is one of a series of Cretaceous NE-SW-trending isolated non-marine
basins. The basins were formed by strike-slip fault movements when subduction of the Pacific Plate occurred muchcloser to the Korean Peninsula. The Haenam Basin was filled by a succession of andesitic tuff, volcaniclastic andepielastic sedimentary sequence (Uhangri Formation), acidic tuff (Hwangsan Tuff), and rhyolite (Jindo Rhyolite) inascending order (Fig. 1). The Uhangri Formation consists of an approximately 400-m-thick sequence of interlayered
conglomerate, gravelly sandstone, sandstone, siltstone, black shale and chert beds (Fig. 1; Chough and Chun, 1987;
Chun and Chough, 1995). The lower part (ca. 130 m thick) of the formation consists mainly of thick, brown,
caliche-bearing siltstones, wedge-shaped disorganized conglomerates and thin gravelly sandstones, which together
represent floodplain environments influenced by occasional debris flows and sheetfloods. The lower middle part (ca.
110 m thick) comprises fining-upward cycles of stratified and/or inverseto- normally graded conglomerate-gravelly
sandstones, laminated sandstones and sandstone/ siltstone couplets (high-concentration turbidites; Chun andChough, 19921, which suggest delta front deposits formed in subaqueous lobes. The upper middle part (ca. 60 m
thick) is characterized by wedge-shaped conglomerates and (gravelly) sandstones bounded by scoured bases, whichindicate delta front deposits formed in distributary channels and mouth bars. The upper part (ca. 35-75 m thick)consists of a laterally continuous sequence of finely laminated mudstones, crudely stratified sandstones, andconvoluted sandstone/chert and laminated chert/black shale couplets. It contains symmetrical ripple marks, tracks ofshorebirds, syneresis cracks, plant fossils and brackish or freshwater ostracodes (Fig. 2), which collectively indicate
shallow lacustrine environments.

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Figure 4-4. Stratigraphic position and simplified geological map surrounding Stop 4, Uhangri Formation, Haenam(above) and columnar sections of the Uhangri Formation (below).

Sedimentary facies and Depositional environments.
Based on vertical and lateral facies analysis, the sedimentary facies described in the foregoing sections are grouped
into four facies associations. These are indicative of distinct depositional environments and sedimentary processes.
They include alluvial fan fringe, delta front and lacustrine margin.
- Facies association I: alluvial fan fringe
Occurrence and interpretation
Facies association I is characterized by thick homogeneous brownish mudstone units intercalated with wedged,
disorganized conglomerate and organized conglomerate-gravelly sandstone. Some massive or normally gradedsandstone units also occur. This association accurs in the lower part of the Uhangri Formation, which is about 130 m inthickness. The brownish colour of the mudstone suggests that they were under oxidizing and periodically wetted
conditions after deposition, reflecting a low water table. Caliche nodules that are made up of glaebules occur
commonly in the brownish mudstone, indicating subaerial exposure. The mudstone most likely results from overbank

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suspension deposition on the fringe of an alluvial fan. Two units of thick, massive, fine tuff are intercalated in the
mudstone. Massive to crudely laminated, greenish coarse ash-rich layers occur ubiquitously in this association.
The wedged conglomerate units are either clastor matrix-supported. In both cases, their matrices are composed ofbrowish mudstone and fine volcanic ash. The disorganized conglomerate units with wavy and irregular geometry canbe interpreted as cohesive subaerial debris-flow deposits. Individual units show either non-erosive orslightly ersive
bases and have a patchy occurrence in both lateral and vertical section. These characteristics are suggestive of subaerial
debris flows. Both the facies association and the architectural patterns are similar to those of the distal volcaniclastic
facies of Vessell & Davies and Smith.
The thinly interlayered conglomerate-gracelly sandstone units are normally graded, inversely graded orinverse-to-normally graded. Each unit is laterally continuous and is clast-supported. Units of massive sandstone andnormally graded sandstone are commonly interlayered with those of homogeneous siltstone and gravelly sandstone.
The massive sandstone is dominantly underlain by inversely or inverse-to-normally graded gravelly sandstone and bynormally graded sandstone, giving facies transitions of G3->S1 and S2->S1 and S2->S1. The facies transitions
represent the depositional sequences developed by rapid frictional freezing of high- and low-concentration utrbidity
currents. Lateral continuity, moderate to good sorting, clast-supported texture and orizontally stratified gravel-sandunits are all suggestive of deposition by unconfined sheetfloods in a non-channellized subaerial setting.
Discussion
The depositional model of facies association I poses two unresolved problems. One is the drainage system and its
channel system on the fringe of the alluvial fan. The other involves the origin of the thick homogeneous siltstone.
Outcrops of association I occur only in the northern coast and wave-cut benches at Byongonri. Flute casts, channel
geometry and cross-stratification in the overlying, subaqueous, coarse-grained sequences suggest that the prominentpalaeoflow directions generally trend north-south. Although exposure of the facies association I is restricted, its
lithological homogeneity suggests that the drainage system in similar to that of a low-sinuosity anastomosing river.
Dominance of homogeneous siltstone, laterally continuous sheetflood deposits and rapidly frozen cohesive suvaerial
devris flows are indicative of low to moderate slope gradient.
The homogeneous brownish siltstones interpreted as overbank brownish siltstones inter-preted as overbank
suspension deposits are variable in thickness, ranging from 10 cm to more than 4m. Fine-grained deposits by overband
flooding are generally thin, because sedimentation rates are rather low 엳 새 the relatively high velocity of flood
currents and low concentration of suspended sediment. During an exceptional flood in 1952, the Missouri Riverdeposited a layer of silt as much as 15 cm thick over wide area of the floodplain. Tunvridge reported that a single flood
event could deposit over 1-5m of parallel-laminated sand in semi-arid ephemeral streams. Very thick units could be
multistory deposits, although they do not show evident internal depositional boundaries. In volcaniclastic basins,
sedimentation is largely controlled by volcanic activity. Catastrophic floods result from explosive volcanic eruptions
and are responsible for the deposition of thick siltstone. The overbank sequences were also aggraded rapidly enough toescape pedogenic modification, similar to the fine-graned facies in the Ellensburg Formation reported by Smith.

163

Stop 4 & 5- Facies association II: delta front (subaqueous lobes)
Occurrence and interpretation
Facies association II consists of stratified conglomerate-gravelly sandstone, laminated sandstone and laminatedsand-siltstone with small-scale fining-upward cycles and largely low-angle trough cross-bedding. Some planar or
trough cross-stratified conglomerate-gravelly sandstone units also occur. This association is about 100m in thickness
and overlies association I in the lower part of the Byongonri section.
Association II is divided into four phases. Phase 1 consists of horizontally or trough cross-stratified gravelly
sandstone, laminated sandstone and laminated sandstone/ mudstone couplets. Stratified and normally orinverse-to-normally graded gravelly sandstone units are interlayered. These facies from a fining-upward sequence withfining-upward cycleds. Phase 1 was presumably deposited mainly by traction-dominand stream flow. Someinterlayered gravelly sand-stones and thin laminated sandstone are suggestive of the influence of turbidity currents.
The facies assemblage and depositional characteristics are similar to those of Phase 4 described later.
Phase 2 consists mainly of crudely stratified conglomerate-gravelly sandstone, thin laminated sandstone andlaminated sandstone/mudstone couplets, which form small-scale fining-upward cycles. Some cross-stratified gravelly
sandstone, inverse-to-normally graded gravelly sandstone and massive sandstone units are also interlayered. They are
low-angle trough cross-bedded and form a thick fining- and thinning-upward sequence. The Phase 2 sequence wasinitiated probably from slumps which scoured the underlying laminated sandstone/mudstone. The slump scar was thenfilled with avalanched gravels and boulder clasts of probable debris flow origin. It was followed by high-concentration
turbidity currents, resulting in fining-upward cycles. The Phase 2 wequence shows a broad lens shape geometry withconcave-up base and convex-up top.
Phase 3 corresponds to a slightly prograding sequence, which was deposited between lobes of phases 2 and 4. The
facies sequence probably represents traction-dominaant streamflow deposits. Although some wedged debris-flow
deposits are observed, most facies units are laterally continuous for more than 50m.
Phase 4 consists mainly of variable facies units deposited by traction-dominant unconfined streamflows andlow-concentration turbidity currents. In contrast to phases 2 and 3, cross-stratified gravelly sandstone and sandstonefacies(Facies G5, S5) are relatively common in this phase. Rapidly frozen deposits(Facies G1, G2, S1, M1) also occur
commonly. This phase comprises several fining-upward cycles, similar to phases 1 and 2. It also shows a broad
lens-shape geometry with concave-up base and convex-up top. This lobe sequence was initiated from channel filling
due to subaqueous channel bar migration by traction-dominant stream flows (Facies G5) and following cohesionlessdebris flows and high-concentration turbidity current (Facies G1). The flows were generally transformed into
low-concentration turbidity current (deposits of Facies S4, S5, S/M1), resulting in a fining-upward sequence.
Discussion
The development of deltas depends on various factors such as water depth, basin shape and energy regime as well as
overall basinal behaviour in terms of subsidence rate, tectonic activity and sea-level fluctuations (Elliott, 1978; Wescott164

