9th International Congress on the Juras ic ys em, Jaipur, India

Abstracts 9th International Congress on the Jurassic System, Jaipur, India

Abstracts

Dhirendra K. Pandey, Franz T. Fiirsich & Matthias Alberti (Eds.)

Beringeria Special Issue 8 - Erlangen 2 014 Cover photographs Front: The facade of the Hawa Mahal or Palace of Winds in Jaipur. Back: A mural in the Nahargarh Fort near Jaipur.

Addresses of the editors: DHIRENDRA K. PANDEY, Department of Geology, University of Rajasthan, Jaipur, 302004, India; E-mail: [email protected] FRANZ T. FiiRSICH, GeoZentrum Nordbayern, Fachgruppe PaUioumwelt der Friedrich-Alexander­ Universitat Erlangen-Niirnberg, Loewenichstr. 28, D-91054 Erlangen, Germany; E-mail: franz. [email protected] MATTHIAS ALBERTI, Institut fiir Geowissenschaften, Christian-Albrechts-Universitat zu Kiel, Ludewig-Meyn-Str. 10, D-24118 Kiel, Germany; E-mail: [email protected]

Beringeria, Special Issue 8: 213 pages Erlangen, 01.12.2013 ISSN 093 7-0242

Publisher: Freunde der nordbayerischen Geowissenschaftene. V.

Editorial Office: GeoZentrum Nordbayern, Fachgruppe Palaoumwelt, Friedrich-Alexander-Universitat Erlangen-N iirnberg Loewenichstr. 28, D-91054 Erlangen, Germany.

Print: Tiwari Printers Jhotwara,Jaipur, 302012, India. 9th International Congress on the Jurassic System - Abstracts 3

Contents

A sequence stratigraphic interpretation of the contact between the Lathi and 11 Jaisalmer formations, Jaisalmer Basin, Rajasthan, India by A. Agarwal, A. S. Kale & P. B. Jadhav

Ammonites of the family Mayaitidae SPATH, 1928 from the Oxfordian of Kachchh, 13 western India by M. Alberti, D. K. Pandey,M. Hethke & F. T. Fiirsich

Stratigraphy, facies analysis and reservoir characterization of the Upper Jurassic 16 Arab "C", Qatar, Arabian Gulf by H. Al-Saad & F. Sadooni

Re-evaluating the Toarcian Oceanic Anoxic Event from the Southern Hemisphere, 17 Neuquen Basin, Argentina by A. H. Al-Suwaidi, G. N. Angelozzi, F. Baudin, D. Condon, S. E. Damborenea, S. P. Hesselbo, H. C. Jenkyns, M. Mancefi.ido& A. Riccardi

Carbon and oxygen isotope record of the Jurassic bulk carbonates and calcareous 19 fossils from the Pieniny Klippen Belt (Carpathians) by A. Arabas, J. Schlogl & A. Wierzbowski

Micropalaeontological study at the Oxfordian-Kimmeridgian boundary in Central 21 Poland - a preliminary report by M. Barski, M. Hodbod, B. A. Matyja & A. Wierzbowski

Palaeoecological significanceof the Callovian-Oxfordian trace fossils of Gangeshwar 23 Dome, southeast of Bhuj, Mainland Kaclichh, India by N. Y. Bhatt & S. J. Patel

Jurassic basins of India: Tectonic set up and sediment fill by S. K. Biswas 26

Early Jurassic (Sinemurian/Pliensbachian) ammonites of the Central Apennines 28 (Monte di Cetona and Acquasparta, Italy) by J. Blau & C. Meister

Life in a Late Jurassic Subboreal Sea and on its coast: a new taphonomic window 29 of exceptionally preserved fauna at Owadow-Brzezinki (Central Poland) by B. Blazejowski, B. A. Matyja, A. Wierzbowski & H. Wierzbowski

Geodynamic events and the drowning history of a Jurassic carbonate platform: a 31 case study from the Aures area (NE Algeria) by El Hadj Y. Brahim & M. Chadi

The Upper Bajocian Cranocephalites-succession in East Greenland: achieving the 32 highest possible biostratigraphic resolution by J. H. Callomon, P. Alsen & F. Surlyk

The Early Toarcian Oceanic Anoxic Event in Western North America: Testing regional 34 vs. global controlling mechanisms by A. H. Caruthers, D. R. Grocke, P. L. Smith, B. C. Gill, S. J. Porter & P. Hou

The impacts of palaeoenvironmental change on benthic and pelagic fauna during 36 the Toarcian Oceanic Anoxic Event by B. A. Caswell & A. L. Coe

Center of gravity and shell volume calculations for some Jurassic ammonoids from 38 Kachchh, India by A. Chaudhari 4 9rh International Congress on the Jurassic System - Abstracts

Ductile deformation in Jurassic sequence of Kachchh rift basin: A clue to Median 39 High tectonics, Western India by G. Chauhan & M. G. Thakkar

Integrated stratigraphy of the Oxfordian succession on the Isle of Skye, Scotland by 40 A. L. Coe

Nodularity vs. geochemistry in Ammonitico Rosso: a preliminary report from the 41 Upper Jurassic (Betic Cordillera, SE Spain) by R. Coimbra & F. Ol6riz

Palaeolatitudinal patterns of diversity and distribution in Early Jurassic South 43 American bivalves by S. E. Damborenea & J. Echevarrfa

The terrestrial Triassic-J urassic boundary in China by S. Deng, Y. Lu, R. Fan & X. Li 45

Continental drainage and oceanic circulation during the Jurassic inferred fromthe 48 Nd isotope composition of biogenic phosphates and sediments by G. Dera, J. Prunier,P. L. Smith, J. Haggart, E. Popov, A. Guzhov, M. A. Rogov, D. Delsate, D. Thies, G. Cuny, E. Puceat, G. Charbonnier & G. Bayon

Palynology of MissaoVelha and Brejo Santo formations (J urassic) of the Araripe 50 Basin, Northeastern Brazil by S. Duarte, M. Arai & N. Jha

Correlation of the Boreal Jurassic-Cretaceous boundary strata by means of 52 belemnites by 0. S. Dzyuba

Bajocian ammonoids and depositional events of the Arequipa Basin (southern Peru): 54 evidence from Rio Pumani area (Ayacucho) by S. R. Fernandez-Lopez, V. C. Caillaux, E. G. Saldivar & C. C. Budiel

The ecological role of the Jurassic seafloor: benthic ecological functioning during 57 the Kimmeridgian OAE by C. L. J. Frid & B. A. Caswell

Fades patterns and environmental evolution of the Amu Darya Basin and associated 59 basins in central Asia during the Jurassic by F. T. Fiirsich,M. Wilmsen & H. Munsch

Palaeobiogeography and evolutionary trends in the Oxfordian subfamily 60 Prososphinctinae Gt.OWNIAK, 2012 (Ammonoidea, Perisphinctidae) by E. Glowniak

Jurassic geology and biostratigraphy of the Early Callovian in the Kanev district area 62 (Cherkassy region, Ukraine) by D. Gulyaev, A. lppolitov & D. Kiselev

Morphological variations in the ichnogenus Hillichnus: a record from the Jaisalmer 65 Formation, Rajasthan, India by S. S. Gurav & K. G. Kulkarni

Early-Middle Jurassic chemostratigraphy, black shale, and sea-level change: 66 evidence for cyclically repeated global change events by S. P. Hesselbo, C. Korte & C. V. Ullmann

Refined palaeoenvironmental analysis based on changes in macrobenthic 6 7 communities - A case study from the Kimmeridgian of Normandy by M. Hethke, T. Felsch & F. T. Fiirsich 9th International Congress on the Jurassic System - Abstracts 5

Foraminifera and the end-Triassic biotic crisis at the T-J boundary in the Northern 70 Calcareous Alps by A. von Hillebrandt

Sinemurian (Early Jurassic) Ammonites fromFive Card Draw, Nevada and Last Creek, 73 British Columbia by P. Hou, P. L. Smith, A. H. Caruthers & S. ). Porter

Evolutionary significance of latest Jurassic-earliest Cretaceous hydrocarbon seep 75 assemblages from Central Spitsbergen, Svalbard by K. Hryniewicz, C. T. S. Little, H. A. Nakrem, 0. Hammer, M. R. Sandy, A. Kaim & V. Olev

Tetragonal serpulids from the Jurassic: testing the phylogenetic relationships by 77 ultrastructural and mineralogical tube studies by A. lppolitov & E. Kupriyanova

Belemnite zonal scale for the Late Sinemurian - Pliensbachian of Eastern Europe: 79 an update based on data from the Ukrainian Carpathians by A. lppolitov & ). Schlogl

Microfossil research using 3D imaging technology: an experimental study ofJurassic 81 radiolarian fossils using X-ray micro-computed tomography by N. Ishida, N. Kishimoto, A. Matsuoka, K. Kimoto, T. Kurihara & T. Yoshino

Paleoenvironment and sedimentation of deep marine spotted limestones and 83 marls, Lower and Middle Jurassic (Western Carpathians, Tatra Mts.) by J. Iwanczuk & K. Sobien

Middle Jurassic Bivalves from Charu area, Jaisalmer district, Rajasthan, India by R. L. 85 jain, R. P. Kachhara & R. L.-jodhawat

Palaeobiogeographic significance of the Middle Jurassic pholadomyoid bivalves 86 from Kachchh, western India by A. K. jaitly

Jurassic-Cretaceous plant mega- and microfossils from subsurface Gondwana 87 sediments of the Jangareddygudem area, Chintalapudi subbasin, India by N. )ha, N. Prakash & H. J oshi

Environmental significance of the trace fossils of Middle Jurassic rocks, Patcham 88 Island, Kachchh, western India by J. K. joseph, S. ). Patel & N. Y. Bhatt

Towards an integrated Jurassic biostratigraphy for eastern Greenland by S. R. A. Kelly, 92 F.). Gregory, B. Braham, D. P. Strogen & A. G. Whitham

Palaeoenvironmental changes through a Panthalassic margin record of the early 93 Toarcian Oceanic Anoxic Event by D. Kemp & K. Izumi

High-resolution microfossil results from the Toarcian Oceanic Anoxic Event, 94 Yorkshire, UK by A. E. Kennedy, A. L. Coe, W. D. Gosling & J. B. Riding

Palaeobiogeographical study of the Middle-Upper Jurassic corals in East-Central 96 Iran by K. Khaksar,M. Farboodi & A. Khaksar

An overview of the Jurassic . dinosaur fossil record from India: Implications for 98 depositional facies and palaeoenvironments by A. Khosla 6 9th International Congress on the Jurassic System - Abstracts

Ostracod biostratigraphical zonation of the MiddleJurassic beds of western India - a 100 review by S. C. Khosla

The Jurassic-Cretaceous short-lived atoll coral reefs around active volcanoes in 101 the Western Tethys (Ukrainian Carpathians) by M. Krobicki, A. Feldman-Olszewska, J. Iwanczuk & 0. Hnylko

Palaeoenvironmental context and palaeoecological significance of microbialites 103 - metazoan assemblages from condensed deposits at the Middle-Upper Jurassic transition (Getic Unit, Southern Carpathians, Romania) by I. Lazar & M. Gradinaru

Jurassic - Early Cretaceous evolution of the passive margin of the Moesian Plate 105 (Danubian Unit, Romanian Carpathians) by I. Lazar, M. Krobicki, M. Gradinaru & M. E. Pop a

Jurassic ammonite faunas of northern Iran and their palaeobiogeographic 107 significance by M. R. Majidifard

Middle Jurassic ostracod fauna fromJaisal mer, Rajasthan, India by K. Manisha, M. M. 108 Lal & S. Vidhya

Recent progress in ecological studies on living radiolarians and its application to 110 the Jurassic ecosystem - End-Triassic mass extinction and early Jurassic recovery in the pelagic realm by A. Matsuoka

On the Oxfordian-Kimmeridgian (Upper Jurassic) boundary - current state of 111 knowledge by B. A. Matyja & A. Wierzbowski

Ammonite distribution in late Middle-Upper Jurassic.deposits of epicratonic Poland: 113 the key to ecology, biogeography, palaeogeography and geotectonic events by B. A. Matyja & A.Wierzbowski

Phricodoceratinae SPATH, 1938 (Mollusca, Cephalopoda): ontogeny, evolution & 115 paleobiogeography by C. Meister & J.-L. Dommergues

Microfacies of the Bathonian sediments of the Jumara Dome, Kachchh, western 116 India: Inference of depositional environments by A. Misra

Ammonite zonation of the Boreal Bathonian Stage of Greenland by V. Mitta & P. 118 Alsen

Boreai-Tethyan correlation of the Bajocian-Bathonian boundary beds in the Sokur 120 section (Central Russia): new insights into an old story by V. Mitta, V. Kostyleva, 0. S. Dzyuba, L. Glinskikh, B. N. Shurygin, V. Seltzer & A. Ivanov

Brachiopod diversity in theJurassic of the Kutch and Jaisalmer basins, western India 122 by D. Mukherjee

Life in a Jurassic shelf lagoon: The Kamar-e-Mehdi Formation of east-central Iran by 124 Y. Pan & F. T. Fiirsich 9th International Congress on the Jurassic System - Abstracts 7

A review of Virgatosphinctes densiplicatus (WAAGEN) from the Tithonian beds of 126 Kachchh Basin, west India by D. K. Pandey & S. Bhaumik

Sequence stratigraphic framework of the Oxfordian to Tithonian sediments 127 (Baisakhi Formation) in the Jaisalmer Basin by D. K. Pandey & D. Pooniya

Record of a condensed late Early to Middle Callovian horizon (Rehmanni- 128 Obtusicostites zones) fromthe eastern part of the Jaisalmer Basin, western India by D. K. Pandey & N. Swami

Sedimentological and palaeoecological significanceof trace fossils from theJurassic 129 succession of the Jhura Dome, Mainland Kachchh, Western India by S. J. Patel & N. J. Pate I

Discovery of Early Bathonian ammonites from Kachchh, western India and their 133 biostratigraphic implications by D. B. Pathak & B. Pandey

Parkinsoniids and garantianids (Late Bajocian Ammonoidea) as guide fossils and 134 biostratigraphic indices by G. Pavia & S. R. Fernandez-Lopez

A firstUpper )urassic 40Ar/39Ar date fromOxfordian ammonite-calibrated volcanic 137 layers (bentonites) from the Rosso Ammonitico Veronese, Italy by P. Pellenard, S. Nomade, L. Martire, F. Manna & H. Guillou

Integrated stratigraphy of the potential candidate Oxfordian GSSP at Thuoux and 139 . Saint-Pierre d�rgen�on (France) by P. Pellenard, A. Bartolini, S. Boulila, P. -Y. Collin, D. Fortwengler,B. Galbrun, S. Gardin, V. Huault, E. Huret, D. Marchand & J. Thierry

Evolution ofVolgian-Valanginian microphyc:oplankton communities in the Olenyok 141 River region, North Siberia by E. B. Pestchevitskaya

Marine (black) and marginal-marine (green) Toarcian shales Europe - carbon 1 143 isotope consistency, TOC inconsistency by G. Pienkowski & M. Hoctuod

End-Triassic biota crisis and earliest Jurassic recovery in continental strata of 145 Poland in relation to rapid climatic reversals associated with CAMP volcanism by G. Pienkowski, G. Niedzwiedzki & P. Branski

New high-resolution geochemistry of Sinemurian marine sections in British 147 Columbia and Nevada by S. J. Porter,P. L. Smith, A. H. Caruthers, P. Hou, D. R. Grocke & D. Selby

An overview of Upper Gondwana fossil floral assemblages of the Kachchh Basin, 148 India by N. Prakash

When did the twain meet? The epeiric Ethiopian Gulf with the Western Indian 150 craton; Coccoliths, the beacon of light! by J. Rai

Integrated nannofossil-dinoflagellatecyst - ammonoid biostratigraphy from Wagad 151 area, Kachchh, Western India by J. Rai, S. Garg, M. Gupta, A. Singh, D. K. Pandey & R. Garg 8 9th International Congress on the Jurassic System - Abstracts

Nannofossil biostratigraphy of the Chari Formation,Jumara Dome, Kachchh, western 153 India by J. Rai, M. Gupta, S. Garg, A. Singh, S. Jain & D. K. Pandey

Middle-Jurassic age calcareous nannofossils from Habo Dome, Kachchh, western 155 India by J. Rai, S. J. Patel, A. Singh, M. Gupta, S. Garg, B. Thakur & H. Shukla

Continental Jurassic of peninsular India - A floristic and stratigraphic riddle by A. 158 Rajanikanth & C. Chinnappa

An overview of yellow Limestone deposit ofJaisalmer Basin of Rajasthan, India by T. 161 S. Ranawat & N. Srivastave

Limit of Upper Bathonian-Lower Callovian in Ankilizato region (Morondava Basin) 162 by H. N. Randrianaly & A. Rasoamiaramanana

Stable isotopes of foraminifera and ostracods for interpreting the Toarcian Oceanic 163 Anoxic Event at the South Iberian palaeomargin by M. Reo lid

Ecostratigraphy of foraminiferal assemblages and geochemistry for approaching 165 the incidence of Early Toarcian environmental changes at the North Gondwana palaeomargin (Traras Mountains, Algeria) by M. Reolid, A. Marok & A. Sebane

The Early Toarcian Oceanic Anoxic Event in the External Subbetic (South Iberian 167 Palaeomargin, westernmost Tethys): geochemistry, nannofossils, and ichnology of the La Cerradura section by M. Reolid, E. Mattioli, L. M. Nieto & F. J. Rodrfguez-Tovar

Preliminary report on the ammonite fauna and stratigraphy of the Beckeri Zone 169 (Upper Kimmeridgian) of the southern Crimea (Ukraine) by M. A. Ro gov

Quantitative and qualitative aspects of changes in shell size through the evolution of 171 Volgian ammonites in the Russian Sea: Cope's rule, Lilliput effect, dimorphism, and polymorphism by M. A. Rogov

New data on the Lower-Upper Kimmeridgian boundary beds of southern Tatarstan, 174 Central Russia by M. A. Rogov, A. Wierzbowski, E. V. Shchepetova & H. Wierzbowski

Distichoceras bicostatum (STAHL) (Ammonoidea) from Kutch, western India; its 176 stratigraphic and palaeoecological significance by P. Roy

Integrated biostratigraphy across the AalenianjBajocian boundary of the Central 177 High Atlas, Morocco by D. Sadki

Middle Jurassic coral biohermal limestones from pelagic carbonate platforms 179 (Pieniny Klippen Basin, Western Carpathians) by J. Schlogl, A. To masorych, D. Ivanova, B. Lathuiliere, L. Villier & M. Golej

Distribution of the Jurassic Pectinoida and Ostreoida from the Tanggula Mountains, 181 China: Biogeographic relations and importance of trans-Pacific migration and the Hispanic Corridor by J. Sha & P. L. Smith

Palaeobiogeography and evolution of Kutch Virgatosphinctinae by S. Shome & S. 182 Bard ban 9th International Congress on the Jurassic System - Abstracts 9

Jurassic Boreal zonal standard: Possibilities of Boreai-Tethyan correlation based on 185 an integrated bio-, magneto- and chemostratigraphic approach by B. N. Shurygin & 0. S. Dzyuba

Ammonite biostratigraphy of the Pliensbachian-Toarcian transition at Westgate, 188 Nevada, USA by P. L. Smith & A. H. Caruthers

Ichnology of the Callovian-Oxfordian of Katrol Hill Range, Southwest of Bhuj, 190 Kachchh, western India by P. M. Solanki, N. Y. Bhatt, S. J. Patel & J. M. Patel

Response of Jurassic strata of Kachchh to Quaternary tectonics in an active intra- 192 plate basin of Kachchh, western India by M. G. Thakkar

Untangling real from apparent seawater temperature variability during the Late 193 Jurassic by A. To masov)lch, D. Jacob, M. Joachimski, M. L6pez Correa, J. Schlogl

Ichnological record of food content change in Middle-Upper Jurassic pelagic 195 sediments of the Fatricum domain in the Tatra Mountains, southern Poland by A. Uchman & R. Jach

First contribution to precise biostratigraphy of Upper Tithonian rocks from the 197 Veracruz Basin (SE Mexico) by A. B. Villasefi.or& F. Ol6riz

Foraminiferal zonation of the Jurassic of the Caucasus and Precaucasus by V. J. Vuks 200

Syn- and post-tectonic palaeomagnetism ofJurassic sediments from the Velebit Mts 204 (Karst Dinarides, Croatia) by T. Werner, I. Vlahovic, M. Sidorczuk & M. Lewandowski

Oxygen and carbon isotope records of uppermost Callovian-Lower Kimmeridgian 205 belemnite rostra and bulk carbonates from the Polish Jura Chain (central Poland): environmental changes in the Submediterranean Province of Europe by H. Wierzbowski

Revised seawater strontium isotope curve for the Late Bajocian-Oxfordian (Middle- 207 Late Jurassic) by H. Wierzbowski, R. Anczkiewicz, J. Bazarnik & J. Pawlak

Orbital cyclicity and its environmental response - a case study from the Upper 209 Bathonian of Central Poland by P. Zi6lkowski, T. Werner, Z. Dubicka & L. A. Hinnov 10 9th International Congress on the Jurassic System - Abstracts 9th International Congress on the jurassic System - Abstracts 11

A sequence stratigraphic interpretation ofthe contact between the Lathi and Jaisalmer formations, Jaisalmer Basin, Rajasthan, India

ANSHIKA AGARWAL 1, ANAND S. KALE1 & PRADEEP B. }ADHAV2

1Bharat Petro Resources Limited, Maker To wer, 'E' Wing, CuffeParade, Mumbai 400005, India; E-mail: [email protected] 2Department of Petroleum Engineering, Maharashtra Institute of Te chnology, Ko thrud, Pune 411 038, India

The Jaisalmer Basin of Rajasthan, India is the interspersed with finer overbank facies. stable shelfal part of the larger Indus Basin and These pass upwards into tabular sandstones, preserves a fairly complete record of sea-level typically with relatively flat bases and convex­ changes during the Jurassic to Early Cretaceous up tops. Internally these are coarsening-up and times varying from deltaic/transitional to hummocky cross-stratified with distinct lateral a widespread carbonate platform setting. accretion, representing a more distal facies Lithostratigraphically, Jurassic sediments in the deposited above the storm wave-base as mouth Jaisalmer Basin are divided into Lathi, Jaisalmer, bars/offshore bars. The sandstones gradually Baisakhi, and Bhadesar fo rmations. Mesozoic become the dominant facies with decreasing sedimentation starts with the siliciclastic­ inter-beds of claystone followed by an interval dominated Lathi Formation (Liassic-Bajocian) with inter-bedded fine sandstones, bioturbated corresponding with the evolution of the Tethyan claystones and arenaceous limestones. The passive margin and subsequent initiation the upper part represents a gradual decrease in East African rifting. The Jaisalmer Formation the siliciclastic supply and the establishment (Bathonian-Oxfordian) r� presents carbonate­ of the carbonate depositional system. Further dominated sedimentation resulting from the up in the succession the arenaceous limestones first major long-term marine transgression of pass into thicker and massive limestones with the basin. well developed internal bedding characters The contact between the Lathi (Liassic­ suggesting that they are re-distributed by Bajocian) and Jaisalmer (Bajocian-Oxfordian) wave and/ or currents in a shallow inner shelf fo rmations has been considered in earlier setting. studies to be gradational and intertonguing in A valley situated west and up-dip ofKheta Sar surface exposures as well as in subsurface. The section shows erosion to cut a level deeper than present work deals with the documentation of in the easterly fa ce of the Kheta Sar section. This the contact between the two fo rmations and NNE oriented valley is underlain by limestones, its interpretation in a sequence stratigraphic which are thinly bedded flaggy, trough cross­ context. Examination of the transition from a stratified and cherty whereas higher up along siliciclastic depositional system to a carbonate the flanks the earlier described succession setting has been done along five transects over is exposed. These limestones in the valley a 30 km stretch along the strike from NE to SW are interpreted to be the initial transgressive of Jaisalmer town, viz. Basanpir, Thaiat, Kheta fill into incisions developed during sea-level Sar, Temde Rai, and Narsingo ki dhani. lowstand. An angular relationship between the Conventionally the intertonguing contact Thaiat Member and overlying Hamira Member between the Thaiat Member of the Lathi is seen in this valley as well as in the area west of Formation and the Hamira Member of the Narsingo ki Dhani, where the ripple- and cross­ Jaisalmer Formation is recognized at the laminated succession of alternating calcareous first appearance of calcareous beds. These sand and aranaceous limestones with clay are overlain by inter-beds of sandstones and interbeds are progressively onlapped by thick claystones and fo llowed by limestones. The limestone beds. Thaiat Member comprises primarily lower From a sequence stratigraphic perspective, delta plain multi-storey channel sandstones the uppermost part of the Lathi Formation 12 9thInternational Congress on the Jurassic System -Abstracts

(Thaiat Member) is interpreted to be a overlying mixed carbonate-siliclastic section transgressive systems tract, as evidenced by represents the subsequent tr ansgressive the appearance of transitional and marine systems tract of the overlying sequence; the fa cies overlying the lower deltaic siliciclastics. maximum flooding zone of this sequence are The paleosol above these represents the the thickly bedded, nearly horizontal limestones sequence boundary between the uppermost of the Hamira Member. The highstand systems Lathi succession and overlying lowermost tract of the underlying sequence in the Thaiat carbonates of the Jaisalmer Formation. This Member would be present further basinward, boundary covers the time span of the high stand concealed beneath the onlapping carbonates. to lowstand regressive systems tracts. The 9rh International Congress on the Jurassic System - Abstracts 13

Ammonites of the family Mayaitidae SPATH, 1928 from the Oxfordian of Kachchh, western India

MATTHIAS ALBERTI1 *, DHIRENDRA K. PANDEY2, MANJA HETHKE3 & FRANZ T. FURSICH3

1/nstitut fu r Geowissenschaftenl Christian-Aibrechts-Universitiit zu Kie/, Ludewig-Meyn-Strafle 10, 24118 Kie/1 Germany; E-mail: [email protected] 2Department of Geolog� Universityof Rajasthanl ]aipur 302 0041 India; E-mail: dhirendrap@hotmail. eo m 3GeoZentrum Nordbayern� Friedrich-Aiexander-UniversitiitErla ngen-Niirnbergl Loewenichstrafle281 91054 Erlangenl Germany; E-mail: manja.hethke@fa u.de�[email protected]

*Corresponding author

The geology of the Kachchh Basin in western been used as the base for a series of articles India has been studied for more than a century planned to enlarge our knowledge on the Upper beginning with the surveys of GRANT (1840) and Jurassic ammonite fauna of the Kachchh Basin WYNNE (1872). Since then several generations (see ALBERTI et al. 2011; PANDEY et al. 2012). of scientists have published articles describing The current study deals with members of the the rich fossil record of the area - especially of family Mayaitidae SPATH, 1928. Ammonites of the Jurassic strata. In this context, ammonites, this group are relatively common in Oxfordian in particular, took a prominent position as they rocks of the Indian subcontinent as well as allowed biostratigraphic correlations and fairly Madagascar (COLLIGNON 1959) and have also precise age determinations of the sedimentary been reported from East Africa, Thailand, the rocks. Following the - early substantial Sula Islands, and New Guinea (ENAY & CARIOU monographs on Jurassic cephalopods of the 1997), but do not occur in the northwestern Kachchh Basin by WAAGEN (1873-1875) and Tethys nor in the boreal realm. SPATH (1927-1933), many articles have been Since several of the mayaitids previously published concentrating either on single described from the Kachchh Basin are long­ ammonite groups, fossils of individual localities ranging taxa and since the spatial distribution and time slices, or defining biostratigraphic of the group is restricted, they have generally successions (e.g., SINGH et al. 1982, 1983; been regarded as comparatively poor index PANDEY & AGRAWAL 1984; AGRAWAL & PANDEY fo ssils and rather neglected in taxonomic 1985; BARDHAN & DATTA 1987; KRISHNA & studies. The present collection includes around WESTERMANN 1987; PANDEY & WESTERMANN 100 mayaitids allowing the first modern and 1988; KRISHNA & PATHAK 1991; PANDEY et al. nearly comprehensive study on the taxonomy of 1994; PANDEY & CALLOMON 1995; ]AIN et al. the group. Most of the morphospecies originally 1996; KRISHNA et al. 1996a, b, 2009a, b). In described by SPATH (1927-1933) could be combination with a deeper understanding of re cognized and confirmed representing the geology of the basin these studies offereda the genera Mayaites SPATH, 1924 (6 taxa), much more detailed view on the development Epimayaites SPATH, 1928 (12 taxa), Dhosaites and composition of the ammonite fauna in the SPATH, 1924 (2 taxa), and Paryphoceras SPATH, area as well as increased the resolution of the 1928 (3 taxa). Specimens were prepared, biostratigraphic record. described, as well as photographed and A collection of more than 800 ammonites depending on the preservational quality, their obtained during four recent field surveys ribbing patterns and suture lines have been concentrating mainly on the Oxfordian · drawn. Cross-sections allowed the study of succession of the Kachchh Basin, however, their allometric growth (i.e., changes in shape showed that the fossil record is still not fully and proportional dimensions of the whorl known. The material was collected with a high section from inner to outer whorls), which is stratigraphic resolution and has consequently characteristic of particular taxa. Since adult 14 9th International Congress on the Jurassic System -Abstracts

JAIN, S., CALLOMON, J.H. PANDEY, D.K. 1996. On the earliest ammonites preserved with complete body & chambers are extremely rare in the Kachchh known occurrence of the Middle Jurassic ammonite genus Reineckeia in the Upper Bathonian of Jumara, Basin (compare PANDEY et al. 2012), the study Kachchh, western India. - Palaontologische Zeitschrift of cross-sections through the available large 70: 129-143. KRISHNA, J. WESTERMANN, G.E.G. 1987. Fauna) specimens enabled reliable identifications of & material representing only inner whorls. associations of the Middle Jurassic ammonite genus Macrocephalites in Kachchh, western India. - The distribution of morphospecies through Canadian Journal of Earth Sciences 24: 15 70-1582. time and space was evaluated leading to KRISHNA, J. PATHAK, D. B. 1991. Ammonoid biochronology & the recognition of taxa indicative of certain of the Upper Jurassic Kimmeridgian stage in Kachchh, ammonite zones in the Kachchh Basin, which India. - Journal of the Palaeontological Society of in the future might enable correlations within India 36: 1-13. KRISHNA, J., PATHAK, D.B. PANDEY, 1996a. Quantum & 8. their distribution area (e.g., between India, refinement in the Kimmeridgian ammonoid Africa, and Madagascar). Promising candidates chronologyin Kachchh (India). - GeoResearch Forum in this context include Epimayaites fa lcoides 1-2: 195-204. KRISHNA, J., MELENDEZ, G., PANDEY, & PATHAK, D.B. 1996b. SPATH, 1928, which is very common in the 8. Middle Oxfordian ammonites (Perisphinctinae) Plicatilis to Transversarium zones (Middle from Kachchh (India): Biostratigraphic and Oxfordian) and Epimayaites subtumidus palaeobiogeographic implications. - Revista Espafi.ola (WAAGEN, 1875), which has been collected de Paleontologfa, No. Extraordinario: 140-147. KRISHNA, J., PANDEY, & 0HJA, J.R. 2009a. Gregoryceras in exclusively from the lower Bifurcatus Zone 8. (lower Upper Oxfordian). Other common taxa the Oxfordian of Kachchh (India): Diverse eventful implications. - Geobios 42: 197-208. Mayaites maya (J. in the Kachchh Basin include KRISHNA, J., PANDEY, & PATHAK, 2009b. 8. 0.8. DE C. SOWERBY,18 40), M. rotundus SPATH, 1928, Characterization of Dichotomoceras in the Oxfordian Ep imayaites polyphemus (WAAGEN, 1875), E. ofKachchh.- Journal of the Geological Society oflndia lemoini (SPATH, 1924), E. axonoides SPATH, 74:469-479. PANDEY, D.K. AGRAWAL, S.K. 1984. On two new species 1928, and E. transiens (WAAGEN, 1875), but & of the Middle Jurassic ammonite genus Clydoniceras their biostratigraphic range is either long or Blake fromKachchh, Western India. - Neues Jahrbuch yet undefined. Other taxa, especially the genera fiir Geologie und Palaontologie, Monatshefte6: 321- Dhosaites and Paryphoceras, are represented 326. PANDEY, D.K. WESTERMANN, G.E.G. 1988. First record of only by solitary specimens. & Bathonian Bullatimorphites (Jurassic Ammonitina) from Kachchh, India. - Journal of Paleontology 62: References 148-150. AGRAWAL, S.K. & PANDEY, D.K. 1985. Biostratigraphy of PANDEY, D.K. CALLOMON, J.H. 1995. Contribution to the & the Bathonian-Callovian beds of Gora Dongar in Jurassic of Kachchh, Western India. Ill. The Middle Pachchham "Island", District Kachchh (Gujarat). - Bathonian ammonite families Clydoniceratidae and Proceedings of the Indian National Science Academy, Perisphinctidae from Pachchham Island. - Beringeria Part A 51: 887-903. 16: 125-145. ALBERTI, M., PANDEY, D.K. & FORSICH, F.T. 2011. Ammonites PANDEY, D.K., CALLOMON, J.H. & FORSICH, F.T. 1994. On the of the genus Peltoceratoides SPATH, 1924 from the occurrence of the Callovian ammonite Parapatoceras Oxfordian of Kachchh, western India. - Neues Jahrbuch tuberculatum (BAUGIER & SAUZE, 1843) in Kachchh, fiir Geologie und Palaontologie, Abhandlungen 262: Western India. - Palaontologische Zeitschrift 68: 1-18. 63-69. BARDHAN, S. & DATTA, K. 1987. Biostratigraphy of Jurassic PANDEY, D.K., ALBERTI, M. & FORSICH, F.T.2012. Ammonites Chari Formation: a study in Keera Dome, Kutch, of the genus Perisphinctes WAAGEN, 1869 from the Gujarat. - Journal of the Geological Society of India Oxfordian of Kachchh, western India. - Revue de 30: 121-131. Paleobiologie 31: 483-587. CoLLIGNON, M. 1959. Atlas des fossiles caracteristiques de SJNGH, C.S.P., JAITLY, A.K. & PANDEY, D.K. 1982. First report Madagascar. Fascicule Ill (Oxfordien). 13 pis., Service of some Bajocian-Bathonian (Middle Jurassic) geologique, Republique malgache, Tananarive. ammonoids and the age of the oldest sediments from ENAY, R. CARIOU, E. 1997. Ammonite faunas and Kachchh, W. India. - Newsletters on Stratigraphy 11: & palaeobiogeography of the Himalayan belt during the 37-40. Jurassic: Initiation of a Late Jurassic austral ammonite SJNGH, C.S.P., PANDEY, D.K. & JAITLY, A.K. 1983. Discovery fauna. Palaeogeography, Palaeoclimatology, of Clydoniceras BLAKE and Gracilisphinctes BucKMAN Palaeoecology134: 1-38. (Bathonian-Middle Jurassic ammonites) in Kachchh, GRANT, C.W. 1840. Memoir to illustrate a geological map Western India. - Journal of Palaeontology 57: 821- of Cutch. - Transactions of the Geological Society of 824. London, Series 2 (5): 289-326. SPATH, L.F.1927-1933. Revision of the Jurassic cephalopod 9th International Congress on the Jurassic System - Abstracts 15

fa una of Kachh (Cutch). Parts I-VI. - Memoirs of the India, Palaeontologia Indica, series 9, 1: part I, 1-22, Geological Survey of India, Palaeontologia Indica, new pis. 1-4 [1873]; part 11, 23-76, pis. 5-14 [1875a]; part series 9, 2: part I, 1-71, pis. 1-7 [1927]; part 72- 77-106, pis. 15-24 [1875b]; part 107-247, pis. 11, Ill, IV, 161, pis. 8-19 [1928a]; part 162-278, pis. 20-47 25-60 [1875c]. Ill, [1928b]; part IV,279-550, pis. 48-102 [1931a]; part WYNNE, A.B. 1872. Memoir of the geology of Kutch to 551-658, pis. 103-124 [1931b]; part VI, 659-945, accompany the map compiled by AB. Wynne and F. V, pis. 125-130 [1933]. Fedden during the seasons of 1867-68 and 1868-69. WAAGEN, W. 1873-1875. jurassic fauna of Kutch. The Memoirs of the Geological Survey of India 9: 1-293. Cephalopoda. - Memoirs of the Geological Survey of 16 9thInternational Congress on the Jurassic System - Abstracts

Stratigraphy, facies analysis and reservoir characterization of the Upper Jurassic Arab "C", Qatar, Arabian Gulf

HAMAD AL-SAAD1 * & FADHIL SADOONI2

1Department of Chemistry and Earth Sciences, Qatar University, P. 0. Box 2713, Doha, Qatar; E-mail: [email protected] 2Environmental Studies Center, Qatar University, P. 0. Box 2713, Doha, Qatar

*Corresponding author

The Arab C reservoir is an economically dolomitization. Present-day rock properties significant member of the Upper Jurassic reflect both depositional and diagenetic Arab Formation, the most important Jurassic controls. Petrophyscial data suggest that the reservoir in the Arabian Basin including Arab C reservoir may have porosity values up to Qatar. This unit represents transgressive 30% and permeability values in excess of 450 systems tracts and consists of oolitic-peloidal md. The lithological and diagenetic features of grainstone, cyanobacterial algal boundstone the formation, its widespread distribution and and lime wackestone and mudstone. Large the high porosity and permeability values make portions of these rocks underwent significant the fo rmation an important exploration target diagenetic modification including dissolution, in most of Qatar's hydrocarbon fields. cementation, evaporite replacement and 9th International Congress on the Jurassic System -Abstracts 17

Re-evaluating the Toarcian Oceanic Anoxic Event from the Southern Hemisphere, Neuquen Basin, Argentina

A. H. AL-SUWAIDI1 *, G. N. ANGELOZZI2, F. 8AUDIN3, D. CONDON4, S. E. DAMBORENEA5, S. P. HESSELB06, H. c. }ENKYNS7, M. MANCENID05 & A. RICCARDI5

1Petroleum Geoscience Dept., Petroleum Institute, University and Research Centre, PO Box 2533, Abu Dhabi, UA E; E-mail: [email protected] 2GEMA S. R.L. Servicios Bioestratigraficos, Avenida CalchaquiKm .23.5, 1888 Florencio Va rela, Argentina; E-mail: [email protected] 3UPMC- Universite de Paris 06 & CNRS, UMR 71 93, /STeP, F- 75252, Paris Cx 05, France; E-mail: fra ncois. [email protected] 4British Geological Survey, Environmental Science Centre, Nicker Hill, Keyworth, Nottingham, NG12 5GG, UK; E-mail: [email protected] 5Departamento Paleontologia lnvertebrados, Museo de Ciencias Naturales La Plata, Argentina, Paseo del Basque S jN, 1900 La Plata, Argentina; E-mail: riccardi@fcny m.unlp.edu.ar; sdambore@fc nym. unlp.edu.ar; mmanceni@fc nym.unlp.edu.ar 6Camborne School of Mines, College of Engineering, Mathematics and Physical Sciences, Universityof Exeter, Penryn Campus, Cornwall, TR1 0 9EZ, UK; E-mail: S.P.Hesse/[email protected] 7 Department of Earth Sciences, University of Oxfo rd, Parks Road, Oxfo rd, OX1 3PR, UK; E-mail: hug h. [email protected]. uk

*Corresponding author

The carbon-isotope composition of organic and the other concerning Arroyo Serrucho in matter and carbonate in terrestrial and marine the Mendoza Province (MAZZINI et al. 2010). sediments from the Early Toarcian ( -183 MAZZINI et al. (2010) provide U-Pb ages Ma) was subject to abrupt and substantial determined by ID-TIMS on zircons from two tuff disturbances of the carbon cycle, recognized beds that they interpreted to be located within as ·a negative carbon isotope excursion (CIE) the negative CIE of the T- OAE. These beds gave disrupting an overall positive excursion. These ages of 181.42 ± 0.24 Ma and 180.59 ± 0.43 Ma, disturbances are associated with extreme cases dates were subsequently used to constrain the of global environmental change and correspond estimated ages of the limits ofthe Toarcian Stage with the formation of the Karoo-Ferrar Large (GRADSTEIN et al. 2012). Here we present new Igneous Province (LIP), possible dissociation data from Arroyo Lapa and Arroyo Serrucho, of methane hydrate, increases in sea-floor comprising high-resolution lithostratigraphy, hydrothermal activity, ocean acidification, and biostratigraphy, organic carbon isotopes widespread deposition of marine black shales (bulk sediment and fossil wood), total organic linked to intervals of oxygen depletion in large carbon, hydrogen index and new ages of ash volumes of ocean water, referred to as Oceanic beds from the Early Toarcian. These new data Anoxic Events or OAE (e.g. HESSELBO et al. 2000; show multiple large-scale negative and positive PALFY & SMITH 2000; }ONES & }ENKYNS 2001; excursions through the Early-Middle Toarcian HESSELBO et al. 2007; SVENSEN et al. 2007; KUMP interval, with multiple abrupt negative shifts in et al. 2009; TRECALLI et al. 2012). Recently, 613C org and values falling below -30°/o o, followed two studies have been published concerning by abrupt positive shifts with 613Corg values of the expression of the Toarcian Oceanic Anoxic >-24%o. In addition to this higher resolution Event (T-OAE) in the Southern Hemisphere organic carbon data, new radio-isotopic Neuqulm Basin, Argentina; one study fo cused ages from volcanic ash layers at Arroyo Lapa on chemostratigraphic and biostratigraphic confirm synchrony of isotopic perturbations identification of the T- OAE at Arroyo Lapa in with eruptive and intrusive phases of the the Neuquen Province (AL-SUWAIDI et al. 2010), Karoo-Ferrar Large Igneous Province (MoULIN 18 9th International Congress on the Jurassic System - Abstracts

}ONES, C.E. }ENKYNS, H.C. 2001. Seawater strontium et al. 2011; SVENSON et al. 2012) and the Chon & Aike Province (PANKHURST et al. 2000). Re­ isotopes, oceanic anoxic events, and seafloor hydrothermal activity in the Jurassic and Cretaceous. evaluation of the record from MAZZINI et al. -American Journal of Science 301: 112-149. (2010) with our data from Arroyo Serrucho KUMP, L.R., BRALOWER, T.J. RIDGWELL, A. 2009. Ocean & suggests that the carbon isotope stratigraphy acidification in deep time. - Oceanography 22: 94- and ages correspond to negative CIE's preceding 107. MAZZINI, A., SVENSON, H., LEANZA, H.A., CORFU, F. PLANKE, the initial excursion; furthermore the ages & S. 2010. Early Jurassic shale chemostratigraphy and determined by MAZZINI et al. (2010) in addition U-Pb ages from the Neuquen Basin (Argentina): to those determined here provide us with new Implications for the Toarcian Oceanic Anoxic Event. insights into the duration of the events and will - Earth and Planetary Science Letters 297: 633-645. aid in refining the absolute ages of the base of doi:10.1016/j.epsl.2010.07.017. MOULIN, M., FLUTEAY, F.,COURTIL LOT, V., MARSH, J., DELPECH, the Toarcian, as well as timing of the onset of G., QUIDELLEAUR, X., GERARD, M. }AY, A.E. 2011. An & the initial negative carbon isotope excursion. attempt to constrain the age, duration and eruptive These new results also raise questions history of the Karoo flood basalt: Naude's Nek section regarding how well the Toarcian global carbon (South Africa). - Journal of Geophysical Research 116: cycle is described by existing records from the B07403, doi:10.1029/2011JB008210.2011.07. PALFY, J. SMITH, P. L. 2000. Synchrony between Early & Tethyan-Laurasian Seaway locations and about Jurassic extinction, oceanic anoxic event, and the the actual timing of the event. Karoo-Ferrar flood basalt volcanism. - Geology 28: 747-750. References PANKHURST, R.J., RILEY, T. R., FANNING, C.M KELLEY, S.P. & AL-SUWAIDI, A. H., ANGELOZZI, G.N., BAUDIN, F.,DAM BORENEA, 2000. Episodic silicic volcanism in Patagonia and S.E., HESSELBO, S.E., }ENKYNS, H.C., MANCENIDO, M.O. the Antarctic Peninsula: chronology of magmatism & RICCARDI, A.C. 2010. First record of the Early Toarcian associated with the break-up of Gondwana. - Journal Oceanic Anoxic Event from the Southern Hemisphere, of Petrology 41: 605-625. Neuquen Basin, Argentina. - Journal of the Geological SVENSON, H., PLANKE, S., CHEVALLIER, L., MALTHE-S0RENSSEN, Society 167: 633-636. CORFU, F. }AMTVEIT, B. 2007. Hydrothermal A, & GRADSTEIN, F.M., 0GG, G.J., SCHMITZ, M.D. 0GG, G.M. venting of greenhouse gases triggering Early Jurassic & 2012. The geological time scale 2012. Vol. 2: 762 pp., global warming. - Earth and Planetary Science Letters Elsevier, Oxford. 256: 554-566. doi:10.1016fj.epsl.2007.02.013. HESSELBO, S.P., GROCKE, D.R., }ENKYNS, H.C., BJERRUM, C.J., SVENSON, H., CORFU, F., POLTEAU, S., HAMMER, PLANKE, 0. & FARRIMOND, P., M ORGANS BELL, H.S. GREEN, O.R. 2000. S. 2012. Rapid magma emplacement in the Karoo & Massive dissociation of gas hydrate during a Jurassic Large Igneous Province. - Earth and Planetary Science oceanic anoxic event. - Nature 406: 392-395. Letters 325-326: 1-9. HESSELBO, S.P., }ENKYNS, H.C., 0UARTE, L.V. OLIVE IRA, L.C.V. TRECALLI, A., SPANGENBERG, J., ADATTE, T. , F6LLMI, K.N. & & 2007. Carbon-isotope record of the Early Jurassic PARENTE, M. 2012. Carbonate platform evidence of (Toarcian) oceanic anoxic event from fo ssil wood ocean acidification at the onset of the early Toarcian and marine carbonate (Lusitanian Basin, Portugal). - oceanic anoxic event. - Earth and Planetary Science Earth and Planetary Science Letters 253: 455-470. Letters 357-358: 214-225. 9th International Congress on the Jurassic System - Abstracts 19

Carbon and oxygen isotope record of the Jurassic bulk carbonates and calcareous fossils from the Pieniny Klippen Belt (Carpathians)

AGNIESZKA ARABAS1 *, }AN SCHLOGL2 & ANDRZEJ WIERZBOWSKI3

1Institute of Geological Sciences, Polish Academy of Sciences, 00-818 Wa rsaw, Poland; E-mail.· [email protected] 2FacultyofNatural Sciences, Comenius Universityin Bratislava, SK-842 15 Bratislava, Slovakia; E-mail: [email protected] s. uniba.sk 3Polish Geological Institute - National Research Institute, 00-975 Wa rsaw, Poland; E-mail: andrzej. [email protected]

*Corresponding author

Secularvariations in carbon isotope composition composition of marine carbonates from the of marine carbonates are correlated with Pieniny Klippen Belt may be used as a proxy fo r changes in global ocean productivity. Isotopic the Jurassic environment of the northern part composition of carbonate oxygen serves as a of the Tethys Ocean. basis of seawater temperature reconstructions, The main aims of the project are: which are indicative of environmental and • to reconstruct the evolution of sea water climatic changes. Carbon and oxygen isotope temperatures using the oxygen isotope

belemnite 613C%o VPDB 2 2.5 3 3.5 -1 -0.5 0 0.5 1 1.5 -1 -0.5 0 0.5 1 ,,....--lr----,r-----,1 I I I I I I I I I I • •

• •

•

• •

•

• •

• • .. 4 • • • •

•

• • • • • • • • • • •• • •• • •• •• • • • • • • • • I ' .. . • ·l. '• • • • • • • • • •• • • • • • • • - ..

lr-��-+� --� - ! I I I I 2 2.5 3 3.5 1-0.5 0 0.5 1 1.5 -1 -0.5 0 0.5 1 bulk-carbonate 613C %o VPDB belemnite 6180o/oo VPDB Carbon and oxygen isotope record of the Middle to Upper Jurassic bulk carbonate and belemnite rostra from the Fig. 1. Stankowa Skala sections at Zaskale, Poland (Pieniny Klippen Belt, Carpathians). Outcrop stratigraphy afterA. WIERZBOWSKI (unpublished): 1-Bajocian, 2-Middle to Upper Oxfordian, 3- Upper Oxfordian to Lower Kimmeridgian, 4-Lower Kimmeridgian, Lowermost Upper Kimmeridgian, 6-Upper Kimmeridgian to 5- Lower Tithonian, 7 - Lower Tithonian. Ammonite zones: A - Transversarium-Bifurcatus, B - Bimammatum-Planula­ Silenum, C-Strombecki-Divisum, D - Acanthicum, F- Hybonotum. 20 qth International Congress on the Jurassic System - Abstracts

composition and Mg/Ca and Sr/Ca ratios Sample screeningforthe state ofpreservation of belemnite rostra; has been conducted using cathodoluminescence

• to trace secular changes in the carbonate microscopy and optical emission spectrometry. carbon isotope composition in order to Preliminary results of the study show:

reconstruct temporal variations in 613C • a slow decrease in 613C values of bulk values of dissolved inorganic carbon in carbonates duringthe Late Pliensbachian­ Jurassic oceans; Toarcian;

• to compare the obtained 613C curves • high Middle Oxfordian 613C values of bulk with the previously reported records of carbonates and calcite fossils correspond the isotope composition of carbonate to the global positive isotope excursion in carbon. carbonate carbon;

The sample set includes the stratigraphically • Late Jurassic belemnite 6180 values well-dated bulk carbonates and belemnite rostra ranging from -0.8 to 0.4 %oVPDB which from several outcrops in Polish, Slovakian, and implies palaeotemperatures of 13 ± 2 °C;

Ukrainian parts of the Pieniny Klippen Belt • seawater temperature increased for (PKB). PKB is a long narrow structure separating about 6°C between the Middle Oxfordian the Outer and Central Carpathians. and Late Kimmeridgian-Early Tithonian. 9th International Congress on the Jurassic System -Abstracts 21

Micropalaeontological study at the Oxfordian-Kimmeridgian boundary in Central Poland - a preliminary report

MARCIN BARSKI1 *, MARTA HODBOD2, BRONISI:.AW A. MATYJA1 & ANDRZEJ WIERZBOWSKI2

11nstitute of Geolog� University of Wa rsa"" PL 02-089 Wa rszawa, ul. iwirki i Wigury 93, Poland; E-mail: [email protected], [email protected] 2Polish Geological Institute-National Research Institute, PL 00-975 Wa rszawa, ul. Rakowiecka 4, Poland; E-mail: [email protected], andrzej. [email protected]

*Corresponding author

Recent studies of the sections in Central Poland and pollen grains as well as of organic-walled (Wielun Upland), rich in Submediterranean dinoflagellate cysts. This finding indicates that ammonites but yielding also Subboreal-Boreal formation of the cherts occurred very early on ammonites, supplemented markedly the in diagenesis which resulted in preservation correlation of the zonal schemes around the of organic matter that is completely absent Oxfordian-Kimmeridgian boundary. The lower in the surrounding limestone matrix. The boundary of the Kimmeridgian Stage of the most abundant taxa within the dinoflagellate standard (Subboreal) subdivision lies in the cyst assemblage include Sy stematophora stratigraphic interval of the Submediterranean areolata, Dingodinium tuberosum, Pareodinia succession ranging from the upper part of the ceratophora, Barbatacysta sp., ?Occisucysta Semiarmatum Subzone up to the Berrense balios, Cribroperidinium globatum, C. sp., Subzone of the Semiarmatum (= Hypselum) Glossodinium dimorphum, Cribroperidinium Zone and lowermost part of the Bimammatum granuligerum, and Leptodinium subti/e, which Zone, and thus close to the boundary of the strongly indicate a correlation with the Borealf Semiarmatum (Hypselum) Zone and the Subboreal uppermost Oxfordian - lowermost

Bimammatum Zone (MATYJA & WIERZBOWS .· Kimmeridgian, but a single recovery of 2014). Cribroperidinium? longicorne suggests even

The section at an abandoned quarry correlation with t e Lower Kimmeridgian (e.g., at Katarowa Hill near tobodno north of RIDING & THOMA� 992; GRADSTEIN et al. 2004; Cz�stochowa is promising for finding the level BARSKI et al. 2 00 s: fhe spores a ne l'lollen taxa are corresponding to the standard (Subboreal/ represented by Baculatisporites sp., Cy athidites Boreal) Oxfordian-Kimmeridgian boundary in sp., Concavisporites sp., Araucariacidites sp., cf. the Submediterranean succession. It shows a Cerebropollenites sp., and a rich undeterminable succession of bedded limestones which contain bisaccate pollen grain assemblage. (according to preliminary studies) ammonites Other palynological samples taken from of the Submediterranean Hypselum Zone cherts, however,are characterized by scarce and (subzone in older stratigraphic subdivisions) poorly preserved organic matter. They yielded a together with Boreal and Subboreal ones. The few non-age diagnostic terrestrial palynomorph co-oocurrence of ammonites belonging to taxa including cf. Ly copodiumsporites sp., different faunal provinces makes a correlation cf. Baculatisporites sp., cf. Cerebropollenites with the uppermost Oxfordian of the Boreal/ sp., cf. Cy athidites sp., cf. Leptolepidites sp., Subboreal primary standard section at Staffin and several bisaccate pollen grains. These Bay (Isle of Skye, Scotland) possible; the preliminary results, revealing the occurrence of younger deposits of the quarry, which should spores and pollen grains as well as of organic­ correspond to the lowermost Kimmeridgian, are walled dinoflagellate cysts in the cherts of the very poorly exposed. Organic matter recovered studied section, may be of great importance from a chert sample of a limestone bed of these for the stratigraphic interpretation of the younger deposits that cropped out for a short deposits and the reconstruction of the climatic distance consisted of well preserved spores changes in the area. New studies are planned 22 9th International Congress on the Jurassic System - Abstracts to fully characterize the section and to obtain BARSKI, M., MATYJA, B.A. & WIERZBOWSKI, A. 2005. Korelacja a uniform biostratigraphic interpretation of podzial6w amonitowych i dinocystowych przy granicy oksfordu i kimerydu na podstawie wiercen Bartoszyce the deposits at the Oxfordian-Kimmeridgian IG 1 i Kcynia IG 1. - Tomy Jurajskie 3: 87-96. boundary in relation to the proposed Global GRADSTEIN, F.M., 0GG, J.G. &SMITH, A.G. 2004. A geologic Stratotype Section and Point (GSSP) of the base time scale 2004. 589 pp., Cambridge University Press, of the Kimmeridgian at StaffinBay (Isle of Skye), Cambridge. MATYJA, B.A & WIERZBOWSKI, A. 2014. On the Oxfordian­ Scotland (MATYJA et al. 2006). Kimmeridgian (Upper Jurassic) boundary - current state of knowledge. 9th International Congress on the The study was financed by the National Science Centre Jurassic System, Jaipur. - Beringeria Special Issue 8: (grant 2012/05/B/ST 10/02121). 103-104. MATYJA, B.A., WIERZBOWSKI, A. & WRIGHT J.K. 2006. The References Sub-BorealfBoreal ammonite succession at the RIDING, J.B. & THOMAS, J.E. 1992. Dinoflagellate cysts of the Oxfordian/Kimmeridgian boundary at Flodigarry, Jurassic System. In: PowELL, A.J. (ed.), A stratigraphic Staffin bay (Isle of Skye), Scotland. - Transactions of index of dinoflagellate cysts: 7-57, Chapman Hall, the Royal Society of Edinburgh: Earth Sciences 96: & London. 387-405. 9rh International Congress on the Jurassic System - Abstracts 23

Palaeoecological significance of the Callovian-Oxfordian trace fossils of Gangeshwar Dome, southeast of Bhuj, Mainland Kachchh, India

NISHITH Y. BHATT1 * & SATISH ). PATEL2

1Department of Geology, M. G. Science Institute, Ahmedabad - 380 009, Gujarat, India; E-mail: [email protected] 2Department of Geology, M. S. University of Baroda, Va dodara - 390 002, Gujarat, India; E-mail: sj [email protected]

*Corresponding author

Kachchh is a peri-cratonic embayed basin, of herringbone cross-bedded, fine- to medium­ extending from the southwest part of Thar grained sandstone, marking the upper boundary Desert and Nagar-Parkar in the north to of Member 11. Member Ill mainly contains Saurashtra in the south, occupying a graben shales with thin bands of bioclastic limestones, (BISWAS 1991). The Gangeshwar Dome lies bioclastic intraformational conglomerates and between N 23°12'05" to 24°10'38" latitudes bioclastic sandstones. Member IV consists of and E 69°41'15" to 69°45'32" longitude and intercalations of shales and oolitic limestone; is situated southeast of Bhuj in the Khatrod its uppermost part comprises hard prominent (Charwar) hill range, south of the Katrol oolitic limestones (Dhosa Oolite) forming a Hill Fault (KHF) on Mainland Kachchh. The distinct marker horizon which separates the Gangeshwar Dome forms a big inlier and jumara Formation from the jhuran Formation the core part comprises rocks of the Jun;tara (BISWAS 1977). Formation (BISWAS 1977). ranging in age from The )umara Formation comprises a 247-m­ Callovian to Oxfordian (BISWAS 1977; BHALLA thick succession of shallow marine deposits of & ABBAS 1978). The shallow marine deposits clastic and non-clastic sediments divided into of the dome contain diverse groups of well­ seven lithofacies based on distinct lithologic preserved trace fossils which offeran excellent features, composition, textures and structures. opportunity to understand the palaeoecological These include Laminate Shale-Siltstone (LSS) parameters and depositional history of the late facies, Sheet Sandstone (SS) facies, Herringbone Middle jurassic time slice. Sandstone (HS) facies, Bivalve Sandstone (BS) BISWAS (1977) classified litho- fa cies, Intraformational Conglomerate (IC) stratigraphically the Mesozoic sediments in fa cies, Bioclastic Limestone (BL) facies, and four units - the Jhurio, jumara, Jhuran, and Bhuj Oolitic Limestone (OL) fa cies. fo rmations. The rocks of the jumara Formation Rocks of the jumara Formation are highly are classified into fo ur informal members I to bioturbated and contain abundant identifiable IV in ascending order (BISWAS 1977, 1993). trace fossils. In total 31 ichnospecies of 25 The formation is well developed and best ichnogenera were identified but indistinct exposed in the Gangeshwar Dome, except the fo rms also occur. The highly diverse trace fo ssils lowermost part of Member I, which is only reveal a wide range of animal behaviour and partly exposed. Member I consists of shale can be interpreted in terms of ecology, strategy with bands of fine-grained greyish to dirty of adaptation and biological parameters, which yellow siltstone and sandstone. The siltstone can directly be related to physical aspects of the and sandstone contain small bivalves and palaeoenvironments. The ichnofauna identified become cherty towards the upper part. The in the study area are Arenicolites carbonarius, uppermost boundary of the Member I is fixed Bifungites isp., Bolonia lata, Chondrites isp., above a dark grey carbonaceous shale band. Coch/ichnus kochi, Didymaulichnus lyel/i, The lower part of Member 11 is characterised Diplocraterion paral/elum, Granularia isp., by thick sandstones, whose lower part is Gy rochorte comosa, Helminthopsis hieroglyphica, mainly massive while its upper part consists Isopodichnus problematicus, Laevicyclus isp., 24 9th International Congress on the Jurassic System - Abstracts

Monocraterion tentaculatum, Muensteria fossils include Planolites, Helminthopsis, isp., Ophiomorpha nodosa, Palaeophycus Protopalaeodictyon, and Bolonia. It is found sulcatus, Phycodes circinatum, P. palmatum, in the SS lithofacies of Member I. The ichno­ P. pedum, P. isp., Planolites annularis, P. assemblage represents predominantly the isp., Protopalaeodictyon incompositum, activity of vagile deposit-feeders where Rhizocorallium irregulare,R.jenense,Scolicia isp., structures are produced within the sediments. Skolithos linearis, Thalassinoides paradoxicus, T. The assemblage indicates low energy conditions isp., Tisoa siphonalis, and Zoophycus brianteus. with low rates of sedimentation in stable and Trace fossils occurring in particular horizons slowly accreting substrates on a well oxygenated are grouped into ichno-assemblages and named middle and lower shoreface zone. after the dominant ichnogenus. These ichno­ The Ophiomorpha ichno-assemblage is assemblages reflects the energy conditions, represented only by Ophiomorpha nodosa. It water depth, nutrients, substrate and bottom occurs in LSS and SS lithofacies of Member I and water oxygenation. Ill. The ichnoassemblage indicates moderate The Chondrites ichno-assemblage is or instantaneously high sediment influx in represented by Chondrites isp. Associated moderate to low energy conditions and shifting trace fossils are Planolites and Zoophycus. It sandy substrates mainly in foreshore to upper occurs in LSS lithofacies in Member Ill and OL and middle shoreface environments. lithofacies in Member IV.The ichno-assemblage The Rhizocorallium ichno-assemblage indicates low energy and calm water condition mainly consists of R. jenense and R. irregulare within oxygen-depleted fine-grained soft and with Laevicyclus, Palaeophycus, Phycodes, thixotropic sediments. It also signifies protected Planolites, Granularia, and Chondrites in shoreface environment. It suggests deposit­ LSS lithofacies of Member I, Ill and IV. This feeding behaviour of the animals. assemblage is characterized by shallow­ The Diplocraterion ichno-assemblage is burrowing deposit-feeders, found in fine­ characterised by Diplocraterion parallelum. to medium-grained sandstone-siltstone Associated trace fossils are Diplocraterion, alternations. It is indicative of a very low rate Laevicyclus, Bifungites, Ophiomorpha, of deposition in less protected, low energy, Skolithos, Planolites, Palaeophycus, Tisoa, and middle to lower shoreface environments with Monocraterion. The ichno-assemblage occurs intermittent currents sweeping the sea floor. in SS lithofacies of Member I, 11 and Ill and HS The Skolithos ichno-assemblage is depicted lithofacies of Member 11. It chiefly represents by Skolithos linearis. Associated trace fossils structures of suspension-feeders produced are Arenicolites, Diplocraterion, Monocraterion, at the sediment-water interface reflecting Ophiomorpha, Tisoa, Palaeophycus, and high energy conditions, shifting substrates, Planolites in SS lithofacies of Member 11 and Ill. frequent physical reworking, and high rates of The ichno-assemblage chiefly represents the sedimentation. It denotes lower fo reshore to activity of suspension-feeders at the sediment­ upper shoreface environments. water interface. High-energy hydrodynamic The Gy rochorte ichno-assemblage is settings or storm-wave influence and shifting characterized by Gy rochorte comosa. Other substrates subject to abrupt erosion and trace fossils are Bolonia, Didymaulichnus, deposition, which are exploited by opportunistic /sopodichnus, Cochlichnus, Planolites, and animals generally populating foreshore and Scolicia. The ichno-assemblage is observed in upper shoreface environments, are indicated. the LSS and SS lithofacies of members I and Ill. The Thalassinoides ichno-assemblage It represents crawling activity produced at the consists of T. paradoxicus and T. isp. Associated sediment-water interface in upper and middle trace fossils are Phycodes, Rhizocorallium, shoreface environments. The ichno-assemblage Granularia, Planolites etc. in SS and IC of generally shows a high degree of bioturbation Member I, 11 and Ill. The ichno-assemblage is indicating relatively low energy, slow usually prevailing in amalgamated sandstones sedimentation, and little physical reworking. and intraformational conglomerate fades. The Muensteria ichno-assemblage is The traces are large, semi-permanent mainly exemplified by Muensteria isp. Other trace horizontal tunnel systems suggesting a deposit- 9th International Congress on the Jurassic System - Abstracts 25 feeding behaviour and display a very low assemblage indicates fluctuations in bottom­ diversity, indicating extremely quiet water water oxygenation, while the Zoophycus conditions. Because of the low energy level, ichno-assemblage had typically exploited less abrupt shifting sediments and fluctuating the calm-water niche in offshore regions. temperature and salinity the bioturbation These ichno-assemblages recur throughout structures are mainly characterised by feeding the succession and belong to SEILACHER's and grazing traces. Overall the ichno-assemblage (196 7) archetypical ichnofacies Skolithos and suggests upper to lower shoreface condition Cruziana ichnofacies, which relate to energy with relatively low energy conditions. gradients, substrate stability, water depth, The Zoophycus ichno-assemblage comprises and feeding mode of invertebrate organisms. chieflyZ. brianteus. Associated trace fossils are Sedimentological and ichnological data suggest Chondrites etc. in OL lithofacies of Member fluctuating environmental conditions from the I'V. BROMLEY (1990) considered Zoophycus upper shoreface to the offshore zone during as produced by an opportunist, appearing deposition of the Jurassic sediments of the together with Chondrites in low resource, Gangeshwar Dome. inhospitable, oxygen-depleted environments. Further,he considered the ichno-assemblage as References BHALLA, S.N. ABBAS, S.M. 1978. Jurassic foraminifera representing deposit-feeding structures, which & comprise the deepest tier structure. According from Kutch, India. - Micropaleontology 24: 160-209. BISWAS, S.K. 1977. Mesozoic rock-stratigraphy of Kutch, to PATEL et al (2009) the sediment input Gujarat. - Quarterly Journal of the Geological, Mining remained fa irly low and depth did not reach and Metallurgical Society of India 49: 1-52. the storm wave base so that the sediments BISWAS, S.K. 1991. Stratigraphy and sedimentary evolution were thoroughly bioturbated by the Zoophycus of the Mesozoic basin of Kutch, Western India. In: Tan don, S.K., Pant, C.C. Cusshyap, S.M. ( eds.), & producer. These indicate low energy and Proceeding of Seminar on Sedimentary Basins of India, probably comparatively deep conditions where Nainital: 74-103, Gyanodaya Prakashan, Nainital. the rate of sedimentation is· rather slow. BISWAS, S.K. 1993. Geology of Kutch: 52-98. K. D. Malaviya The opportunistic Diplocraterion and Institute of Petroleum Exploration, Dehradun. Skolithos ichno-assemblages show a high BROMLEY, R.G. 1990. Trace Fossils. Biology and Ta phonomy. - Special Topics in Palaeontology: 1-280, Unwin diversity and typically consist of horizontal Hyman. ichnospecies, which mark a gradient from PATEL, S.J., DESAI, B.G. SHUKLA, R. 2009. Paleoecological & foreshore to near-shoreface conditions. The significance of the trace fossils of Dhosa Oolite Gy rochorte, Rhizocorallium, Muensteria, and Member (Jumara Formation), Jhura Dome, Mainland Kachchh, Western India. - Journal of the Geological Thalassinoides ichno-assemblages indicate Society of India 74: 601-614. typicallya lower energy zone of the shoreface­ SEILACHER, A. 1967. Bathymetry of trace fo ssils. - Marine offshore region. The Chondrites ichno- Geology 5: 413-428. 26 9th International Congress on the Jurassic System - Abstracts

Jurassic basins of India: Tectonic set up and sediment fill

S. K. BISWAS

E-mail: sanjibkbiswas2001 @yahoo.co.in

In India Jurassic rocks are present only in a deltaic sediments (Pariwar, Habur, and Goru few peri-cratonic basins and in the Central fo rmations) prograded over the Late Jurassic Himalayan orogenic belt. The maximum interval sediments (Baisakhi and Bhadasar formations). of Jurassic sedimentary succession occurs in Drilled well data indicate the continuation of the western peri-cratonic basins of Jaisalmer in the Jurassic deposits westward in the Indus Rajasthan and Kutch in Gujarat. Jurassic rocks foreland with progressive thickening below the are conspicuously absent in Late Paleozoic­ Tertiary formations. Early Cretaceous intra-cratonic Gondwana Rifting of the Kutch Basin in the southern basins excepting the Kotah Limestone (?Early/ part of the Indus Shelf started in Late Triassic Middle Jurassic) of the Pranhita-Godavari or Early Jurassic when the western part of the Basin. In the eastern pericratonic basins only Indian plate was undergoing crustal extension continental Late Jurassic rocks are present in due to pre-break up crustal distension in the Krishna-Godavari and Kaveri-Palar basins. Eastern Gondwanaland. This prolonged crustal Jurassic rocks of Tethyan origin in the central distension continued till the Late Cretaceous Himalayan orogenic belt were caught up in the as India with Madagascar first separated from thrust sheets. In this paper I present a brief Africa, followed by separation of Madagascar overview on the tectonic set up, stratigraphy, and Seychelles during the Late Cretaceous. Rift­ and sediment dynamics of the Jurassic deposits fill sedimentation in Kutch continued till then of the Rajasthan and Kutch basins. in cycles of transgression-regression coeval The maximum Jurassic interval (Lias to with the Jaisalmer depositional cycles. Marine Tithonian) is exposed in the Jaisalmer Basin transgression over the pericratonic embayment of Rajasthan. In Kutch the Middle (Bajocian) of Kutch started in Early Mid-Jurassic through to Late Jurassic (Tithonian) succession is well the narrow channel that opened up between developed and extensively exposed. Deep Somalia of the African plate and the Pakistan­ borehole data show the presence of (?)Aalenian­ Kutch-Saurashtra part of the Greater Indian Bajocian sediments above the Precambrian plate, due to pre-break up fracturing during basement. Bajocian-Bathonian time (167 Ma).The initial The Jaisalmer Basin is a passive margin transgression started during the early riftstage shelf basin, whereas Kutch is a rifted basin at in the early Mid-Jurassic and continued through the western continental margin of India. Both the synrift stage in the Middle Jurassic till the basins are integral parts of the Indus shelf and early post-rift stage during Late Jurassic-Early received sediments from the transgressive Cretaceous time. The Kaladongar, Goradongar, Neo-Tethys during Jurassic times. Sediments Khadir, and Jhurio fo rmations were deposited in the Jaisalmer Basin were deposited in during the early synrift stage in Aalenian­ open marine shallow shelf environments. Bathonian time. The Jumara and Washtawa Sedimentation started with Late Triassic fo rmations were deposited during the synrift marine transgression (Bhuana Formation) over climax stage in Callovian-Early Oxfordian Precambrian basement covered by patches of time, while the Jhuran and Wagad sandstones Permo-Carboniferous deposits (Bap/Badhaura were deposited during the late synrift stage formations, mostly fluvio-glacial boulder (Kimmeridgian-Tithonian). During post­ conglomerates and sandstones ). Marine rift stage in Neocomian-Albian time marine sedimentation continued till the Late Jurassic Jurassic sediments were unconformably in repeated transgressive-regressive cycles. covered by prograding delta sediments of Jurassic marine sedimentation was terminated the Bhuj Formation. Maximum flooding took during an Early Cretaceous regression when place during synrift climax in Late Callovian 9th International Congress on the Jurassic System - Abstracts 27

- Early Oxfordian time (Jumara Formation). graben, Banni half-graben, and Rann graben are The maximum flooding surface is marked by the three different domains of sedimentation a conspicuous green oolitic limestone band giving rise to different successions of described as Dhosa Oolite Member on top of fo rmations. This resulted in the identifications the Jumara Formation. Sedimentation in the of three main groups of fo rmations in the Kutch rifted Kutch Basin was more complex than in lithostratigraphy namely, Mainland Group, the Jurassic shelfal basin of Jaisalmer. A rift Pachchham Group and Eastern Kutch Group. basin is differentiated into intra-basin highs These groups are well correlated by marker and lows: horst-grabens and tilted horst-half units which include biostratigraphic marker grabens. Each half-grabenfgraben is a sub­ beds also. This made it possible to work out basin in the rift profile. Such differentiation a chronostratigraphic classification which is into separate domains of sedimentation is under fi nalization. Drilled well data indicate the responsible fo r variation in lithofacies and continuous occurrence of the Jurassic sediments lithologic associations. Further, variation in beneath the Deccan Trap and Tertiary deposits relative sea levels during sedimentation causes in Southern Kutch and beyond into the offshore submergence/ emergence of intra-basinal highs shelf basin. In Kutch, the Jurassic rocks are during sediment accommodation affecting the intensively intruded by basic igneous rocks as lithofacies. In Kutch, the Gulf of Kutch half- has been noted in other major riftbasins. 28 9th International Congress on the Jurassic System - Abstracts

Early Jurassic (SinemurianfPiiensbachian) ammonites of the Central Apennines (Monte di Cetona and Acquasparta, Italy)

1 2 }OACHIM 8LAU & CHRISTIAN MEISTER

1/nstitut fu r Geowissenschaften Goethe-Universitiit, 60438 Frankfu rt am Main, Germany; E-mail: ][email protected] 2Natural History Museum of Geneva, Department of Geology and Paleontology, CH-1211 Geneva, Switzerland; E-mail: [email protected]

The Central Apennines (Italy) are a classical can be distinguished covering a time interval and historical region for Tethyan Liassic from the Davoei up to the Margaritatus (p.p.) ammonites, especially Monte di Cetona and Zone. Since both sections overlap in terms of Acquasparta. The fauna collected in several biochronology a synthetic biostratigraphic little quarries arround the area of San Casciano scheme can be constructed which ranges from the dei Bagni was first studied in a series of papers Upper Sinemurian to the Upper Pliensbachian. by FUCINI (1901-05). Since most of FUCINI's A worldwide (Euroboreal, Tethyan, and East material had not been collected by horizons, Pacific Domains) comparison and correlations FISCHER (1971, 1972) collected two quarries of the Lower - Upper Pliensbachian boundary (Murate and Acquasparta sections) bed-by­ are proposed (Fig. 1). bed. The revision of these sections allows to precise the systematics and the biostratigraphy References BLAU, J. MEISTER, C. 2011. Resolving the Monte di of this area. For Murate, a sequence of six faunal & Cetona biostratigraphical enigma - a revision of R. horizons indicating Obtusum, Jamesoni, Ibex, Fischer's Sinemurian and Pliensbachian (Liassic) and Davoei zones is established. This sequence ammonite collection from Central Appenines is well comparable to already published data (Tuscany, Italy). - Neues Jahrbuch fur Geologie und from other Tethyan localities. With our revision Palaontologie, Abhandlungen, DOl 10.1127/0077- 7749/2011/0151. the systematic and biostratigraphic problems MEIST:ER, C. 2010. Worldwide ammonite correlation at the resulting from FISCHER's studies are solved. In Pliensbachian Stage and Substage boundaries (Lower the Acquasparta section five faunal horizons Jurassic). - Stratigraphy 7: 83-101.