Stop 4 & 5& Ethridge, 1980; Ethridge & Wescott, 1984). The type of basin is a prime control on the nature of basinal regime,
which includes the effects of wave-induced processes, tidal processes and current and wind effects((Elliott, 1978). At
an ocean-facing continental margin, the full range of basinal processes affects the deltas(Allen, 1965), whereas insemi-enclosed and enclosed seas, wave energy is limited due to reduced fetch, and tidal influence is narrow elongate
basins or gulfs connected to an ocean experience considerable tidal effects because tidal current are amplified(Coleman, 1969; Fisher et al., 1969; Coleman & Wright, 1975). In smaller-scale deltas prograding into
barrier-sheltered lagoons or lakes, the influence of basinal processes is limited and the deltas are dominated by fluvial
processes(Donaldson et al., 1970; Kanes, 1970; Larson & Steel, 1978; Sneh, 1979; Clemmensen & Houmark-Nielsen,
1981; Nemec et al., 1984). Delta systems may be affected by basement-related tectonics (Leeder et al., 1988; Robles etal., 1988; Colmenero et al., 1988).
In fluvial-dominated deltas, the abandonment(destuctional) phase initiated by avulsion of the alluvial or distributarychannel system plays an important role in delta sedimentation (Elliot, 1978) as well as in the constructional
phase(Scruton, 1960). Channel switching or avulsion causes the pre-existing delta or lobe to be abandoned and a newlobe to be initiated elsewhere. These lobes are commonly developed in sub-aqurous parts of fluvial-dominated deltas,
resulting in multistory lens-shaped sequences of lobes(Frazier, 1967; Elliott, 1978; van der Meulen, 1983). In the
Uhangri Formation, the initiation of subaqueous lobes was also related to slumping(Phase 2) as well as channel
switching(Phase 4). The formation of fining-upward lobe sequences in most deltas has been generally underestimated.
Rapid progradation and steep slope gradient probably hinder the development of lobe sequences and instead cause
broad coarsening-upward progradation of Gillbert-type sequences. Much lesser gradient is also unsuitable for fulldevelopment of lobe sequence because avulsion is less frequent. Perhaps both high-discharge streams and moderateslope gradient are mist likely favourable for the development of lobe sequences. In addition, they commonly developed
where the effects of basinal processes, e.g. from waves and tides, are minimal.
- Facies association Ⅲ: delta front
Occurrence and interpretation
Facies association Ⅲ is characterized by wedged conglomerate-gravelly sandstone (Facies G1, G2, G5) andinterfingering massive sandstone (Facies S1)(Fig. 11). This association occurs in the upper part of the Byongonri
section, and is about 50m in thickness (Fig. 11). It begins with a trough cross-stratified conglomerate unit which deeply
scours the laminated sand-siltstone unit of facies association Ⅱ.
The gravel facies in the lower part (c. 240-265m in Fig. 11) of association Ⅲ comprises dominantly stratified andfining-upward composite units with deeply scoured bases. Trough and planar cross-stratified gravel facies (Facies G5)
also occur. The gravels are dominantly clast supported and partially concentrated. Most units are independent of otherfacies. These depositional features suggest multistory channel fillings by traction-dominant stream flows. In a few
cases, the facies transitions of G5→S4 and G5→G4 are developed. They are also suggestive of channel-fill sequences.
The stratified gravel and sand facies are rare in the upper part(c. 265-295m in Fig. 11) of association Ⅲ, whereas

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the wedged and normally graded gravel, disorganized gravel and massive sand facies are dominant. Facies G1 iscommonly overlain by Facies S1, forming a facies transition of G1->S1, which is interpreted as resulting from sandy
debris flows or distal high -concentration turbidity currents. The interfingering and amalgamated massive fine tomedium sandstone units probavly represent ansd lobes deposited from frequent unconfined density currents. These
dominant sedimentary facies suggest that rapid suspension dedimentation by unconfined flows plays an important role.
This part was also influenced by episodically protruded confined flows, resulting in the deposition of Facies G2. In theuppermost part, homogeneous and laminated calcareous silt-mudstone units are interlayered, suggesting intermittent
basinal suspension sedimentation.
The upper part of association III is represented by the common occurrence of small-scale coarsening-upward
sequences, resulting from progradation and truncation of fluvialdistributary channels and mass flows. Facies
association III is suggestive of a fluvial-dominated delta-front sequence, widely recognized in geological records. The
delta front is the area in which sediment-laden fluvial currents enter the basin and are dispersed whilst interacting withbasinal processes. In the Uhangri Formation, the basinal reworking processes played a minor role and instead
distributary channels were dominantly developed on the front of subaqueous delta lobes with decreasing water level.
This is evidenced by the delta-front wequence on the convex-up lobe surface.
Discussion
The recognition of a delta sequence requires the identification of three principal facies associations, geneticallylinked within the same formation: delta plain, delta abandonment and delta front. The delta abandonment facies
association comprises a depositional sequence accumulated by the abandonment of a delta or a lobe. The delta front isgenerally represented by record a passage from fine-grained offshore or prodelta facies upwards into a sand-dominatedshoreline facies. The regime of the delta front has been used to define delta type and detailed studies have concentrated
on its operating processes. The fluvial-dominated delta front in the Uhangri Formation is a large-scale fining-upward
sequence, althouhg small-scale coarsening-upward cycles are developed. The sequential pattern is probably attributed
to the continuous rise of lake level concomitant with the relative decrease of sediment input during the deposition of
facies association III.
- Facies association IV: shallow lacustrine environamentOccurrence and interpretation
Facies association IV is characterized by laterally continuous, laminated black shale, crudely stratified sandstone
and convoluted sandstone/cherty mudstone: massive sandstone is ubiquitous and variable in thickness. This association
accurs largely in the uppermost part of the Byongonri section and most subsections in the Uhangri, Uhangpo, Sinsungriand Naesanri sections. Most facies units in this association are sharply bounded and are correlated bed-by-bed for a

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distance of more than 5km.
The sequences of sandstone/cherty mudstone and black shale/cherty mudstone are intimately associated with thefinely laminated black shale, suggesting that the basin experienced several major facies changes from a clastic to achemical system and vice versa. Water chemistry probably controlled the deposition of inorganic cherty mudstone andblack shale/cherty mudstone as well as that of laminated black shale. The cherty mudstone can be inorganically
precipitated when supersaturated silica solutions encounter a certain chemical condition, I.e, a rapid decrease in pH.
High organic matter content and common framboidal pyrite in the black shale, inorganic precipitation of silica andsome evaporite minerals suggest that the deposition occurred in alkaline and euxinic conditions.
Water level remained rather low, as evidenced by shorebird footprints and by symmetrical wave ripples. They are,however, obserbed dominantly in the Uhangri section. In the western part, prograding cross-bedded sequences occur.
The sequence consists of conglomerate, gravelly sandstone and coarse to medium sandstone units. Massive sandstone
units are also common in this part. Disorganized or inverse-to-normally graded conglomerate units with carbonate
gravel clasts occur commonly in the Naesanri section. The inverse-to-normally graded units probably resulted fromdebris flows on the margin. These differences suggest that the western margin of the Haenam Basin is deeper andsteeper than its eastern margin.
Association IV is also characterized by the common occurrence of penecontemporaneous depormation structures,water-escape structures and rip-down clasts. Most deformation structures were probably formed as a result of reverse
density gradients and differential loading, corresponding to Rayleigh-Taylor instability phenomena: the rip-down clasts
are here interpreted as the result of Kelvin-Helmholtz instability. In the northern part massive emplacement of
tuffaceous sands and gravels was culminated, causing the basin to be inactive. This was followed by deposition of
thick-bedded tuff.
Discussion
The cyclical association of clastic and chemical sedimentations is characteristic of a lacustrine margin depositional
environment. Wave-formed ripples, syneresis cracks and the association of laminated shale and sandstone are all
suggestive of a lake margin. Rapid vertical facies changes are consistent with previous studies of lacustrine facies.
Lateral continuity of most sandstone and silt-mudstione units and common penecontemporaneous deformation featuresindicate that facies association IV was formed on the margin of a relatively small lake. The dominant influence ofdensity in flows suggests that the basin margin was mainly controlled by fluvial processes. Turbidity currents induced
by density inflows would strongly affect the basinal sedimentation even in relatively deeper parts of the basin.

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Figure 4-5. Summarized sequential pattern and a lacustrine depositional model of the Uhangri Formation, Haenam, Korea.

Reference
Chun S.S. and S. K. Chough, 1992, Depositional sequence from high-concentration turbidity currents, Cretaceous
Uhangri Formation (SW Korea), Sedimentary Geology, 77, 225-233.
Chun S.S. and S. K. Chough, 1995, The Cretaceous Uhangri Formation, southwest Korea: Lacustrine margin facies,
Sedimentology, 42, 293-322.

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Stop 4 & 5

Stop 5. Sangjokam section, Goseong County, Gyeongsangnam-do Province
At Stop 5 we will observe the Upper Cretaceous Jindong Formation in the Gyeongsang Basin. This stop is locatedon the southern coast of Goseong County, Gyeongsangnam-do Province (Fig. 5-1). The outcrops of this formation iswell exposed along the coastline. Before describing the Jindong Formation, a brief introduction of the Gyeongsang
Basin in which the Jindong Formation is distributed will be provided.
Geological Setting
The Gyeongsang Basin, located in the southeastern part of the Korean Peninsula (Fig. 5-1), is the largest Cretaceousnonmarine sedimentary basin, comprising a 9,000 m thick sequence of deposits assigned to the Gyeongsang
Supergroup. The basin is surrounded by Precambrian metamorphic rocks and pre-Cretaceous granites. The
Gyeongsang Supergroup is divided stratigraphically into the Sindong (prevolcanic), Hayang (sporadic volcanic),
Yucheon (climatic volcanic) Groups, and the Bulguksa granites with decreasing age (Chang, 1975) (Fig. 5-1). The
Sindong and Hayang Groups are composed of sandstone, shale, and minor amounts of conglomerate and marlstone
deposited in continental environments consisting of an ascending sequence of alluvial fan, fluvial, and lacustrine
deposits, respectively. After deposition of the Hayang Group, active volcanism dominated in and around the basin, andformed the Yucheon Group that comprises primarily volcanic rocks with subordinate volcaniclastic rocks deposited inalluvial and lacustrine environments. Upper Cretaceous to Paleogene granitic rocks, which are interpreted to beco-magmatic with the Yucheon volcanic rocks (Lee et al., 1987), intruded into all of the preexisting sequences. The
Sindong and Hayang Groups consist of an ascending sequence of alluvial fan, fluvial, and lacustrine deposits,
respectively, whereas the Yucheon Group is composed mainly of volcanics with some alluvial and lacustrine deposits(Um et al., 1983; Choi, 1985).

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Fig. 5-1. Simplified geologic map of the Gyeongsang Basin and the stratigraphy of its basin-fill, the Gyeongsang
Supergroup, in the Milyang Subbasin (the red-circled area in the geologic map) (after Lee, 2012). Ages were compiledby Hong and Lee (2012).

During the last two decades, numerical age measurements have been obtained using various age-dating techniques
and yielded new age data. U-Pb ages of detrital zircons of the Sinding Group using the LA-ICP-MS range from 137.9± 7.1 Ma to 106 ± 3.7 Ma (Lee et al., 2010). The youngest detrital zircon U-Pb ages of three formations in the Sindong
Group becomes progressively younger stratigraphically, as expected: 118 Ma for the Nakdong Formation, 109 Ma for
the Hasandong Formation, and 106 Ma for the Jinju Formation. Accordingly, the depositional age of the Sindong
Group ranges from late Aptian to late Albian, which is younger than indicated by biostratigraphic data. From a
volcanic pebble of the Silla Conglomerate in the lower part of the overlying Hayang Group, Kim et al. (2005) obtained
an 40Ar/39Ar hornblende age of 113.4 ± 2.4 Ma, indicating the depositional age of the Silla Conglomerate is younger
than late Aptian. For the Gusandong Tuff, which occurs in the upper part of the Hayang Group, Jwa et al. (2009)
reported a LA-ICP-MS U-Pb zircon age of 97-96 Ma. The K-Ar whole-rock age of pyroclastic clasts in the Jindong
Formation was recovered at 86-85 Ma (Paik et al., 2001a). In addition, the boundary between the Hayang Group andthe overlying Yucheon Group has been interpreted to be 81-80 Ma (Kim et al., 2005). Considering these data, theHayang Group is interpreted to have been deposited during the late Albian to early Campanian (Lee et al., 2010) (Fig.
5-1).

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Stop 4 & 5Jindong Formation
The Jindong Formation is the uppermost part of the Hayang Group, and is the thickest lacustrine deposit in the
Gyeongsang Supergroup (Um et al., 1983; Kim and Paik, 1985). This formation conformably overlies the Haman
Formation, which consists mainly of floodplain deposits of purple sandstones and shales. The Yucheon Group overlies
the Jindong Formation unconformably (Um et al., 1983). The Jindong Formation dips generally southeastwards 10o too20 , and its apparent thickness is measured up to 2400 m. The depositional age of the Jindong Formation has been
established as Cenomanian to Campanian based on LA-ICP-MS zircon U-Pb age of the Gusandong Tuff (Jwa et al.,2004).
The lithology of the Jindong Formation is rather homogeneous. Thin-bedded, dark gray to gray fine-grainedsandstone and shales are stacked throughout the Jingdong Formation (Fig. 5-2). These deposits are characterized bymud cracks and packages of cross-laminated units with small-scale symmetrical ripples. The cyclic deposits, consistingof an alternation of dark gray laminated to thin-bedded fine-grained sandstone and siltstone-mudstone, deposited inshallow lake and marginal environments, respectively, are prominent in the Jindong Formation. Thickness of the single
sedimentary cycles ranges from a few decimeters to a few meters. Accordingly, the Jindong Formation consists ofshallow to marginal lacustrine deposits. Planar- to cross-laminated sandstone to siltstone, megarippled sandstone, andflaser- to lenticular-bedded fine sandstone to siltstone/mudstone are interpreted to have been deposited by sheet
flooding as lacustrine hyperpycnal flow deposits (Paik and Kim, 2006; Houck and Lockley, 2006). Sediments in the
Jindong Formation contain a large amount of pyroclastic material, both as tephra and as reworked ash (Houck andLockley, 2006). Some thin limestone beds were also reported from the Jindong Formation (Houck and Lockley, 2006),
but more common carbonates are palustrine calcretes occurring intermittently as nodular and lenticular to bedded
carbonates throughout the Jindong Formation (Paik and Kim, 2003), indicative of evidence for pedogenic modification
due to fluctuating lake levels. Evaporites are absent in the Jinddong Formation, but traces of evaporite minerals
including halite and sulfate are commonly observed in these deposits (Paik and Kim, 2006).