SOUTH AMERICA NW EUROPE WESTERN TETHYS

Bioevents potential (= biohorizons) Biohorizons Zonulas

·c: ·c:en � ! F. leptodiscus

Biohorizons present in Monte di Cetona and Acquasparta around the Lower and Upper Pliensbachian boundary, Fig. 1. and correlations with the zonations of Western Tethys, NW Europe, and the Americas (MEISTER 2010). 9th International Congress on the Jurassic System - Abstracts 29

Life in a Late Jurassic Subboreal Sea and on its coast: a new taphonomic window of exceptionally preservedfa una at Owadow-Brzezinki (Central Poland)

Bt.AZEJ Bt.AZEJOWSKI1 *, BRONISt.AWA. MATYJA2, ANDRZEJ WIERZBOWSKI3 & HUBERT WIERZBOWSKI4

1Institute of Paleobiology, Polish Academy of Sciences, ul. Twarda 51/55, PL 00-818 Wa rsa� Poland; E-mail: [email protected] 2Institute of Geology, Universityof Wa rsa� ul. iwirki i Wig ury93, PL 02-089 Wa rsa� Poland; E-mail: [email protected] 3 Polish Geological Institute - National Research Institute, ul. Rakowiecka 4, PL 00-975 Wa rsaw; E-mail: andrzej. [email protected] 4Institute of Geological Sciences, Polish Academy of Sciences, ul. Twarda 51/55, PL 00-818 Wa rszawa, Poland; E-mail: [email protected]

*Corresponding author

The recently discovered paleontological site Zone), Nusplingen (uppermost Kimmeridgian, of the Slawno limestones in the Owad6w­ Beckeri Zone) and at newly discovered locality Brzezinki Quarry, about 19 km southeast of (Owad6w-Brzezinki Quarry, Zarajskensis Tomasz6w Mazowiecki (central Poland), has Subzone of the Scythicus Zone), under closely yielded unusually well preserved fossils of related environmental conditions. latest Jurassic terrestrial and marine organisms. The fossils identified in all localities indicate At the moment, the Owad6w-Brzezinki quarry a similar geological age and environment. Both is the only place in extra-Carpathian Poland marine and terrestrial organisms are very similar where the Scythicus Zone (Middle Volgian) and allow comparative paleontological studies strata corresponding to some lower parts �f at a previously unattainable level of taxonomic the Upper Tithonian are available fo r study (tl, resolution. The recent identification of a new classic locality Brzost6wka is now within the species of dragonfl ' (family Eumorbaeschnidae) Tomasz6w Mazowiecki town limits; quarries in and grasshopper fa mily Prophalangopsidae), Pomerania are flooded). The exposed carbonate families previous known from the Solnhofen succession belongs to the Kcynia Formation area, is an exat�.ple. Clearly, �-t,e Owad6w­ (KUTEK 1994), and can be divided into the Brzezinki Quarry may be regarded as a new following four successive units (Fig. 1 ) . 'taphonomic window' into the living world of the The lowermost part of the unit (Ill) is highly latest Jurassic and it represents the first near­ fossiliferous. Numerous specimens ofhorseshoe contemporary palaeontological 'supplement' to crabs (Limulus sp. n. and Crenatolimulus sp. n.) the previously known Fossil-Lagerstiitten. The were found in association with an enormously small palaeochronological distance (S-7 Ma) rich assemblage of the bivalves Corbulomima separating all central European Late Jurassic obscura and Mesosacce/la sp., remains of various localities may enable us to trace lineages, with fishes and marine reptiles, rare ammonites, different stages of evolutionary advancement crustaceans, land insects (dragonflies, beetles, recorded by fossils from differentloc ations. grasshoppers), and pterosaurs. The uniqueness The study was supported by the Polish National Science of this new locality lies in its very close Centre (grant no.2012/07/B /ST10/04175). stratigraphic relationship to the famous Fossil­ References Lagerstiitteloc alities Solnhofenand Nussplingen KIN, A., GRUSZCZYNSKI, M., MARTILL, D., MARSHALL J. Bt.AZEJOWSKI B. 2013. Palaeoenvironment and in southern Germany, with approximately 5 & and 7 Ma, respectively separating them (KIN taphonomy of a Late Jurassic (Late Tithonian) Lagerstatte from central Poland. - Lethaia 46: 71-81. et al. 2013). Marine and terrestrial organisms KuTEK, J. 1994. The Scythicus Zone (Middle Volgian) lived and died during the Late Jurassic at in Poland: its ammonites and biostratigraphic Solnhofen (Lower Tithonian, Hybonotum subdivisions. - Acta Geologica Polonica 44: 1-33. 30 9thInternational Congress on the Jurassic System - Abstracts

Fig. 1. A. Location of the Owad6w-Brzezinki Quarry in Poland. B. Stratigraphic units: Unit I is composed of indistinctly laminated massive fine-grained limestone (total thickness -6.6 m) with Deltoideum delta, which fo rms a few beds 40-80 cm in thickness. The overlying c. 2-m-thick unit is represented by thinly bedded, fine-grained limestones with occasional 11 distinct parallel lamination and mass occurrence of calcareous polychaete tubes in one horizon. Unit Ill, c. 15.6 m thick, is highly fo ssiliferous and has yielded the fo ssils that are the subject of proposed research. Unit IV, c. 2.3 m thick, the top not being exposed, is developed as organo-detrital limestone rich in the oyster Nanogyra, bryozoans, and serpulids, the latter oftenfo rming small bioherms. In general, units I, and Ill probably represent a transition from an offshore tonearshore, 11, perhaps lagoonal, setting, whereas Unit IV bears evidence of a return to more open marir.1econditions. Below the Kcynia Fm. yellowish marls and marly clays of the Paluki Formation occur. ,

Fig. 2. Part and counterpart of an articulated horseshoe crab exoskeleton - Crenatolimulus sp. 9th International Congress on the Jurassic System - Abstracts 31

Geodynamic events and the drowning history of a Jurassic carbonate platform: a case study from the Aures area (NE Algeria)

EL HADJ YOUCEF BRAHIM1 * & MOHAMED CHADI2

1Universityof Batna BP 25, Merouana-Batna 05013, Algeria; E-mail: [email protected] 2Normal Superior School, Zo uaghi Faculty, Constantine zip: 25000, Algeria

*Corresponding author

This study focuses on an area located at the stratigraphic interpretation and correlation southern fringe ofthe Alpine Belt external zones. of the Jurassic succession of the study area, The objective of this work is to reconstruct the based on a few cross-sections, have allowed drowning history of the Jurassic carbonate to highlight the platform physiography during platform and to discuss its relationship with the this geological period and to recognise three geodynamic evolution of the southern Tethyan stratigraphic units. margin. The identification and interpretation The synthesis of bio-sedimentological data of drowning events of platforms can help reveals diversified fa cies, involving various significantly to reconstruct the depositional, depositional environments ranging from tectonic and eustatic history of these supratidal to deep pelagic. These facies have platforms. evolved on the subsiding carbonate ramp. The The drowning of carbonate platforms was ramp experienced a drowning phase (Toarcian) the subject of stratigraphic and sedimentological and filling phases (Tithonian, Berriasian), research in different places of our planet ?nd related to eustatic sea-level changes and at different periods of the Phanerozoic. The regional tectonics. 32 9thInternational Congress on the Jurassic System - Abstracts

The Upper Bajocian Cranocephalites-succession in East Greenland: achieving the highest possible biostratigraphic resolution

}OHN H. CALLOMON, PETER ALSEN1 * & FINN SURLYK2

1Geolog ical Survey of Denmark and Greenland (GEUS), ester Vo ldgade 10, DK-1350 Copenhagen K, Denmark; E-mail: PA L@GEUS. DK 2Department of Geosciences and Natural Resource Management, University of Copenhagen, ester Vo ldgade 10, Dk-1350 Copenhagen K, Denmark; E-mail:[email protected]

*Corresponding author

Professor }OHN H. CALLOMON died April recognized (CALLOMON 1993) to 34 today. 1st 2010. The last two decades before his The zonal stratigraphy ofthe Cranocephalites death he had been working on establishing beds up to 1993 was encompassed bythreezones, the faunal succession of the Middle Jurassic the Borealis, Indistinctus and Pompeckji zones, Cranocephalites beds in East Greenland. He based on the then recognized succession of just leftan unfinished manuscript, which his family eight fa unal horizons. Of these, five were in an entrusted the co-authors to complete. We here undifferentiated Pompeckji Zone. These zones present the main results of CALLOMONS work form part of the secondary standard zonation - post-humously- and intend to publish it in a fo r the Boreal Province of the biogeographic monograph-format in the Geological Survey of Boreal Realm of the Middle Jurassic and were Denmark and Greenland Bulletin. classed into the so-called Boreal Bathonian In compiling the faunal succession of the Stage (CALLOMON 1959, 1993). With the existing Middle Jurassic ammonite zonation refinement available today, it is possible and (CALLOMON 1993), the greatest difficulty lay in useful to subdivide the Pompeckji Zone with the lower part, in the Indistinctus-Pompeckj i its 23 faunal horizons into four subzones. They zones of the Cranocephalites beds. The refl�ct four successive basic morphologies of Arctocephalites and Arcticoceras beds appeared Cranocephalites that should be recognizable to be widely represented in Jameson Land and more widely, making possible correlations - and elsewhere in the Arctic, and their ammonite hence age determinations - at subzonal level of faunas well sampled in the collections from precision even when assignment to individual Hurry Fjord made by A. ROSENKRANTZ in horizons is not possible. 1926-7 and H. ALDINGER and others in later The evolutionary tempo of the years. What was known of the Cranocephalites Cranocephalites lineage allows us to follow the beds was, in contrast, largely based on a microevolutionoftheammonitesataleveloftime­ single collection made by T. HARRIS during an resolution with few biostratigraphic rivals in the excursion in 1927 up the valley of Ugleelv, west geological record. If the 34 transients represent of inner Hurry Fjord, to its headwaters around evolution over the duration of the Late Bajocian, Katedralen (RosENKRANTZ 1934). This is also whose rocks make up the three standard zones the type area of the oldest named species of this of the European primary scale (Subfurcatum - genus, Cranocephalites pompeckji, brought back Parkinsoni zones), the time-resolution achieved in 1900 (MADSEN 1904). here is close to the achievable limit, set by the Opportunities arose in 1994 and 1996 to ability to recognize morphological changes in revisit the area of Ugleelv and to concentrate successive assemblages. Hence, on this time­ on the ammonite biostratigraphy of the scale, evolution appears to be continuous. Yet Cranocephalites beds. The results obtained the observed record in the rocks continues to exceeded all expectations. Some 750 ammonites be highly discontinuous. This punctuation of were collected bed by bed from 17 sections. the record is determined not by punctuation The number of faunal horizons that could be - discontinuities in the sense of ELDREDGE & distinguished grew from the nine previously GOULD 1972) - in the phyletic development of 9th International Congress on the Jurassic System - Abstracts 33 the ammonoid genome but by the environment species of ammonites from the Inferior Oolite of in which the ammonites lived and died. The Dorset. - Quarterly Journal of the Geological Society of London 37: 588-608. sedimentary record is incomplete, both CALLOMON, J.H. 1959. The ammonite zones of the Middle vertically and horizontally. The present account Jurassic beds of East Greenland. - Geological Magazine shown by the ammonites has revealed the 96: 505-13. existence of non-sequences in the Middle CALLOMON, J.H. 1993: The ammonite succession in the Jurassic sediments of Jameson Land whose Middle Jurassic of East Greenland. - Bulletin of the Geological Society of Denmark 40: 83-113. presence in the rocks is reflected in nothing ELDREDGE, N. GOULD, S.J. 1972. Punctuated equilibria: & more than a simple bed parting. As noted by an alternative to phyletic gradualism. In SCHOPF, BucKMANN (1881), the more the complete the T.J.M (ed.), Models in Paleobiology: 82-115, Freeman biostratigraphical record becomes, the less Cooper, San Francisco. MADSEN, V. 1904. On Jurassic fo ssils from East Greenland. complete the lithostratigraphic record turns - Meddelelser om Gnmland 29: 157-211. out to be. RosENKRANTZ, A. 1934. The Lower Jurassic rocks of East Greenland. Part 1. - Meddelelser om Grfimland 110 References (1): 1-122. BucKMANN, S.S. 1881. A descriptive catalogue of some 34 9th International Congress on the Jurassic System - Abstracts

The Early Toarcian Oceanic Anoxic Event in Western North America: Testing regional vs. global controlling mechanisms

ANDREW H. CARUTHERS1 *, DARREN R. GROCKE2, PAUL L. SMITH\ BEN C. GILL3, SARAH ). PORTER1 & PENGFEI Hou1

1Department of Earth, Ocean and Atmospheric Sciences, University of British Columbia, Va ncouver V6T 1Z4, Canada; E-mail: caruthers. [email protected], psmith@eos. ubc.ca, [email protected], [email protected] 2Department of Earth Sciences, Durham University, Sciences Laboratories, Durham DHl 3LE, UK; E-mail: [email protected]. uk 3Department of Geosciences, Virginia Te ch University, Blacksburg 24061, USA; E-mail: [email protected]

*Corresponding author

Currently it is understood that volcanogenic (McARTHUR et al. 2008). Black shale deposition outgassing of C0 during the Karoo-Ferrar and coeval geochemical perturbations reflect 2 igneous province eruption initiated a period of eux1n1c conditions resulting from local prolonged global warming and mass extinction upwelling together with increased freshwater during the Pliensbachian-Toarcian interval input that caused a salinity driven pycnocline to of the Early jurassic (PALFY & SMITH 2000). develop (McARTHUR et al. 2008 and references Warmer water temperatures are thought to therein). It is possible that both hypotheses are have caused a series of environmental changes applicable and that simultaneous regional and during the Early Toarcian that include methane global controls reinforced each other during hydrate release (HESSELBO et al. 2000) and this event. a period of global marine anoxia dubbed the In our poster we report preliminary Toarcian Oceanic Anoxic Event or T-OAE geochemical data frpm the Sonomia Basin of (JENKYNS 1988; 2010 and references therein). N ev.ada(USA) in order to assess whether anoxic This is evidenced in the Tethys Ocean area by water mass conditions developed in a restricted deposition of organic-rich black shale and basin on the eastern edge of the northeast pal eo­ coeval perturbations in a variety of geochemical Pacific Ocean that may have been analogous to systems that include carbon (JENKYNS 1988; the European basins. Preliminary results are 2010; HESSELBO et al. 2000), nitrogen (jENKYNS also compared with geochemical data from et al. 2001), manganese (SABATINO et al. the Haida Gwaii region of British Columbia, 2011), sulfur (McARTHUR et al. 2008; GILL Canada, which was located in an open paleo­ et al. 2011), and molybdenum (PEARCE et al. Pacific Ocean setting during the Early Toarcian 2008; McARTHUR et al. 2008). It is believed and shows no evidence of the T-OAE. Results that disruption of these geochemical systems is generated in our study will therefore test the evidence for the rapid injection and oxidation controlling mechanisms for the T-OAE and of methane which reduced oceanic 02 levels shed light on the debated 'global' vs. 'restricted and increased organic carbon burial leading basin' models for marine anoxia. to marine euxinic conditions on a global scale (JENKYNS et al. 2010 and references therein). References GILL, B.C., LYONS, T.W., }ENKYNS, H.C. 2011. A global However, recent studies have questioned & perturbation to the sulfur cycle during the Toarcian the timing, evidence for, and geographic extent Oceanic Anoxic Event. - Earth and Planetary Science of the T-OAE (WIGNALL et al. 2005; VAN DE Letters 312: 484-496. SCHOOTBRUGGE et al. 2005; McARTHUR et al. HESSELBO, S.P., GROCKE, D.R., jENKYNS, H.C., BJERRUM, C.J., FARRIMOND, P., M ORGANS BELL, H.S. GREEN, O.R. 2000. 2008 and references therein). An alternative, & Massive dissociation of gas hydrate during a Jurassic regional hypothesis invokes local controls oceanic anoxic event. - Nature 406: 392-395. within several silled basins developed across }ENKYNS, H.C. 1988. The Early Toarcian (Jurassic) event: the epicontinental seaway of NW Europe stratigraphy, sedimentary and geochemical evidence. 9th International Congress on the Jurassic System - Abstracts 35

-American Journal of Science 288: 101-151. during the Early Jurassic. - Geology 36: 231-234. doi: JENKYNS, H.C. 2010. Geochemistry of oceanic anoxic events. 10.1130/G24446A.l. - Geochemistry, Geophysics, Geosystems 11: Q03004, SABATINO, N., NERI, R., BELLANCA, A., JENKYNS, H.C., doi:10.1029/2009GC002788. MASETTI, D. SCOPELLITI, G. 2011. Petrography and & JENKYNS, H.C., GROCKE, D.R. HESSELBO, S.P. 2001. Nitrogen high-resolution geochemical records of Lower Jurassic & isotope evidence for water mass denitrification during manganese-rich deposits from Monte Mangart, the early Toarcian (Jurassic) ocean anoxic event. - Julian Alps. - Palaeogeography, Palaeoclimatology, Paleoceanography 16: 593-603. Palaeoecology 299: 97-109. McARTHUR, J.M., ALGEO, T.J., VAN DE SCHOOTBRUGGE, B., LI, VAN DE SCHOOTBRUGGE, B., BAILEY, T. R., ROSENTHAL, Y., KATZ, Q. HowARTH, R.J. 2008. Basinal restriction, black M.E., WRIGHT, J.D., MILLER, K.G., FEIST-BURKHARDT, S. & & shales, Re-Os dating, and the Early Toarcian (Jurassic) FALOWSKI, P. 2005. Early Jurassic climate change and oceanic anoxic event. - Paleoceanography, 23: 1-22. the radiation of organic-walled phytoplankton in the PALFY, J. SMITH, P. L. 2000. Synchrony between Early Tethys Ocean. - Paleobiology 31: 73-97. & Jurassic extinction, oceanic anoxic event, and the WIGNALL, P. B., NEWTON, R.J. LITTLE, C.T.S. 2005. The & Karoo-Ferrar fl ood basalt volcanism. - Geology 28: timing of paleoenvironmental change and cause-and­ 747-750. effect relationships during the Early Jurassic mass PEARCE, C.R., COHEN, AS., CoE, AL. BURTON, K.W. 2008. extinction Europe. - American Journal of Science 305: & Molybdenum isotope evidence for global ocean 1014-1032. anoxia coupled with perturbations to the carbon cycle 36 9th International Congress on the Jurassic System - Abstracts

The impacts of palaeoenvironmental change on benthic and pelagic fauna during the Toarcian Oceanic Anoxic Event

BRYONY A. (ASWELL 1 * & ANGELA L. COE2

1School of Environmental Sciences, University of Liverpool, Nicholson Building, Brownlow Street, Liverpool, L69 3GP, UK; £-mail: b.a.caswel/@liverpool.ac.uk 2Department of Environment, Earth and Ecosystems, Centre fo r Earth, Planetary, Space and Astronomical Research, Th e Open University, Wa lton Hall, Milton Keynes, MK7 6AA, UK; £-mail: [email protected] .

*Corresponding author

The Toarcian (Early Jurassic) Oceanic for the basinal areas. Ammonite species ranges Anoxic Event (OAE) was a period of severe and high-resolution one measurements from global palaeoenvironmental change. It was Holwell Quarry show thatorg the lowermost part characterised by global deposition of organic­ of one negative excursion is not represented org rich mudrocks (JENKYNS 2003), a negative one in this area (CASWELL & CoE 2012). excursion (e.g. KEMP et al. 2005; HESSELBO et The Early Toarcian OAE represents a good al. 2007; AL-SUWAIDI et al. 2010), increased analogue for anthropogenically induced climatic weathering (CO HEN et al. 2004), higher seawater change because the rates of pC0 increase and 2 temperatures (BAILEY et al. 2003), ocean de­ warming during the Toarcian are comparable oxygenation (PEARCE et al. 2008), and a marine with those at present day. The palaeontological mass extinction (LITTLE 1996; (ASWELL et al. changes that occurred during the Toarcian OAE 2009). are directly comparable with the ecological We present a new, large high temporal changes being observed in present day systems resolution dataset ( -4.5-11 cm) fo r species facing increasing �arine hypoxia (LEVIN ranges, and body-size and abundance changes 2009). Therefore, understanding how the biota

(n � 36,000) for the two bivalve species that responded during the Toarcian OAE can show dominate the benthos ( Bositra radiata and how organisms within present day oceans might Pseudomytiloides dubius; CASWELL et al. 2009) respond to increasing hypoxia on millennia} during the Toarcian OAE in the Cleveland Basin, timescales. Yorkshire, UK. Our results show quantitative relationships, at a thousand year resolution, References between geochemical proxies for environmental AL-SUWAIDI, A. H., ANGELOZZI, G.N., BAUDIN, F.,DA MBORENEA, S.E., HESSELBO, S.P., jENKYNS, H.C., MANCENIDO, M.O. & change and changes in the size and abundance RICCARDI, A. C. 2 010. First record of the Early Toarcian of benthic fa una during the Toarcian OAE. A Oceanic Anoxic Event from the Southern Hemisphere, comparison and correlation of the bivalve size Neuquen Basin, Argentina. - journal of the Geological and abundance data with geochemical proxies, Society, London 167: 633-636. BAILEY, T. R., ROSENTHAL, Y., McARTHUR, j.M., VAN published data on the pelagic macrofauna, and DE SCHOOTBRUGGE, THIRLWA LL, M.F. 2003. 8. & new data on the abundance of fish debris from Paleoceanographic changes of the Late Pliensbachian­ the Cleveland Basin sections suggest there were Early Toarcian interval: a possible link to the genesis two phases of persistent de-oxygenation that of an Oceanic Anoxic Event. - Earth and Planetary extended into the photic zone. Science Letters 212: 307-320. CASWELL, B.A., COE, A.L. COHEN, A.S. 2009. New range & Our study of the Holwell Quarry, data for marine invertebrate species across the early Leicestershire that represents a shallower Toarcian (Early jurassic) mass extinction. - journal of water area (East Midland Shelf) adjacent to the the Geological Society, London 166: 859-872. CASWELL, B.A. CoE, A.L. 2012. A high-resolution shallow Cleveland Basin shows that the benthic fauna & was more diverse and abundant. This area is marine record of the Toarcian (Early jurassic) Oceanic Anoxic Event from the East Midlands Shelf, UK. - interpreted to have been more hospitable and Palaeogeography, Palaeoclimatology, Palaeoecology a possible source of new invertebrate recruits 365-366: 124-135. 9th International Congress on the Jurassic System - Abstracts 37

COHEN, AS., COE, AL., HARDING, S.M. SCHWARTZ, L. Jurassic period. - Nature 437: 396-399. & 2004. Osmium isotope evidence for the regulation of LEVIN, L.A, EKAU,W., GOODAY, A.J., }ORISSEN, F.,MI DDELBURG, atmospheric C0 by continental weathering. - Geology J.J., NAQVI, S.W.A, NEIRA, C., RABALAIS, N.N. ZHANG, J. 2 & 32: 157-167. 2009. Effects of natural and human-induced hypoxia HESSELBO, S.P., }ENKYNS, H.C., DUARTE, L.V. OLIVE IRA, L.C.V. on coastal benthos. - Biogeosciences 6: 2063-2098. & 2007. Carbon-isotope record of the Early Jurassic LITTLE, C.T.S. 1996. The Pliensbachian-Toarcian (Lower (Toarcian) Oceanic Anoxic Event from fossil wood Jurassic) extinction event. In: RYDER, G., FASTOVSKY, and marine carbonate (Luisitanian Basin, Portugal). - D. GARTNER, S. ( eds.), The Cretaceous-Tertiary event & Earth and Planetary Science Letters 253: 455-470. and other catastrophes in Earth history. - Geological }ENKYNS, H.C. 2003. Evidence for rapid climate change Society of America, Special Papers 307: 505-512. in the Mesozoic-Palaeogene greenhouse world. - PEARCE, C.R., COHEN, AS., COE, AL. BURTON, K.W. 2008. & Philosophical Transactions of the Royal Society of Molybdenum isotope evidence fo r global ocean anoxia London A 361: 1885-1916. coupled with perturbations to the carbon cycle during KEMP, D.B., COE, AL., COHEN, AS. SCHWARK, L. 2005. the early Jurassic. - Geology 36: 231-234. & Astronomical pacing of methane release in the Early 38 9thInternational Congress on the Jurassic System - Abstracts

Center of gravity and shell volume calculations for some Jurassic ammonoids from Kachchh, India

ALOK CHAUDHARI

Center of Advanced Study in Geology, Banaras Hindu University, Va ranasi 221 OOt India; E-mail: alok. [email protected]

Ammonoids constitute the most diverse fossil method. invertebrates during the Mesozoic Era. One of The Jurassic succession of Kachchh is well the most striking features of ammonoids is its known for its diverse fossil record particularly chambered shell, which aided them to remain its richness in ammonoids. In view of the above, buoyant at different depths. This significant an attempt has been made to apply the modified attainment may partly explain their dominance equations given by RAUP and CHAMBERLAIN to in the Mesozoic. Earlierworkers have elaborated calculate the shell volume and center of gravity mathematical models to explain the parameters of about 20 Jurassic ammonoid specimens from associated with ammonoid buoyancy, which Kachchh, India. Such calculations will allow me accounts fo r the center of gravity and shell to comment on their mode of life and swimming volume. capabilities. To minimize the complexities, I use MosELEY (1938) in his pioneering paper on here MatLab (Mathematical Software) fo r all molluscan geometry derived the equations fo r kinds of desired calculations. It is a preliminary shell volume and surface area for planispirally work in context of Indian Jurassic ammonoids, coiled shells, which incorporated several which has never been attempted before. intrinsic shell parameters. TRUEMAN (1941) gave a modified equation for the shell volume assuming the ammonoid shell to be a right cone References wrapped about around an axis. Both TRUEMAN MosELEY, H. 1938. On the geometrical fo rms of turbinated and discoid shells. - Philosophical Transactions of the and MosELEY laid the foundation fo r the R�yal Society London 1838: 351-370. ammonoid hydrostatics calculations. RAuP & RA.UP, D.M. CHAMBERLAIN, J.A., Jr. 1967. Equations fo r & CHAMBERLAIN (196 7), with slight modification volume and center of gravity in ammonoid shells. - of TRUEMAN's and MOSELEY's works, applied Journal of Paleontology 41: 566-574. TRUEMAN, A.E. 1941. The ammonite body chamber, with these equations to actual ammonoid specimens special reference to the buoyancy and mode of life of and compared the calculated volume with the the living ammonite. - Quarterly Journal Geological actual volume obtained by water displacement Society, London 96: 339-383. 9th International Congress on the Jurassic System - Abstracts 39

Ductile deformation in Jurassic sequence of Kachchh riftbas in: A clue to Median High tectonics, Western India

GAURAV CHAUHAN & M. G. THAKKAR

Department of Earth and Environmental Science, KS.K V. Ka chchh University, Bhuj-Kachchh-370001

The Kachchh peri-cratonic riftbasin originated intra-basinal fault located in the central part during break-up of the eastern Gondwanaland of the basin and formed in a reverse tectonic and superposed by the Tertiary sag basin. environment. The fault is neotectonically During post-collision compressive regime of and seismically active, fo rming a prominent the Indian plate, the basin became a shear escarpment facing due north. It separates the zone with strike-slip movements along sub­ Bhuj Formation to the North and the Jhuran parallel rift faults. The major uplifts along the and Jumara formations to the south. The ductile basinal faults trending E-W in Kachchh expose deformation in the Jurassic sequences in the Mesozoic sediments. The most striking feature core region of the KHR indicates early activities of the basin is the structural high or ridge in the along the MH during the reverse tectonics of basement which cuts across the mainland uplift, the basin. The flexure zone is identified by the Banni graben and Pachchham uplift.It is known complex foldings, faults and shearings south as Median High (MH) that separates the higher of Bhuj in the Katrol hill range. The sheared eastern part of the basement from the gradually rocks are sandstones and shales of the Jumara dipping western part. In post-Oxfordian time Formation, while some shearings are also the MH arch was rejuvenated affectingthe facies observed in the Cretaceous sandstones. The of upper Jurassic to Cretaceous viz. Jhuran and ductile condition is only possible when the Bhuj formations. rocks are at considerable depth and when The present work focuses on the flexure they are not consolidated. The sheared zone is zone of the MH in the core of Katrol Hill Range confined to a small area where transverse fa ults (KHR) of mainland Kachchh. The flexures are are dominating and dissecting the KHF. The fo und near the Katrol Hill Fault - KHF and whole study implies the pre- and post-collision associated transverse faults. KHF is a secondary tectonic activities along the MH region. 40 9th International Congress on the Jurassic System - Abstracts

Integrated stratigraphy of the Oxfordian succession on the Isle of Skye, Scotland

ANGELAL. COE

DepartmentofEnvironment, Earth and Ecosystems, Centrefo r Earth, Planetary,Sp aceandAstronomical Research, The Open University, Wa lton Hall, Milton Keynes, MK7 6AA, UK; Email: [email protected]

The Oxfordian at Staffin Bay in the northern of the succession is the proposed site fo r the part of the Isle of Skye, Scotland is represented base Kimmeridgian GSSP at Flodigarry on the by about 100 m of interbedded mudstones and north side of Staffin Bay (MATYJA et al. 2006; siltstones rich in ammonites. The succession is WIERZBOWSKI et al. 2006). stratigraphically fa irly complete but the outcrop A further Oxfordian succession is exposed is composed of a complex series of fault blocks on the south side of the Isle of Skye but this exposed in the foreshore making correlation is much coarser-grained, not well constrained challenging and the amount of exposure variable biostratigraphically and is likely to be fa irly depending on the position of the overlying incomplete. Low grade thermal metamorphism storm beach. Detailed examination shows the of the succession due to the proximity of the succession is composed of many, centimetre­ Cullin Igneous Complex prevent construction to decimetre-sized, fining upward cycles. The of a palaeomagnetic or chemostratigraphic base of each cycle is composed of a dark-grey stratigraphy. The succession, however, provides silty mudstone with abundant plant debris and large-scale sedimentological patterns that are this rapidly fi nes upward into medium- and interesting sequence stratigraphically. pale-grey mudstones. These cycles are most A high resolution integrated graphic log of likely to represent changes in sediment supply the Staffin Bay succession showing the fa cies, driven by climatic fluctuation. Changes in the biostratigraphy, sequence stratigraphy and stacking pattern of these small-scale cycles magnetostratigraphy will be presented. The · allows a sequence stratigraphical interpretation suc�ession with be compared and correlated to be made which shows eight depositional with other Oxfordian records. sequences similar to other sections in NW References HESSELBO S.P. CoE, A.L. 2000. Jurassic sequences of the Europe (HESSELBO & CoE 2000). What is unusual & Hebrides Basin, Isle of Skye, Scotland. In: GRAHAM, about this particular Oxfordian succession is J.R. RYAN, A. (eds) International Association of & that most of the key sequence stratigraphical Sedimentologists. Field Trip Guidebook, Dublin surfaces are gradational, in common with some 2000: 41-58, Department of Geology, Trinity College, other Mesozoic mudrock successions. Dublin. MATYJA, B.A. WIERZBOWSKI A. WRIGHT, J.K. 2006. The Palaeomagnetic analysis on samples taken & Sub-BorealfBoreal ammonite succession at the about every 50 cm through the lower and Oxfordian/Kimmeridgian boundary at Flodigarry, upper part of the succession was successful in Staffin Bay (Isle of Skye), Scotland. - Transactions of all but the occasional sideritic carbonate bands the Royal Society of Edinburgh, Earth Sciences, 96: and shows a detailed pattern of normal and 387-405. 0GG, J.G., COE, A.L., PRZRBYLSKI, P.A. WRIGHT, J.K. 2010. reversed polarity (OGG et al. 2010; PRZYBYLSKI & Oxfordian magnetostratigraphy of Britain and its et al. 2010; WIERZBOWSKI et al. 2006) The correlation to Tethyan regions and Pacific marine palaeomagnetic results provide further magnetic anomalies. - Earth and Planetary Science key constraints on the biostratigraphic and Letters 289: 433-448. sequence stratigraphic correlation between the WIERZBOWSKI, A., COE, A.L., HOUNSLOW, M.W., MATYA, B.A., 0GG, J.G., PAGE, K.N., WIERBOWSKI, H. WRIGHT, & differentammo nite provinces and sections. The J.K. 2006. A potential stratotype for the Oxfordian/ succession is important because it is the most Kimmeridgian boundary: Staffin Bay, Isle of Skye, UK. stratigraphically complete Oxfordian section in - Volumina Jurassica 4: 17-33. the UK, was deposited in comparatively deep PRZYBYLSKI, P.A., 0GG, J.G., WIERZBOWSKI, A., (OE, A.L., HOUNSLOW, M.W., WRIGHT, J.K., ATROPS, F., SETTLES, water,is suitable for a wide range ofstratigr aphic E. 2010. Magnetostratigraphic correlation of the techniques and a key reference section for the Oxfordian-Kimmeridgian Boundary. - Earth and Boreal/Sub-Boreal ammonite province. The top Planetary Science Letters 289: 256-272. gth International Congress on the Jurassic System - Abstracts 41

Nodularity vs. geochemistry in Ammonitico Rosso: a preliminary report from the Upper Jurassic (Betic Cordillera, SE Spain)

RUTE COIMBRA & FEDERICO 0LORIZ

Departamento de Estratigraffa y Paleontologfa, Universidad de Granada, 18071 Granada, Sp ain; £-mail: [email protected], fo [email protected]

Ammonitico Rosso fa cies (AR) provides some in situ and intraformational components are of the most typical rocks from the Tethyan often suitable criteria, other aspects as textural Jurassic. Variations in colour, nodularity, and fabrics and potential distinct origins must also fo ssil content are common, and the wide be discussed. array of features in which this facies occurs The term nodule is here restricted to within­ complicates attempts fo r descriptive rather sediment nuclei of comparatively accelerated than genetic classifications of identified AR lithification regarding the surrounding variability (HOLLMANN 1962; }ENKYNS 1974; matrix. Since nodule differentiation is an in FARINACCI & ELMI 1981; CLARI et al. 1984; situ, progressive and very early diagenetic NICOSIA 1991; CLARI & MARTIRE 1996; MARTIRE process, nodule boundaries will depend on the 1996; CoiMBRA et al. 2009). This contribution degree to which differential lithification, and fo cuses on testing the descriptive concept of synsedimentary and subsequent compaction/ "nodularity" and its wide use to designate dissolution ( stylolitic contacts), operate the result of distinct processes. Although with respect to the surrounding matrix composition, shape, boundaries and size of AR (dissolution seams, matrix adaption). Nodules

Fig. 1. Examples of analyzed Ammonitico Rosso samples. A to E: Va riable degree of nodularity. F: Average intra-sample geochemical variability and mean absolute values obtained fo r samples A to E. 42 9th International Congress on the Jurassic System -Abstracts can be reworked with resulting boundary a slightly more variable record, with intra­ reinforcement. However, uncertainty is sample abundance variability <24o/o for Mg and evident when dealing with sub-rounded to Sr, and higher for Fe and Mn, showing intra­ more angular lithoclasts in AR, and their sample scattering from 6% up to 75°/o (mean interpretation as nodules under the assumption values in Fig. 1). Interestingly, a high visual of reworking cannot be conclusive. Sea-bottom differentiation does not always correspond to surface and biogenically mediated processes high variability in elemental abundance (Fig. such as biogenic ( oncoids, oncolites) and mixed lA-C), and no strict relationships seem to be (aggregate grains, cortoids) growths precede recorded between elemental and 6180 records. lithification processes s.str. and therefore are The highest intra-sample variability obtained not interpreted as nodules in the genetic sense for samples containing lithoclasts (Fig. 10, here chosen. Nodule recognition was conducted E) could be expected. These preliminary data on macroscopic observation of polished slabs indicates that incipient lithification during very of hand-samples, hence accounting only early diagenesis of AR sediments promoted the for formation of centimetre-sized nodules. preservation of both its isotope and elemental Petrographic analysis complemented nodule signature. This occurs in all macroscopically inspection. differentiated patches of incipient nodule In a context of high variable nodularity formation, nodules and investigated reworked in more or less calcareous horizons of the lithoclasts - the latter being a particular sub­ investigated AR and related fades, the sample of intraformational components. geochemical signature of different macroscopic sedimentary components is compared in order References to evaluate homogeneity /heterogeneity in their CLARI, P.A. MARTIRE, L. 1996. Interplay of cementation, & geochemical signatures. Representative cases mechanical compaction and chemical compaction in of intra-sample variability were chosen among nodular limestones of the Rosso Ammonitico Veronese samples selected from six sections belonging (middle - upper Jurassic, northeastern Italy). - Journal to the S-E Iberian pal eo margin. The studied of Sedimentary Research 66: 447-458. CLARI, P.A., MARINI, P., PASTORINI, M., PAVIA, G. 1984. material, obtained under strict biostratigraphic & 11 Rosso Ammonitico l nferiore (Baiociano-Calloviano) control, corresponds to Late Jurassic epioceanic hei monti lessini settentrionali (Verona). - Rivista settings, from the middle Oxfordian to the latest Italiana di Paleontologia e Stratigrafia 90: 15-86. (OIMBRA, R., IMMENHAUSER, A. 0LORIZ, F. 2009. Matrix Tithonian. & micrite l>13C and l>180 reveals synsedimentary marine Petrographic analysis was performed lithification in Upper Jurassic Ammonitico Rosso through microfacies, cathodoluminescence and limestones (Betic Cordillera, SE Spain).- Sedimentary scanning electron microscopy (SEM) analyses, Geology 219: 332-348. FARINACCI, A ELMI, S. (eds.) 1981. Rosso Ammonitico allowing the evaluation of the degree of & diagenetic alteration of the studied carbonates. Symposium, Roma, Proceedings: 602 pp., Tecnoscienza, Roma. Three to six powder sub-samples were drilled HOLLMANN, R. 1962. Ober Subsolution und die from each rock slab for analysis ofC and 0 stable "Knollenkalke" des Calcare Ammonitico Rosso isotopes and major and trace elements (Ca, Mg, Superiore im Monte Baldo (Maim, Norditalien). - Sr,Fe, and Mn). Neues Jahrbuch fiir Geologie und Palaontologie, Monatshefte 1962 : 163-179. In a context of fair preservation of the }ENKYNS, H.C. 1974. Origin of red nodular limestones studied material and negligible degree of (Ammonitico Rosso, Knollenkalke) in the diagenetic imprint (COIMBRA et al. 2009), it Mediterranean Jurassic: A diagenetic model. In: HsO, K.J. }ENKYNS, H.C. (eds.), Pelagic sediments: on Land seems of relevance that very early diagenesis & produced a wide spectrum of nodularity. and under the Sea. - International Association of Sedimentologists, Special Publication 1: 249-271. Regarding intra-sample variability (Fig. 1 ), a MARTIRE, L. 1996. Stratigraphy, facies and synsedimentary very stable C isotope record is observed, with tectonics in the Jurassic Rosso Ammonitico Yeronese mean value of 2.3%o (maximum scattering (Altopiano di Asiago, NE Italy). - Facies 35: 209-236. NICOSIA, U., CONTI, M.A., FARINACCI, A., ALTINER, D. 0.2%o), accompanied with only slight variations & Koc;:YIGIT, 1991. Western Anatolia Ammonitico A in oxygen isotope values, with a mean value Rosso type sediments. Depositional history and of 0.03%o (maximum scattering 0.3%o). The geodynamic meaning. - Geologica Romana 27: 101- elemental abundance distribution shows 112. 9th International Congress on the Jurassic System - Abstracts 43

Palaeolatitudinal patterns of diversity and distribution in Early Jurassic South American bivalves

SUSANA E. DAMBORENEA* & }AVIER ECHEVARRIA

Consejo Nacional de lnvestigaciones Cientificasy Tecnicas. Departamento Paleontologfa Invertebrados, Museo de Ciencias Naturales La Plata, 1900 La Plata, Argentina; E-mail: sdambore@fc nym.unlp.edu. ar

*Corresponding author

One of the global-scale relationships between is especially evident fo r Pliensbachian and biogeography and ecology is the existence Toarcian times. This local break may be due to of latitudinal gradients in species diversity, an abrupt change in geographic settings at that known both in past and living faunas (CRAME latitude, with the establishment of favourable 2000; VA LENTINE & }ABLONSKI 2010). Although conditions and an increased variety of habitats it is generally acknowledged that the global within the extensive Neuquen Basin, which pattern of decreasing diversity towards at that time was a quasi-isolated shallow­ higher latitudes may be altered locally due epeiric sea, very different from the coasts and to several factors, these are not well-known. environments to the north of that latitude. The In this contribution we present an integrated analysis of southernmost and northernmost study taking into account several aspects of geographic occurrences also shows a somewhat the latitudinal patterns of distribution and bounded range of major change in species diversity of marine bivalves during the Early distribution instead of the expected gradient. Jurassic along the western South Ameri�an In order to statistically check fo r gradational margin of the Palaeopacific and their changes patterns, the changes in the proportional values through time. Presence-absence bivalve species of systematic- and palaeobiogeographic-kinship data were compiled from about 200 localities species categories were evaluated by means of in Chile and Argentina, grouped into zo units generalized linear models (CRAWLEY 2007). between 20° and 46° present-day latitude, The analysis revealed a significant trend of and recorded separately fo r each of the fo ur decreasing relative diversity at higher latitudes Early Jurassic stages. Data and methods were for the superfamily Trigonioidea in the fo ur updated from previous reports (DAMBORENEA considered stages. During the Pliensbachian, 1996; DAMBORENEA et al. 2012). A set of the superfamilies Arcoidea, Nuculanoidea, analytical methods was applied to the study of and Inoceramoidea showed a southward the latitudinal ranges of species thus obtained. increasing trend in proportion of species, while The first approach was cluster analysis, but this Pholadomyoidea showed an opposite trend. method, although useful, imposes a hierarchical For the Toarcian the superfamilies Limoidea structure on the data. Since a gradation along and Lucinoidea decreased southwards in latitudinal range is expected, the distribution relative number of species, while Monotoidea, of species was then analysed using techniques Pectinoidea, and Crassatelloidea tended to similar to those considered fo r origination/ increase their relative diversity in that same extinction analysis (HAMMER & HARPER 2006), direction. The analysis of the distribution counting the number of species per zo unit, produces a break when palaeobiogeographic and substituting first and last appearances by affinity groups are considered. This suggests northernmost and southernmost geographical the existence of two main biogeographic units, occurrences. The results do not show the a northern (or Tethyan) and a southern (or expected decrease in species diversity towards Austral) one, with a boundary zone within higher latitudes in the geographic range the study area (DAMBORENEA 2002). Some considered here, but instead a consistent local other general trends through time, which diversity increase between 30° and 40°, which are consistent with Northern Hemisphere 44 9th International Congress on the Jurassic System - Abstracts bivalve data (HALLAM 1977; HAYAMI 1990; Publication 177: 347-360. CRAWLEY, M.J. 2007. The R Book. John Wiley and Sons, LIU 1995), include: a slight decrease in the Ltd. percentage of "local" species through time DAMBORENEA, S.E. 1996. Palaeobiogeography of Early from the Hettangian to the Toarcian; a diversity Jurassic bivalves along the southeastern Pacific maximum in the Pliensbachian; and a shift margin. - 13Q Congreso Geol6gico Argentina y 3Q (for about eight degrees of latitude) towards Congreso de Exploraci6n de Hidrocarburos (Buenos higher latitudes of the boundary zone between Aires) Aetas 5: 151-167. DAMBORENEA, S.E. 2002. Jurassic evolution of Southern southern and northern faunas for the time Hemisphere marine palaeobiogeographic units based involved (DAMBORENEA 2002). This last result on benthonic bivalves. - Geobios 35, MS24: 51-71.