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Stop 4 & 5

Fig. 5-2. Typical lithology of the Jindong Formation excellently exposed at Sangjokam site (Stop 3), Goseong
County, Gyeongsangnam-do Province where we will visit on the second day of this field trip (after Lee, 2012).

The Jindong Formation yields very rare body fossils. In this formation stromatolites are absent, but dinosaur tracks
are abundant and invertebrate trace fossils are common. Especially, The Jindong Formation is well known by theoccurrence of innumerable dinosaur tracks of both sauropods and ornithopods (Lim et al., 1994; Paik et al., 2001;
Lockley et al., 2006) and some bird tracks (Lockley et al., 1992, 2006). The tracks are usually preserved on the
mudstone surfaces of alternation of laminated to thin-bedded fine-grained sandstone and siltstone-mudstone. Polygonal
mud cracks are common on the track-bearing deposits, and transect the dinosaur tracks. The dinosaur trackways aresubperpendicular or subparallel to the crestlines of wave ripples. The occurrence of small wave ripples, dinosaur
tracks, invertebrate burrows, and mud cracks suggests that the Jindong Lake is inferred to have been shallow andephemeral in nature (Houck and Lockley, 2006). Wave ripple-crest orientations are consistently WNW-ESE, indicatinga prevailing wind direction from the NNE or SSW (Paik and Kim, 2006; Houck and Lockley, 2006). Also these wave
ripple-crest orientations reflect the development direction of the Jindong Lake shoreline. Considering that the Jindong
Formation is mostly composed of fine-grained and the ash beds are thin, the Jindong Lake at this stop is inferred tohave been located a distal lowland setting, far away from erupting volcanoes.

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Stop 4 & 5

Sangjokam Section
At the Sangjokam section (Fig. 5-3), we will observe the Jindong Formation from the stratigraphically upper part
downwards. The section is about 100-200 m thick. The Jindong sequence at the stop 3 consist mainly of rhythmicallybedded fine sandstone, siltstone, mudstone and/or shale (Fig. 5-2). Thin intervals of coarser sandstone, limestone, andash tuff are also present. Small wave ripple marks, invertebrate burrows, tracks and mud cracks are ubiquitous throughthe stop sequence. The representative columnar section of the Sangjokam section is shown in Figure 5-4.
The occurrence of invertebrate burrows and/or bioturbation indicates that the lake floors were oxygenated in thestop site. The abundance of small wave ripple marks indicates that the lake was shallow and periodically well-mixed
throughout the water column. The abundance of mud cracks and dinosaur-track horizons provides evidence forfrequent exposure of the lake sediments.
We envision a low-gradient, ramp-type setting for this portion of the basin, as little coarse clastic material is present,
and small decreases in lake level would provide widespread exposure surfaces for the formation of mud cracks anddinosaur tracks.
The most abundant dinosaur trackways are those of iguanodontids (c. Caririchnium or Iguanodontipus) that often
traveled in herds (Lockley et al., 2006). They also noted that sauropod tracks, by contrast, show little or no evidence ofgregarious behavior and rarely occur on the same bedding planes as orninthopod trackways.

Fig.5-3. Google Earth view of Stop 3 (Sangjokam section, Goseong County). The field observation proceeds fromeast to west (stars). The cross represents points where we can observe dinosaur tracks. Yellow dots with numbers
represent stop sites.

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Stop 4 & 5

Fig. 5-4. Representative stratigraphic section of the Jindong Formation at Sangjokam site (after Paik and Kim, 2003).

Stop 5-1.
The first site we will observe is near the parking lot. The first outcrop we will meet is a succession containing
trough cross-bedded sandstones in the upper part, which overlies alternation of ripple-cross laminated fine sandstone
and light gray-gray siltstone/mudstone (Fig. 5-5a). The trough cross-bedded sandstone is medium to very coarse
sandstone and contains mud-chip lags at bases of beds. Beds are about 30 cm thick with a distinct erosional contact atbase. This sandstone is interpreted as channel-fill formed by deposition of coarse bedload during migration ofmegaripples in fluvial channels. Just beneath the trough cross-bedded sandstone, we can observe a horizon containing
multiple stacking of large symmetrical wavy bedforms (Fig. 5-5b) and the underlying horizontally laminated very finesandstones. The association of these sandstone facies suggests that fluvial channels entered into the shallow lacustrine
environments.

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Stop 4 & 5

Fig. 5-5. a) Cosets of trough cross-bedded medium to very coarse sandstones containing mud-chip lags at basesof beds. b) Multiple stacking of wavy bedforms composed of fine sandstone and the underlying horizontally laminated very fine sandstones.

Stop 5-2.
Bedding planes of the Jindong Formation are well exposed on the wave-cut terrace at this site (Fig. 5-6). The
Jindong Formation show low-angle dipping. On the bedding plane, we can observe plant-eating dinosaur (sauropod
and ornithopod) tracks (Fig. 5-7).

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Stop 4 & 5

Fig. 5-6. General view of Stop 3-2. Bedding planes are well exposed during the low tide.

Fig. 5.7. Dinosaur tracks. Single sauropod trackway (above) and single ornithopod trackways (below).

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Stop 4 & 5

Stop 5-3
At this stop we can observe buff to rust-colored, irregularly shaped carbonate nodules exposed as a coastal platform
with a surface of over 400 km2 (Fig. 5-8). The sectional view of these deposits can be observed on a cliff outcrop at
Stop 3-4 (Fig. 5-9). The stratigraphic position at two sites is displaced due to local faulting. This structure has beeninterpreted as dinoturbated structure by Paik et al. (2001). It is distinguished by its very rugged surface withbuff-weathering color. On the bedding surface, however, footprints are indistinct and appear as randomly distributed,
irregular depressions at least 10 cm deep. It is not certain that the depressions resulted from dinoturbation, but it isquite likely. They are not a weathering feature and clearly predated the deposition of the overlying sediments. Some
depressions are circular, and dinosaur footprints are common in layers below and above this deposit. Polygonal mud
cracks occur on both presumed dinoturbated and clearly non-dinoturbated flat surfaces. Paik et al. (2001) interpreted
that the dinoturbated deposit was originally calcareous silty mud, reflecting deposition in a shallow lake of low energy.
It is characteristic of this presumed dinoturbated deposit that pedogneic calcrete occurs in the form of massive
hardpan about 40 cm thick (Fig. 5-9). Much of pedogenic calcretes have been eroded out. The original lithology of thedeposit was calcareous, quartzose, silty mudstone with some ostracod and charophyte fragments. The pedogenic
features include downward calcretezation that resulted in a sharp upper contact and a gradational lower contact,
circumgranular cracks, fitted peloids, brecciation, microstromatactis cavities, and irregular fenestrae. These arecharacteristic of alpha-calcrete (Wright and Tucker, 1991), and have been documented in other pedogenic calcretes.
Above the presumed dinoturbated deposit, calcrete layers a few centimeters thick are commonly intercalated withcalcareous silty shales.
We welcome any alternative explanations for these sedimentary structures.

Fig. 5-8. Surface overview of dinoturbated deposit. Preservation of rugged surface may have been resulted from
calcretization of dinoturbated surface. Was this mudflat a dancing (trampling) place of dinosaurs? Polygonal mud
cracks occur on the surface.

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Stop 4 & 5

Fig. 5-9. Sectional view of dinoturbated deposit observed at Stop 3-4. Pedogenic nodular to bedded calcrete (rust-colored) formed in the upper layers of dinoturbated deposit.

Stop 5-4
At this stop we expect to observe interesting dinosaur footprint-related structures in the cliff-forming outcrop by thewooden deck walkway (Fig. 5-10) as well as wave ripples (Fig. 5-11a), mud cracks (Fig. 5-11b), and a tuff layer (Fig. 5-11c).
Most dinosaur tracks are observed on bedding surfaces. Trampling by dinosaurs can leave impressions not only on
depositional surface, but also on subjacent deposits. Such impressions on underlayers are called undertracks orunderprints (Lockley, 1991). We can observe these undertracks at the vertical cliff section.
The sectional traces occur in interlaminated fine-grained sandstones and siltstones-mudstones in common with the
trackway deposits, and are recognized by asymmetrical depression and syndepositional deformation. There are three
types of asymmetrical depressions: (l) low-angle, shallow depressions (Fig. 5-10a); (2) subveritcal, deep depressions(Figs. 3-10b,c); and (3) pointed depressions (Paik et al., 2001).
The low-angle shallow depressions (Fig. 5-10a) are generally 20-40 cm wide and mostly less than 10 cm deep. The
central parts of the underlayers are downwarped and their rims are bulged. In places, the less steep rims show kinked
deformation. The depression shown in Fig. 3-10 b is 40 cm wide and deep. The steeper side of the depression, which isnearly vertical, has formed faulted walls with drag folds in the underlayer. The upper part of less steep side also has
faulted wall, but the underlayer of the lower part are downwarped, and the central part is rarely deformed. Fig. 3-10c
show a depression with backthrusted walls on both sides with a folded and deformed trampled bed. The depression isabout 10 cm wide in the lower part and 6 cm wide between the upper rims. The thickness of the underlying thinsandstone bed varies laterally, and the thickness of the trampled area is thinner and its immediate vicinity becomes
thicker.

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The preservation of footprints as track infilling is recognized in some profiles of depressions (Figure 5-10). The
trapping sediments occur as downward convex lenses. These commonly occur in couples about 20-30 cm apart, andare deemed to be transverse sections of trackway deposits. The trapping
sediments are planar stratified, and some drape over the depressions. These draped trap sediments form subcirculardepressions on some weathered bedding surfaces (Fig. 3-10b). Such depressions made on overlayers of the tracks canbe called ‘overprints’ or ‘overtracks’ (Paik et al., 2001).

Fig. 5-10. Sectional views of dinosaur tracks preserved in the Jindong Formation as diverse modes of depression.

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Stop 4 & 5

Fig. 5-11. a) wave ripples, b) mud cracks (arrow), and c) a tuff layer (arrow).

Stop 5-5
At this stop we can also observe sauropod trackways well exposed on the bedding surface (Fig. 5-12).

Fig. 5-12. Sauropod trackways.

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Stop 4 & 5

Stop 5-6
We will observe the excellent sea cliff and wave-cut platform at this stop (Fig. 5-13). At this section Lockley et al.
(2006) described the closely spaced track-bearing beds (Fig. 5-14). Four thin limestone beds are observed in the lower
part of the cliff (Fig. 5-14). On the platform surface we can observe the ubiquitous presence of mud cracks (Fig. 5-15)
and sauropod trackways (Fig. 5-16). When the tide is high, the platform is immersed in sea water, which causes may
barnacles and mussels to attach to the platform surface. This causes problems in the management of sauropod
trackways. A silicified volcanic ash bed (Fig. 5-17) can be also observed. Lockley et al (2006) reported an average ofabout two track-bearing levels per meter, making it one of the richest track-bearing sections on record and providing
evidence of the activity of hundreds of individuals.

Fig. 5-13. Panoramic view of Stop 3-6.

Fig. 5-14. Sea cliff and dinosaur and bird tracks reported interval. The stratigraphic column with vertebrate tracks
is from Lockley et al. (2006).

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Fig. 5-15. Mud cracks.

Fig. 5-16. Sauropod trackways on the wave-cut platform.

Fig. 5-17. A silicified volcanic ash bed is shown in the foreground and as light green color in the middle of the succession in the background.

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Summary
The Jindong Formation was deposited as a thick succession of fine-grained volcaniclastic sediments in a rapidly
subsiding intra-arc basin. The main lithologies in the Jindong Formation are ash-rich mudstone, siltstone, and very finesandstone. Minor lithologies are coarser sandstone, conglomerate, carbonates, and ash tuff. The Jindong Formation isinterpreted to have been deposited in a distal lowland areas, adjacent, but with some distance, to an active volcano or
volcanoes. Most deposits were deposited subaqueously, but emergence and subaerial exposure occurred commonly
between episodes of deposition. The abundance of track-bearing layers in the Jindong Formation is likely the result of
rapid aggradation, which is typical of sedimentation in volcanic settings. It is inferred that the Jindong Formation
exhibits the world’s greatest concentration of track-bearing horizons hitherto documented.
References
Chang, K. H., 1975, Cretaceous stratigraphy of southeast Korea. Journal of Geological Society of Korea, 11, 1-23.
Choi, H. I., 1985, Sedimentology and its implication for stratigraphic classifications of the Cretaceous Gyeongsang
Basin. Journal of Geological Society of Korea, 21, 26-37.
Hong, S. K. and Lee, Y. I., 2012, Evaluation of atmospheric carbon dioxide concentrations during the Cretaceous.
Earth and Planetary Science Letters, 327-328, 23-28.
Houck, K. J. and Lockley, M. G., 2006, Life in an active volcanic arc: Petrology and sedimentology of dinosaur
track beds in the Jindong Formation (Cretaceous), Gyeongsang Basin, South Korea. Cretaceous Research, 27,
102-122.
Jwa, Y. J., Lee, Y. I. and Orihashi, Y., 2009, Eruption age of the Kusandong Tuff in the Cretaceous Gyeongsang
Basin, Korea. Geosciences Journal, 13, 265-273.
Kim, C. S., Park, K. H. and Paik, I. S., 2005, 40Ar/39Ar age of the volcanic pebbles in the Silla Conglomerate and thedeposition timing of the Hayang Group. Journal of Petrological Society of Korea, 14, 38-44 (in Korean withEnglish abstract).
Kim, H. J. and Paik, I. S., 2001, Sedimentary facies and environments of the Cretaceous Jindong Formation in
Goseong-gun, Gyeongsangnamdo. Journal of Geological Society of Korea, 27, 235-256 (in Korean withEnglish abstract).
Lee, G., Besse, J. and Courtillot, V., 1987, Eastern Asia in the Cretaceous: New paleomagnetic data from South
Korea and a new look at Chinese and Japanese data. Journal of Geophysical Research, 92, 3580-3596.
thLee, Y. I., 2012, Geology and paleoenvironments of the Korean Mesozoic. Presentation at the 11 Mesozoic

Terrestrial Ecosystems.
Lee, Y. I., Choi, T., Lim, H. S. and Orihashi, Y., 2010, Detrital zircon geochronology of the Cretaceous Sindong183