DAMBORENEA, S.E., ECHEVARRIA, J. Ros - FRANCH, S. is here interpreted as due to a combination & of factors involving both climatic change and 2012. Southern Hemisphere palaeobiogeography of Triassic-Jurassic marine bivalves. Springer Briefs in continental latitudinal drift. The present study Earth System Sciences, 141, Springer,Dordrecht. indicates that large-scale geographic conditions HALLAM, A. 1977. Jurassic bivalve biogeography. - are important factors to be taken into account Paleobiology 3: 58-73. HAMMER, HARPER, D.A.T. 2006. Paleontological data for the analysis of latitudinal diversity trends of 0. & benthic faunas, confirming similar conclusions analysis. Blackwell Publishing. HAYAMI. I. 1990. Geographic distribution of Jurassic faunas based on living faunas along the same latitudinal in Eastern Asia. In: ICHIKAWA, K., MIZUTANI, S., HARA, range (VALDOVINOS et al. 2003). In contrast, I. HADA, S. YA o, A. ( eds.), Pre-Cretaceous terranes of & the coeval changes in relative proportions of Japan. - Publication of IGCP Project 224, Osaka. different bivalve superfamilies towards either Lm, C. 1995. Jurassic bivalve palaeobiogeography of the Proto-Atlantic and the application of multivariate higher or lower latitudes are probably not so analysis methods in palaeobiogeography. - Beringeria heavily dependent on geography but reflect 16: 3-123. VALDOVINOS, C., NAVARRETE, S.A. MARQUET, P.A. 2003. instead latitudinal trends most probably related & to temperature gradients. Mollusk speciesdiversity in the Southern Pacific: Why are there more species towards the pole? - Ecography References 26: 139-144. CRAME, J.A. 2000. The nature and origin of taxonomic VALENTINE, J.W. JABLONSKI, D. 2010. Origins of marine & diversity gradients in marine bivalves. In: HARPER, patterns of biodiversity: some correlates and E.M., TAYLOR, J.D. CRAME, J.A. (eds.), The evolutionary applications. - Palae ntology 53: 1203-1210. & � biology of the Bivalvia. - Geological Society Special 9th International Congress on the Jurassic System - Abstracts 45

The terrestrial Triassic-Jurassic boundary in China

SHENGHUI DENG*, YUANZHENG Lu, Ru FAN & XIN LI

Research Institute of Petroleum Exploration & Development PetroChina, Beijing10 0083, China; E-mail: [email protected]; [email protected]; [email protected]; lixin@petrochina. com.cn

*Corresponding author

The Late Triassic and Jurassic strata in China stratigraphic successions are represented by the are dominated by terrestrial rocks except succession in the Junggar Basin of Northwest those in Tibet and the Pacific Ocean marginal China, which is composed of the Haojiaguo, areas (Guangdong Province of South China for Badaowan, and Sangonghe formations, in example). Thus, the Triassic-Jurassic (Tr-J) ascending order. These strata yield abundant boundary in China is represented by continental plants, spore-pollen, megaspores, bivalves, beds. Due to lack of marine fossils and any other and conchostracans (DENG et al. 2003, 2010). definite evidence, the Tr-J boundary in China is The Tr-J boundary should be placed at the still controversial. base of the Badaowan Formation based on In 2010, the GSSP fo r the base of the the palaeontological evidence and isotopic Hettangian Stage, namely the Tr-J boundary,had excursion. been ratified by the IGU. The Tr-J boundary GSSP Lithological fe atures. - The lower part of was placed at the Kuhjoch section, Northern the . Badaowan Formation is characterized Calcareous Alps, Austria. It coincides with the lithologically by grey or whitish grey sandstones, first appearance of the ammonite Psiloc'eras siltstones, mudstones, and conglomerates with - spelae GUEX subsp. tiro/icum HILLEBRANDT coal interbeds; while the underlying beds, & KRYSTYN and with an approximately the upper part of the Haojiaguo Formation, is simultaneous brief negative excursion in characterized by greyish green and yellowish organic carbon isotopes and a palynological green rocks intercalated by coal-bearing beds. assemblage of Cerebropollenites thiergartii This general colour differencereflects somewhat (RHUL et al. 2009). Both the isotopic event and the change of sedimentary environments palynological assemblage are very valuable for through the Late Triassic to the Early Jurassic determining the continental Tr-J boundary. age.

In order to correlatethe Mesozoic oil­ Palaeontological evidence. - There are two bearing terrestrial strata in China, the authors different floral assemblages in the Haojiaguo have investigated the Upper Triassic Series and Formation. One is the Danaeopsis-C/adophlebis Jurassic System of the major oil-bearing basins, ichunensis Assemblage from the lower and such as the Tarim, Junggar, and Turpan-Hami middle part of the formation, which has been basins of Xinjiang, Northwest China, and the assigned to the Late Triassic as it consists Sichuan Basin of Southwest China during the chiefly of Late Triassic elements, such as recent years. The Tr-J boundary is one of the Danaeopsis. The assemblage from the upper issues of the studies. part of the formation is named Hausmannia­ Clathropteris minoria Assemblage, which lacks The Tr-J boundary in northern China typical Jurassic elements but is composed of During the Late Triassic and Early Jurassic some taxa that are usually recorded in the Late Epochs in northern China, namely north of Triassic, such as Thinnfe ldia? sp., Cladophlebis the Kunlun Mountains, Qinling Mountains, kaoiana, Sp henopteris chowkiawanensis, and and Dabie Mountains, the climate was Cy cadocarpidium sp.. It is, therefore considered predominantly temperate-humid and the strata as possibly Late Triassic in age. The Badaowan are characterized by coal-bearing formations. Formation yields two palaeobotanical The Upper Triassic and the Lower Jurassic assemblages. The upper one is definitely 46 9th International Congress on the Jurassic System - Abstracts of Early Jurassic age containing Coniopteris and Lower Jurassic are usually continuous and gaojiatianensis and numerous species that well exposed. The Tr-J boundary was previously are commonly encountered in Jurassic floras. determined at the base of the Zhengzhuchong The Lower one, in contrast, should be of Early Formation, marked by first appearance of Jurassic age containing abundant To dites red beds or by a quartzitic sandstone bed princes and Clathropteris elegans, which are (WANG et al. 2010). However, as a result of our the major species of the early Early Jurassic investigations of a dozen outcrop sections and Thaumatopteris Zone of Greenland. So, the numerous well sections in recent years, the Tr-J Tr-J boundary can be placed at the base of the chronostratigraphic boundary in the northern Badaowan Formation. Sichuan Basin should be placed in the black The spore-pollen from the Haojiaguo shales oftheupperpartoftheXujiahe Formation, Formation indicates a Triassic age due which is generally assigned to the Upper Triassic. to numerous Triassic or older elements, This boundary has been determined chiefly by including Aratrisporites, Chordasporites, palynological and palaeobotanical evidence and Lueckisporites tatooensis, Hamiapollenites an organic carbon isotopic excursion. Below bullaefo rmis, Remysporites and Endosporites the boundary the palynological assemblage is ornatus. A sharp peak of fern spores, including characterized by Late Triassic spores, such as Densosporites scanicus, Densosporites crassus, Dictyophyllidites, Ky rtomisporis, Lunzisporites, and Cy athidites, occurs near the base of the and Ta eniaesporites, whereas; above the Badaowan Formation, indicating a major boundary the content of the pollen Classopol/is change in floral evolution. Besides, the major sharply and that of the fern spore Cy athidites taxa of the megaspore Hughesisporites gibbosus greatly increases and that of Triassic spores - Calamospora rhaeticus assemblage from the greatly decline. The macro-plant fossils from Haojiaguo Formation and the Horstisporites the rocks close to and below the boundary harrisis - Trileites murrayi - Echitriletes hispidus are dominated by dipteridaceous ferns and assemblage from the Badaowan Formation Cycadopsida, indicating a Late Triassic age; show they can be assigned to the Late Triassic the dicksoniaceous fern Coniopteris appears and Early Jurassic respectively. at about 10 m above .the boundary. A negative Organic carbon isotope excursion. - Organic organic carbon isotopic excursion of -3o/oo PDB carbon isotope analyses of rock and charcoal and --4%o PDB value is found in the rocks close samples from the Middle to Upper Haojiaguo to the biostratigraphic Tr-J boundary. Formation and Lower Badaowan Formation demonstrate that there is a major negative References excursion ( -2%o PDB in whole rock samples and DENG, S., Lu, Y., FA N, R. et al. 2010. The Jurassic of Northern -4.0%o PDB as the maximum value in charcoal Xinjiang. 279 pp., University ofScienceand Technology samples) in the topmost beds of the Haojiaguo of China Press. Hefei (in Chinese). DENG, S., YAO, Y., YE, D. et al. 2003. Jurassic System in Formation and through the lowermost beds the North of China (I), Stratum. 399 pp., Petroleum of the Badaowan Formation. It is correlated Industry Press, Beijing (in Chinese with English with the main negative excursion event at the abstract). GSSP of Kuhjoch section of Austria (RHUL et al. McROBERTS, C.A., WA RD, P. D. & HESSELBO, S. 2007. A proposal for the base Hettangian Stage = base 2009), Nevada (WA RD et al. 2007; McRoBERTS ( Jurassic System) GSSP at New York Canyon (Nevada, et al. 2007), East Greenland, and England USA) using carbon isotopes. - ISJS Newsletter 34: (HESSELBO et al. 2002). This implicates that the 43-49. Tr-J biostratigraphic boundary coincides with HESSELBO S.P., ROBINSON, S.A., SURLYK, F.. & PIASECKI, the Tr-J chronostratigraphic boundary at the S. 2002. Terrestrial and marine extinction at the Triassic-Jurassic boundary synchronized with major Haojiaguo section of the Junggar Basin. carbon-cycle perturbation: A link to initiation of massive volcanism? - Geology 30: 251-254. The Tr-J boundary in South China RHUL, M., KUSCHNER, W. M. & KRYSTYN, L. 2009. Triassic­ The well exposed continental Tr-J boundary Jurassic organic carbon isotope stratigraphy of key sections in South China are located in the sections in the western Tethys realm (Austria). - Earth and Planetary Science Letters 281: 169-187. Sichuan and Yunnan provinces of Southwest WA NG, Y., Fu, XIE, X. et al. 2010. The terrestrial Triassic 8., China. In the Sichuan Basin, the Upper Triassic and Jurassic System in the Sichuan Basin, China. 160 9th International Congress on the Jurassic System -Abstracts 47

pp., University of Science and Technology of China across the Triassic-jurassic boundary at the candidate Press, Hefei. GSSP section at Ferguson Hill, Muller Canyon, WARD, P. D., GARRISON, G.H., WILLIFORD, K.H., KRINGS, D., Nevada, USA. - Palaeogeography, Palaeoclimatology, GOODWIN, D., BEATTIE, M. & McROBERTS, C. 2007. The Palaeoecology24 4: 281-289. organic carbon isotopic and paleontological record 48 9th International Congress on the Jurassic System - Abstracts

Continental drainage and oceanic circulation during the Jurassic inferred from the Nd isotope composition of biogenic phosphates and sediments

GUILLAUME DERAl, }ONATHAN PRUNIERl, PAUL L. SMITH2, }IM HAGGART2•3, EVGENY Popoy4,ALEX ANDER GUZHOV5, MIKHAIL A. ROGOV6, DOMINIQUE DELSATE7, DETLEV THIES8, GILLES CUNY9, EMMANUELLE PUCEAT10, GUILLAUME CHARBONNIER11 & GERMAIN BAYON12

1Laboratoire GET, University of To ulouse, 14 avenue Edouard Be/in, 31400 To ulouse, France; E-mail: [email protected] 2Department of Earth, Ocean and Atmospheric Sciences, University of British Columbia, 2207 Main Mall, Va ncouver,British Columbia V6T 1Z4, Canada 3Geological Survey of Canada, 101-605 Robson Street, Va ncouver, British Columbia V6B 5]3, Canada 4Department of Palaeontology, Geological Fa culty, Saratov State University, 83 Astrakhanskaya Str., 40012 Saratov, Russia 5Paleontologica/ Institute, Russian Academy of Sciences, 123 Profs oyuznaya ul., 117997 Moscow, Russia 6Geo/ogical lnstitute, Russian Academy of Sciences, 7 Pyzhevskyla ne, 11901 7 Moscow, Russia 7Museum National d'Histoire Nature/le, 25 rue Munster,21 60 Luxembourg, Luxemburg 8lnstitutfiirGeolo gie, Leibniz UniversitiitHa nnover, Callinstr. 30, D-30167 Hannover, Germany 9The Natural HistoryMuseum of Denmark, flster Vo ldgade 5-7, 1350 Copenhagen, Denmark 10Laboratoire Biogeosciences, Universite de Bourgogne, 6 Bd Gabriel, 21000 Dijon, France 11Laboratoire IDES, Universite Paris Sud XI, Batiment 504, 91405 Orsay, France 12lfr emer, Unite de Recherche Geosciences Marines, 29280 Plouzane, France

The Jurassic period marked the onset ofPangean al. 2011). dislocation that led to our modern geography. In this study, we attempt to better constrain The initiation of this major continental oceanic connections as well as the modifications reorganisation involved numerous geodynamic in continental drainage that resulted from the processes whose timing, interaction and Jurassic paleogeographic reorganisation. For fe edback had important paleoclimatic and this purpose, we present 53 new neodymium geochemical consequences. Among them, the isotope values (noted ENdCtJ) measured on opening of the northern Atlantic Ocean and fossil fish teeth, ichthyosaur bones, phosphate the development of transcontinental seaways ooids, and sediments from Europe, European across the Laurasian and Gondwanan cratons Russia, and North America. Application of this caused major modifications to global oceanic geochemical proxy is based on the principle that circulation which significantly affected heat rocks weathered on continents have different Nd and moisture transport (DONNADIEU et al. isotope compositions according to their origin 2006). At the same time, the incipient growth (volcanic vs. cratonic) and age (Precambrian of the Pacific plate triggered increases in to recent). Through fluvial discharge, seawater plate subduction rates, terrane accretion, and acquires its ENd signal (recorded by phosphate volcanism all around the Panthalassan ocean during early diagenesis) reflecting all potential (BARTOLINI & LARSON 2001). Similarly, many sources in the drainage area (TACHIKAWA et al. subduction and accretion events occurred in 2003). As the Nd residence time is relatively other domains, leading to progressive closures short compared with the global oceanic ofthe Paleotethyan and Mongol-Okhotskoceans. mixing rate, this geochemical proxy is deemed This global reorganisation of both continental conservative and very suitable for tracking masses and oceanic circulation patterns likely exchanges of water masses with different affected the Jurassic climate by shifting the isotopic signatures (MARTIN & SCHER 2004). climatic belts, changing albedo, and modulating For example, STILLE et al. (1996) showed that atmospheric pC0 through volcanic degassing during the Triassic period, Panthalassan and 2 or changes in silicate weathering rates (DERA et Tethyan ocean waters were very radiogenic 9rh International Congress on the Jurassic System - Abstracts 49 owing to extensive volcanic sources. During the Precambrian Fenno-Scandian sources to the Pangean dislocation, climate changes caused north and radiogenic Cimmerian volcanic inputs stronger weathering of the cratons, leading to to the east. Finally, we note that the ENdCtJ values less radiogenic Tethyan seawaters. Here we of Euro-boreal and Russian seawaters strongly reappraise the evolution of circulation patterns fluctuate through time and reflect short-term at high stratigraphic resolution (ammonite changes in water mass circulation patterns biozone) by specifying both the potential and/ or sporadic modifications of drainage sources and the drainage pathways that areas during the Jurassic. influenced seawatersignatures throughout the References Jurassic period. BARTOLINI, A. & LARSON, R. 2001. Pacific microplate and Combined with an exhaustive compilation the Pangea supercontinent in the Early to Middle of worldwide ENd data from the literature, our Jurassic. - Geology 29: 735-738. new results show that the sources of Nd were DERA, G., BRIGAUD, B., MaNNA, F., LAFFONT, R., PUcEAT, E., DECONINCK, JF., PELLENARD, P., }OACHIMSKI, M. very different according to oceanic domains. & DURLET, C. 2011. Climatic ups and downs in a In contrast to current patterns showing that disturbed Jurassic world. - Geology 39: 215-218. DERA, G., PUCEAT, E., PELLENARD, P., NEIGE, P., DELSATE, all circum-Pacific volcanic areas of the ring 0., fire contribute to the radiogenic signal of }OACHIMSKI, M.M., REISBERG, L. & MARTINEZ,· M. 2009. Water mass exchange and variations in seawater the Pacific Ocean (JEANDEL et al. 2007), the temperature in the NW Tethys during the Early radiogenic signature of Panthalassan waters Jurassic: Evidence from neodymium and oxygen isotopes of fish teeth and belemnites. - EPSL 286: (� -3.9) was mainly dependant on North­ American and southern Gondwanan volcanic 198-207. arc inputs. Indeed, the sediments of Asian OONNADIEU, Y., GODDERIS, Y., PIERREHUMBERT, R., DROMART, G., FLUTEAU, F. &}ACOB, R. 2006. A GEOCLIM simulation Panthalassan margins show very low EN dCtJ ofclimaticand biogeochemical consequences ofPangea values presumably resulting from the dilution of breakup. - Geochemistry, Geophysics, Geosystems local volcanic sources by massive Precambrian 7(11): Q11019, doi:10.1029/2006GC001278 cratonic input from rising Amurian relief. In }EANDEL, C., ARSOUZE, T., LACAN, F.,TE CHINE, P. & DUTAY, J.-C. 2007. Isotopic Nd compositions and concentrations the Tethyan domain, the tropical seawater of the lithogenic inputs into the ocean: A compilation, ENdCtJ values are comparatively less radiogenic with an emphasis on the margins. - Chemical Geology 239: 156-164. ( � -6.3). This probably reflects a mixing of radiogenic sources such as Panthalassan MARTIN, E. E. & ScHER, H.D. 2004. Preservation of seawater waters or volcanic Cimmerian inputs and non­ Sr and Nd isotopes in fo ssil fish teeth: bad news and good news. - EPSL 220: 25-39. radiogenic influxes from former Laurasian and STILLE, P., STEINMANN, M. & RIGGS, S.R. 1996. Nd isotope Gondwanan crust. Toward higher latitudes, evidence for the evolution of the paleocurrents in the the Nd isotope composition of Tethyan waters Atlantic and Tethys Oceans during the past 180 Ma. - strongly decreases in the Euro-boreal domain EPSL 144: 9-19. TACHIKAWA, K., ATHIAS, V. & }EANDEL, C. 2003. Neodymium ( -8.6) but remains higher in the Russian budget in the modern ocean and paleo-oceanographic seaway (-7.4). This differencecould result from implications. - Journal of Geophysical Research 108: the respective influences of non-radiogenic 10/1-10/3. so 9rh International Congress on the Jurassic System - Abstracts

Palynology of MissaoVelha and Brejo Santo formations (Jurassic) of the Araripe Basin, Northeastern Brazil

SARAH DUARTEl, MITSURU ARAI2 & NEERJA jHA3

1Laboratoryof Nannofo ssils, Geoscience Institute, Departament of Geology, Federal University of Rio de Janeiro, Rio de Janeiro, Brazil; Email: Sarahpa/[email protected] 2PetrobrasjCENPES/PDGEO/BPA, Biostratigraphy & Palaeoecology, Rio de Janeiro, Brazil; Email: [email protected] 3Birbal Sahni Institute of Palaeobotany, Luckno� India; E-mail: [email protected]

The present communication records spores and (CouPER) DaRING et al., R. tenuis (BALME) pollen grains recovered from jurassic sediments BACKHOUSE, Sestrosporites pseudoalveolatus of the Araripe Basin (northeastern Brazil). Five (COUPER) DETTMANN, Stereisporites bujargiensis samples belonging to the MissaoVelha and (BoLKHOVITINA) SCHULZ, Ve rrucosisporites Brejo Santo formations in borehole 2-AP-1-CE asymmetricus (COOKSON & DETTMANN) POCOCK, between a depth of 923.65 m and 1,450.50 m V. jonkeri (JANSONIUS) 0UYANG & NORRIS, and V. were processed with traditional palynological sp. (*). methodology for recovery of palynomorphs. Pollen grains (gymnosperms): Alisporites The recovered assemblage contains 72 taxa, out austra/is DE jERSEY, A. bilatera/is ROUSE, A. of which 44 belong to spores and 28 to pollen, grandis (COOKSON) DETTMANN, Araucariacites which are listed below. austra/is CooKSON (*), A. sp. (*), Cal/ialasporites Spores: Baculatisporites comaumensis dampieri (BALME) DEV (*), C. triangularis (CooKSON) PoTONIE, B. aff. comaumensis (*), (LEVET-CARETTE) REYRE, C. aff. triangularis, C. Cicatricosisporites australiensis (CooKSON) trilobatus (BALME) DEV (*), C. turbatus (BALME) POTONIE, C. crassistriatus BURGER (*), C. SCHULZ, Cedripites sp. (*), Cerebropollenites imbricatus (MARKOVA) SINGH, C.magnus DaRING mesozoicus (CoUPER) NILSSON (*), Classopollis (*), C. purbeckensis NORRIS (*), C. shalmaricus sp. (*), Cy cadopites sp. (*), Dicheiropollis sp. A Srivastava (*), C. sternum VA N AMERON (*), (in CoiMBRA et al. 2002); Equisetosporites sp. Clavatisporites hammenii (HERBST) DE jERSEY, (*), Eucomiidites spp. (*), Exesipollenites tumulus Converrucosisporites pnce1 McKELLAR, C. BALME (*), Inaperturopollenites dettmanniae saskatchewanensis PococK, C. variverrucatus PococK, Monosu/cites sp. (*), Parvisaccites (CouPER) NoRRIS (*), Deltoidospora australis sp. (*), Perinopollenites elatoides CoUPER, (COUPER) POCOCK (*), D. germanica DaRHaFER, Podocarpidites multesimus (BOLKHOVITINA) D. sp. (*), Densoisporites perinatus CoUPER PococK, P. ornatus PococK, P. sp. (*), Sergipea (*), D. velatus WEYLAND & KRIEGER, D. sp. spp. (*), Vitreisporites contectus DE jERSEY, V. (*), Dictyophyllidites eqwexmus (CouPER) jurassicus POCOCK, and V. pallidus (REISSENGER) DETTMANN, D. harrisii COUPER (*), Dictyotriletes NILSSON (*). southeyensis PococK, Gemmatriletes c/avatus The presence of Ischyosporites crateris, BRENNER, Impardispora apiverrucata (CouPER) I. punctatus, I. scabris, Januasporites VENKATACHALA, Ischyosporites crateris spinosireticulatus, Retitrileles c/avatoides, BALME, /. punctatus COOKSON & DETTMANN, /. Retitriletes tenuis, etc. indicates a jurassic scaberis CooKSON & DETTMANN, Januasporites affinity. The taxa marked by asterisks (*) are spinosireticulatus McKELLAR, Klukisporites sp. known also from Cretaceous strata of Brazil. A (*), Laevigatosporites sp. (*), Leptolepidites preliminary study, including Cretaceous well argenteaefo rmis (BOLKHOVITINA) MORBEY, sections, was performed by ARAI et al. (2001). L. major COUPER, L. sp. (*), Ly copodiacidites Laevigatosporites sp. is a long-ranging taxon and eminulus DETTMANN, Pilosisporites is also reported from Palaeozoic and Cenozoic ingramii BACKHOUSE, P. trichopapillosus strata of Brazil and India. It has no stratigraphic (THIERGART) DELCOURT & SPRUMONT (*), P. aff. significance. trichopapil/osus, P. sp. (*), Retitriletes c/avatoides The palynofloristic spectrum indicates 9th International Congress on the Jurassic System - Abstracts 51 a humid tropical palaeoclimate during the Bacias interiores do nordeste, 2., 1997, Crato. Atas ... deposition of the MissaoVelha and Brejo Santa Crato: DNPM-URCA-SBP: 109-117, 122-124 (Cole�ao Chapada do Araripe, No. 1). fo rmations. The palynoflorais similar to that of BLANCO-GONZALEZ, M. 1998. Palinologia del jurasico the San Cayetano fo rmation (Jurassic of Cuba) Superior en Cuba Central. In: Geologia y Mineria'98 (BLANCO-GONZALEZ 1998; DUENAS-)IMENEZ Memorias 2:271-273, Centro Nacional de lnformaci6n et al. 2003), suggesting that these localities Geol6gica, La Habana. belonged to same palaeoclimatic zone. The COIMBRA,j.C.,ARAI,M.&CARRENO,A.L.2002.Biostratigraphy of Lower Cretaceous microfossils from the Araripe palaeoclimate at the time of deposition of these Basin, northeastern Brazil. - Geobios 35: 687-698. formations was more humid than is interpreted DUENAS-jiMENEZ, H., LINARES-CALA, E. & GARciA-SANCHEZ, traditionally for Brazilian Jurassic and earliest R. 2003. Palinomorfos em las rocas de La Formaci6n Cretaceous times (e.g., FREITAS et al. 2008; PI RES SanCayetano, Pinar Del Rio, Cuba. - Mineria y Geologia 19: 59-70. & GUERRA-SOMMER 2009). The relatively humid FREITAS, F.l. DE, HESSEL, M.H. & NOGUEIRA NETO, j. DE A. climate is suggested also by the scarcity of the 2008. Troncos f6sseis da Forma�ao Missao Velha na ephedroid pollen and C/assopollis grains. por�ao leste da Bacia do Araripe, Ceara. - Revista de Geologia 21: 193-206. References PIRES, E. F. & GUERRA-SOMMER, M. 2009. Plant-arthropod ARAI, M., COIMBRA, j.C. & SILVA-TELLES jR, A.C. 2001. Sintese interaction in the Early Cretaceous (Berriasian) of Bioestratigrafica da Bacia do Araripe (Nordeste the Araripe Basin, Brazil. - journal of South American do Brasil). In: Simp6sio sobre a Bacia a Araripe et Earth Sciences 27: 50-59. 52 9th International Congress on the Jurassic System - Abstracts

Correlation of the Boreal Jurassic-Cretaceous boundary strata by means of belemnites

0XANA S. DZYUBA

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

Belemnites (mainly Cylindroteuthididae) are East Siberian high-resolution succession of well known from the Boreal Jurassic-Cretaceous belemnite zones and beds is recorded in the (J-K) boundary sediments, which are widely West Siberian sections almost completely, distributed in northern Eurasia, northern North excluding the Tehamaensis Zone. In the eastern America and the Arctic islands. Cylindroteuthid foothills of the Northern and Subpolar Urals belemnites were also recorded from J-K (northwestern margin of Western Siberia) boundary sections containing mixed Boreal within the Volgian and Ryazanian stages, the and Tethyan faunas, being found in Northern following East Siberian biostratons have been California, Western Canada, Russian Platform; documented: Mamillaris Zone, Napaensis recently they have been reported from Central Zone, Knoxvillensis Zone, Russiensis Zone, and Japan (SANO et al. 2012). These belemnites Curvulus Zone, Explanata Beds, and Gustomesovi can abound where such biostratigraphically and Porrectiformis Beds (DzvuBA 2004, 2012, important macrofossils as ammonites and 2013). In addition, the local Explorata Beds buchias are absent or rare. Therefore, belemnite and Compactus Beds have been established zonal scales based on cylindroteuthids have here. Some Siberian zones (in the beds' rank) been developed intensely over the last few and beds are traceable to the Pechora Basin decades. (Mamillaris Beds, Explorata Beds, and Curvulus The J-K boundary in the Boreal regions is not Beds), northwestern Europe (Explanata Beds) characterised by a sharp change in belemnite and northern Califo�nia (Tehamaensis Beds, assemblages (SAKS & NALNYAEVA 1973; DZYUBA and J

Bajocian ammonoids and depositional events of the Arequipa Basin (southern Peru): evidence from Rio Pumani area (Ayacucho)

SIXTO R. FERNANDEZ-LOPEZ1 *, VICTOR C. CAILLAUX2, EDWIN G. SALDIVAR2 & CESAR C. BUDIEL2

1Departamento Paleontologfa, Facultad Ciencias Geol6gicas, calle Jose Antonio Novais,2, Universidad Complutense de Madrid, 28040-Madrid, Spain; E-mail: [email protected] 2/nstituto Geo16gico Minero y Metalurgico {INGEMMET), Av. Canada 1470, San Borja, Lima, Peru; E-mail: [email protected], [email protected]; [email protected]

*Corresponding author

Bajocian ammonoids are scarce in the central thick, and overlies volcanic rocks of the Permo­ Andes, although marine deposits are well Triassic Mitu Group. Above the Chunumayo developed in the southern areas of Peru. The Formation, there are 300 m of the Yura Group Rio Pumani area, 300 km SE of Lima, displays (Middle-Upper J urassic) corresponding an unusual Bajocian succession mainly because to fluvial-deltaic deposits. Southward of its high biostratigraphic completeness within the Arequipa Basin, these deposits reach the southern Peruvian outcrops (WESTERMANN thicknesses greater than 2000 m and developed et al. 1980; RICCARDI et al. 1992). in deeper depositional environments going During the Early jurassic, the Pucara Basin from turbidites to slope and shelf deposits·with in the North and the Arequipa Basin in the South the development of olistoliths. were separated from each other by structural In the area of the Rio Pumani and Quebrada highs with distinctive depositional areas. The Pucayacu, 17 km S of Totos, at the boundary Totos-Paras structural high, meridionally between the Sarhua and Lucanamarca districts, delimited by the Abancay-Andahuaylas­ grey and brown limestones with microfilaments Totos fault system (AAT in Fig. lA), was a (Bositra sp.) of the Socosani Formation prolongation of the Cusco-Puno High, defined repr�sent Aalenian and Bajocian open marine by the Cusco-Lagunillas-Mafiazoand the Urcos­ platform and ridge deposits, equivalent to the Sicuani-Ayaviri fault systems (CLM and USA in Chunumayo Formation. However, they display Fig. lA, CARLOTTO et al. 2011), due to sinistral microbial laminae and centimetric, domal transtensive tectonics. structures in the uppermost levels, indicative In the septentrional area of Totos and Paras, of sedimentary starvation (Fig. lB). Above, the Chunumayo Formation is composed of two well differentiated lutaceous stratigraphic Toarcian-Bajocian marine deposits, 200-500 m intervals surpass 700 m in thickness. The lower

Gray, green and yellow shales with intercalations of calcareous sandstones. Deep Synsedimentaryfolded calciturbidites Q) marine and slump deposits are common. ""§. to deltaic Prevalent olistoliths in the upper levels. � Conglomerates in local levels. .c Cl c: � �------� ro Brown, black and green shales 65 with intercalations of limestones and calcareous sandstones. Offshore m Decimetric carbonate concretions � with septarian cracks in the basai levels.

Gray and brown limestones Shallow N with microfilaments (Bositra sp.). to deep 1�go Contorted beds and microbial laminae m marine 200 km 75• in the levels.

Fig. 1. Location, age, column, lithology, depositional cycle, and setting of the Rio Pumani section. 9th International Congress on the Jurassic System -Abstracts 55

lutaceous interval consists of brown, black and dominant, and Megasphaeroceras [M & m] is green shales with intercalations of limestones the most common ammonoid genus ( 45°/o ) and calcareous sandstones. The upper lutaceous with a species endemic to the southeastern interval is composed of grey and green shales Pacific borderlands. This monospecific group is with intercalations of calcareous sandstones, recorded by shells with unimodal size-frequency where isolated blocks of lowermost Upper distribution of positive asymmetry, dominant Bajocian marine deposits, tens of metres in juveniles, and well displayed dimorphism. Also thickness, are surrounded by at least middle locally common are Leptosphinctinae (26°/o) Upper Bajocian marine deposits. These blocks, and Spiroceratinae (15%). Leptosphinctes [M] observable for a distance of several kilometres - Cleistosphinctes [m] display juvenile and pre­ and interpreted as olistoliths, correspond to adult individuals in the lower lutaceous interval, Late Bajocian and Bathonian deep-water slope whereas Ve rmisphinctes [m] - Prorsisphinctes and basinal deposits. Associated with extensive [M] are mainly represented by pre-adult and thick beds, locally arkosic sandstones with individuals within the upper lutaceous interval. rounded detrital quartz grains and angular Sp iroceras orbignyi is represented by dominant pebbles of Jurassic limestones occur, identified juveniles in the lower lutaceous interval, but S. as olistostromes. These metric olistostromes annulatum is very scarce and restricted to the and the decametric olistoliths composed of, upper lutaceous interval. Cadomitinae (6°/o), and included within, deep-water slope and Lissoceratinae ( 4%), Phylloceratinae (2%), basinal deposits probably are the result of Oppeliinae (1°/o ), and Strigoceratinae (1 °/o ) synsedimentary regional tectonics. are very scarce. Consequently, most of these Bajocian ammonites are scarce in the Bajocian ammonoid genera correspond to adult calcareous interval, but Upper Bajocian individuals and were the result of regional ammonites are locally common in the two necrokinesis and/ or local immigration, without lutaceous intervals. The uppermost Aalenian evidence of sustained colonization, from more Malarguensis Biozone and lowermost Bajocian open marine or exotic oceanic areas. In contrast, levels have been identified by the occurrence Late Bajocian, monospecific populations of Puchenquia (Gerthiceras) cf. mendozana dominated by juvenile individuals and indicative WESTERMANN [Macroconch] and Tmetoceras cf. of sustained-colonization bioevents by eudemic flexicostatum WESTERMANN [M] in the lower part taxa (i.e., in their breeding area) were abundant of the calcareous interval. At the upper levels in the case of Megasphaeroceras [M & m] of this lithologic subdivision, two fragmentary and Sp iroceras [M & m]. These populations specimens of Dorsetensia sp. [M] allow to inhabiting the Arequipa Basin belong to species recognize the Lower Bajocian Humphriesianum endemic to the Andean Province of the Eastern Zone. In the lutaceous intervals, several Pacific Sub realm and to pandemic species of the successive ammonite assemblages characterize Tethys-Panthalassa Realm, respectively. the Upper Bajocian Magnum Biozone. The In conclusion, these Late Bajocian bioevents identified taxa indicate a time span from the of regional appearance of immigrant ammonite latest Niortense Zone to the Garantiana Zone. taxa and even sustained colonization should The uppermost Niortense Zone is characterized be associated with an episode of maximum by the occurrence of Megasphaeroceras cf. deepening, maximum relative sea-level rise, magnum RICCARDI & WESTERMANN [M & m], and highest oceanic accessibility of a second­ Sp iroceras orbignyi (BAUGIER & SAUZE) and order, transgressive-regressive fa cies cycle in Leptosphinctes spp. [M & m]. The Garantiana the Arequipa Basin during the Upper Bajocian Zone is recognized in the upper lutaceous Niortense Zone, although disturbed by regional interval with Megasphaeroceras cf. magnum, tectonics. Sp iroceras orbignyi, S. cf.annul atum (DESHAYES), and Ve rmisphinctes spp. [m & M]. The finding of The research was supported by the scientific projects a single Iniskinites suggests the first Bathonian CGL2011-23947 (MICINN) and GR-6 INGEMMET.

deposits including the uppermost olistoliths at References the top of the upper lutaceous interval. (ARLOTTO, V., RODRIGUEZ, R., ACOSTA, H., CARDENAS, J. Late Bajocian Eurycephalitinae are & }AILLARD, E. 2009. Alto estructural Totos-Paras 56 9thInternational Congress on the Jurassic System - Abstracts

(Ayacucho): lfmite Paleogeografico en la evoluci6n Antartica. In: WESTERMANN, G.E.G. (ed.), The Jurassic mesozoica de las cuencas Pucara (Triasico Superior­ of the Circum Pacific: 122-161, Cambridge University Liasico) y Arequipa (Jurasico-Cretacico). - Sociedad Press, London. Geol6gica del Peru 7: 1-46. WESTERMANN, G.E.G., RICCARDI, A., PALACIOS, 0. & RANGEL, RICCARDI, A.C., GULISANO, C.A., MOJICA, J., PALACIOS, 0. C. 1980. Jur.isico medio en el Peru. - Boletin lnstituto & ScHUBERT, C. 1992. Western South America and Geo16gico Minero y Metalurgico 9: 1-47. 9th International Congress on the Jurassic System - Abstracts 57

The ecological role ofthe Jurassic seafloor:ben thic ecological functioning during the Kimmeridgian OAE

CHRIS L. J. FRID1 * & BRYONY A. CASWELL2

1School of Environmental Sciences, University of Liverpool, Liverpool L69 3GB UK; E-mail: c.l.j.frid@ liv.ac.uk 2School of Environmental Sciences, Universityof Liverpool, Liverpool L69 3GB UK; E-mail: b.a.caswel/@ liv.ac.uk

*Corresponding author

The Late Jurassic Kimmeridge Clay Formation marginal basins than the more extreme periods (KCF; -148-15 5 M a) was deposited in a shallow of global oceanic anoxia. This study uses a semi-restricted basin, the Wessex Basin, in the contemporary multi-disciplinary approach UK. The KCF represents the longest period ( -8 Biological Traits Analysis (BTA) to explore the million years; Weedon et al. 2004) of organic impacts of fluctuating regional hypoxia on the carbon accumulation during the Mesozoic composition and functioning of 21 benthic (TYSON 2004), and it was deposited under palaeocommunities from the KCF in the Wessex fluctuating levels of oxygenation that ranged Basin, Dorset, UK (data from WIGNALL 1990). from dysoxic to anoxic (PEARCE et al. 2010). We could not find any prior application of The presence of isorenieratane biomarkers BTA with palaoentological data. However, it (breakdown products of photosynthetic sulphur is particularly well suited to palaeoecological reducing bacteria) in the KCF indicates that at data as it can be used to compare spatially and times the water column was euxinic (SINNING HE temporally separated communities that may DAMSTE et al. 2001). significantly differ in terms of their species At present day oceanic hypoxia is rapidly composition. increasing globally due to anthropogenic The KCF palaeocommunities contained activities such as climate change and gastropods, brachiopods, scaphopods, eutrophication. We know that deoxygenation bryozoans, serpulids, hydroids, and has profound effects on the marine biota and crustaceans, but were dominated by bivalves. potentially therefore also on the delivery of Significant changes in species composition are ecological functions in benthic systems. The shown within periods of less intense hypoxia ecological functions that could be impacted (CASWELL & FRID 2013), but during these include nutrient regeneration, carbon periods trait composition did not significantly sequestration, and provision of food to differ implying conservation of ecological higher trophic levels. However, we know little function. However, significant changes in about how marine ecosystems will respond palaeoecological functioning occurred between to deoxygenation over long timescales or periods of extremely different palaeo-redox the consequences it will have fo r ecological states. Proportionally more surface living or functioning. Periods of ancient environmental shallow burrowing species with traits suggestive change provide an opportunity to learn lessons of opportunists occurred during periods of low and apply them to the current environmental oxygen availability. The hypoxic communities challenges that we fa ce. had a higher relative abundance of organisms The areal extent of anoxia during the with thinner skeletons ( <0.5 mm) composed of Kimmeridgian of the UK was greater than less soluble fo rms of calcite that may be linked today but less than during the oceanic anoxic to acidity. These changes observed from the events of the past (PEARCE et al. 2010) and thus KCF are similar to those fo r modern benthos represents regional hypoxia-anoxia. Therefore exposed to hypoxia (e.g. Wu 2002). the KCF is a more appropriate analogue for The fu nctional changes that occurred during present-day hypoxia in eutrophic shelf seas and ancient hypoxic events can be used to infer the 58 9thInternational Congress on the Jurassic System -Abstracts magnitude, thresholds, and rates of long-term SAELEN, G. et al. 2000. Contrasting watermass conditions functional change in modern communities. during deposition of the Whitby Mudstone (Lower Jurassic) and Kimmeridge Clay (Upper Jurassic) Results from this study suggest that during de­ fo rmations, UK.-Palaeogeography, Palaeoclimatology, oxygenation benthic functioning will initially be Palaeoecology 163: 163-196. SINNINGHE DAMST J.S. et al. 2001. lsorenieratene maintained, but will collapse once thresholds E are reached. This is consistent with the patterns derivatives in sediments: Possible controls on their emerging fo r contemporary systems where distribution. - Geochimica Cosmochimica Acta 65: 1557-1571. functional collapse is associated with hysteresis TvsoN, R.V. 2004. Variation in marine total organic carbon and threshold effects (CoNLEY et al. 2009). through the type Kimmeridge Clay Formation (Late Jurassic), Dorset, UK. - Journal of the Geological References Society, London 161: 667-673. CASWELL, B.A. & FRID, C.L.J. 2013. Learning from the past: WEEDON, G.P. et al. 2004. Cyclostratigraphy, orbital tuning functional ecology of marine benthos during eight and inferred productivity fo r the type Kimmeridge million years of aperiodic hypoxia, lessons from the Clay (Late Jurassic), Southern England. - Journal of Late Jurassic. - Oikos, in press. the Geological Society, London 161: 655-666. CONLEY, D.J. et al. 2009. Ecosystem thresholds with hypoxia. WIGNALL, P. B. 1990. Benthic palaeoecology of the Late - Hydrobiologia 629: 2129. Jurassic Kimmeridge Clay of England. - Special Papers PEARCE, C.R. et al. 2010. Seawater redox variations during in Palaeontology 43: 1-7 4. the deposition of the Kimmeridge Clay Formation, Wu, R.S. 2002. Hypoxia: from molecular responses to United Kingdom (Upper Jurassic): Evidence from ecosystem responses. - Marine Pollution Bulletin 45: molybdenum isotopes and trace metal ratios. 3545. -Paleoceanography 25: 1-15. 9th International Congress on the Jurassic System - Abstracts 59

Facies patterns and environmental evolution of the Amu Darya Basin and associated basins in central Asia during the Jurassic

FRANZT. FURSICH1 *, MARKUSWI LMSEN2 & HERMANN MUNSCH3

1FG Paliioumwelt GeoZentrum Nordbayern FA U Erlangen-Niirnberg, Loewenichstrasse 28, D-91054 Erlangen, Germany; E-mail: [email protected] 2Senckenberg Naturhistorische Sammlungen Dresden, Ko nigsbriicker Landstrafie 159, 01109 Dresden, Germany 3Total E&P, 2 place de la coupole, 92078 Paris la Defense cedex, France

*Corresponding author

In the Amu Darya Basin of southern Uzbekistan and was followed by a rapidly subsiding rift (Kugitang Mts., Ghissar Mts.), Mesozoic basin filled with marine shales in the Aalenian. sedimentation started in the Early Jurassic. Uplift in connection with the Early Bajocian Late Palaeozoic basement rocks (granites, Mid-Cimmerian tectonic event was followed metamorphics) are covered by paleosol and by a conspicuous transgression starting in the followed by conglomerates and coarse-grained Late Bajocian. Concomitantly, sedimentation sandstones of braided river origin. General changed from a siliciclastic setting to a mixed fining of the sediments up-section is related to carbonate-siliciclastic setting and finally to a levelling of the topography and the development carbonate-dominated system in the Callovian to of an extensive peneplain. Due to the warm, Tithonian. The latter consisted oflarge carbonate humid climate, meandering rivers and la}{es platforms (Lar Formation) and associated slope prevailed, the latter characterized by organic­ and basinal sediments (Dalichai Formation). rich muds and coal layers. This 400-460 m thick In the Koppeh Dagh, sedimentation started succession is late Early Jurassic to Early Bajocian with the marine Kashafrud Formation in the in age. Subsequently, the sea transgressed Late Bajocian, which accumulated in a rapidly across the coastal plain and until the Early subsiding rift basin. Similar to the situation in Bathonian storm-influenced siliciclastic shelf the Alborz region, a carbonate system (Chaman sedimentation prevailed. Sedimentation rate Bid Formation, Mozduran Formation) became decreased up-section and culminated in a established from the Callovian onwards. highly fossiliferous "condensed" unit of Early In SW Kygryzstan, in contrast, non-marine Bathonian age. This deepening trend continued conditions persisted throughout the Jurassic in the Early Callovian with a 200-m-thick marl characterized by rapid subsidence and high unit which represents offshore,lo w-energy shelf rates of sedimentation. Prevailing environments conditions. During the Callovian-Oxfordian were floodplain s swamps and lakes. these strata grade into a several 100-m-thick Sedimentation in all these basins was unit of thick-bedd-ed carbonates of a generally controlled by extensional tectonics up to low-energy carbonate ramp and are replaced in the Middle Jurassic. In addition, climate also the Kimmeridgian up to the end of the Jurassic exerted a major control: Humid conditions in by evaporites. the Early Jurassic changed to increasingly arid This sedimentary succession shows some conditions towards the end of the Jurassic and similarities with those of the Alborz Mts and replaced siliciclastic sediments by carbonates Koppeh Dagh of northern Iran (WILMSEN et and, finally, by evaporites. al. 2009): In the Alborz Mts, an overfilled foreland basin represented by non-marine References WILMSEN, M., FURSICH, F.T., SEYED-EMAMI, K., MAJIDIFARD, siliciclastic sediments (alluvial, fluvial and M.R. & TA HERI, j. 2009. The Cimmerian orogeny in lacustrine systems with widespread coal northern Iran: tectono-stratigraphic evidence from swamps) developed during the Early Jurassic the foreland. - Terra Nova 21: 211-218. 60 9rh International Congress on the Jurassic System - Abstracts

Palaeobiogeography and evolutionary trends in the Oxfordian subfamily Prososphinctinae Gt.OWNIAK, 2012 (Ammonoidea, Perisphinctidae)

EWA GtOWNIAK

Fa culty of Geology, University of Wa rsaw, ul. Zwirki i Wig ury 93, 02-089 Wa rsaw, Poland; E-mail: [email protected]

The phenomenon of palaeobiogeographic margin of the Tethys Ocean from Early to early differentiationof Late Jurassic ammonite faunas Late Oxfordian. Later it disappeared. Offshoots has been noticed as early as in the 19th century of this lineage should be sought outside the area (ZITTEL 1870; NEUMAYR 1873) and soon has of Submediterranean Europe (see e.g., KRISHNA become the basis fo r the modern concept of et al. 1995). We propose a new interpretation of provinces (e.g., WESTERMANN 2000; PAGE 2008). the evolutionary diversification of the Oxfordian Two main ammonite domains (provinces) perisphinctid stock with emphasis on the have been distinguished in the Jurassic marine Prososphinctinae lineage. Based on some new basins in Europe: the Mediterranean Province biostratigraphic and taxonomic evidence (e.g. with the Submediterranean (Sub) Province, and GtOWNIAK et al. 2010), and taking into account the Boreal Province with the Subboreal (Sub) some older contributions (WIERZBOWSKI 1976; Province. While much attention has been paid MELENDEZ et al. 1988; OLORIZ et al. 2008) we to the Late Oxfordian and Early Kimmeridgian regard that the Prososphinctinae lineage splits ammonite biogeography due to its impact in the Middle Oxfordian into two branches: The on the inter-provincial biostratigraphic first is the Subboreal branch, which gave rise to correlations (e.g., MATYJA et al. 2006), we know the species of Decipia ARKELL and its successors still relatively little about the early stages of in the lineage of the family Aulacostephanidae palaeobiogeographic ammonite differentiation SPATH, in the areas of northern Europe. The in the Early Oxfordian. Our studies are intended second is the Mediterranean-Submediterranean to supplement this gap. The research is aimed bra�ch which, fo r example, gave rise to the at the Submediterranean ammonites broadly genus Vinalesphinctes and its allies in the assigned to the Oxfordian perisphinctids, with perisphinctid subfamily Vinalesphinctinae special attention to the Early Oxfordian genus MELENDEZ & MYCZYNSKI, in Cuba. Both Prososphinctes SCHINDEWOLF. The purpose of new lineages, Aulacostephanidae and this study is to characterise the stratigraphic Vinalesphinctinae, emerged in the late Middle and palaeobiogeographic significance of the Oxfordian. Stratigraphic horizons of their recently erectedsubfamily Prososphinctinae appearance roughly correlate with, but are GtOWNIAK, 2012, based on Prososphinctes. The slightly younger than, the level of early Middle subfamily embraces a lineage of some Early to Oxfordian maximum of sea-level rise (e.g., early Late Oxfordian species. Taxonomically, WIERZBOWSKI 2002). The latter is marked by they are assigned to the following successive occurrence of the Platysphinctes bioevent­ genera: Prososphinctes Liosphinctes, horizon as evidenced in the neritic carbonate

Platysphinctes - and Larcheria, plus a few less fades of southern Poland (GtOWNIAK 2000, known taxa whose usefulness for taxonomy of 2006a). This, and also a lower biovent-horizon Oxfordian ammonites is disputable (e.g., GYGI (Prososphinctes Acme Horizon in the Lower 1998; GtOWNIAK & WIERZBOWSKI 2007). The Oxfordian of southern Poland) point to the distinctive character of this lineage lies in the species of the subfamily Prososphinctinae as discontinuous palaeobiogeographic spread of a useful potential tool for multi-proxy marine its species and their recurrent stratigraphic palaeoenvironmental studies. ranges, with a tendency to fo rm bioevent­ References horizons (GtoWNIAK 2000, 2006a, b, 2012). Gt.OWNIAK, E. 2000. The Platysphinctes immigration The lineage of Prososphinctinae persisted in event in the Middle Oxfordian of the Polish Jura seas of southern Europe adjoining the northern Chain (Central Poland). - Acta Geologica Polonica 50: 9th International Congress on the Jurassic System - Abstracts 61

143-160. MATYJA, B.A., WIERZBOWSKI, A. & WRIGHT, J.K. 2006. The Gt.OWNIAK, E. 2006a. The Platysphinctes immigration Sub-BorealjBoreal ammonite succession at the event: biostratigraphic and paleobiogeographic Oxfordian/Kimmeridgian boundary at Flodigarry, implications for the Middle Oxfordian (Late Jurassic) Staffin Bay (Isle of Skye), Scotland. - Transactions of seas of central Europe (NW Germany and Poland). the Royal Society of Edinburgh, Earth Sciences 96: - Neues Jahrbuch fur Geologie und PaHiontologie, 387-405. Abhandlungen 241: 155-201. MELENDEZ, G., SEQUEIROS, L., BROCHWICZ-LEWINSKI, W., Gt.OWNIAK,E. 2006b. The correlation of the zonal schemes MYCZYNSKI, R. & CHONG, G. 1988. Paleobiogeographic at the late Middle to early Late Oxfordian boundary relationship between Oxfordian ammonite faunas from (Jurassic) in the Submediterranean Province: Poland the Mediterranean, Caribbean, and Andean provinces. and Switzerland. - Acta Geologica Polonica 56: 33- In: WIEDMANN, J. & KULLMANN, }. (eds.), Cephalopods 50. Present and Past. 425-436, Schweizerbart'sche Gt.OWNIAK, E. 2012. The perisphinctid genus Verlagsbuchhandlung, Stuttgart. Prososphinctes SCHINDEWOLF (Ammonoidea, NEUMAYR, M. 1873. Die Fauna der Schichten mit subfamily Prososphinctinae nov.): an indicator of Aspidoceras acanthicum. Abhandlungen der palaeoecological changes in the Early Oxfordian kaiserlich-koniglichen Geologischen Reichsanstalt 5: Submediterranean sea of southern Poland. - 141-257 Neues Jahrbuch fiir Geologie und Palaontologie, OLORIZ, F.,VILLASENOR, A.B. & LOPEZ-PALOMINO, I. 2008. Abhandlungen 264: 117-179. Middle Oxfordian ammonite biostratigraphy of Gt.OWNIAK, E. & WIERZBOWSKI, A. 2007. Taxonomical the Lower Santiago Formation at Taman, San Luis revision of the perisphinctid ammonites of the Upper Potosi, Mexico, with notes on Mexico-Caribbean Jurassic (Plicatilis to Planula zones) described by ochetoceratins. - Revista Mexicana de Ciencias J6zef Siemiradzki (1891) from the Krak6w Upland. ­ Geol6gicas 25: 261-283. Volumina Jurassica 5: 27-137. PAGE, K.N. 2008. The evolution and geography of Jurassic Gt.OWNIAK, E., KISELEV, D.N., ROGOV, M., WIERZBOWSKI, ammonoids. - Proceedings of the Geologist's A. & WRIGHT, J.K. 2010. The Middle Oxfordian to Association 119: 35-5 7. lowermost Kimmeridgian ammonite succession at WESTERMANN, G.E.G. 2000. Marine fa unal realms of Mikhalenino (Kostroma District) of Russian Platform, the Mesozoic: review and revision under the new and its stratigraphical and palaeobiogeographical guidelines for biogeographic classification and importance. - Volumina Jurassica 8: 5-48. nomenclature. - Palaeogeography, Palaeoclimatology, GYG R. 1998. Taxonomy of perisphinctid ammonites of the Palaeoecology 163: 49-68. 1, Early Oxfordian (Late Jurassic) from near Herznach, WIERZBOWSKI, A. 1976. Oxfordian ammonites of the Pinar Canton Aargau, Switzerland. - Palaeontographica A del Rio province (western Cuba), their revision and 251: 1-37. stratigraphical significance. -Acta Geologica Polonica KRISHNA, J., MELENDEZ, G., PANDEY, B. & PATHAK, D.B. 26: 137-260. 1995. Characterisation of the ammonite genus WIERZBOWSKI, H. }R. 2002. Detailed oxygen and isotope Larcheria (Middle Oxfordian) in Kachchh (India): stratigraphy of the Oxfordian in Central Poland. - biostratigraphy and palaeobiogeographic evaluation Geologische Rundschau 91: 304-314. in the context of Tethyan occurrences. - Comptes ZITTEL, K.A. 1870. Die Fauna der alteren Rendus de l�cademie des Sciences de Paris, ser. 2a, Cephalopodenfiihrenden Tithonbildungen. 321: 1187-1193. Palaeontographica, Supplement 2: i-vii, 1-373. 62 9th International Congress on the Jurassic System - Abstracts

Jurassic geology and biostratigraphy of the Early Callovian in the Kanev district area (Cherkassy region, Ukraine)

DENIS GULYAEV1 *, ALEXEI IPPOLITOV2 & DMITRY KISELEV3

1/nterdepartmenta/ Stratigraphic Committee (ISC) of Russia, 25-7 Chekhov St., 150054 Ya roslavl, Russia; E-mail: dg [email protected] 2Geo/ogica/ Institute of Russian Academy of Sciences, 7 Pyzhevski Lane, 11901 7 Moscow, Russia; E-mail: [email protected] 3Yaros/avl State Pedagogical University, Respub/ikanskaya st., 150000 Ya roslav/, Russia; E-mail: dnkise/[email protected]

*Corresponding author

The Jurassic deposits of the Kanev district area Biostratigraphic analysis of the ammonite (Fig. 1) are known since the first half of the 19th record of the Lower Callovian succession century, but yet studied poorly. Biostratigraphic allowed to distinguish the presence of 13 schemes, available for the area, are still fa r biohorizons (Fig. 2), 12 of which are known from satisfyingconsider ing the modern level of from NW Europe and European Russia, and knowledge in ammonite biostratigraphywith its one is new, with the index species transitional detailed infrazonal subdivisions, and contains between typical Paracadoceras e/atmae and several inconsistencies. However,Jur assic rocks Cadochamoussetia tschernyschewi and yet to of the Kanev area potentially should provide be described. The sequence of biohorizons a key to interregional correlations due to the characterize four ammonite zones, the lower location near the Pripyat strait connecting two of which (Elatmae and Subpatruus zones) East European epicontinental seas with West are part of the regional succession of European European ones. Russia, and the upper two (Koenigi Zone During the fi eld seasons of 2011 and 2012 including Gowerianus, Curtilobus, Galilaeii ten Jurassic sections, together fo rming the full subzones and Calloviense Zone, including succession, were studied by the authors in the Calloviense and Enodatum subzones) are part Kanev area, accompanied with careful bed-by­ of the Euporean Subboreal zonal standard. bed sampling of ammonites and belemnites. Early Callovian ammonite successions of Collection of studied fossils totally counts about 300 ammonites and over 750 belemnites. Some preliminary biostratigraphic results have already been published (KISELEV & IPPOLITOV J .: 2011). ·�--" The Jurassic ofthe Kanev district is strongly \ . \ , . ,,,.. · ... -.\ . , . tectonically disturbed and split into numerous .... . · . tectonic slivers during the Pleistocene glacial .... , , epochs. The deposits are composed of a thick

. __ _ series of coastal terrigenous rocks (clays and ... � .., sands) of mostly Bathonian age with no marine \ -. macrofossils, overlain by silt to clay deposits ·[b�\Yl[]& '· I ·, with abundant carbonate matter and numerous . ., ...... ,.� marine macrofossils of Early Callovian age. ( ! Contrary to old literature data, younger Jurassic rocks were not found in the district. Middle 100 km Jurassic strata are covered everywhere by sands � of Cretaceous and Paleogene age, tectonically disturbed in the same way. Location of the Kanev district area (arrowed). Fig. 1. 9th International Congress on the Jurassic System -Abstracts 63 the Kanev district also have a good potential to solely boreal forms belonging to the family provide further detailed infrazonal subdivision Cylindroteuthidae occur. In this interval 4 or 5 in the interval of the subgenus Kepplerites biohorizons can be established, and this is close ( Gowericeras) range (biohorizons K. toricelli to the resolution of the ammonite infrazonal to K. galilaeii), as it was proposed for Central scale. However, Boreal belemnite assemblages Europe and England by M6NNIG (2010). from this interval are almost not known in the Belemnite data can also provide detailed adjacent regions (E and W Europe, European subdivision of the succession, in particularly, in Russia) either due to the rarity of finds or to poor the interval ofthe Elatmae Zone to K. gowerianus preservation. Thus, tracing this unit outside the biohorizon of the Gowerianus Zone, where the Kanev area is a challenge fo r the future.

North-West Europe Eastern Europe (modified after Callomon et al., 1988, 1989; Cariou Hantzpergue & �------1997; Cox, Sumbler, 2002; Dietze et al., 2007 etc.) European Russia (by Gulyaev, 2001, 2005; w w England Germany Gulyaev et al., 2002 etc.) z z 0 0 N N B i o h orizons

C. enodatum aeeta Lacune C. enodatum enodatum [=enodatum w y] w (/) C. enodatum planicerclus C. enodatum planicerclus (/) z [=enodat. 13] (A. difficilus) [=enodatum 131 z w w > C. pagei [=enodatum a] > 0 ensis 0 ..J ....I ..J ?Lacune ..J et G) S. micans S. micans et 0 r::1/) 0 G) ·;: S. calloviense S. calloviense .B S. calloviense c;; 0 S. ' · i ci:s � � � � � ��; ���r!!�� f0� � � � ��. K. galilaeii :; :; (!) ?Lacune 1/) curtilobus 5 ::1 K. 5 z -'l z . w ..2 w � 0 0 ::1 densicostatus � 0 K. � G)' Ill ::I gowerianus � r:: �-a - K. Ons ;;: (!)· ·------toricelli toricelli ----·------K. K.

1/) M. polyptychus ::1 (M. kamptus - y) ?Lacune E0. M. kamptus 13 C-ch. subpatruus �CIS M. kamptus a C-ch. surensis (M. herveyi) 11 Lacune ------C-ch. surensis M. terebratus I > 1/) y w ::1 C-ch. tschernyschewi > c;.... . M. terebratus 13 0:: -'l w Lacune :I: e ? {:!. M. terebratus a elatmae P. w et chvadukasyense MS M. verus Cad. quenstedti P. :E ·;;:G) (Cad. quenstedti) � Q. ....I a. w keppleri G) keppleri keppleri � K.(M. jacqu- K. 11 M. jacquoti (M.K. jacquoti) ------oti) keppleri poultoni K. I P. 2. Infrazonal ammonite scale for the Early Callovian of the Kanev district area (grey column) and its correlation Fig. with infrazonal scales for European Russia and NW Europe. Abbreviations: A. Anaplanulites, C. Catasigaloceras, Cad. - - Cadoceras, Ch. Chamoussetia, C-ch. Cadochamoussetia, K. Ke pplerites, M. Macrocephalites, 0. Oxycerites, P. ------Paracadoceras, Pr. Proplanulites, S. Sigaloceras. - - 64 9thInternational Congress on the Jurassic System -Abstracts

The study was supported by RFBR grant NQ12-05- Callovium m it Si.idenglandund Frankreich. - Zitteliana 00380-a. A47: 105-125. GULYAEV, D.B. 2001. Infrazonal ammonite scale for the References Upper Bathonian-Lower Callovian of Central Russia. CARIOU, E. HANTZPERGUE, H. ( eds.) 1997. Biostratigraphie - Stratigraphy and Geological Correlation 9: 65-92. & du Jurassique ouest-europeen et mediterraneen: GULYAEV, D.B. 2005. Infrazonal subdivision of the Upper zonations paralleles et distribution des invertebres Bathonian and Lower Callovian of the East-European et microfossiles. - Bulletin des centres des recherches Platform by ammonites. Jurassic System of Russia: Elf, Exploration et Production, memoire 17: 1-440. Problems of stratigraphy and paleogeography. First CALLOMON, J.H., DIETL, G. & PAGE, K.N. 1988. On the All-Russian meeting. - Scientific materials: 64-70. [in ammonite fauna) horizons and standard zonations Russian] of the Lower Callovian Stage in Europe. - 2nd GULYAEV, D.B., KISELEV, D.N. & ROGOV, M.A. 2002. International Symposium on Jurassic Stratigraphy, Biostratigraphy of the Upper Boreal Bathonian and Lisboa: 359-376. Callovian of European Russia. - 6th Intern. Symposium CALLOMON, J.H., 0IETL, G. & NIEDERHOFER, H.-J. 1989. on the Jurassic System, Mondello, September 16-19, Die Ammonitenfaunen-Horizonte im Grenzbereich 2002. Abstracts and Program: 81-82. BathoniumfCallovium des Schwabischen Juras und KISELEV, D.N. IPPOLITOV, A.P. 2011. New data on & deren Korrelation mit W-Frankreich und England. - Callovian biostratigraphy of Kanev Dislocation area. Stuttgarter Beitrage zur Naturkunde B 148: 1-13. - Jurassic System of Russia: Problems of stratigraphy Cox, B.M. SuMBLER, M.G. 2002. British Middle Jurassic and paleogeography. Fourth AII-Russian meeting. & Stratigraphy. - Geological Conservation Review 26: Scientific materials: 103-106. [in Russian] 508 p. M6NNIG, E. 2010. On the systematic of the ammonite DIETZE, V., SCHWEIGERT, G., CALLOMON, J.H., DIETL, G. & genus Ke pplerites and its occurrence in the Koenigi KAPITZKE, M. 2007. Der Mitteljura des Ipf-Gebiets Zone (Callovian, Middle Jurassic) of Central Europe (ostliche Schwabische Alb, Si.iddeutschland). and England. - Earth Science Frontiers 17, Special Korrelation der si.iddeutschen Ammoniten­ Issue: 117-119. Faunenhorizonte vom Ober-Bajocium his zum Unter- 9th International Congress on the Jurassic System -Abstracts 65

Morphological variations in the ichnogenus Hillichnus: a record from the Jaisalmer Formation, Rajasthan, India

SHWETA S. GURAV1 & KA.NTIMATI G. KULKARNl' *

Agharkar Research Institute, G G Agarkar Road, Pune 411 004, India; 1E-mail: [email protected]; 2E-mail: kg ku/[email protected]; kantimatik@gmail. com

*Corresponding author

The compound bivalve trace fossil Hillichnus of the succession point towards a fluctuating /obsensis has been discovered on the upper rate of sedimentation. Towards the top, the surface of a yellow, cross-bedded, gently dipping sediments became rich in organic matter as is calcarenite of the Hamira Member, Jaisalmer indicated by the presence of abundant repichnia Formation (Bajocian) exposed southeast and fodinichnia. of Jaisalmer city. Four morphological levels The Level C is indicated by a feather-like described by BROMLEY et al. (2003), viz. A, B, meandering structure fo rmed due to a cluster C, and D are very well represented. Signatures of lateral lamellae arranged on both side of of Level E are hardly present but can be a central line. The basal tube, in contrast, unequivocally established when its expression giving rise to thick-lined oval to bean-shaped in 3D becomes available. The dominance of structures arranged in zigzag fashion points a deposit-feeding strategy of the organism is towards the level D morphology of Hillichnus. indicated by the maximum development oflevel B and C. The trace fossils Gy rochorte, Ta enidium, References Rosse/ia, and Rhizocoral/ium are also present BROMLEY, R.G ., UCHMAN, A., GREGORY, M.R. & MARTIN, A.J. 2003. Hillichnus lobosensis igen. et isp. nov., a in the Hillichnus-bearing calcarenite unit. The complex trace fo ssil produced by tellinacean bivalves, alternation of argillaceous and sandy sediments Paleocene, Monterey, California, USA. - Palaeogeography, and low-angle cross-bedding in the upper part Palaeoclimatology, Palaeoecology 192: 157-186. 66 9rh International Congress on the Jurassic System - Abstracts

Early-Middle Jurassic chemostratigraphy, black shale, and sea-level change: evidence for cyclically repeated global change events

STEPHEN P. HESSELB01 *, CHRISTOPH KORTE2 & CLEMENS V. ULLMANN3

1Department of Earth Sciences, University of Oxfo rd, South Parks Road, Oxfo rd OX1 3AN, UK; E-mail: [email protected] 2Department of Geography and Geology & Nordic Center fo r Earth Evolution (NordCEE), Universityof Copenhagen, Copenhagen, Denmark; E-mail:[email protected] 3 Department of Geography and Geology & Nordic Center fo r Earth Evolution (NordCEE), Universityof Copenhagen, Copenhagen, Denmark; E-mail:[email protected]

*Corresponding author

OfJurassic palaeoenvironmental change events, boundary (KORTE & HESSELBO 2011) and also the Toarcian Oceanic Anoxic Event (T-OAE) another within the Sinemurian (RIDING et al. stands out as being potentially the premier 2013). More uncertain are putative 'ice house' 'supergreenhouse' episode. In addition to interludes in the Late Pliensbachian and during clear carbon-isotope signatures, a range of the Aalenian and Bajocian. New high-resolution other isotopic, elemental, sedimentological and stratigraphically extensive elemental and palaeontological anomalies have been and isotopic datasets are now allowing us to described by multiple authors over the last place all these warm and cold events firmly three decades. The T- OAE palaeoenvironmental in a chronological context, and to determine changes clearly affected both marine and non­ relationships to other Earth system events such marine settings and recent studies confirm both as LIPs more accurately. the global impact of the T- OAE on a multitude of Earth systems and also the unique magnitude of change represented by the event. On the other References hand it is also becoming clear that several other KORTE, C. & HESSELBO, S.P. 2011. Shallow-marine carbon- and oxygen-isotope and elemental records times in the Jurassic are likewise characterised indicate icehouse-greenhouse cycles during the by repeated global carbon-cycle perturbations Early Jurassic. - Paleoceanography 26: PA4219, and associated palaeoenvironmental changes, doi:10.1029/20 11PA002160. these greater in magnitude than anything RIDING, J.B., LENG, M.J., KENDER, S., HESSELBO, S.P., & FEIST- 8URKHARDT S. 2013. Isotopic and palynological experienced by the planet during the Cenozoic. evidence fo r a new Early Jurassic environmental Of particular significance are a major black perturbation. - Palaeogeography, Palaeoclimatology, shale event at the Sinemurian-Pliensbachian Palaeoecology 374: 16-27. 9rh International Congress on the Jurassic System - Abstracts 67

Refinedpalaeoen vironmental analysis based on changes in macrobenthic communities - A case study from the Kimmeridgian of Normandy

MANJA HETHKE*, TOBIAS FELSCH & FRANZ T. FiiRSICH

GeoZentrum Nordbayern, FG Pa/iioumwe/t, Universitiit Erlangen-Niirnberg, Loewenichstrafie 28, D-91 054 Erlangen, Germany; Email: manja.hethke@fa u.de

*Corresponding author

The reconstruction of past ecosystems involves 0°03'57.S"E; 49°33'15.51"N, 0°05'14.S"E; the identification of abiotic components and 49°34'34.12"N; 0°6'9.06"E) were considered the biotic response, documented particularly in this study. Section 1 was measured in Lower in ecological communities. Here, we use Kimmeridgian strata near Cap de La Heve; community relicts from marine Kimmeridgian sections 2 and 3 belong to different members deposits of the Normandy coast, France, to of the Upper Kimmeridgian Argiles d'Octeville. reconstruct subtle changes in environmental The base of Section 2 extends downwards into parameters, comparing sedimentological the upper members of the Lower Kimmeridgian, evidence with biogenic signals. represented by Assemblage 2 in Fig. 1. Kimmeridgian deposits in NW-Europe are Lithologies range from calcareous mudstones to widely regarded as having been deposited under siliciclastic mudstones, both often featureless. a range of environmental regimes from oxic to The environment represented by sections 2 and oxygen-depleted conditions (e.g., WIGNALL & 3, drawn from the rather uniform lithological NEWTON 1998). Major controls on the faunal evidence, is characterized by soft substrates distribution in the English Kimmeridge Clay below the storm wave-base. In contrast, Section Formation are oxygen levels, substrate, and the 1 can easily be distinguished from the other two dispersal rate of organisms (WIGNALL 1990). by its sedimentary features. Carbonate contents Kimmeridgian rocks of the Normandy coast were higher and substrates more compacted and crop out between Cap de la Heve (Le Havre) and firm. Soft substrates alternated with firm- and Ecqueville with a northward regional dip and a hardgrounds, which are indicated by glauconite­ generally argillaceous lithology,disp laying more impregnated, bored, and encrusted surfaces, calcareous levels near the base (SAMSON et al. implying strongly reduced sedimentation rates 1996). Three short sections ( -49°30'43.5"N, at times.

b 2 0 SO % 25 Aulacomye/la sp.

CO 0 1

<0 0 Corbulomima prora IUII�IIPfaunal rfb 2 n-feeder

Pa/aeonucu/a menkii N 0 3 al mobile it-feeder

0 0 Ass 3 Protocardia morinica Section 3 Section 2 w infaunal �I ension-feeder

Hierarchical cluster analysis (a) and guild distribution in assemblage 2 of section 2 (b). Sample groupings delineate Fig. 1. the three studied sections very well. 68 9th International Congress on the Jurassic System - Abstracts

Dominantecological guilds lnfaunal suspenslon·feecle111 • . Eplfaunalsuspension- feeders D Epifaunalgrazers

N lnfaunal camlvores .!! >. ci !-& :8�c: � s-c: c: � A2 ·-�� lti • :::J � i� N O• fJ) O C �·u; � o;��� "CO

N • 9 A1

-0.2 0.0 0.2 0.4 0.6 MDS1 (34.04%)

firm- to softgrounds hardgrounds 2. Principal coordinates analysis. The first three PCO axes explain 34.04 %, 25.68 % and 14.84 % ofthe total variance Fig. in the dissimilarity matrix. Ecological guilds of the most abundant fa unal elements within each sample are colour-coded. Mixed guild compositions were signified, when the most abundant taxon was below SO % and the ecological guild of the second most abundant taxon different from the fo rmer.