Stop 4 & 5Group, SE Korea: Implications for depositional age and Early Cretaceous igneous activity. The Island Arc, 19,647-658.
Lim, S. K., Lockley, M. G., Yang, S. Y., Fleming, R. F. and Houck, K., 1994, A preliminary report on sauropod
tracksites from the Cretaceous of Korea. Gaia: Revista de Geosciencias, Museu Nacional de Historia Natural,
Lisbon, Portugal 10, 109-117.
Lockley, M. G. 1991. Tracking Dinosaurs: a New Look at an Ancient World. Cambridge University Press,
Cambridge, 238p.
Lockley, M. G., Houck, K., Yang, S.-Y., Matsukawa, M. and Lim, S.-K., 2006, Dinosaur-dominated footprint
assemblages from the Cretaceous Jindong Formation, Hallyo Haesang National Park area, Goseong County,
South Korea: Evidence and implications. Cretaceous Research, 27, 70-101.
Lockley, M. G., Yang, S. Y., Matsukawa, M., Fleming, F. and Lim, S. K., 1992, The track record of Mesozoic birds:
evidence and implications. Philosophical Transactions of Royal Society of London: Biological Sciences, 336,
113-134.
Paik, I. S. and Kim, H. J., 2003, Palustrine calcretes of the Cretaceous Gyeongsang Supergroup, Korea: Variationand paleoenvironmental implications. The Island Arc, 12, 110-124.
Paik, I. S. and Kim, H. J., 2006, Playa lake and sheetflood deposits of the Upper Cretaceous Jindong Formation,
Korea: Occurrences and palaeoenvironments. Sedimentary Geology, 187, 83-103.
Paik, I. S., Kim, H. J. and Lee, Y. I., 2001, Dinosaur track-bearing deposits in the Cretaceous Jindong Formation,
Korea: occurrence, palaeoenvironments and preservation. Cretaceous Research, 22, 79-92.
Um, S. H., Choi, H. I., Son, J. D. et al., 1983, Geological and Geochemical Studies on the Gyeongsang Supergroupin the Gyeongsang Basin. Korea Institute of Energy and Resources Bulletin 36. Korea Institute of Energy andResoures, Daejeon (in Korean with English abstract).
Wright, V. P. and Tucker, M. E., 1991, Calcretes: an introduction. In: Wright, V. P. and Tucker, M. E. (eds.),
Calcretes. International Association of Sedimentologists Reprint Series 2, Blackwell Scientific Publications,
Oxford. pp. 1-22.

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The Fifth International Symposium of International GeoscienceProgramme IGCP Project 608

Stop 6
Oct. 25. 2017 (Wednesday)

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Stop 6. Songdo Peninsula Geosite, Busan National Geopark(Late Cretaceous Dadaepo Formation, Dadaepo Basin)
At Stop 6, we will observe the Late Cretaceous Dadaepo Formation in the Dadaepo Basin. This stop is located on
the southern coast of Busan City (Fig. 6-1). Busan is the second largest city in Korea. Its deep harbor and gentle tides
have allowed it to grow into the largest container handling port in the country and the fifth largest in the world. The
city's natural endowments and rich history have resulted in Busan's increasing reputation as a world class city of
tourism and culture, and it is also becoming renowned as an international convention destination.
A geopark is a unified area with geological heritages of international significance. Busan became a national geoparkof Korea in November 2013. The Busan National Geopark are composed of 12 geosites of the Nakdong Estuary,Morundae, Dusong Peninsula, Songdo Peninsula, Dudo, Taejongdae, Oryukdo, Igidae, Jangsan, Geumjeongsan,
Orbicular Gabbros, and Baekyangsan. In this field excursion, we will tour the Songdo Peninsular Geosite of the BusanNational Geopark and observe Late Cretaceous Dadaepo Formation exposed in the geosite.

Fig. 6-1. A map of the Busan National Geopark.

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Geological Setting
The Korean Peninsula, situated on the eastern margin of the Eurasian continent, is an important tectonic link
between eastern China and the Japanese Arc (Fig. 6-2a; Chough and Sohn, 2010). During the Cretaceous, the area was
located to the west of the volcanic arc produced by oblique subduction of the proto-Pacific (Izanagi/Kula) plate
beneath the Eurasian plate (Chough et al., 2000; Chough and Sohn, 2010). The Gyeongsang Basin is the largest
Cretaceous sedimentary basin in Korea, of which the basin-fill sequence is divided into three major lithostratigraphic
units on the basis of their occurrence and the amount of volcanic material (Fig. 6-2b; Chang, 1975, 1977; Choi, 1986;
Chough et al., 2000): the non-volcanic sedimentary strata of the Sindong Group, the partly volcanic strata of the
Hayang Group, and the dominantly volcanic strata of the Yucheon Group, from oldest to youngest.
The NNE-striking YFS, which is composed of the Jain, Miryang, Moryang, Yangsan, Dongnae, and Ilgwang faults
from west to east, is developed in the eastern part of the Gyeongsang Basin (Fig. 6-2c). Of these faults, the Yangsan
Fault has the most conspicuous damage, gouge zone, and displacement (Chang et al., 1990; Hwang et al., 2007, 2008;
Choi et al., 2009; Kang and Ryoo, 2009). Deciphering the movement history of the Yangsan Fault is thus important forunderstanding the basin evolution and volcanic activity in SE Korea during the Cretaceous. The Dadaepo Basin, which
is bounded by the Yangsan and Dongnae faults, is an isolated small-scale sedimentary basin located on the southeastern
tip of the Miryang Subbasin (Fig. 6-2c, 6-3).

Fig. 6-2. (a) Tectonic outline of the eastern Eurasian margin (modified after Xu et al., 1987; Lin et al., 2003; Itohet al., 2006). NCB: North China Block, SCB: South China Block, MTL: Median Tectonic Line. (b) Distributionof Cretaceous sedimentary basins (greenish areas) in the Korean peninsula (after Chough et al., 2000). (c) Simplified
geologicalmap of the Gyeongsang Basin and NNE-striking Yangsan Fault System.

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Dadaepo Basin
The Dadaepo Basin is a small Late Cretaceous sedimentary basin in SE Korea, located on the eastern margin of
Asia. The basin is an isolated extensional basin situated between the NNE-striking Yangsan and Dongnae faults (Fig.
6-3). The basin-fill sediments, named the Dadaepo Formation, consist of channelized conglomerates and sandstones
intercalated with dominantly purple mudstones in the lower part. The upper part is dominated by fine- tocoarse-grained tuffaceous sandstones and olive to dark gray mudstones with abundant volcanic interbeds. The overall
configuration of the strata of the Dadaepo Formation indicates syndepositional tilting of the basin floor to thenorth-northeast. A number of outcrop-scale faults are observed in the basin-fill sediments, of which the majority are
NW-striking normal faults, including syndepositional growth faults. The orientations of mafic (magmatic) and clastic
dikes, interpreted as being approximately contemporaneous with the deposition of the Dadaepo Formation, are alsonearly parallel to the strikes of outcropscale normal faults. All these extensional structures consistently indicate
NE-SW extension of the basin and obliquely intersect the basin-bounding Yangsan and Dongnae faults at angles of
40°-60°. Cho et al. (2016) concluded that the Dadaepo Formation was deposited in a pull-apart basin that subsided as aresult of NNE-striking sinistral strike-slip faulting in the southeastern part of the Korean Peninsula during theCampanian (Late Cretaceous). Also, this strike-slip faulting was related to north-northwestward oblique subduction of
the proto-Pacific (Izanagi/Kula) or Pacific plate under the eastern margin of the Eurasian plate.

Fig. 6-3. Geological map of the Dadaepo Basin (modified after Chang et al., 1983; Cho et al., 2011, 2016, 2017).

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Dadaepo Formation
The Dadaepo Formation is subdivided into the lower and the upper Dadaepo formations on the basis of the presenceof red beds and the abundance of volcanic material (Chang et al., 1983). The lower Dadaepo Formation consists
mainly of purple mudstones and siltstones, conglomerate and coarse-grained sandstones, gray to olive gray mudstones
and sandstones, and interbeds of straw-colored marl without volcanic material (Fig. 6-4a, b). At least three
conglomerate beds, each 1-5 m thick, occur in the lower Dadaepo Formation. These conglomerates contain angular torounded and moderately sorted gravel clasts of chert, quartzite, and volcanic and sedimentary rocks (Fig. 6-4d).
Cross-stratification, graded bedding, and lenticular bed geometry are the characteristic features of the conglomerateinterbeds (Fig. 6-4c). The purple mudstones and siltstones of the lower Dadaepo Formation contain abundant calcrete
nodules or calcic paleosol layers (Fig. 6-4e), reduction spots (Fig. 6-4f), and the remains of dinosaur nests (Fig. 6-4h)
and bones. Thick marl layers containing petrified wood are also intercalated within the mudstones (Fig. 6-4g).

Fig. 6-4. Outcrop photographs of the basin-fills (Lower Dadaepo Formation). (a, b) Panoramic view of the lower
Dadaepo Formation composed of thick andmassive purplemudstones and conglomerate/sandstone interbeds. (c,d) Cross-stratified and graded conglomerates and pebbly sandstones. The coin is 2.3 cm in diameter. (e) Angularcalcrete intraclasts in purple siltstones. (f) Reduction spots in purple mudstones. (g) Petrified wood in compound
calcrete and marl layer. (h) Dinosaur egg fossils in purple mudstones.

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A massive silicic ignimbrite layer, about 2.5 m thick, is intercalated between the lower and the upper Dadaepo
formations (Fig. 6-5a, b). The upper Dadaepo Formation overlying the ignimbrite consists mainly of greenish andolive-gray tuffaceous sandstones intercalated with tuffaceous sedimentary rocks (conglomerates, coarse-grainedsandstones, and siltstone) and tuffs. The uppermost part of the upper Dadaepo Formation comprises cross-stratified
tuffaceous sandstones (Fig. 6-5c) that are rich in andesitic and basaltic clasts (Fig. 6-5d). The Dadaepo Formation isinterpreted to have been deposited in alluvial, fluvial, and lacustrine environments (Lee, 1975; Shin, 1997). Paik et al.
(1997) also reported that the formation is composed of fluvial plain and floodplain-lake deposits. Kim (2009)
suggested that the lower Dadaepo Formation at the Morundae was deposited in an alluvial fan environment, and on the
Dusong and Songdo peninsulas was deposited in a fluvial environment. Chough and Sohn (2010) suggested further
that there was an abrupt basin subsidence, as indicated by the abrupt facies change from the alluvial-fan to the deep
lacustrine environment of the lower and the upper Dadaepo formations, respectively, and that the stratigraphic
development of the formation was influenced by syndepositional tectonism and associated volcanism, based on thefelsic ignimbrite layer between the lower and upper parts, and the presence of volcanic material in the upper Dadaepo
Formation (Fig. 6-5a).
Volcanic rocks overlying the Dadaepo formation
The uppermost part of the upper Dadaepo Formation consists mainly of tuffaceous sandstones and pebbly
sandstones, and is overlain by lavas and pyroclastic rocks (Fig. 6-3 and 6-5e). The overlying volcanic rocks areinterpreted as resulting from alternating andesitic lava effusion and pyroclatic eruption, which possibly led to theconstruction of a stratovolcano. The volcano formed in a continental/island arc setting, as inferred from petrochemical
data that indicate a medium to high-K orogenic suite (Kim and Yun, 1993; Yun et al., 1996).
Dark gray lavas (~50 m thick) rest on cross-stratified tuffaceous sandstones of the Dadaepo Formation on theSongdo Peninsula (Fig. 6-5e), and are in turn overlain by thick volcanic breccias. The contact between the lavas andtuffaceous sandstones is irregular (Fig. 6-5f). Load structures, formed by sinking of the overlying lavas, and flame
structures produced by squeezing upward of sediments into the overlying lavas are frequently observed along thecontact. The feldspar phenocrysts in the lavas are aligned nearly parallel to the bedding of the underlying sandstone
beds. Auto-brecciated fragments and stretched vesicles are also observed in the lavas (Fig. 6-5g-i). Cho et al. (2011)
reported that the lavas are basaltic andesites, based on major-element analyses. These rocks commonly exhibit
vitrophyric to microporphyritic textures, consisting of plagioclase, clinopyroxene, and amphibole phenocrysts in a
glassy or fine-grained groundmass.
Volcanic rocks of basin basement
Basement rocks are exposed only in the southern part of the Dusong Peninsula and Dudo in the southern part of thestudy area, because of the north or north-northeastward dip of the overlying Dadaepo Formation (Fig. 6-3). On thesouthern coast of the Dusong Peninsula, conglomerates and pebbly sandstones of the lowermost Dadaepo Formation

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unconformably overlie dacitic basement. Although the unconformable contact is irregular, it generally dips toward thenorth-northeast, subparallel to bedding in the lower Dadaepo Formation. On Dudo Island to the south of the Songdo
Peninsula, the same stratigraphic relationship is observed between the lowermost Dadaepo Formation and the
dacitic-andesitic basement, as on the Dusong Peninsula. The uppermost part of the basement consists of lapilli or ash
tuffs. Toward the lower part, weakly stratified volcanic breccias are intercalated with tuffaceous conglomerates/
sandstones. The basement strata of the Dadaepo Basin are dacitic-andesitic volcanic rocks, from which we interpretthat vigorous volcanic activity took place before deposition of the Dadaepo Formation.

Fig. 6-5. Outcrop photographs of the basin-fills (Upper Dadaepo Formation and volcanic rocks). (a) An exposure
showing the sharp contacts between the massive purple mudstone of the lower Dadaepo Formation, a few meter-thickand massive dacitic ignimbrite layer in the middle, and the well-bedded sandstone/gray mudstone succession of theupper Dadaepo Formation. (b) Close-up of the dacitic crystal-rich and pumice-free ignimbrite. The coin is 2.5 cm
in diameter. (c) Cross-stratified tuffaceous sandstones with volcanogenic clasts. The pocketknife is 9 cm in length.
(d) Volcanogenic clasts (VC, white arrows) in the tuffaceous sandstones and conglomerates. (e) Panoramic view of
the upper Dadaepo Formation, composed of greenish/gray cross-stratified tuffaceous sandstone and arkosic sandstone,
and the overlying basaltic andesite (lava flow). (f) Close-up of irregular loaded scoured contact between the basaltic
andesite and the underlying tuffaceous sandstone and overlying captured in the underlying sandstone. (g, h) Close-upof the basaltic andesite showing auto-brecciated lava fragments and stretched vesicles and feldspar phenocrysts.

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Songdo Peninsula Geosite
Along the shore, various rocks, such as the sedimentary rocks of Dadaepo Formation, basalt, pyroclastic rocks, andintrusive rhyolite are exposed with dinosaur bones, egg nest fossils, and calcareous paleosols. We can enjoy the various
geologic records with the marvelous landscape of Hallyeohaesang.

Fig. 6-6. Geotrail map of the Songdo peninsula geosite.