Qualitative biogenic evidence in Section 1 of Corbulomima, Protocardia, and Palaeonucu/a. came from trace fossils, such as scratch marks Association 2 is entirely made up of Section preserved on the walls and fills of Thalassinoides 3 samples, which are characterized by burrows, implying firm substrates. Podichnus the shallow infaunal, suspension-feeder traces on brachiopod shells show that Corbulomima prora. Notable other taxa are secondary hardgrounds were exploited by Nicaniel/a extensa, Nanogyra virgula, and the brachiopods. Quantitative biogenic evidence gastropod To rnatel/aea. Assemblage 3 is an involved the collection of abundance data almost monospecific shell bed of Nanogyra for a set of horizons and the identification of virgula. Diversities are highest in Association 3 underlying environmental signals with the help with Nanogyra virgula and Corbulomima prora of ordination techniques. Palaeocommunity dominating. Other notable species are Gervil/el/a differences should reflect changes in ancient cf. aviculoides, Grammatodon concinnus, and physico-chemical parameters (abiotic Protocardia morinica. components). Main ecological guilds identified are The statistic treatment of the dataset epifaunal suspension-feeders, infaunal resulted in three associations (Ass. 1-3) suspension-feeders, infaunal carnivores, and and three assemblages (A1-A3; Figs 1, 2). epifaunal grazers. Various transitions between Taxa responsible for the sample groupings these four occur. All species of the above are as follows. Assemblage 1 is governed by mentioned ecological guilds of sections 2 and 3 terebratulids. Association 1 is characterized are adapted to softsub strates, consistent with by Nanogyra nana with minor occurrences of the sedimentary evidence. brachiopods, gastropods, and Corbulomima Palaeocommunity analysis picks up a more prora. Assemblage 2 is dominated by refined signal than the sedimentary evidence Aulacomyel/a, with less abundant occurrences does, clearly separating section 2 from section 3, 9rh International Congress on the Jurassic System -Abstracts 69 which are dominated by epifaunal and infaunal parameters that shape the distribution pattern suspension-feeders, respectively. However, of the benthic macrofauna, often much better single assemblages may represent episodic than sedimentary analysis does. fluctuations in environmental parameters. Assemblage 2 (Fig. 1 b), for example, reveals an oxygen-restricted, soft substrate environment. References In addition, the biotope must have been similar SAMSON, Y., LEPAGE, G., HANTZPERGUE, P., GUYADER, J., in sections 2 and 3 during the time the epifaunal SAINT-GERMES, M., 8AUDIN, F. & 8IGNOT, G. 1996. Revision lithostratigraphique et biostratigraphique reclining oyster Nanogyra virgula colonized the du Kimmeridgien de la region havraise (Normandie). Kimmeridgian sea floor (A3 and Ass. 3). The - Geologie de la France 3: 3-19. ordination picks up a substrate signal ranging WIGNALL, P. B. 1990. Benthic palaeoecology of the Late from softgrounds to firm- and hardgrounds on Jurassic Kimmeridge Clay of England. - Special Papers MDSl, and possibly increasing sedimentation in Palaeontology 43: 1-7 4. WIGNALL, P. B. & NEWTON, R. 1998. Pyrite framboid rates and nutrient supply towards Association diameter as a measure of oxygen deficiency in ancient 2 on MDS2. In summary, palaeocommunity mudrocks. - American Journal of Science 298: 537- analysis unravels the physico-chemical 552. 70 9rh International Congress on the Jurassic System - Abstracts

Foraminifera and the end-Triassic biotic crisis at the T-J boundary in the Northern Calcareous Alps

AxELVO N HILLEBRANDT

Institut fii r Angewandte Geowissenschaften, Te chnische Universitiit Berlin, Ernst-Reuter-Platz 1, 10587 Berlin; £-mail: axe/. vonhillebrandt@campus. tu-berlin.de

Sections with continuous sedimentation across species of which are described, are rare in all the T-J boundary are found in the Northern samples. Allochthonous and autochthonous Calcareous Alps in three basins, which extend in fo raminifers mainly occur in the upper part west-eastdirection. In the North, in theareaofthe of the Zlambach Beds. The allochthonous Lechtal and Allgau nappes, existed a carbonate fo raminifers are derived from shallower areas platform with intraplatform depressions, the and can make up a considerable part of the (1) Allgau Basins, and sedimentary sections assemblages. On top of the Zlambach Beds across the T-J boundary. South of that area the follow some meters of mm-bedded, silty to fine­ (2) Eiberg Basin is located, an intraplatfrom sandy, weakly calcareous beds, which mostly depression with Triassic and J urassic sediments, lack fo raminifers or contain only tiny and which can be traced over 200 km from the probably reworked Nodosarioidea. One sample Salzkammergut (Upper Austria) in the East to (probably from the lower part) yields a low the Lahnewiesgraben Gorge (Bavaria) in the diverse fo raminiferal assemblage (e.g. Annulina, West. Many T-J boundary sections of this basin compressed Trochammina, Marginulinopsis), have been studied. In the western part of this which also occurs in the Eiberg Basin in a similar basin the Karwendel Syncline contains the GSSP stratigraphic position (Fig. 1). Above these of the T-J boundary (HILLEBRANDT et al. 2007). beds there exist outcrops with more or less In its south-eastern part the Eiberg Basin is argillaceous and micaceous marls ( =Diirrnberg bordered by a Rhaetian platform with locally Formation), which are at least 10 to 20 m thick, fringing reefs and, further to the South, with containing the earliest Jurassic ammonites an outer shelf, the (3) Hallstatt Basin, which is (Psiloceras spe/ae tirolicum in the middle and P. transitional to the Tethys Ocean. cf.til manni in the upper part). These marls yield The T- J boundary sediments mostly consist a diverse and normal-sized fo raminiferal fauna. of washable marls and clays containing more Nodosarioidea predominate but agglutinated or less rich and well preserved microfaunas fo raminifers may also be abundant. Apart from of foraminifers, ostracods, and additional Dentalina, Ichthyolaria mesoliassica n. spp. microfossils (HILLEBRANDT et al. 2007). sensu KRISTAN-TOLLMANN (1964) and Lingulina Changes in sedimentation and palaeoecological tenera col/enoti are abundant. The latter both conditions in time and space are reflected by the rarely occur in the Zlambach marls. L. tenera micro faunas. The three basins are characterized collenoti is most common in the Pre-Planorbis by differentfo raminiferal assemblages. Beds and Planorbis Zone of Britain. Within a The probably more than 150-m-thick lumachelle of the upper part of the section some Rhaetian Zlambach marls of the Hallstatt Basin foraminifers reappear that already existed in yield a high-diverse fauna of foraminifers. the Zlambach Beds. Oberhauserellidae are more KRISTAN-TOLLMANN (1964) described 54 genera or less abundant. with 245 species. Nodosarioidea predominate The most complete boundary sections of with 14 genera and 136 species, but they the Eiberg Basin are fo und in the Karwendel are taxonomically oversplit. Textulariina are Syncline. Marly interlayers of the Upper represented in this monograph by 19 genera Rhaetian Oxycolpella Beds contain a diverse and 39 species, and some additional genera and microfauna of Nodosarioidea (Fig. 1). The species have been recorded. Large-sized species Koessen Formation ends with a bed (T Bed, Fig. of Annulina, Ammodiscus, and Glomospira can 1), which contains high-diverse Nodosarioidea be abundant. Miliolina, eight genera and 13 at its marly base. Within this bed the diversity 9th International Congress on the Jurassic System - Abstracts 71

12< Hippocrepina, -;:!.-;:!.-;: Trochammina A-A-A--::. =A A -A-A- -- -- 1/) A - - ,_ "iii A A Q) A-A-A--=- LJ ·0;:: =A A Peak E -A-A- 0 -::. Schattwald Beds phase Q) () -AA=-A-A A 1'1! A -=- � () -A-A=A -A c: -- -- Q) A-A-A LJ -A-A- c: � A =A -=- A 0 C> 11< = !:- ] -=: Marginu/inopsis :g c: !,.- A =� c: � - Q) � t= c: ==== w Medium «< -:. Marginulinopsis, ·- 10< -=.. -=.. -=.. phase - ::::-��1--rew. lnvolutinidae Q) 9.,�:;��===� �Troch. , NoQosar. parv. sp. «< R.' ��--- ....T rochammma - � "" Nodosarioidea div. sp 0:::.r= �Choristoceras marsfii . Initial T Bed 6... 7 E 'f.!:7 ..., ;!;'?±�;!; 'Nodosarioidea div. sp. phase { 7 _ Q) �Nodosarioidea mult. sp. - 1 1 1 1 1 «< I I I I ..J J l I J 1 I I I I I I I I I I I I I I I I I I I I I I Q) c: I I I I I 0 I I I I N I I I I I I I I I (ii :;:� I I I I I LJ I I I I E en c: 0 Q) E I I I I I Cl) :g Equi- � � I I I I c: e> Q) m librium Q) u 1 I I I I I � LJ .9 phase I I I I (J.) m � -� I I I I I Nodosarioidea mult. sp. 0 4 a.. (.)� I I I I I I I I I 3 Nodosarioidea mult. sp. I I I I I I I I I I I I I Nodosarioidea mult. sp. 2- =+=+=+= I I I I I I I I I

Nodosarioidea div. sp. 1 ( : : : : ---- I I I I I I I - + - CaC03 Om I I I I I 31 -29 -27 -25 I I I I saturation

Schlossgraben Section (HILLEBRANDT & KMENT 2009), ICIE = Initial Carbon Isotope Excursion (RUHL et al. 2009). Fig. 1. decreases and the top of the bed is formed and are transitional to the grey Tiefengraben by a laminated, approximately 1-cm-thick, Member with the Rhaetian-Jurassic boundary bituminous layer with a strongly reduced in its lower part. A large-sized Ammobaculites Rhaetian fo raminiferal fauna. The following species is common to very abundant in many 3-cm-thick argillaceous, nearly non-calcareous samples of this member. In the lower part it eo­ bed contains only compressed Trochammina. occurs with common to abundant small-sized Above a bed with cylindrical traces and a poor Eoguttulina, less common are Dentalina and fauna of Nodosarioidea follows. Large-sized smooth-shelled Lingulina. The Lingulina tenera Marginulinopsis characterize the bordering group is very rare. Uncompressed, small-sized grey to yellowish marls (Fig. 1). These Trochammina are present in some samples of marls grade into red, mostly well-bedded, the lowest part. Nodosarioidea are low diverse, weakly calcareous, red clayey marls with in the middle part of the member their diversity Hippocrepina and compressed Trochammina. is a little higher. Attached Ammodiscidae can These Schattwald Beds are some meters thick be abundant in the upper part of the lower 72 9th International Congress on the Jurassic System - Abstracts member and up to the lower part of the upper the beginning CAMP volcanism and the first member. Ammobaculites disappears in the step of the biotic crisis at the T-J boundary uppermost samples of the member. Lenticulina, interval, and is connected with the ICIE (Fig. 1). Astacolus, and the Lingulina tenera group can be Trochamminaandlarge-sizedMarginulinopsisor abundant in the uppermost part of the member. Trochammina and Oberhauserella characterize Oberhauserellidae are rare to abundant. A this event. A relatively rapid sea-level fall took very similar evolutionary lineage compared place which continued until the deposition with that of the Hallstatt Basin eo-occurs with of the Schattwald Beds. The interval of the Praegubkinel/a turgescens at the T-J boundary Schattwald Beds and the corresponding beds of interval. A new Reinholdel/a species appears 1 the Hallstatt Basin are characterized by a low to 1.5 m above the T-J boundary. Together with content of carbonate caused by a strong rise of Ammobacu/ites this new species dominates the C0 , with the consequence of a further faunal 2 fo raminiferal faunas of many samples from the crisis. Mainly foraminifers adapted to shallow middle part of the Tiefengraben Member. marine conditions could not survive this Only low-diverse and undersized continuous crisis. The majority ofN ososarioidea fo raminiferal assemblages were found in most survived the crisis and many of them returned samples from the Koessen Beds of the Allgau gradually from their withdrawal regions within Basins. A relatively diverse foraminiferal the Tethyan Realm. This migration spread from assemblage has been described by }AEGER the South to the North. New genera and species (1997). The surface of the uppermost Koessen originated slowly and mostly not before the limestone bed is irregular and black (manganese end of the Early Hettangian. Only the aragonitic crust). A stagnation of sedimentation and Oberhauserellidae and the Reinholdellinae dissolution of the surface must have occurred. produced new genera and species even during Above this surface 8 cm of grey marls with and immediately afterthe crisis. compressed Trochammina and inner casts of Oberhauserella praerhaetica occur. The References Schattwald Beds are 4 m thick. No micro fossils HILLEBRANDT, A.V. & KMENT, K. (2009): Die TriasjJura­ of animals have been recorded. These beds Grenze und der Jura in der Karwendelmulde und pass into grey marls with Eoguttulina and dem Bayerischen Synklinorium. - Exkursionsfiihrer, small-sized Oberhauserella. 40-60 cm above Jahrestagung der Deutschen Stratigraphischen Kommission fiirJurastratigr aphie in Fall 2009: 1-45; the Schattwald Beds Praegubkinella turgescens Erlangen (published by the authors). has been recorded, marking the T-J boundary. HILLEBRANDT, A.V., KORSCHNER, W. M. & KRYSTYN, L. From there onwards the foraminiferal fauna is 2007. A candidate GSSP for the base of the Jurassic impoverished; tiny Oberhauserella specimens in the Northern Calcareous Alps (Kuhjoch section, Karwendel mountains, Tyrol, Austria). - International are rare, and simple-built agglutinating Subcommission on Jurassic Stratigraphy ISJS fo raminifers predominate. Some meters higher Newsletter 34: 2-20. a normal-sized fauna of diverse Nodosarioidea, }AEGER, R.J. 1997. Foraminiferen und Ostracoden with Planularia inaequistriata and lchthyolaria aus den Fleckenmergeln des kalkalpinen Lias - densicostata, of probably Middle Hettangian Biostratigraphie und PaUiookologie. - Miinchner GeowissenschaftlicheAbhandlungen A, 33: 1-111. age, appears. KRISTAN-TOLLMAN, E. 1966. Die Foraminiferen aus den As shown above, abundance, size, and rhatischen Zlambachschichten der Fischerwiese diversity of foraminifers of the basins bei Bad Aussee im Salzkammergut. - Jahrbuch der decrease from the South to the North, but also Geologischen Bundesanstalt, Sonderband 10: 1-189. RUHL, M., KORSCHNER, W. M. & KRYSTYN, L. 2009. Triassic­ conformities exist. At the end of the Zlambach Jurassic organic isotope stratigraphy of key sections and Koessen beds the diversity of foraminifers in the western Tethys realm (Austria). - Earth and rapidly decreases. This can be explained by Planetary Science Letters 281: 169-187. 9th International Congress on the Jurassic System - Abstracts 73

Sinemurian (Early Jurassic) Ammonites from Five Card Draw, Nevada and Last Creek, British Columbia

PENGFEI Hou*, PAUL L. SMITH, ANDREW H. CARUTHERS & SARAH J. PORTER

Department of Earth Ocean and Atmospheric Sciences, Universityof British Columbia, Va ncouver, V6 T 1Z4, Canada; £-mail: [email protected], [email protected], [email protected], sporter@ eos.ubc.ca

*Corresponding author

The Sinemurian ammonite zonation for western Harbledownense zones. The Involutum Zone is North America (TAYLOR et al. 2001) is based on characterized by the restricted occurrences of successions in northwest United States and species of Coroniceras together with Arnioceras Mexico, also incorporating the work of PALFY nevadanum. Tmaegoceras nudaries, and the et al. (1994) which dealt with successions in endemic Tipperocerasmullerense. The LesleiZone Haida Gwaii (former Queen Charlotte Islands) is characterized by various species ofArnioceras in British Columbia, Canada. However, a large including Arnioceras humboldti, A. arnouldi, data set for the rest of Canada has not yet and A. miserabile. The upper part of the zone is been included. This work aims at testing and characterized by the occurrences of Arnioceras refining the present zonation. Two fossiliferous /aevissimum and the endemic Bartoliniceras successions were selected for study: the Sunrise les/ei. The Carinatum Zone is characterized by Formation in Five Card Draw, west-central the occurrences of Epophioceras carinatum, and Nevada and the Last Creek Formation in L�st Asteroceras cf. varians. Some poorly preserved Creek, southern British Columbia. specimens of Asteroceras cf. jamesi were fo und There are fo ur zones recognized in the ex situ from this interval. Due to its difficulty Five Card Draw section, namely in ascending in recognition, the Jamesi Zone in TAYLOR et order the Involutum, Leslei, Carinatum, and al. (2001) is provisionally included within the

Western North America Northwest Europe Age (Ma)

Imlayi Pliensbachian Jamesoni

-- 190.8 ±1.0 Raricostatum

Harbledownense Oxynotum Jamesi Obtusum Carinaturn Sinemurian -- 195.3 +_;_·: Tumeri Leslei Semicostatum

Involutum

Trigonatum Bucklandi

Columbiae -- 199.3 ±1.0 Rursicostatum Hettangian Angulata Mineralense

Correlation of the Sinemurian Zonation in western North America with northwest Europe (after DEAN et al. 1961; Fig. 1. SMITH et al. 1988; TAY LOR et al. 2001; LONGRIDGE et al. 2006 ) . Ages of stage boundaries and uncertainties are from GRADSTEIN et al. (2012); the age of the equivalent of the basal Obtusum Zone is from PALFY et al. (2000). 74 9th International Congress on the Jurassic System - Abstracts upper part of the Carinatum Zone as an horizon. References The Harbledownense Zone is characterized by CARIOU, E., & HANTZPERGUE, P. ( eds.) 1997. Biostratigraphie du Jurassique Quest-Europeen et mediterraneen: the occurrences of abundant echioceratids and zonations paralleles et distribution des invertebres oxynoticeratids. et microfossiles. - Bulletin du Centre Recherches Elf The two zones recognized in the Last Creek Exploration Production, Memoire 17: 1-440. section, are the Involutum Zone and Leslei DEAN, W.T., DONOVAN, D.T. & HOWARTH, M.K. 1961. The Zone of the Lower Sinemurian. Some ex situ Liassic ammonite zones and subzones of the north­ west European province. - Bulletin of the British ammonites from the top of the succession Museum (Natural History) 4: 438-505. indicate that the Carinatum Zone may be present GRADSTEIN, F.M., 0GG, J.G., SCHMITZ, M.D. & 0GG, G.M. (eds.) (MACCHIONI et al. 2005). The lnvolutum Zone is 2012.- The Geologic Time Scale 2012: 793 p., Elsevier characterized here by the restricted occurrence BV, Waltham, USA. LONG RIDGE, L.M., SMITH, P. L. & TIPPER, H.W. 2006. The Early of various species of Coroniceras. The top of Jurassic ammonite Badouxia from British Columbia, the zone is marked by the first appearance of Canada. - Paleontology 49: 795-816. Arnioceras. Tipperoceras is known from this MACCHIONI, F., SMITH, P. L. & TIPPER, H.W. 2005. Late interval. The lower part of the Leslei Zone is Esarly Sinemurian (Early Jurassic) ammonites from characterized by the restricted occurrences of the Taseko Lakes map area, British Columbia. - Paleontology 49: 557-583. Arnioceras cf.ceratitoides, and A. miserabile. The PALFY, J., SMITH, P. L. & TIPPER, H.W. 1994. Sinemurian upper part is characterized by the occurrences (Lower Jurassic) ammonoid biostratigraphy of the of Arnioceras cf. humboldti, Caenisities brooki, Queen Charlotte Islands, Western Canada. - Geobios C. turneri, C. pulchellus, Ly totropites fu cinii, 27: 385-393. PALFY, J., SMITH, P. L. & MORTENSEN, J.K. 2000. A U-Pb Proc/iviceras striatocostatum, Togaticeras and and 40Ar/39Ar time scale fo r the Jurassic. - Canadian sp. juv. Arnioceras arnou/di ranges throughout Journal of Earth Sciences 37: 923-944. this zone. A detailed description of the fauna in PAGE, K.N. 2003. The Lower Jurassic of Europe: its this interval in Last Creek is given by MACCHIONI subdivision and correlation. - Geological Survey of et al. (2005). Denmark and Greenland Bulletin 1: 23-59. TAY LOR, D.G., GUEX, J. & RAKUS, M. 2001. Hettangian and The primary standard zonal scheme for the Sinemurian ammonoid zonation for the Western Sinemurian Stage was established by DEAN et Cordillera of North America. - Bulletin de la Societe al. (1961) based on successions in northwest vaudoise des Sciences Naturelles, 87: 381-421. Europe, with numerous subsequent refinements TAY LOR, D.G. 1998. Late Hettangian-Early Sinemurian '(Jurassic) ammonite biochronology of the western summarized in PAGE (2003) and including Cordillera, United States. - Geobios 31: 467-497. the work of CARIOU & HANTZPERGUE (1997). SMITH, P. L., TIPPER, H.W., TAYLOR, D.G., & GUEX, J. 1988. An The secondary Sinemurian zonal scheme fo r ammonite zonation for the Lower Jurassic of Canada western North America, including reference and the United States: the Pliensbachian. - Canadian assemblages in Canada, is correlative with the Journal of Earth Sciences 25: 1503-1523. primary zonation as indicated in Fig. 1. 9th International Congress on the Jurassic System - Abstracts 75

Evolutionary significance of latest Jurassic-earliest Cretaceous hydrocarbon seep assemblages from Central Spitsbergen, Svalbard

KRZYSZTOF HRYNIEWICZ1 *, CRISPIN T. S. LITTLE2, HANS ARNE NAKREM\ 0YVIND HAMMER\ MICHAEL R. SANDY3, ANDRZEJ KAIM4 & VINN 0LEV5

1Natural History Museum, Universityof Oslo, 1172 Blindern, 0318 Oslo; Email-krzysztofhryniewicz@ nhm.uio.no; £-mail: [email protected], oy [email protected] 2School of Earth and Environment, Wo odhouse Lane, University of Leeds, Leeds LS2 9f T, United Kingdom; E-mail: [email protected] 3Departament of Geology, University of Dayton, Dayton OH 45469-2364, USA; E-mail: msandyl @ udayton.edu 4/nstitute of Palaeobiology, Polish Academy of Sciences, ul. Twarda 51/55, 00-818 Wa rszawa, Poland; E-mail:[email protected] 5Departament of Geology, University of Ta rtu, Ravil/a 14A, 5041 1 Ta rtu, Estonia; E-mail: olev.vinn@ ut.ee

*Corresponding author

Fifteen seep carbonate bodies from latest distributed species and Boreal endemics. J urassic to earliest Cretaceous black shales of Bivalves are represented by Nucinel/a, two the middle to outer shelf Slottsm0ya Member protobranch species, the pectinid Ca mptonectes contain a diverse (>30 species) assemblage and a number of Buchia species, with other of bivalves, gastropods, brachiopods, and taxa being only locally common. The seep fauna polychaete tubes. Up to 14 bivalve species have contains also atleasteightgastropod taxa, known been identified. They form a mixture of globally predominantly from contemporary normal

Fig. 1. Field view of one of the Jurassic-Cretaceous seep carbonates from Svalbard. 76 9th International Congress on the Jurassic System - Abstracts marine settings. Possible hokkaidoconchids single locality only. None of these genera is are the only gastropods encountered, which characteristic of seep environments since they are known to be restricted to vent and seep occur in Mesozoic reduced marine sediments environments. A lingulid Lingularia similis? as well. The dominance of normal marine fauna and at least five rynchonelliform brachiopods, from contemporary shelf settings in a seep which are also known from contemporary environment is an expression of colonization of normal marine environments, comprise a the seep environments by the shallow marine brachiopod element of the Svalbard seep taxa. fauna. Serpulid tubes with organic tubes of possibly vestimentiferan affinity represent References CAMPBELL, K.A. 2006: Hydrocarbon seep and hydrothermal polychaetes that have so far been identified. vent paleoenvironments and paleontology: Past The Jurassic-Cretaceous seeps of Svalbard developments and future research directions. - contain a high diversity fauna composed of a Palaeogeography, Palaeoclimatology, Palaeoecology mixture of various molluscs, with subordinate 232: 362-407. brachiopod and polychaete taxa, most of which HAMMER, 0., NAKREM, H.A., LITTLE, C.T.S., HRYNIEWICZ, K., SANDY, M.R., HURUM, J.H., DRUCKENMILLER, P., are also known from normal marine settings KNUTSEN, E.M. & H0YBERGET, M. 2011: Hydrocarbon in the Jurassic and Cretaceous of the Arctic. seeps from close to the Jurassic-Cretaceous boundary. Predominance of normal marine molluscs - Palaeogeography, Palaeoclimatology, Palaeoecology in seep assemblages from Svalbard contrast 306: 15-26. HJALMARSDOTTIR, H.R., NAKREM, H.A. & NAGY, J. 2012: Peregrinella with brachiopod-dominated Foraminifera from Late Jurassic - Early Cretaceous seep assemblages, known from some Early hydrocarbon seep carbonates, central Spitsbergen, Cretaceous localities. The palaeobiogeographic Svalbard - preliminary results. - Norwegian Journal separation of the Boreal Realm is reflected by of Geology 92: 157-165. a predominantly Boreal shallow water fauna HOLMER, L.E. & NAKREM, H.A. 2012. The lingulid brachiopod Lingularia from lowermost Cretaceous hydrocarbon with a few world-wide distributed species. The seep bodies, Sassenfjorden area, central Spitsbergen, high diversity, background fauna-dominated Svalbard. - Norwegian Journal of Geology 92: 167- assemblage reflects a strong connection with 174. the surrounding shallow marine environments. HRYNIEWICZ, K., HAMME�, 0., NAKREM, H.A. & LITTLE, �.T.S. 2012. Microfacies of the Volgian-Ryazanian The most common chemosymbiotic bivalves (Jurassic-Cretaceous) Sassenfjorden hydrocarbon are species of Nucinella and Solemya, whereas seep carbonates from central Spitsbergen, Svalbard. - a thyasirid and a lucinid are known from a Norwegian Journal of Geology 92: 113-131. 9th International Congress on the Jurassic System -Abstracts 77

Tetragonal serpulids from the Jurassic: testing the phylogenetic relationships by ultrastructural and mineralogical tube studies

ALEXEI IPPOLITOV1 * & ELENA KUPRIYANOVA2

1Geological lnstitute of Russian Academy of Sciences, Moscow 11901 7 Russia; E-mail: ippolitov.ap@ gmail.com 2The Australian Museum, 6 College Street Sy dney NSW 2010 Australia; E-mail: elena.kupriyanova@ austmus.gov.au

*Corresponding author

Serpulid polychaetes typically inhabit fossils"), widely distributed in shallow water cylindrical calcareous tubes that are attached communities during certain geological epochs, to hard substrates and well-preserved in the today ofteninhabi t refugia of the deep sea. fossil record from the Triassic onwards, being To examine the relationship between fo ssil an important element of Jurassic (especially and Recent forms with similar morphology, of Middle and Upper Jurassic) benthic we used SEM to analyse tube ultrastructure of communities. The fossil record of this group is, numerous fossil serpulid tubes collected from however, extremely poorly studied, mainly due more than lS localities in Europe and compared to insufficiently developed taxonomy, which them with the representative Recent material. makes comparisons of fossil with Recent fo rms Additionally, diffraction X-ray analysis was difficult. As a result, serpulids cannot provide performed in order to determine mineralogical clear paleoecological interpretations of fo ssils composition of the tubes. based on analogy with Recent forms. Examination of the fossil material has During the last 10 years, outstanding shown that most of the specimens (excluding ultrastructural variations among the evidently diagenetically altered material from Serpulidae were discovered (VINN et al. 2008), several localities) show a simple prismatic type and, consequently, ultrastructures are now of ultrastructure (SP,sensu VINN et al. 2008), and considered as a perspective tool for taxonomic are purely calcitic. Preservation of fine original investigations of fossils. growth patterns of prismatic crystallites is a This case study deals with coiled and straight powerful argument for the primary nature of tetragonal tubes of serpulid polychaetes, ultrastructures. Common structure confirms well-known to paleontologists under the close phylogenetic relationship between generic names Nogrobs and Te traserpulaj coiled (Nogrobs) and uncoiled (Tetraserpulaj Te traditrupa. These taxa originated and Te traditrupa) tube morphology. diverged during the Middle Jurassic and later On the contrary, Recent tetragonal tubes spread worldwide. During the Mesozoic these were found to be a taxonomic "conglomerate" serpulids were among the most common comprising numerous unrelated species with and abundant elements of serpulid faunas. very different types of tube ultrastructure, Species in morphologically identical tubes, such as irregularly oriented prismatic (lOP), both coiled and straight, known as Sp irodiscus semi-ordered irregularly oriented prismatic and Bathyditrupa, respectively, inhabit bathyal (SOIOP), and spherulitic irregularly oriented and abyssal environments in Recent oceans up prismatic (SlOP) sensu VINN et al. (2008). to over 6000 m depth. First palaeontologists Ultrastructures are stable within each species, (J.AGER 2005) and later zoologists (TEN HovE & but none of them is comparable with the simple KUPRIYANOVA 2009) supported the opinion that prismatic structure fo und in the fossil material. Recent and Mesozoic forms are congeneric. The Additionally, mineralogical composition in idea of their close relationship looks even more most cases was found to be a mixture of calcite appealing considering a long-held view that and aragonite, thus, differing fromcalcitic fossil ancient faunal elements (oftenknown as "living species. 78 9th International Congress on the Jurassic System - Abstracts

The results of our study mean that making discovery and examination of Cenozoic direct comparisons, including ecological material. interpretations, between Recent and fossil References tetragonal serpulid tubes is essentially jAGER, M. 2005. Serpulidae und Spirorbidae (Polychaeta incorrect. Similar tube morphology is most sedentaria) aus Campan und Maastricht von probably the result of adaptation to similar Norddeutschland, den Niederlanden, Belgien und angrenzenden Gebieten. - Geologisches jahrbuch soft-bottom environments, atypical for most A157 (for 2004): 121-249. serpulids. However, the huge stratigraphic TEN HOVE, H.A. & KUPRIYANOVA, E.K. 2009. Taxonomy of gap (65 ma.) between the youngest known Serpulidae (Annelida, Polychaeta): the state of affairs. fossil free tetragonal tubes and their recent - Zootaxa 2036: 1-126. counterparts still allows for the possibility of VINN, 0., TEN HOVE, H.A., MUTVEI, H. & KIRSIMAE, K. 2008. Ultrastructure and mineral composition of serpulid gradual evolution of the tube ultrastructures, tubes (Polychaeta, Annelida). - Zoological journal of a hypothesis that could be verified by further the Linnean Society 154: 633-650. 9th International Congress on the Jurassic System - Abstracts 79

Belemnite zonal scale for the Late Sinemurian - Pliensbachian of Eastern Europe: an update based on data from the Ukrainian Carpathians

ALEXEI IPPOLITOV1 * & }AN SCHLOGL2

1Geological Institute of Russian Academy of Sciences, Pyzhevski Lane 7, 11901 7 Mosco� Russia; E-mail: [email protected] 2Department of Geology and Paleontology, Facultyof Natural Sciences, Comenius University,Mlynska dolina, 842 15 Bratislava, Slovakia; E-mail: [email protected] s.uniba.sk

*Corresponding author

Despite belemnites are widely considered by abundant belemnite rostra, which are the geologists to be a stratigraphically important predominant fo ssils here. Detailed bed-by-bed group, in fact they are used as a basic tool for sampling ofbelemnite rostra, accompanied with stratigraphic subdivision and correlation only ammonite record, allowed us to reconstruct the fo r the Late Cretaceous of Europe. Numerous belemnite succession in great detail, including scales were elaborated fo r other Mesozoic tracing the phylogenetic lineages between intervals, but they mostly remain unused certain species. This analysis is used as a due to their low resolution. However, newest basis for the review of the existing belemnite investigations (jANSSEN et al. 2012), based biostratigraphic data, and it allows us to on careful morphological analysis of large propose some emendations and improvements sets of samples allowing to trace intraspecific fo r the Early jurassic belemnite scale. variations, have shown that belemnites �till AllfourzonalsubdivisionsoftheSinemurian­ can provide detailed zonal scales, comparable Pliensbachian interval of Bulgaria (STOYANOVA­ in resolution with ammonite zones and even VERGILOVA 1978) are well-recognizable in the biohorizons. Priborzhavskoe section. The Nannobelus sp. Formal belemnite scales for the Early jurassic Zone, originally dated as Late Sinemurian, is were elaborated only by STOYANOVA-VERGILOVA characterized by the presence of small-sized (1978) for Bulgaria, DOYLE & BENNETT (1995) representatives ofthe single genus Nannobelus. for NW Europe, and COMBEMOREL (1997) Our material shows that the uppermost part of fo r the NW and Mediterranean Europe. The this zone is characterized by a diversification most remarkable thing about all these scales event and, therefore, can be subdivided into is that the zones based on the same species two separate units. The belemnite fauna is may be of different age - for example, the accompanied by a rich ammonite association Bisulcata Zone in Doyle's scale covers the indicating the Raricostatum Zone of the Late whole Late Pliensbachian to Early Toarcian, Sinemurian. but is restricted to the Early Toarcian in The Apicicurvata Zone, characterized by Combemorel's scale; the Apicicurvata Zone even more diverse belemnite assemblages, has covers the whole Early Pliensbachian in the a complicated structure. The studied material Doyle and in the Stoyanova-Vergilova scale, but from the Priborzhavskoe section shows that it only the late Early Pliensbachian in the scale of can be clearly subdivided into 4 to 5 separate Combemorel. This artifact is based mainly on belemnite units, and 3 of them are based on the different interpretation of certain species by elements of the same lineage and, therefore, taxonomists. have high correlation potential. The index Material fo r the present study comes from species of the zone, Passaloteuthis apicicurvata the Priborzhavskoe Quarry (WIERZBOWSKI et. s.str., is restricted to the uppermost part of the al. 2012), located in the Transcarpathian Region zone, and the "classic" lower boundary of the of West Ukraine. Sinemurian-Pliensbachian unit at the base of the Pliensbachian is based rocks here are represented by marls and marly on the appearance of large-sized rostra of the limestonefsiltstone alternations, and contain genus Passaloteuthis. The age estimated in the 80 9th International Congress on the Jurassic System - Abstracts

Priborzhavskoe section is ?latest Raricostatum Although the obtained belemnite succession and J amesoni to Ibex zones (Early Pliensbachian). looks quite clear, it is still far from being well­ Questionably it includes also Davoei Zone of the correlated with existing ammonite data. late Early Pliensbachian, but ammonites of this Ammonite finds provide several important "tie­ age were still not found there. points" for the belemnite scale, but still most The Gastrobelus Genozone was originally boundaries of the belemnite scale are not well­ recognised and traced only in several sections dated in terms of ammonite zones, subzones, in Bulgaria (STOYANOVA-VERGILOVA 1978). This and biohorizons. zone was never used by subsequent authors, Phylogenetic considerations, supporting and even omitted in further discussions (see the proposed belemnite subdivision, together DOYLE & BENNETT 1995). However, in the with the uniform sedimentation character Priborzhavskoe section this zone looks quite and absence of recurrent communities in the clear and well-defined. Further subdivision Priborzhavskoe section, almost exclude the (into three sub units) is again possible here, possibility that these belemnite complexes are based on fast-evolving early representatives of ecological rather than evolutionary. Therefore, Parapassaloteuthis. The originally defined early it can be stated that belemnites of the Early Late Pliensbachian age of the zone is accepted J urassic in Priborzhavskoe allow to subdivide the here due to absence of ammonites in the Late Sinemurian - Early Pliensbachian interval corresponding interval. In Germany, however, into 12 units, approaching the resolution of well-recognizable Gastrobelus ventroplanus ammonite subzones. rostra appear in the Davoei Zone of the Early Pliensbachian (SCHUMANN 1974); thus the The study was supported by RFBR grant NQ12-05- Early/Late Pliensbachian boundary can be 00380-a. located within the unit. References The base of Bruguieriana Zone is reflected COMBEMOREL, R. 1997. Belernnites. In: CARIOU, E. & in the reduction of belemnite biodiversity - HANTZPERGUE, P. ( coord.), Biostratigraphie du now the single genus Passaloteuthis dominates Jurassique ouest-europeen et mediterraneen. the assemblage. This zone again can be Zonations paralleles et distribution des invertebres et microfossiles. - Bulletin de la Centre des Recherches subdivided by erecting two sub-units, based on • Elf Exploration-Production, Memoire 17: 157-167. two different phylogenetic lineages. However, DOYLE, P. & BENNETT, M.R. 1995. Belemnites in it has to be mentioned that the index species biostratigraphy. - Palaeontology 31: 815-829. }ANSSEN, N.M.M., CLEMENT, A. & BONT, 2012. Passaloteuthis bruguieriana should be revised w. Mediterranean Neocomian belemnites, part 4: and its variability is to be redefined. A Late belemnites of the Barremian stratotype section. - Pliensbachian age of the zone, assumed by Carnets de Geologie, Memoires 2012/02: 201-274. Stoyanova-Vergilova, is supported by isolated ScHUMANN, H.O. 197 4. Die Belemniten des norddeutschen finds of ammonites belonging to the genus Lias Gamma. - Geologisches Jahrbuch, Reihe A 12: Amaltheus of the Margaritatus Zone, as well 1-85. STOYANOVA-VERGILOVA, M. 1978. Zonal subdivision of the as by the belemnite Pleurobelus compressus, Lower Jurassic in Bulgaria by means of belemnites. indicating the same zone. The uppermost part - God. Sofisk. Univ. (Geol., Geogr.) 70 (1977-1978): of this stratigraphic unit is condensed and 161-192. [in Bulgarian] contains ammonites of the Spinatum Zone WIERZBOWSKI, A., KROBICKI, M. & MATYJA, B.A. 2012. The stratigraphy and palaeogeographic position of the (WIERZBOWSKI et al. 2012), indicating that the Jurassic successions of the Priborzhavske-Perechin Bruguieriana Zone in Priborzhavskoe covers Zone in the Pieniny Klippen Belt ofthe Transcarpathian most part of the Late Pliensbachian. Ukraine. - Volumina Jurassica 10: 25-60. 9th International Congress on the Jurassic System - Abstracts 81

Microfossil research using 3D imagingtechnology: an experimental study of Jurassic radiolarian fossils using X-ray micro-computed tomography

NAOTO ISHIDA 1 *, NAOKO KISHIMOT02,ATSUSHI MATSUOKA3, KATSUNORI KIMOTO\ TOSHIYUKI KURIHARA5 & TA KASHI YOSHIN06

1Centerfo r Fostering Innovative Leadership, Niigata Universi� Niigata 950-2181,japan; E-mail: nao. ishida21 @mbn.nifty. com 2Department of Mechanical Engineering, Setsunan Universi� Neyagawa 572-8508, japan; E-mail: [email protected] 3Department of Geology, Fa culty of Science, Niigata Universi� Niigata 950-2181, japan; E-mail: [email protected] 4Research Institute of Global Change, jA MSTEC, Yo kosuka 237-0061, japan; E-mail: kimopy@jamstec. go.jp 5Graduate School of Science and Te chnology, Niigata University, Niigata 950-2181, japan; E-mail: [email protected] 6Department of Mechanical Engineering, Toyo Universi� Ka wagoe 350-8585, japan; E-mail: [email protected]

*Corresponding author

X-ray micro-computed tomography (Micro­ been recovered from Middle to Upper Jurassic CT) is a non-destructive method of obtaining sediments in Japan and the Tethys region. a three-dimensional image of a millimetre­ This species was first described by MATSUOKA to micrometer-sized object from a set of (1983) based on conventional observation with X-ray cross-sectional images. To evaluate the a biological microscope and a scanning electron potential of Micro-CT imaging technology microscope (SEM). A Micro-CT device (SkyScan for the investigation of microfossils, we have Micro-CT in SEM) attached to a SEM (JEOL JSM- experimentally examined the skeletons of 6510) was used to take images of the internal radiolarians, fo raminifers, ostracods, and structures and surface ornamentation of this diatoms (e.g., MATSUOKA et al. 2012). This species. This device has an image resolution of investigation of Protunuma (?) ochiensis 300 nm/pixel. MATSUOKA emphasizes the utility of Micro-CT A roentgenogram of Protunuma (?) ochiensis fo rthepaleontological description ofradiolarian is shown in Fig. lA. After adjusting X-ray fossils. properties such as wavelength and intensity, Protunuma (?) ochiensis MATSUOKA is a internal structures could be recorded through four-segmented closed-end nassellaria that has the thick (ea. 10 lJ.m) exterior wall composed

X-ray photograph of Protunuma (?) ochiensis taken using the Micro-CT device. (B) Computer graphic images Fig. 1. A constructed from a set of X-ray photographs. (C) A SEM image of the same species. 82 9th International Congress on the Jurassic System - Abstracts of silica. Important taxonomic characters of nassellarians (ISHIDA et al. 2013). Micro-CT this species, especially those documented imaging may become an efficient method for in the original description such as outline, radiolarian investigation in the near future. number of segments, and pore arrangement, were represented almost perfectly in the 30 computer graphics (Fig. lB) synthesized from References MATSUOKA, A. 1983. Middle and Late Jurassic radiolarian a set of cross-sectional images. In particular, biostratigraphy in the Sakawa and adjacent areas, characteristics of the plicae, an important Shikoku, Southwest Japan. - Journal of Geosciences, surface ornamentation of this species, were Osaka City University 26: 1-48. clearly represented. The height and width of the MATSUOKA, A., YOSHINO, T., KISHIMOTO, N., ISHIDA, N., specimen were easily calculated by software as KURIHARA, T., KIMOTO, K. & MATSUURA, S. 2012. Exact number of pore frames and their configuration in the 97 11m and 78 jlm, respectively. Mesozoic radiolarian Pantanellium: An application of Based on the results of this experiment, the X-ray micro-CT and layered manufacturing technology Micro-CT device is adequate fo r imaging the to micropaleontology. - Marine Micropaleontology taxonomic characters of Jurassic radiolarians. 88-89: 36-40. ISHIDA, N., KISHIMOTO, N., MATSUOKA, A., KIMOTO, K., Furthermore, we have succeeded in obtaining KURIHARA, T. & YO SHINO, T. 2013. Microstructures of 30 images of more delicate radiolarian plankton skeletons using 30 imaging technology. - structures such as the initial spicules of Recent Bulletin of the Society for Science on Form 27. 9th International Congress on the Jurassic System - Abstracts 83

Paleoenvironment and sedimentation of deep marine spotted limestones and marls, Lower and Middle Jurassic (Western Carpathians, Tatra Mts.)