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Stop 6-1. Lower Dadaepo Formation
About 70-80 million years ago, the Songdo Peninsula area started pulling apart to create the bowl-shaped Dadaepo
Basin, and sediments deposited to form the Dadaepo Formation. The beginnings of this formation were made byrepeated river flooding. As the basin deepened it became a lake, and the Upper Dadaepo Formation was deposited. The
Lower Dadaepo Formation is easy to observe near the coastal cliffs of the Songdo peninsular geotrail. The Lower
Dadaepo Formation is comprised of channelized conglomerates and sandstones that are intercalated in dominantly
purple mudstones, indicating repeated flooding. Unlike the Upper Dadaepo Formation, only a small amount of
volcanic materials can be found in the Lower Dadaepo Formation. Various structures like reduction spots, bioturbation,and calcretes can be seen in red beds, with chert clasts, cross-bedding, scour-and-fill structures in the conglomerate.
White to light greenish grey circular structures called reduction spots can be observed in the red sandstone andsiltstone of the Lower Dadaepo Formation. These spots usually are elliptical, with a nuclear in the middle thatoriginated from the outside. Although the beds were originally red, the burial migration of groundwater has caused the
reduction of ferric oxide to ferrous oxide, which is slightly soluble. The resulting color change is caused by theleaching of reduced iron.
Thick conglomerates of the Lower Dadaepo Formation can be well observed at this site. In this area, there are six toeight layers of conglomerate that have been formed by channel flooding. These conglomerates are composed of manykinds of clasts, including chert, having various sizes and shapes.
Characteristically there are many chert clasts in conglomerate. Chert is formed by either, deposits of dead silicate
skeletals of organisms, or precipitation of silicate components. Chert clasts in conglomerates are usually translucent brickcolored, including white, grey, and brown clasts from time to time. Very small radiolarians can be seen under a microscope.

Fig. 6-7. Outcrop photograph of Stop 4-1. (a) Lower Dadaepo Formation. (b) Conglomerate layers. (c) Chert clasts
in the conglomerates. (d) Reduction spots observed in reddish siltstone.

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Stop 6-2. Calcic paleosol (calcrete) and normal fault
Following the Songdo Peninsula trail, there are nodules in sedimentary rocks that are either white or light pink.
These are pedogenic calcretes (calcic palesols). Calcrete generally forms in arid or semi-arid climate when minerals
leach from the upper layer of the soil and accumulate in the next layer. The form of calcrete differs by the maturity,
which can be either nodular or bedding-like. If the maturity is low, calcrete nodules are usually small, and it becomesbigger in size or forms a layer with increasing maturity. Calcretes are important indicators of the past climate.
Commonly found calcretes in red beds of Dadaepo Formation indicate that the climate was arid during that time.
Red sandstone with siltstone, grey conglomerate, and calcic paleosol are piled in order until they suddenly lose
consistency at this site due to a fault. This fault has a hanging wall below the footwall, displaying a good example of anormal fault. Near the main fault, smaller faults can be seen. Because the Dadaepo Formation is interpreted to haveformed in a pull-apart basin that was opened by NNEtrending strike-slip faults, many normal faults that have formed
due to tension can be observed in the Dadaepo Formation. They can provide important information about the tectonic
environment and formation mechanism of the Dadaepo Basin.

Fig. 6-8. Outcrop photograph of Stop 6-2. (a) Normal fault and calcic paleosol layer. (b) Intra-clast type calcrete.

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Stop 6-3. Dinosaur egg nest fossils and rhyolitic dike swarms
The Songdo Peninsula was a paradise for dinosaurs when the Lower Dadaepo Formation was under deposition
during the late Cretaceous (70 Ma). Dinosaurs roamed the land and the area surrounding the lake to find nesting
grounds. This evidence is well preserved in the Lower Dadaepo Formation in the form of footprints, eggs, and bone
fossils. Recently, attention has been drawn to the area as dinosaur eggs in the red siltstone and sandstone have been
discovered. The size of the eggs are about 10 cm, 10 of which were found in nearly perfect condition.
Following the Songdo Peninsula trail, yellowish rocks that cut through the wooden-panel-like parallel bedding canbe observed. These bright rocks are rhyolitic dykes made from intruding rhyolitic magma. Three dykes can be seen
tilting to the same direction, and this kind of group of multiple dykes are called a dyke swarm. Because rhyolitic dykes
withstand erosion better than surrounding sedimentary rocks, exotic and beautiful landforms are created by differential
erosion. Take a picture at the soaring rhyolitic dyke with Basan beach behind in the background!

Fig. 6-9. Outcrop photograph of Stop 6-3. (a, b) Dinosaur egg fossils in the lower Dadaepo Formation. (c, d) Rhyolitic
dike swarms.

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Stop 6-4. Ignimbrite (dacitic tuff) and Upper Dadaepo Formation
At this stop, the red beds changes to dark grey tuffaceous sediment. So we can define this site as a boundary
between the Lower and Upper Dadaepo formations. Such a dramatic change is thought to have been caused byenvironmental changes from a river to a lake. An unusual red bed containing a lot of white feldspar crystals can befound in the transition zone from the Lower to the Upper Dadaepo formations. This is the ignimbrite that flowed into
the lake during an explosive volcanic eruption. This ignimbrite is a keystone that tells us that there was active
volcanism during the deposition of the Upper Dadaepo Formation, and the environmental change to a deep lake wasrelated to this volcanic activity. The Upper Dadaepo Formation is dominated by tuffaceous sediments derived fromvolcanic activity, and bedding plane, crossbedding, ripple marks, and scour-and-fill structures are well preserved. Volcanic
rock fragments derived from volcanic activity that occurred near the lake margins are common in this formation. The
transition from the Lower to Upper Dadaepo formation is demarcated by an intercalation of a silicic ignimbrite.

Fig. 6-10. Outcrop photograph of Stop 6-4. (a) An exposure showing the sharp contacts between the massive purple
mudstone of the lower Dadaepo Formation, a few meter-thick and massive dacitic ignimbrite layer in the middle,
and the well-bedded sandstone/gray mudstone succession of the upper Dadaepo Formation. (b) Close-up of thedacitic crystal-rich and pumice-free ignimbrite. (c) Cross-stratified tuffaceous sandstones with volcanogenic clasts.
(d) Volcanogenic clasts in the tuffaceous sandstones and conglomerates.

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Stop 6-5. Basaltic lava overlying the upper Dadaepo Formation
There was a big lake called the Dadaepo Basin in the Songdo area during the late Cretaceous Period, and sediments
were deposited at lake margins to form the Dadaepo Formation. One day, a volcano erupted near this area to create ageological site such as this, with lava flowing into the lake to cover the Dadaepo Formation, which existed before. The
radiometric age of the basalt here is estimated to be about 70 million years old. The boundary between basalt and the
Dadaepo Formation is irregular, with the basalt showing typical characteristics of lava, such as porphyritic andvesicular textures, and auto brecciation.
Dark gray lavas rest on cross-stratified tuffaceous sandstones of the Dadaepo Formation on the Songdo Peninsula,and are in turn overlain by thick volcanic breccias. The contact between the lavas and tuffaceous sandstones isirregular. Load structures, formed by sinking of the overlying lavas, and flame structures produced by squeezing
upward of sediments into the overlying lavas are frequently observed along the contact. The feldspar phenocrysts in thelavas are aligned nearly parallel to the bedding of the underlying sandstone beds. Auto-brecciated fragments andstretched vesicles are also observed in the lavas.

Fig. 6-11. Outcrop photograph of Stop 4-5. (a) Panoramic view of the upper Dadaepo Formation, composed of greenish/gray cross-stratified tuffaceous sandstone and arkosic sandstone, and the overlying basaltic andesite (lava flow).
(b) Close-up of irregular loaded scoured contact between the basaltic andesite and the underlying tuffaceous sandstone and overlying captured in the underlying sandstone. (c-e) Close-up of the basaltic andesite showing auto-brecciated lava fragments and stretched vesicles and feldspar phenocrysts.

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