}OLANTA IWANCZUK & KATARZYNA SOBIEN

Polish Geological Institute - National Research Institute, Rakowiecka 4, 00-975 Wa rszawa, Poland; E-mail: [email protected]/, [email protected]

The study area is located in the eastern part with marly shales (radiolarian wackestone/ of the Polish Tatra Mts. The Jurassic rocks packstone with an admixture of mica and there represent deep marine facies of the quartz grains). The terrigenous material diffe rs Krizna Basin, (western branch of the Tethys), in its composition. In this succession MS values with a dominance of gray spotted limestones are highly variable with a general tendency to and marls, of the Fleckenkalk/Fleckenmergel decrease towards the top. However, in thin­ type. The characteristic feature of the studied sections we do not observe any changes in sections is an alternation of limestones, marly the amount of siliciclastic grains. Decrease in limestones, and shales in various proportions, the MS value up-section is caused by changes depending on the stratigraphic interval. Based in mineral composition, caused by changes in on the ammonite fa una, described by MYCZYNSKI the source area which supplied clastic material (2004) and IWANCZUK et al. (2012, 2013) the to the basin. Petrographic observation leads age of sediments has been identified as Late to the conclusion that the detrital grains Sinemurian - Early Bathonian. might be derived from destruction of the Microfacies analysis, together with magnetic older sedimentary cover, perhaps the Triassic susceptibility (MS) measurements on .cut carbonate platform. samples were performed in order to reconstruct In addition we can observe first- and second­ the palaeoenvironment during sedimentation order fluctuations. The second-order rhythmic of marl and spotted limestone. In addition, changes show a systematic delivery of detrital geochemical analyses were executed to evaluate material into the basin and/or a cyclic decline redox conditions and to prove terrigenous of carbonate sedimentation. Consequently, a origin of magnetic susceptibility. greater share of siliciclastic material could be Lithological and microfacies analysis controlled by paleoclimate changes (HALLAM allowed to subdivide the studied sediments into 2000; 0GG et al. 2012). three main sequences. Magnetic susceptibility However, the general trend of the first­ fl uctuations are clearly visible along the order changes in magnetic susceptibility can be studied profiles and reflect changes in the correlated with the eustatic sea-level changes supply of detrital material into the basin, which within the Tethys basin (HALLAM 2000). The MS is confirmed by the local tectonic events and curve indicates four transgressive-regressive eustatic sea level changes. cycles with a clear deepening trend up-section .. In the lower part of the section (Late A significant increase in supply of detrital Sinemurian - Early Pliensbachian) spiculitic material in the central part of the profile can limestone ( spiculitic wackestone fpackstone) be explained by local tectonic events (Devin rift dominates. The average value of the magnetic phase), described by PLASIENKA (2003). susceptibility is low and varies little, with a In the uppermost part of the section tendency to increase up-section. It coincides (Late Bajocian - Early Bathonian) radiolarian with the global eustatic curve of sea level limestones and radiolarites ( radiolarian changes and indicates a regressive cycle of Late wackestone with subordinate filament Sinemurian - early Pliensbachian age (HALLAM wackestone) appear. MS values are less variable 2000). and clearly decrease, which might point to a The middle part of the section (Late reduction of detrital material supply to the Pliensbachian - Early Bajocian) consists of basin. This is probably due to deepening of the limestones and calcareous marls interbedded basin (HALLAM 2000). 84 9th International Congress on the Jurassic System - Abstracts

References Bratislava. HALLAM, A. 2000. A review of the broad pattern of IWANCZUK, J., IWANOW, A. & WIERZBOWSKI, A. 2013. Lower jurassic sea level changes and their possible causes Jurassic to lower Middle jurassic succession at Kopy in the light of current knowledge. - Palaeogeography, Soltysie and Placzliwa Skala in .eastern Tatra Mts Palaeoclimatology, Palaeoecology 167: 23-37. (Western Carpathians) of Poland and Slovakia: MYCZYNSKI, R. 2004. Toarcian, Aalenian and Early Bajocian stratigraphy, facies and ammonites. - Volumina (Jurassic) ammonite faunas and biostratigraphy Jurassica, in press in the Pieniny Klippen Belt and the Tatra Mts, West OGG, J.G., HINNOV, L.A. & HUANG, C. 2012. Jurassic. In: Carpathians. - Studia Geologica Polonica 123: 7-131. GRADSTEIN, F.M., 0GG, J.G., SCHMITZ, M. & 0GG, G. IWANCZUK, J., IWANOW, A. & WIERZBOWSKI, A. 2012. Lower (eds.), The geologic time scale: 731-791. Elsevier, Jurassic to lowermost Middle Jurassic at Kopy Sohysie Amsterdam. in the High Tatra Mts., Poland: stratigraphy, fa cies and PLASIENKA, D. 2003. Dynamics of Mesozoic pre-orogenic ammonites. In: j6zsA, S., REHAKOVA, D. & VOJTKO, R. rifting in the Western Central Carpathians. - (eds.), Environmental, structural and stratigraphical Mitteilungen der Osterreichischen Geologischen evolution of the Western Carpathians. - 8th Gesellschaft94: 79-98. Esseweca Conference 6-7.12.2012, Abstract book: 19, 9th International Congress on the Jurassic System - Abstracts 85

Middle Jurassic Bivalves from Charu area, Jaisalmer district, Rajasthan, India

R. L. )AIN1, R. P. KACHHARA2 & R. L. )ODHAWAT3

1Palaeontology Division 1, Geological Survey of India, 15 A & B Ky d Street, Ko lkata-700016, India; E-mail: [email protected] 231, Mayurvan Colony, Panariyo ki Madadi, Udaipur-313002, Rajasthan, India; E-mail: kachharar@ yahoo.com 325/A, Sahe/i Nagar,Near Sahelion ki Bari, Udaipur-313001, Rajasthan, India

jaisalmer is known for its marine Jurassic assemblage bears a similarity with Middle fa unal assemblages. Thirteen specimens of jurassic (Bathonian) faunas of England and Bivalvia have been collected from the yellow Germany. The Bathonian ammonite genus limestone horizon of the Bada Bag Member Clydoniceras BLAKE was reported from the same of the Jaisalmer Formation from the Charu locality by PRASAD et al. (2007). Based on the area, Jaisalmer district, Rajasthan. The taxa above data and on the faunal assemblage the are figured and described in the present Bada Bag Member of the Charu area is broadly paper to update the stratigraphy of the Bada assigned a Middle jurassic (Bathonian) age. Bag Member in the Charu area. Eight taxa: Parallelodon sp., Modiolus (M.) patchamensis Cox, Modiolus sp., Pinna (Pinna) sp., Pteroperna References sp., Eopecten sp., Homomya sp., and Pleuromya PRASAD, S., jAIN, R.L. & SRIVASTAVA, M.S. 2007. Record of Middle Jurassic (Bathonian) Ammonite genus uniformis (J. SOWERBY) have been identified. Clydoniceras BLAKE from Jaisalmer Basin, western � These bivalve genera have � much longer ra ge Rajasthan. - Journal of the Geological Society of India than ammonites and brachiopods. The faunal 69: 53-56. 86 9th International Congress on the Jurassic System -Abstracts

Palaeobiogeographic significance of the Middle Jurassic pholadomyoid bivalves fromKachchh, western India

ANAND K. jAITLY

Center of Advanced Studies in Geology, Banaras Hindu University, Va ranasi 221 005, India; E-mail: [email protected]

Situated on the western margin of the Indian Platymoidea Cox, 1964, and Thracia J. DE C. plate at a plaeolatitude of 33°S, the Kachchh SOWERBY, 1823. The genus Agrawa/imya SINGH, Basin is known world over for its rich }AITLY & PANDEY is endemic whereas the rest occurrence of Middle to Late Jurassic mollusks. is cosmopolitan in distribution. These genera During that time, the basin received a thick pile are represented by 30 constituent species, of of marine sediments, about 750 m in thickness, which only six species are endemic and the representing sediments of a silicilastic ramp and remaining ones are cosmopolitan. Distribution a carbonate ramp, as well as mixed carbonate­ of these bivalves was much affected by the siliciclastic sediments. These Middle Jurassic evolutionary history of the basin which is a sediments range in age from Bajocian (possibily rift basin that has been inundated by the sea Aalenian) to Callovian. sometime during the Middle Jurassic owing to Amongst the Middle Jurassic benthic the opening of the Arabian Sea. By and large communities of Kachchh, pholadomyoid these faunas are characteristic of the southern bivalves are one of the dominant groups in both hemisphere and belonged to the East African diversity and quantity. These are represented biochore of the Tethyan Realm or to the so­ by 13 genera , viz. Pholadomya G.B. SowERBY, called Ethiopian faunal province. An attempt has 1823, Agrawa/imya SINGH, }AITLY & PANDEY, been made to ascertain the usefulness of these 1982, Girardotia DE LORIOL, 1903, Goniomya pholadomyoids by analysing their (palaeo-) AGASSIZ, 1841, Homomya AGASSIZ, 1843, autecology and dist�ibution pattern in different Osteomya MOESCH, 1874, Pachymya J. DE C. par;ts of the globe in evaluating the Middle SOWERBY, 1826, Machomya DE LORIOL, 1868, Jurassic palaeobiogeography and to establish Ceratomya SANDBERGER, 1864; Ceratomyopsis the migrating routes within the Tethyan Realm COSSMANN, 1915, P/euromya AGASSIZ, 1843, vis-a-vis the Boreal Realm. 9th International Congress on the Jurassic System - Abstracts 87

Jurassic-Cretaceous plant mega- and microfossils from subsurface Gondwana sediments of the Jangareddygudem area, Chintalapudi subbasin, India

NEERJA }HA*, NEERU PRAKASH & HARINAM }OSHI

Birbal Sahni Institute ofPalaeobota� 53 UniversityRoad Lucknow- 226007� India; £-mail: neerjajha@ yahoo.co. uk

*Corresponding author

The Godavari Graben - one of the biggest of Pachypteris, Equisetalian axes, Ptilophyllum, Gondwana basins of India, contains a more Elatocladus, and Pagiophyllum. or less complete succession from Permian to Palynological studies carried out on Cretaceous age. Regional exploration for coal these megafossil-bearing sediments of and other minerals in the Jangareddygudem area borehole MJR-11 have revealed the presence of the Chintalapudi sub-basin was undertaken of Jurassic-Cretaceous palynomorphs in by SCCL and MECL in order to establish the the Jangareddygudem area. A variety of structure, stratigraphy, and coal potentiality palynomorphs has been recorded between of the area. Core samples from different depth 293-398 m depth in borehole MJR-11. The levels were collected for palynological studies. palynoassemblage consists of Cal/ia/asporites Impressions/compressions of plant fossils trilobatus, Ischyosporites, Matonisporites, at various depth levels were observed in the Fo veosporites,Aequitriradites,Appendicisporites, core samples of borehole MJR- 11. In spite 'of Lametatriletes, Coronatispora, Impardecispora, the fragmentary nature of fo ssils, the external Concavissimisporites, Podocarpidites, Astropol/is, morphological features, i.e. shape and venation Triporoletes, Deltoidospora, Klukisporites, pattern ofthe leaves are quite distinct and permit Contignisporites, G/eicheniidites senonicus, identification up to specific level. Occurrence of Chasmatosporites, Minutosaccus, Cy athidites, the well preserved Mesozoic Upper Gondwana Brachysaccus, Osmudacidites, Hamiapollenites, "Ptilophyllum" flora comprising Ptilophyllum Alisporites, Playfordiaspora, Schizosporis, cutchense, P. acutifolium, Pachypteris indica, ?Goubinispora, and Laevigatosporites. Tricolpate Elatocladus jabalpurensis, Pagiophyllum and monocolpate pollen are very rare. gollapalensis, and equisetaceous axes have been The present paper deals with the integrated recovered from the depth range of 293-398 palaeobotanical and palynological studies of meters in the borehole MJR-11.The assemblage terrestrial deposits of the Jangareddygudem is dominated by bennettitalean fronds and area. Both plant mega- and micro fossils indicate conifers. Pteridosperms are represented a Late Jurassic - Early Cretaceous age of these only by the genus Pachypteris. Ferns are sediments. absent. Gingkgoales and Pentoxylales are not recorded. The assemblage is quite similar to References PANDYA & SuKH-DEV 1990. Fossil Flora of Gollapalle the Gollapalle Formation described by PANDYA Formation. In: jAIN K.P. & TIWARI R.S. ( eds.). - & SUKH-DEV (1990) and the Sehora flora of the Proceedings of Symposium Vistas in Indian Jabalpur Formation in the common occurrence palaeobotany. - Palaeobotanist 38: 147-154. 88 9th International Congress on the Jurassic System - Abstracts

Environmental significance of the trace fossils of Middle Jurassic rocks, Patcham Island, Kachchh, western India

)AQUILIN K. )OSEPH\ SATISH ). PATEL1 * & NISHITH Y. 8HATT2

1Departmento[Geology, The M. S. Universityo[ Baroda, Sayajiganj, Va dodara - 390 002, India; E-mail: [email protected] 2Department of Geology, M. G. Science Institute, Navrangpura, Ahmedabad - 380 009, India

*Corresponding author

The Patcham Island is the westernmost island Kaladongar Formatipn comprises a -465-m­ of the island belt of northern Kachchh and is thick sequence and is subdivided into three 70 km north of Bhuj, the district headquarter. informal members; (i) Dingy Hill/Kuar Bet It lies between N23°43'43" to 24°00'22" and member (Bajocian), (ii) Kaladongar Sandstone E69°40'00" to 69°58'40" and covers an area member (Bathonian), and (iii) Babia Cliff of -550 km2• The present investigation was Sandstone member (Bathonian). These rocks also extended to Kuar bet, a small islet that lies are highly fossiliferous containing abundant 2 km northwest of Patcham Island, between bivalves, gastropods, brachiopods, corals, and N23°58'30" to 24°03'30" and E69°42'00" to echinoderms. A succession of limestones, 69°45'30". The Patcham Island consists of two shale, and sandstones, above the Kaladongar hill ranges, Kaladongar and Goradongar. The Formation is grouped under the Goradongar study area comprises the well developed oldest Formation. This formation is -152 m thick Mesozoic succession of Kachchh which ranges and has been is subdivided into four informal in age from Bajocian to Callovian. members: the (i) Goradongar Flagstone, (ii) BISWAS (1977) classified the Mesozoic rocks Gadaputa Sandstone, (iii) Raimalro Limestone of Patcham Island into two fo rmations, the and (iv) Modar Hil� members (BISWAS 1977). lower Kaladongar and the upper Goradongar It i,s Bathonian-Callovian in age (FORSICH et al. Formation (Fig.1 ); both formations have been 1994) and mainly consists of mixed siliciclastic­ further subdivided into seven members. The carbonate sediments with shales and limestones

GREAT RANNOF KACHCHH

Location and geological map of study area. Fig. 1. 9th International Congress on the Jurassic System - Abstracts 89

Table 1. Distribution of trace fossils in different ichnoassemblage and their probable depositional environments. lchnoassemblage Associated trace fossils Characteristics Depositional environments

Arenicolites Arenicolites carbonarius, A. statheri, A. isp., Thalassinoides Dominance of Foreshore to assemblage nodosus, Palaeophycus tubularis, Rhizocorallium irregulare, suspension- over middle shoreface Monocraterion tentaculatum, Skolithos linearis, P/anolites deposit-feeders beverleyensis, Diplocraterion parallelum, Ta enidium serpentinum, Ophiomorpha nodosa, He/icolithus sampelayoi, Chondrites targionii

Asterosoma Asterosoma radiciforme, A. cf. radiciforme, A. ludwigae, Deposit-feeders Transitional zone to assemblage Phycodes palmatus, Rhizocorallium irregulare, dominant over offshore Th alassinoides horizontalis suspension-feeders; probable makers are crustacean decapods

Gyrochorte Gyrochorte comosa, Didymaulichnus /yel/i, Th alassinoides Deposit-feeders Transitional zone to assemblage isp., Arenicolites carbonarius, Palaeophycus tubularis, dominant over offshore Laevicyclus isp., Lockeia siliquaria, Gordia arcuata, Pilichnus suspension-feeders; isp. producers of these traces are crustaceans and polychaetes

Rhizocorallium Rhizocorallium jenense, R. irregulare, R. uraliense, Suspension-feeders Middle shoreface to assemblage Diplocraterion paralle/um, Gyrochorte comosa, Arenicolites and deposit-feeders offshore carbonarius, Palaeophycus tubularis, Skolithos linearis, both dominant; Phycodes palmatum, Asterosoma radiciforme, Ophiomorpha structures formed by nodosa, Lockeia siliquaria, L. amygdaloids, Wa lcottia deposit feeders and devilsdingli, Protovirgularia dichotom

isp., Opportunistic animals Upper shoreface to Th alassinoides Th alassinoides horizontalis, T. suevicus, T. Gordia assemblage arcuata, Rhizocorallium irregulare, R. jenense, Ophiomorpha that exploited similar Lower shoreface nodosa, Arenicolites isp., Phycodes cf. palmatum, kind of niches; probable Palaeophycus tubularis, Pilichnus isp. trace makers are crustaceans

Planolites­ Palaeophycus alternatus, P. striatus, P. tubularis, P. Characterized by Transitional zone to Palaeophycus annulatus, Planolites beverleyensis, Lockeia si/iquaria, feeding and grazing offshore assemblage Thalassinoides horizontalis, Arenicolites isp. , Rhizocorallium traces; producers irregulare, R. jenense, Chondrites targionii most probably like polychaetes

Phycodes Phycodes circinatum, P. palmatus, P. cf. palmatus, P. cf. Predominance of Transitional zone to assemblage curvipalmatus, Asterosoma radiciforme, Rhizocoral/ium deposit-feeders over offshore irregulare, Hartsellea sursumramosa, Thalassinoides suspension-feeders; suevicus, Planolites beverleyensis probable trace makers are vermiform annelids and crustaceans

Ophiomorpha Ophiomorpha nodosa, Rhizocorallium irregulare, R. jenense, Opportunistic behavior Offshore to middle assemblage Skolithos linearis, P/anolites beverleyensis, Arenicolites of organisms shoreface carbonarius, Th alassinoides nodosa, Palaeophycus tubularis, Chondrites targionii, Ta enidium serpentinum, Rhabdog/yphus isp.

Skolithos Skolithos linearis, Planolites beverleyensis, Arenicolites Suspension- as well Foreshore to assemblage carbonarius, A. isp., Monocraterion tentaculatum, as the deposit-feeders; middle shoreface Ophiomorpha nodosa, Palaeophycus tubularis, Chondrites probable makers are targionii, Ta enidium baretti vermiform annelids 90 9th International Congress on the Jurassic System - Abstracts

2m

2. Composite litholog showing the distribution of trace fossils in Middle Jurassic rocks of Patcham Island. Fig.

(PATEL et al. in press a, b). the MouNT (1985) classification scheme. A The whole succession chiefly consists of composite litholog of the Mesozoic succession mixed siliciclastic-carbonate dominated units of the Patcham Island based on bed forms, whereby pure limestones and sandstones lateral and vertical continuity, and structural commonly are interbedded with shales characteristics is prepared. The shale also (Fig. 2). Sedimentologically, the succession shows variation in composition: the lower part shows clear demarcation in composition; of the succession is more argillaceous, while the the Kaladongar Formation is characterized upper part is more calcareous in nature. The by siliciclastic-dominated mixed sediments, base of the Kaladongar Formation consists of while the Goradongar Formation is composed a granite-cobble-conglomerate but occasional of carbonate-dominated mixed sediments. intraformational conglomerates are also seen The mixed sediments shows a wide range in at differentstratigr aphic levels. their composition and are classified based on The whole succession is highly bioturbated 9th International Congress on the Jurassic System - Abstracts 91 and consists of diverse groups of trace fossils; shoreface, and fo reshore facies (Table 1 ). The indistinct fo rms are also abundant. A total of 6 7 ichnoassemblages of the Mesozoic succession ichnospecies of 43 ichnogenera were identified of the Patcham Island indicate cyclicity in and further were grouped into five ethological environmental facies and reflect fluctuating categories based on behavioural patterns. energy conditions and sea levels during Bajocian Many trace fossil species reappear throughout to Callovian times. the succession and are observed with different combinations leading to an increase in trace fo ssils diversity but each layer is characterized References by a single ecologically-related group of trace BISWAS, S.K. 1980. Mesozoic rock stratigraphy of Kutch, Gujarat. - Quarterly Journal of the Geological, Mining fossils forming nine recurringichnoassemblages and Metallurgical Society of India 49: 1-52. [for namely, Arenicolites, Asterosoma, Gy rochorte, 1977] Rhizocorallium, Thalassinoides, Planolites­ FORSICH, F.T., PANDEY, D.K., CALLOMON, J.H., 0SCHMANN, Palaeophycus, Phycodes, Ophiomorpha, and W. & }AITLY, A.K. 1994. Contributions to the Jurassic of Kachchh, western India. Bathonian stratigraphy Sko/ithos 11. assemblage. and depositional environment of the Sadhara Dome, Each ichnoassemblage is distinguishable Pachchham Island. - Beringeria 12: 95-125. by a number of ecological parameters and MoUNT, J. 1985. Mixed siliciclastic and carbonate sediments: hence reflects the most dominant physical a proposed first order textural and compositional parameter that is responsible fo r the deposition classification. - Sedimentology 32: 435-442. PATEL, S.J., }AQUILIN, K.J. & BHATT, N.Y. in press, a. Sequence of the sedimentary succession of the Patcham Stratigraphic Analysis of the Mixed Siliciclastic­ Island. The ichnoassemblages indicate the Carbonate Sediments (Middle Jurassic) of the Patcham development of the Skolithos, Mixed Skolithos­ Island, Kachchh, Western India: An Ichnological Cruziana and Cruziana ichnofacies. The trace Approach. - Journal of Geological Society of India. PATEL, S.J., JAQUILIN, K.J., AND BHATT, N.Y. in press, b. fossils data reveal six distinct depositional facies Ichnology of the Goradongar Formation, Goradongar which include offshore, offshore transitional Hill Range, Patcham Island, Kachchh, Western India. ­ zone, lower shoreface, middle shoreface, upper Journal of Geological Society of India. 92 9th International Congress on the Jurassic System - Abstracts

Towards an integrated Jurassic biostratigraphy for eastern Greenland

SIMON R. A. KELLY1 *, F. jOHN GREGORY2, BILL BRAHAM3, DOMINIC P. STROGEN4 & ANDREW G. WHITHAM1

1CASP, University of Cambridge, West Building, 181a Huntingdon Road, Cambridge CB3 ODH, United Kingdom; E-mail: [email protected] 211 Corner Hall,Hemel Hempstead, Herts HP3 9HL, United Kingdom; E-mail: billbraham1 957@yahoo. co.uk 3Petrostrat Ltd, Ta n-y-Craig, Pare Caer Seion, Conwy, Wa les LL32 BFA, United Kingdom; E-mail: john. [email protected] 4GNS Science, 1 Fa irway Drive, Avalon, PO Box 30-368, Lower Hutt, New Zealand; E-mail: dominic. [email protected]

*Corresponding author

The thick and relatively complete Jurassic such as ammonites recovered. succession of eastern Greenland provides a Reliance upon any single organism group unique biostratigraphic record fo r the North can only provide an incomplete biostratigraphic Atlantic region. The main biostratigraphic picture, especially when one moves from control for the succession has been provided by marine to non-marine environments. This is molluscs, especially ammonites and to a lesser particularly so for the Early jurassic rocks of extent by bivalves and belemnites. For example eastern Greenland. Integrated data is very the late John Callomon and colleagues recognised important here as no single biostratigraphic 86 boreal ammonite-bearing horizons in the Mid group can be used successfully throughout, to Late Jurassic, allowing an average duration and there are only three significant ammonite of less than 300,000 years fo r each interval. faunas during this period. Palynological and micropalaeontological CASP field-work from 1990 to 2012 schemes fo r Greenland remain less has resulted in the collection of much comprehensive, but continue to improve. biostratigraphic material which has been Offshore in the North Sea a precision of about documented using Stratabugs. In this article 700,000 and 1,000,000 years can be achieved published data are summarised together with by palynomorphs and micropalaeontology previously unpublished data in table form. The respectively. The Greenland succession integrated charts have detailed columns fo r provides an important opportunity to integrate ammonite biozones and horizons, palynological the micropalaeontology and palynology into the and microfossil biozones. More limited well-documented and more detailed ammonite information is available on belemnites, bivalves macrofaunal succession. Collecting directly and macroflora. This integrated biostratigraphy from outcrop often achieves better and more fo r eastern Greenland is of importance fo r the accurate results than from recovered chippings offshore oil-industry in the northern North from cored samples. Seldom are continuous Atlantic and Barents Shelf as well as to students cores available for analysis from mudstone of the Jurassic outcrops of Scotland, onshore successions and only rarely are macrofossils Norway and Svalbard. 9th International Congress on the Jurassic System - Abstracts 93

Palaeoenvironmental changes through a Panthalassic margin record of the early Toarcian Oceanic Anoxic Event

DAVID KEMP1 * & KENTARO IZUMI2

1Environment, Earth and Ecosystems, The Open University, Wa lton Hall, Milton Keynes, MK7 6AA, UK; E-mail: [email protected] 2Department of Earth and PlanetaryScien ce, Universityof To kyo, 7-3-1 Hongo, Bunkyo-ku, To kyo 113- 0033, japan; E-mail: [email protected]

*Corresponding author

The early Toarcian Oceanic Anoxic Event (OAE, exposed in the Sakuraguchi-dani valley, Toyora 182 Ma) represents one of the most severe area of SW Japan, consists of organic-rich environmental perturbations ofthe Phanerozoic. siltstones and mudstones, with intercalated A key diagnostic feature of the event is a -4 to sandstone horizons. We have defined more -8°/o o excursion in the C-isotope composition of precisely the structure of the C-isotope event marine organic matter, marine carbonate and in this succession by augmenting previously terrestrial plant material. In addition, there is published C-isotope data with higher evidence during the event fo r elevated rates of resolution C-isotope analyses of organic matter. faunal turnover, seawater warming, an increase Moreover, we have allied these isotopic data in global weathering rates, and widespread with high-resolution elemental (XRF) and seawater deoxygenation. To date, the majority organic geochemical data. We have used these of the evidence fo r palaeoenvironm�ntal data to assess in detail the precise nature of change during the early Toarcian OAE has palaeoredox changes occurring before, during come from European (i.e. Tethyan and Boreal) and after the event, and how these changes localities, and the record of the event from the relate to coeval changes in C-isotopes. Our data Panthalassic Ocean margin is poorly known. highlight differences in the timing of seawater Previous studies have identified the event from deoxygenation relative to C-isotope changes in Panthalassic successions based on the negative the Tabe Basin compared to European sections. C-isotope excursion (e.g., AL-SUWAIDI et al. In addition, our elemental data across the event 2010; IzuMI et al. 2012). Presently however, suggest the presence of changes in the nature geochemical data that can be used to inform and flux of sediment into the basin, possibly our understanding of weathering and redox in relation to changes in relative sea level, but conditions through these successions have not also perhaps as a consequence of hydrological been reported. This is important, however, changes driven by the event itself. because although it has been demonstrated that the carbon cycle perturbation during the event was a global phenomenon, outstanding References questions remain over the precise extent and AL-SUWAIDI, A.H. et al. 2011. First record of the Early Toarcian Oceanic Anoxic Event from the Southern timing of weathering and redox changes in Hemisphere, Neuquen Basin, Argentina. - Journal of different parts of the world. To address this the Geological Society of London 167: 633-636 issue, we have sampled and studied at high IZUMI, K. et al. 2012. Early Toarcian (Early Jurassic) resolution a record of the early Toarcian OAE oceanic anoxic event recorded in the shelf deposits in the northwestern Panthalassa: Evidence from deposited on the shelf of the western margin of the Nishinakayama Formation in the Toyora area, the Panthalassic Ocean. The succession, part of west Japan. - Palaeogeography, Palaeoclimatology, the Nishinakayama Formation of the Tabe Basin Palaeoecology 315-316: 100-108. 94 9th International Congress on the Jurassic System - Abstracts

High-resolution microfossil results from the Toarcian Oceanic Anoxic Event, Yo rkshire, UK

ALICE E. KENNEDY1 *, ANGELA L. CoEl, WILLIAM D. GOSLING1 & jAMES B. RIDING2

1Department of Environment, Earth and Ecosystems, Centre fo r Earth, Planetary, Sp ace and Astronomical Research, Th e Open University, Wa lton Hall, Milton Keynes, MK7 6AA, UK; E-mail: a/ice. [email protected], [email protected], [email protected] 2British Geological Survey, Keyworth, Nottingham, NG12 SGG, UK; E-mail: [email protected]

*Corresponding author

The ecological specialism of microfossils, Previous micro fossil studies on the Toarcian together with their ability to produce in high OAE show a number of profound changes numbers, good preservation in the fo ssil record, including a decrease in size of fo raminifera and small size makes them highly sensitive fo llowed by a barren interval (HYLTON and very suitable as a proxy fo r examining 2000), changes in abundance of terrestrial environmental change on short time-scales. In palynomorphs and dinoflagellates and an this study, we present new high-resolution data increase in the abundance of extremophiles, on the range and abundance of fo raminifera, Ta smanites,andsphaeromorphswhichcoincides terrestrial palynomorphs and dinoflagellates with a disappearance event of dinoflagellates fromstratarecordingtheextremeenvironmental (BUCEFALO PALLIANI et al. 2002). However, all of changes driven by the Toarcian Oceanic Anoxic these studies were completed prior to the high­ Event. resolution geochemical and macrofossil data The To arcian (Early J urassic) Oceanic Anoxic set for the Toarcian OAE which demonstrates Event (OAE) is marked by the widespread changes on the 1000 to 10,000s year scale. deposition of organic-rich mudrocks and a To achieve a higher resolution and pronounced carbon-isotope excursion that regular data set directly comparable with contains fo urabruptshifts (e.g. KEMP et al. 2011). the geochemistry, we have collected samples A wide range of other geochemical proxies through the Toarcian OAE every 2.5 cm. We indicate that extreme environmental change have used the same stratigraphic positions occurred at this time including: a shiftin oxygen­ and North Yorkshire, UK coast sections as isotope composition interpreted to represent a 7 the published high-resolution geochemical to 13°C rise in global temperatures (BAILEY et al. proxies (e.g., KEMP et al. 2011; PEARCE et al. 2003; DERAet al. 2009); changes in the osmium­ 2008) and macrofossils (CASWELL et al. 2009). and strontium-isotope compositions indicating Our results show: (i) extensions to the range enhanced rates of chemical weathering (CO HEN of some foraminifera species; (ii) changes in et al. 2004) and a change in the molybdenum­ the diversity of foraminifera; (iii) changes in isotope composition interpreted as reflecting the relative abundance of foraminifera and a global increase in the areal extent of marine microgastropodsfmicrobivalves and (iv) anoxia (PEARCE et al. 2008). The interval that the abundance of palynomorphs and between the Pliensbachian-Toarcian boundary dinoflagellates varies on short time-scales that and the Toarcian OAE is associated with a mass are closely linked to environmental changes extinction. This extinction affected the marine indicated by the geochemical proxies. invertebrate realm most severely. CASWELL et Our preliminary results demonstrate al. (2009) present a summary of the evidence that the previously used, and fairly standard, for the extinction from previous studies and, extraction technique for Toarcian foraminifera with the additional of new data, identify one from indurated organic-rich mudrocks using true extinction horizon which corresponds hydrogen peroxide (e.g., HYLTON 2000; REO LID with the first abrupt negative carbon-isotope et al. 2012) resulted in corrosion and may shiftduring the Toarcian OAE. have extended or potentially caused the 9th International Congress on the Jurassic System - Abstracts 95 apparent foraminiferal barren interval. We have the Geological Society 166: 859-872. developed a new method involving repetitive COHEN, AS., CoE, AL., HARDING, S.M. & SCHWARK, L. 2004. Osmium isotope evidence fo r the regulation of freeze-thawing followed by soaking in white atmospheric C02 by continental weathering. - Geology spirit and sodium hexametaphosphate. This 32: 157-160. has resulted in increased disaggregation of DERA, G., PUcEAT, E., PELLENARD, P. , NEIGE, P., DELSATE, D., the sample from 5 to SO% and the extraction jOACHIMSKI, M.M., REISBERG, L. & MARTINEZ, M. 2009. Water mass exchange and variations in seawater of a more diverse and abundant assemblage of temperature in the NW Tethys during the Early fo raminifera than previously reported from the Jurassic: Evidence from neodymium and oxygen same stratigraphic interval. The microfossils isotopes of fish teeth and belemnites. - Earth and also demonstrated no evidence of damage. Planetary Science Letters 286: 198-207. HYLTON, M. 2000. Microfaunal investigation of the Early Toarcian (Lower Jurassic) extinction event References in N.W. Europe. - Unpubl. PhD Thesis, University of BAILEY, T.R., ROSENTHAL, Y., McARTHUR, J.M., VAN Plymouth. DE SCHOOTBRUGGE, B. & THIRLWALL, M.F. 2003. KEMP, D. B., CoE, AL., COHEN, AS. & WEEDON, G.P. 2011. Paleoceanographic changes of the Late Pliensbachian­ Astronomical forcing and chronology of the early Early Toarcian interval: a possible link to the genesis Toarcian (Early Jurassic) oceanic anoxic event in of an Oceanic Anoxic Event. - Earth and Planetary Yorkshire, UK.- Paleoceanography 26: 1-17. Sciences 212: 307-320. PEARCE, C.R., COHEN, A.S., CoE, A.L, & BURTON, K.W. 2008. BUCEFALO PALLIANI, R.B., MATTIOLI, E. & RIDING, J.B. Molybdenum isotope evidence for global ocean anoxia 2002. The response of marine phytoplankton and coupled with perturbations to the carbon cycle during sedimentary organic matter to the early Toarcian the Early Jurassic. - Geology 36: 231-234. (lower Jurassic) oceanic anoxic event in northern REOLID, M. SEBANE, A., RODRIGUEZ-TOVAR, F.J. & MAROK, England. - Marine Micropaleontology 46: 223-245. A. 2012. Foraminiferal morphogroups as a tool CASWELL, B.A., COE, AL. & COHEN, A.S. 2009. New range to approach the Toarcian Anoxic Event in the data fo r marine invertebrate species across the early Western Saharan Atlas (Algeria). - Palaeogeography, Toarcian (Early Jurassic) mass extinction. - Journal of Palaeoclimatology, Palaeoecology 323-325: 97-99. 96 9th International Congress on the Jurassic System - Abstracts

Palaeobiogeographical study of the Middle-Upper Jurassic corals in East­ Central Iran

KA.VEHKHAKSAR1 *, MANOOCHEHR FARBOODI2 & ALIREZA KHAKSAR3

1Department of Civil Engineering, Rudehen Branch, Islamic Azad University - Rudehen, Iran; E-mail: k. [email protected] 2Department of Soil Science, Islamic Azad University, Mianeh branch, Mianeh City, Iran; E-mail: fa [email protected] 3 Islamic Azad University, Karaj branch, Ka raj-Iran

*Corresponding author

During the Jurassic the Iranian platform was ends with red siliciclastic strata or evaporates. situated north of the equator and near the Rocks in this sedimentary cycle have been Euroasian platform. Corals are one kind of the deposited between two tectonic events; the most abundant Jurassic fossils in Iran, because Mid-Cimmerian (Middle Jurassic) and the Late ofthe best environmental conditions for growth Cimmerian (early Cretaceous) event. This and survival. sedimentary cycle is named Magu Group. On the Iran Plate (Sanandaj-Sirjan, Central Located as a triangle in the middle of Iran, Iran, Alborz and Azerbaijan), Jurassic rocks are Central Iran is one of the most important and representative of two large and independent complicated structural zones in Iran. According sedimentary cycles whose boundaries have to STOCKLIN (1968), Central Iran is bordered by been attributed to tectonic events. The first cycle the Alborz Mountains in the north, Lut Block is pertaining to the Lower to Middle Jurassic in the east, and Sanandaj-Sirjan in the south­ and contains coal-bearing shale and sandstone, southwest, whereas NABAVI (1976) considers which have been deposited in lagoonal and the northern part of t�e Lut Block as part of the nearshore environments. Its thickness varies Cen�ral Iran (Fig. 1). from several meters to over 3,000 meters. The Fossiliferous marine beds of Early Jurassic lower boundary of this group is identified by age occur in the form of thin, ammonite-bearing the Early Cimmerian disconformity and the sandstone and limestone intercalations in upper boundary by the Mid-Cimmerian event. the plant bearing succession, the oldest ones, The second sedimentary cycle is composed of of Early Liassic (Sinemurian) age, have been ammonite-bearing limestones and marls and found in the Kerman area. Paleontological

D ��tral lran

• AlbQrz-�ayjan

1. Structural units of Iran. Fig. 9rh International Congress on the Jurassic System - Abstracts 97

evidence for marine Pliensbachian is uncertain. from east-central Iran and by KHAKSAR (2010) A widespread marine transgression is indicated from the the Middle Shale Member of Qal-eh­ in the Toarcian-Bajocian (Bathonian) of the Dokhtar Formation (Tabas area, East Iran). Kerman-Yazd-Tabas area (Badamu Limestone). If we exclude corals with endemic character, Calcareous deposits prevail in the Middle­ there are 30 genera in the Jurassic of Central Upper Jurassic and in the Upper Jurassic (Qaleh Iran. Nine coral provinces have been established Dokhtar Fm., Esfandiar Limestone Fm. of East in the Jurassic: Europe, North America, South Iran). America, Australia, Madagascar, south-west The coral fauna from the Jurassic of Central Asia, south-east Asia, Euroasia, and Africa. Each Iran comprise 38 genera and have been studied province includes several zoogeographic areas. fo r the first time by FLUGEL (1966) from the The Jurassic corals of Iran have been compared Shotori Mountains, PANDEY & FURSICH (2003) with corals of the different provinces (Table 1). As Table 1 shows the corals assemblages of Ta ble 1. Coral genera of Central-East Iran and their Central-East Iran have the greatest similarity distribution in the different biogeographic provinces of jurassic time. (23 common genera) with the European Province. For this reason the Central-East Iran basin is part of the European province in J urassic Provinces -m :.0 paleozoogeography. East Asia and North Africa c: Ctl Ctl Ctl -0 ·c;; 0 Ctl ·c;; also exhibit important similarity with Central­ 0 <( <( ....Ctl ·cQ) ·Q)c �Ctl 0 East Iran (15 genera in common). West Asia and E E (;)Ctl (;)Q) "E Ctlen <( <(Q) -� Q) Euroasia show a stronger relationship towards <( I :: I Ctl CtlC) .c 0� Ctlen .c .c 0 "'0 Species c: "5 .ct .ct "5 "5 the Late Jurassic with 13 genera in common. Ctl 0 0 ::1.... 0 0 0 ·c Ctl = en z w::; w c: en en India has important similarity with the corals � � Actinastrea from the Central-East Iranian basin because * * * * * * * * Cyathophora of ten genera in common. Seven genera are * * * * * Cyathophylliopsis shared with South America, and the common * * * * Confusastraea elements with provinces of northern America * * * * * * Montlivaltia and Madagascar decrease to five genera. The * * * * * * * * * * Cyathophylliopsis greater the distance to other provinces, such as * * Latiphyllia northern America and Madagascar, the smaller * * * Confusastraea is the degree of similarity. * * * * * * Favites The similarity of the Central-East Iranian * * * Tri gerastra ea coral assemblage with European corals * * * * * * * Ampakabastraea is accountable because both areas were * * * * * * * Stibastrea comparatively close to each other,being situated * * * Ca/amophylliopsis on the northern margin of the Tethys during the * * * * * * Dermosmilia Jurassic. * * * * Dimorphomeandra * * References Craterastra ea * * * * FLOGEL, E. 1966. Mitteljurassische Korallen vom Ostrand Latomeandra * * der Gro8en Salzwiiste (Shotori-Kette, Iran). - Dimorpharaea Neues jahrbuch fiir Geologie und Palaontologie, * * * * * * * Periseris Abhandlungen 126: 46-91. * * * KHAKSAR, K. 2010. Stratigraphical position of jurassic Acrosmilia * * * corals from Middle Shale Member of Gala-Dokhtar Microsolena * * * * * * * Formation (Tabas Area-East Iran). - The 8th Tro choplegma * * * * International Congress on the jurassic system, August Rhipidogyra 9-13, 2010, Shehong ofSuining, Sichuan, China. * * * * NABAVI, M.H. 1976. An introduction to geology of Iran. - Codonosmilia * * Geological Survey of Iran, Tehran. [in Persian] Acanthogyra * * * PANDEY, D.K. & FURSICH, F.T. 2003. jurassic corals of east­ Th ecosmilia * * * * * * * central Iran. - Beringeria 32: 1-140. Epistreptophyl/um STOCKLIN, j. 1968. Structural history and tectonics of * * * * * * * Tro charea Iran. A review. - American Association of Petroleum * * * * * Geologists Bulletin 52: 1229-1258. Columnaphyllia * * 98 9rh International Congress on the Jurassic System - Abstracts

An overview ofthe Jurassic dinosaur fossil record from India: Implications for depositional fa cies and palaeoenvironments

ASHU KHOSLA

Centre of Advanced Study in Geology, Panjab University,Sector-1 4, Chandigarh-160014, India; E-mail: khosla1 [email protected]

The record of Indian sauropod dinosaurs is material includes parts of skull, teeth, large now well known from the Lower Jurassic of number of body armour plates, vertebrae, and Pranhita Godavari Valley, Adilabad District, parts of girdle bones (NATH et al. 2002). The Andhra Pradesh, southern India, and the Early sediments of the Dharmaram Formation are Middle Jurassic of Kachchh, Gujarat. The Indian represented by alternating pebbly, coarse cross­ dinosaurian record starts with the Upper bedded sandstones, red clays, and mudstones Dharmaram Formation (Andhra Pradesh), and show an upward-fining sequence, which which is of Early Jurassic age (Sinemurian) and seems to have been deposited under a laterally has yielded three sauropodomorph dinosaurs shifting meandering stream (RuoRA 1982). namely Lamplughsaura dharmaramensis, The Kota Formation conformably overlies the Pradhania gracilis, and an indeterminate Dharmaram Formation. The Kota Formation one (KUTTY et al. 2007). Lamplughsaura represents a typical continental deposit and, dharmaramensis was a heavily built adult based on lithologies, shows two differentkinds individual measuring about 10 m in length and of facies. The lower part of Kota Formation is represented by a partial postcranial skeleton composed of fine-grained cross-bedded, poorly containing teeth with hardly any or missing sorted arkosic sandstones (250 m) with pebbles coarse denticles on the mesial edge. Other ofbanded chert, red mudstones and yellow green characteristic features include the caudal clays (SO m) at the base, and was deposited in a cervical neural spines exhibiting a vertically fluvialenvir onment (river deltas). The sequence oriented ligamentous furrow on the cranial is O\;"erlain by creamy, bedded limestone and and caudal surfaces and the distal end of tibia calcareous shale, which are further overlain covering about 66 % of transverse width of the by a lOO-m-thick sequence of mudstones, astragalus (KuTTYetal. 2007). Pradhaniagracilis sandstones, siltstones, and ferruginous clays is a small ( 4 m) adult dinosaur and is known with desiccation cracks suggesting deposition by fragmentary material such as maxilla with in inland lakes (YADAGIRI & RA.o 1987; FEIST et a very prominent longitudinal ridge medially al. 1991). The invertebrate fauna is represented (KUTTY et al. 2007). The overlying early Jurassic by ostracodes, charophytes, and floral elements Kota Formation of the Pranhita Godavari Valley such as pollens but the vertebrate fauna has yielded three types of dinosaur skeletal especially of the Kota Formation is represented material. The first type contains numerous by semionotid fishes (Lepidotes, Parapedium cranial and postcranial bones of a large and Te tragonolepis), sauropod dinosaurs, a sauropod, Barapasaurus tagorei, which has pterosaur (Campylognathoides), a coelacanth slender limbs, and spoon-shaped teeth with (lndocoelacanthus robustus), teleosaurid coarse denticles. The ilium possesses a well­ crocodiles, turtles, lizards, and mammals that developed anterior process, the ischium is are indicative of aquatic, terrestrial, playa-type relatively slender and rod-like distally, and the lakes with increased salinity possibly resulting pubis has a well-developed terminal expansion from an arid climate and arboreal habitat (JAIN (JAIN et al. 1975). The second sauropod et al. 1975; RUDRA 1982; LOYAL et al. 1996; Ko tasaurus yamanpalliensis is represented by NATH et al. 2002). more than twelve individuals and characterized In Western India, Kachchh (Gujarat) by dorsal vertebrae and a low iliac blade represents the classical area fo r the study of (YADAGIRI 1988, 2001). The third dinosaur type jurassic dinosaurs. Fragmentary dinosaur belongs to ornithischia ( ankylosauria) and the skeletal material comprising vertebrae and 9th International Congress on the Jurassic System - Abstracts 99 limb elements along with large petrified wood relationship with the Porocharaceae. - Bulletin de la pieces has been recorded from a coarse-grained Societe botanique de France 138: 25-32. }ANA, S.K. & DAS, S.S. 2002. A report of a 157.8 m.y.­ sandstone and conglomerate horizon of Kuar old dinosaur bone from the Jurassic marine Chari Bet, Patcham Island which is of ? Aalenian­ Formation, Kutch, Gujarat and its taphonomic Early Bajocian age (earliest Middle Jurassic; significance. - Current Science 82 (1): 85-88. SATYANARAYANA et al. 1999). Dinosaur bone­ JAIN, S.L., KUTTY, T.S., ROY CHOWDHURY, T. & CHATTERJEE, S. 1975. The sauropod dinosaur from the Lower Jurassic rich horizons are well exposed in the Dingy Kota Formation of India. - Proceedings of the Royal Hill member of the Kaladongar Hill range Society, London Series A 188: 221-228. (Patcham Island) and Kuar Bet of northern KUTTY, T.S., CHATTERJEE, S., GALTON, P. M. & UPCHURCH, Kachchh. The Kaladongar Formation (a 450-m­ P. 2007. Basal sauropodomorphs (Dinosauria: thick sequence), consists of mixed siliciclastic­ Saurischia) from the Lower Jurassic of India: Their anatomy and relationships. - Journal of Paleontology carbonate sediments intercalated with shales, 81: 1218-1240. and this formation represent six differentfa des JOSEPH, J.K., PATEL, S.J. & BHATT, Y. 2012. Trace fossil ( micritic mudrock, micritic sandstone, muddy assemblages in mixed siliciclastic-carbonate micrite, sandy micrite, allochemic sandstone sediments of the Kaladongar Formation (Middle Jurassic), Patcham Island, Kachchh, Western India. and sandy allochemic limestone (J OSEPH et al. - Journal of the Geological Society of India 80: 189- 2012). Based on sedimentological and trace 214. fossil studies the depositional environments LOYAL, R.S., KHOSLA, A. & SAHNI, A. 1996. Gondwanan of the dinosaur-bearing Kaladongar Formation dinosaurs of India: affinities and palaeobiogeography. represent nearshore (SATYANARAYANA et al. - Memoirs ofthe Queensland Museum 39: 627-638. MOSER, M., MATHUR, U.B., FURSICH, F.T., PANDEY, D.K. 1990) and foreshore to offshore environments & MATHUR, N. 2006. Oldest camarasauromorph under fluctuating wave and current energy sauropod (Dinosauria) discovered in the Middle (JosEPH et al. 2012). The overlying marine jurassic (Bajocian) of the Khadir Island, Kachchh, Chari Formation, which is Callovian in age, western India. - PaHiontologische Zeitschrift80: 34- 51. is 200 m thick and is rimarily composed p NATH, T.T., YA DAGIRI, P. & MOITRA, A.K. 2002. First record of shale, sandstone and limestone and has of armoured dinosaur from the Lower jurassic Kota yielded the proximal part of a hind limb bone Formation, Pranhita-Godavari valley, Andhra Pradesh. (tibia) of a sauropod dinosaur from Jumara, - Journal of the Geological Society of India 59: 575- Kachchh Mainland (JANA & DAS 2002). The 577. RuoRA, D.K. 1982. Upper Gondwana stratigraphy and dinosaur bone was associated with ammonites sedimentation in the Pranhita-Godavari Valley, India. and was deposited in warm, shallow marine - Quarterly Journal of the Geological, Mining and shelf fades (JANA & DAs 2002). More recently, Metallurgical Society of India 54 (3 and 4): 56-79. fragmentary scattered remains of massive SATYANARAYANA, K., DASGUPTA, D.K., DAVE, A. & DAS, K.K. 1999. Record of skeletal remains of dinosaur from sauropods of Middle Jurassic (Bajocian) age early Middle Jurassic of Kuar Bet, Kutch, Gujarat. - have also been recovered from non-marine Current Science 77: 639-641. parts of the Khadir Formation of Khadir Island YA DAGIRI, P. 1988. A new sauropod Ko tasaurus (Kachchh). The material includes a metacarpal, yamanpalliensis from Lower Jurassic Kota Formation a first pedal claw and a fibula, which belongs of India. - Records of the Geological Survey of India 11: 102-127. to the Camarasauromorpha and represents the YA DAGIRI, P. 2001. The osteology of Ko tasaurus oldest evidence of that derived dinosaur group yamanpalliensis, a sauropod dinosaur from the (MOSER et al. 2006). Early jurassic Kota Formation of India. - Journal of Vertebrate Palaeontology 21: 242-252. YA DAGIRI, P. & RAo, B.R.J. 1987, Contribution to the References stratigraphy and vertebrate fauna of Lower Jurassic FEIST, M., BHATIA, S.B. & YA DAGIRI, P. 1991. On the oldest Kota Formation, Pranhita-Godavari valley, India. - representative of the family Characeae and its The Palaeobotanist 36: 230-244. 100 9th International Congress on the Jurassic System - Abstracts

Ostracod biostratigraphical zonation of the Middle Jurassic beds of western India - a review

S. C. KHOSLA

GA -11, Sector 5, Hi ran Magri, Udaipur - 313 002, India; E-mail: sckhosla1 @yahoo.com

The Middle Jurassic beds in western India are (middle Late Callovian) and Majungaella widely exposed in the Kachchh and Jaisalmer perforata kachchhensis - Galliaecytheridea basins of Gujarat and Rajasthan states, remota Concurrent Range Zone (middle Late respectively. These beds represent marine facies Callovian). and are rich in both macro- and microfaunas. In Five range zones are recognized in the Kachchh Basin the beds crop out in three the Northern Island Belt. They are the east-west trending anticlinal hill ranges and Trichordis hadibhadangensis Range Zone the isolated landmass of Wagad. The three hill (Bajocian-Bathonian), Cytheropteron ranges are broken up by transverse undulations micropunctata Range Zone (Bathonian), into number of domes, the erosion of which has Progonocythere laeviscula Range Zone (Late exposed successive beds in a concentric series of Bathonian-Early Callovian), Fastigatocythere small scarps, which afford an ideal opportunity (Habocythere) mouwanaensis Range Zone to the fo ssil collector. In the Jaisalmer Basin, the (Callovian), and Majungaella perforata beds are exposed in a stretch extending between kachchhensis Galliaecytheridea remota Thaiyat Village in the east and Ludharwa Village Concurrent Range Zone (middle Late in the west of Jaisalmer city. Callovian). We (S.C. KHOSLA and his Ph.D. students S.R. Four range zones are recognized }AKHAR, M.H. MOHAMMED, MANISHA KUMARI, in the Jaisalmer District. They are the A. DARWIN FELIX, and SANJAY DUBEY) of the Trichordis hadibhadangensis Range Zone Department of Geology, Mohanlal Sukhadia (Bajocian-Bathonia�), Majungaella perforata University, Udaipur have carried out extensive kacl}.chhensis- Fastigatocythere (Batella) falcula research work on the Middle Jurassic ostracods Concurrent Range Zone (Late Bathonian-Early ofKachchh and Jaisalmer baisins during the last Callovian ), Majungaella perforata kachchhensis two decades. We have described a total of 130 Galliaecytheridea remota Concurrent species from the Habo, Jhura, and Jumara domes Range Zone (middle Late Callovian), and of the Kachchh Mainland, Pachchham, Khadir, the Majungaella perforata kachchhensis - and Bela islands of the Northern Island Belt in Galliaecytheridea remota Interval Zone (middle the Rann of Kachchh and from the Jaisalmer Late Callovian). Basin. The common zones in the Kachchh Mainland On the basis of the distribution of ostracods and the Jaisalmer Basin compare well with each three range zones are recognized in the Middle other and are extremely useful in interbasinal Jurassic of the Kachchh Mainland. These are correlation. They have been standardized with the Progonocythere laeviscula Range Zone fo raminiferal and ammonite zones, wherever (Late Bathonian - Early Callovian), Majungaella possible. perforata kachchhensis Partial Range Zone 9th International Congress on the Jurassic System - Abstracts 101

The Jurassic-Cretaceous short-lived atoll coral reefs around active volcanoes in the Western Tethys (Ukrainian Carpathians)

MICHAt. KROBICKI1•2, ANNA FELDMAN-0LSZEWSKA3, }OLANTA IWANCZUK3 & 0LEH HNYLK04

1Polish Geological Institute - National Research Institute, Kr6lowej ]adwigi 1, 41-200 Sosnowiec, Poland; E-mail: [email protected] 2AGH Universityof Science and Te chnology, Mickiewicza 30, 30-059 Krak6w,Po land; E-mail- krobicki@ geol.agh.edu.pl 3Polish Geological Institute - National Research Institute, Rakowiecka 4, 00-975 Wa rszawa, Poland; E-mail: [email protected], [email protected] 4Institute of Geology and Geochemistryof Combustible Minerals of NAS of Ukraine, Naukova 3a, 79060 Lviv, Ukraine; E-mail: [email protected]

The Outer Flysch Carpathians is one of the of dark cherts. Sedimentologically we can biggest belt of stack of flysch nappes in Europe. interpret them as distal deep-marine lobes of It occupied a large part of central-European turbidite fans. In contrast, more coarse-grained countries and is almost exclusively constructed pyroclastic sandstones and fine-grained by siliciclastic flysch-type rocks. In the frontal pyroclastic conglomerates could represent more part of the Marmarosh Massif in the Ukrainian proximal turbidites. All these rocks type exhibit Carpathians the Outer Dacides-Severinides typical flysch features including sharp base of are represented by the Kaminnyi Potik and beds with clasts of allochthonous material, Rachiv units (nap pes). The Rachiv nappe is fractionation of grains, ripple lamination, and represented by folded Lower Cretaceousflysch increase of pelagic character of the topmost part dipping generally toward the southwest under of beds (up to micritic limestones). The most the Kaminnyi Potik unit and is overthrust on proximal fa des displays a chaotic calcareous­ the Porkulets Nappe (SLACZKA et al. 2006 with pyroclastic breccia with blocks of the micritic references). and organodetritic limestones and basalts The other types of the flysch-type rocks are (even as pillow lava fragments) which occur represented by rare occurrences of calcareous within a volcanicjtuffitic matrix, and represent, flysch (e.g., the Jurassic-Cretaceous so-called most probably, submarine debris flows. In our Cieszyn Formation in Czech Republic and reconstruction, this fades has a continuous Poland or its facial and stratigraphic equivalent transition to proximal flysch-type fades in the - the Sinaia Beds in Romania), full of allodapic same basin on the one side, and to massive carbonate intercalations with shallow-water basaltic pillow lava flows on the other side, resedimented elements such as ooids, fragments which ofteneo-occur with these debris flows. of thick-shelled benthic fossils, green-algae, etc. The volcanic-sedimentary complex of Extremely sporadic are pyroclastic the Chyvchyn Mt. does not form a single turbidites which are concentrated within stratigraphic sequence, as was assumed in the Transcarpathian Ukrainian part of previous studies. Recently, our geological the Flysch Carpathians and occur in the mapping work showed that this complex forms Ukrainian-Romanian transborder zone the tectonic klippe which consists fo ur small (Kaminnyi Potik Unit). tectonic scales (HNYLKO et al. 2012). Structurally, TheKaminnyiPotikUnit(Nappe) occursinthe the lowermost is developed as thin-bedded vicinity of Rachiv cityand in the SE prolongation light- and dark-grey micritic limestones with of this unit to the Chyvchynian Mountains. Such lenses of dark cherts. It is interbedded with unique flysch-type rocks are usually developed coarse-/fine-grained calcareous pyroclastic as more or less thin intercalations both of turbidites (flysch) (Kaminnyi Potik Fm.) and is coarse- and fine-grained calcareous pyroclastic similar to the stratotypeof this formation in the beds within thin-bedded light- and dark-grey Kaminnyi Potik stream near Rakhiv (KROBICKI micritic limestones occasionally with lenses 2012). The second scale mostly consists of 102 9thInternational Congress on the Jurassic System -Abstracts calcareous-pyroclastic breccia with blocks of Transilvanides (MEDVEDEV & VA RITCHEV 2000). the micritic and organo-detritic limestones and Final clarification of this problem is impossible basalts which occur within a volcanicftuffitic without the correlation of the Chyvchyn Mt. matrix, which represents, most probably, structures with the volcanic formations of the submarine debris flows (KROBICKI et al. 2013a, Romanian Carpathians (especially Farcaul and b). The third scale is composed of breccia with Mihailecul mounts). volcanic matrix and clasts of the effusive rocks (occasionally as pillow lava fragments) and rare References limestones. The fourth scale crops out on the HNYLKO, 0., KROBICKI, M., FELDMAN-0LSZEWSKA, A. & Chyvchyn peak and is represented by massive IWANCZUK, J. 2012. Volcanic-sedimentary complex basalts with typical pillow lava structures. These of the Kaminnyi Potik Unit on the Chyvchyn Mount (Ukrainian Carpathians). In: Jo A, REH Ko , D. successions have probably been formed during zs S., A vA & VOJTKO, R. (eds.), Environmental, Structural and latest Jurassicjearliest Cretaceous time in the Stratigraphical Evolution of the Western Carpathians. Outer Dacide-Severinide part of the Carpathian 8th Conference 2012, Abstract Book: 14, Bratislava,. basins. KROBICKI, M. 2012. Field trip. In: KROBICKI, M. (ed.), In both cases, in the Kaminnyi Potik section JURASSICA X: Jurassic-Lower Cretaceous deposits and the Chyvchyn Mt., we fo und biodetritic of the Pieniny Klippen Belt and sourrounding areas (Ukraine - Transcarpathians, Eastern Slovakia). - limestones full of corals and remains of Abstracts and field trip guide-book, Rakhiv-Beiiatina other benthic fauna (brachiopods, bivalves, 25-30.06.2012: 31-56. Panstw. Inst. Geol. - PIB, crinoids, etc ). In the fo rmer section this Warszawa. [in Polish only] type of limestones is overlain by biodetritic KROBICKI, M., HNYLKO, 0., FELDMAN-0LSZEWSKA, A. & IWANCZUK, J. 2013a. Kaminnyi Potik Unit in the crinoidal limestones with several pyroclastic Ukrainian Carpathians and its volcanogenic rocks. In: layer intercalations, which occur also within FODOR, L. & KOVER, S. (eds.) 11th Meeting ofthe Central coral-bearing limestones. In the latter section European Tectonic Studies Group (CETeG), Vargesztes a large thickness of debris flow is full of large (Western Hungary, Vertes and Gerecse Hills, M or wine blocks of coral limestones. In our opinion, most region), 24-27th April 2013,- Abstract Book: 38-40. KROBICKI, M., IWANCZUK, J., FELDMAN-0LSZEWSKA, A. probably they represent short-lived atoll coral & HNYLKO, 0. 2013b. Jurajsko-kredowe utwory reefs, which surrounded volcanoes. The coral wulkanogeniczne jednostki kamiennopotockiej reefs did not survive for a long time due to (gora Czywczyn, Karpaty Ukrainskie) - wstepne extensive volcanic activity with huge amounts badania sedymentologiczne. In: KROBICKI, M. & FELDMAN-OLSZEWSKA, A. (eds.), V Polska Konferencja of pyroclastic ash and due to synsedimentary Sedymentologiczna POKOS 5'2013. - Glebokomorska gravitydebris flows that originated after rapid, sedymentacja fliszowa - sedymentologiczne aspekty big explosions of volcanoes. historii basenow karpackich, 16-19.05.2013, Zywiec: In our opinion, the latest Jurassic - earliest 189-191. Cretaceous volcanic activityin this part of the MEDVEDEV, A.P. & VA RITCHEV, A. 2000. Pra-Carpathians (Construction and de-construction). 115 p., Lviv [in Carpathian basins could be one of the best keys Ukrainian only] to understanding the geodynamic history of SLJ\CZKA, A., KRUGLOV, S.S., GOLONKA, J., OSZCZYPKO, N. & POPADYUK, 2006. Geology and hydrocarbon the northernmost part of the N eotethys. These 1., successions have probably been formed during resources of the Outer Carpathians, Poland, Slovakia, and Ukraine: general geology. In: GoLONKA, J. & PICHA, the Jurassic-Cretaceous time in the Outer F. (eds.), The Carpathians and their foreland: geology Dacide-Severinide part ofthe Carpathian basins. and hydrocarbon resources. - AAPG Memoir 84: 221- The Chyvchyn nappe could be a remnant of the 258. 9th International Congress on the Jurassic System - Abstracts 103

Palaeoenvironmental context and palaeoecological significance of microbialites - metazoan assemblages from condensed deposits at the Middle-Upper Jurassic transition (Getic Unit, Southern Carpathians, Romania)

IULIANA LAZAR* & MIHAELA GRADINARU

Department of Geolog� Facultyof Geology and Geophysics, Universityof Bucharest, 1 N. Biilcescu Bd, 010041 Bucharest, Romania; E-Mail: [email protected]; [email protected]

*Corresponding author

Condensed deposits and different types of stromatolites) and different metazoans (such as related discontinuities represent distinguished serpulid tube worms, agglutinated polychaete patterns of the peri-Tethyan Jurassic tube worms, bryozoans, and even arthropods) successions, which were extensively studied documented within the fossil assemblages of for the evaluation of the palaeoenvironmental Middle Jurassic condensed sequences from the features of different parts of the sedimentary southern Carpathians in Romania. basins during the time intervals characterized Eight J urassic sections represented by mixed by reduced sedimentation (FURSICH et al. carbonate-siliciclastic condensed sequences 1992 and references therein) and also for the (Bajocian-Oxfordian) were studied, which are fascinating palaeoecology and evolution of located in two main zones: the Rudir-Bran zone their characteristic hard substrate communities and the Bucegi Mountains. The methodology (TAYLOR & WILSON 20.03 and extensive for this study included complementary pal­ references therein), as well as for the interesting aeontological, sedimentological, mineralogical, taphonomy of their fossil assemblages. Sections geochemical, and taphonomic approaches. with condensed deposits at the Middle-Upper One-hundred-fifty petrographic thin-sections Jurassic transition are well known from the have been prepared and analysed to determine peri-Tethyan Europe (Portugal, Spain, France, the grain composition and the types of Switzerland, Germany, Poland, Hungary, and carbonate cements, microstructures, and Romania). Numerous hypotheses have been microfacies types; thirty polished slabs were proposed fo r the origin of these deposits, most examined under the cathodoluminescence (CL) of them being related to the tectonic events microscopy. Samples were also analysed for generated during the Jurassic by the recognized carbon and oxygen stable isotopes. general extension in the Tethyan domain. In The sector of the Leaota ridge the southern Carpathians the effects of these (corresponding to the studied zones) evolved tectonic events are recognized within the during the Bajocian-Oxfordian interval from sedimentary successions belonging to the Getic a mid- to distal shelf setting to a deep-water Nappe, one of the major geotectonic units of setting near the topmost part of the slope. Due the Median Dacides (SANDULESCU 1984). In the to the faulting and differential subsidence of southern Carpathians, the sedimentary cover this ridge, the resulting fault blocks acted like of the Getic Domain is represented by Triassic­ short-lived swells where condensed deposits Lower Cretaceous rocks preserved in different and Fe-mineralized hardgrounds formed. zones (e.g., Rudir-Bran zone, Bucegi Mountains, Contemporaneous tectonic activity related to Piatra Craiului Mountains), which evolved as the extensional processes within the strongly segments of a ridge area (e.g., Leaota Ridge; cf. deformed European continental margin are, for PATRULIUS 1969). the first time, documented in the studied zone The aim of this contribution is to describe the by differences in thickness and stratigraphic interactions between different types of micro­ extension of the condensed members within bialites (such as ferruginous stromatolites/ the studied sections, as well as by the presence microstromatolites and agglutinated of neptunian dykes, clastic dykes and tectonic 104 9thInternational Congress on the Jurassic System - Abstracts breccias developed at submarine fault scarps. with peloidal agglutinated stromatolites; Specific environments/micro-environments these assemblages were observed in the appropriate fo r development of different topmost part of the Callovian limestone types of deep-water microbialites associated beds. with certain types of metazoans developed in connection with the previously mentioned The described microbialite-metazoan events. Three types of microbialite-metazoan assemblages are palaeoecologically significant assemblages have been observed in the studied as they represent records of short-term events successions: producing fluctuations of palaeoenvironmental parameters (such as water energy, degree of

• The first one is referring to the ferruginous oxygenation, availability of fo od resources, microstromatolites that cover the availability of grains of specific sizes and hardground surfaces and erosional shapes, and of protected hard substrates cavities or fo rm the cortex of oncoids suitable for settlement) during prolonged and macro-oncoids, associated with intervals of condensed sedimentation. The dense colonies of serpulids, agglutinated multi-disciplinary approach of the present polychaete tube worms, bryozoans, and study allows the evaluation of small-scale encrusting foraminifera. This is the first changes within past environments where such record of agglutinated polychaete tube interactions are recorded. Such studies are of worms - ferruginous microstromatolite importance as they could be correlated with assemblages. These assemblages are synsedimentary tectonic events that likely were developed in the topmost part of the associated with locally hydrothermal vents, Bathonian - Early Callovian condensed but they also reflects the effects of regional level; the morphology of the ferruginous and global changes documented for this time microstromatolites, their microbial origin, interval in different peri-Tethyan areas. and the palaeoenvironmental context of their genesis have been discussed in detail The present study represents the results of an extensive project supported by CNCS PN-11-ID-PCE-2011-3-0025. in a previous paper (LAZAR et al. 2013).

• The second one is referring to sub­ Refetences horizontal, irregular cavities of variable FURSICH, F.T., 0SCHMANN, W., SINGH, 1.8. & }AITLY, A.K. thickness(0.1-0.3 m), filled by red 1992. Hardgrounds, reworked concretion levels and bioclastic packstone-wackestone; intensive condensed horizons in the Jurassic of western India: their significance for basin analysis. - Journal of microbial activity within these submarine Geological SocietyLondon 149: 313-331. cavities is documented by the presence LAZAR, 1., GRADINARU, M. & PETRESCU, L. 2013. Ferruginous of Fe-endostromatolites, Frutexites-like microstromatolites related to Middle Jurassic structures, and by the local development condensed sequences and hardgrounds (Bucegi Mountains, Southern Carpathians, Romania). - Facies of agglutinated stromatolites containing 59: 359-390. doi:10.1007fs10347- 012-0313-S numerous crustacean microcoprolites of PATRULIUS, D. 1969. Geologia Masivului Bucegi �i a Fa vreina carpatica (SENOWBARI-DARYAN Culoarului Dambovicioara. 329 pp., EdituraAcademiei et al. 2013). These cavities occur in the RSR, Bucure�ti. topmost part of a pink bioclastic, micritic, SANDULESCU, M. 1984. Geotectonica Romaniei. 336 pp., Ed Tehnidi, Bucure�ti. and pelmicritic limestone (1.5 m) containing SENOWBARI-DARYAN, LAZAR, I. & BUCUR, 1.1. 2013. 8., Middle to Late Callovian ammonites. Fa vreina carpatica nov. ichnosp. (crustacean­ microcoprolite) from the Middle Jurassic of Rucar­ • The third type is represented by stromatactis cavities and other types of Bran zone (Southern Carpathians, Romania). - Rivista italiana di Paleontologia e Stratigrafia 119: 175-182. submarine fissures and cavities containing TAYLOR, P. D. & WILSON, M.A. 2003. Palaeoecology and troglobite metazoans such as the ostracod evolution of marine hard substrate communities. - Pokorniopsis and rare serpulids associated Earth Science Reviews 62:1-103. 9th International Congress on the Jurassic System - Abstracts 105

Jurassic - Early Cretaceous evolution of the passive margin of the Moesian Plate (Danubian Unit, Romanian Carpathians)

IULIANA LAZAR1 *, MICHAt.KR OBICKI2• 3, MIHAELA GRADINARU1 & MIHAI E. POPA1

1Department of Geology, Faculty of Geology and Geophysics, University of Bucharest, 1 N. Bii/cescu Bd, 010041 Bucharest, Romania; E-mail: [email protected], [email protected], [email protected] 2Po/ish Geological Institute - National Research Institute, Kr6lowej ]adwigi 1, 41-200 Sosnowiec, Poland; E-mail: [email protected] 3AGH Universityof Science and Technology, Mickiewicza 30, 30-059 Krak6w, Poland; £-mail: krobicki@ geol.agh.edu.pl

*Corresponding author

The Southern Carpathians are built up of a carbonate-siliciclastic deposits in the lower part, succession of nappes and thrust sheets with a and by more and more pelagic carbonates in its complicated geotectonic structure within the middle part with carbonate-siliceous rocks, and Carpathian Fold Belt. The studied successions by nodular limestones with cherts and allodapic belong to the sedimentary cover ofthe Danubian intercalations in the upper part, being finally Units, one of the most complex geotectonic units covered by pelagic, micritic limestones with of the Marginal Dacides that are interpreted cherts. The whole sequence could be subdivided as part of the strongly deformed European into at least 10 lithofacies units. The oldest continental margin (SANDULESCU 1994). The strata (1) are yellow and whitish arcosic-type, Danubian nappes represent the most external terrestrial sandstones with paleosoils, macro­ Carpathian units, as they continue south of and microflora (Glavcina Formation, Hettangian the Danube in Miroc (Serbia) and in the Stara - Early Sinemurian in age). The younger beds Planina and Prebalkan (Bulgaria) tectonic are strictly marine (2; about 60 m in thickness) units (SANDULEscu 1994; KRAUTNER & KRSTIC developed as brownish massive, medium­ 2002). The Danubian Units include several and thick-bedded calcareous sandstones, full thrust complexes while the studied succession both of benthic fauna (e.g., bivalves - mostly (Munteana-Dumbravita section) belongs to the grypheids, brachiopods - occasionally fo rming Upper Danubian nappe complex (according to mass occurrences and producing brachiopod IANCU et al. 2005), largely exposed in the western coquinas) and nektonic fauna (levels with part of the Danubian window in the Svinita area ammonites and rich in belemnites ), but large (western part of the Southern Carpathians). pieces of driftwood are rare. Some beds with Here, a unique, continuous succession, over abundant fe rruginous ooids occur as well, 300 m in thickness, represented by the jurassic especially in the lower and middle part of this - Early Cretaceous strata of Munteana­ area. Sedimentary structures such as cross­ Dumbravita section along the Danube River bedding and storm-induced fe atures occur in Romania has been studied in detail. This occasionally and document shallow-marine succession belongs to the Sirinia Basin (also regimes below the fair-weather wave-base. But known as the Svinita-Svinecea Mare sedimentary the shallowest episode is represented by fine­ zone), which was studied by RAILEANU (1960), and coarse-grained sandstones with big (up to 4 among other researchers. This large outcrop cm in diameter) quartz pebbles and mudstones, documents a deepening-upwards sequence with coal layers in the uppermost part of these with a full record of an opening marine/oceanic beds. Still younger (3; 62 m) are grey, pseudo­ realm since the earliest jurassic up to the nodular, coral-bearing, bioclastic limestones ·earliest Cretaceous, along the southern passive in the lower part, rich in branching corals margin of the Moesian Plate. This sequence is which also fo rm small patch reefs. Numerous generally represented by siliciclastic, and mixed bivalve borings occur in these coral colonies. 106 9th International Congress on the Jurassic System - Abstracts

Another fauna is represented by brachiopods, bedding (Upper CallovianfOxfordian-Lower bivalves, and isolated crinoids. In the upper Kimmeridgian; Zeli�te Formation). part occur well-bedded biodetritic limestones, The transition to the. - y-o unger part of occasionally with Lithiotis-type bivalves sequence (8; at least 60 m) is gentle and is and Aptyxiella-type gastropods, with thin represented by the occurrence in the topmost intercalations ofmudstones (up to 1.5 m thick). part of this unit of some beds of pseudo­ Sedimentologically, this part of the outcrop nodular limestones. However, this younger unit is represented by short-lived shallow-marine starts with red nodular Ammonitico Rosso-type carbonate platforms, primary with a coral­ limestones (more similar to Rosso ad Aptichi in dominated ramp, later influenced by terrestrial Italian nomenclature), and in the lower part material of little deeper environments. These contains cherts, but in the middle and upper units (1-3) represent most probably the Lower parts the thickness of allodapic limestone Jurassic(Middle-Late SinemurianuptoToarcian interbeds (up to an 6.4-m-thick bed) increases. - ?Early Aalenian; the Munteana Formation, a Several clasts in such type of beds represent lateral fa cies of the Sirinia Basin). shallow-water carbonates (occasionally with The next episode of sedimentation ( 4; corals and/ or ooids and algae) and document 5.5 m) is represented by a rapid change of rapid and huge re-deposition from a carbonate carbonate production and recorded by cherry­ source area, probably a carbonate platform red crinoidal limestones of deeper regimes, with coral reefs and oolitic shoals. This unit showing condensation features which include corresponds to the Kimmeridgian - Tithonian Fe-Mn laminated crusts (bacterial microbialites) interval, belonging to the Greben Formation. to the topmost part of this unit. It is also the last Still younger beds (9 and 10; at least 50 m or occurrence of isolated, fine grains of quartz, and more) are thin- and medium-bedded light­ this is why these fa cts could be interpreted as grey micritic limestones similar to Maiolica final drawing of macrobenthic fauna-bearing facies (the Murguceva Formation; uppermost carbonate environments of the shallow (1-3) Tithonian - Lower Hauterivian). This part of and moderate deep (4) sea bottom, documenting the outcrop is tectonically incomplete but it one of the most important re-organization of the documents still a pelagic type of sedimentation wide opening ocean. This unit ( 4) represents the in quiet, deep-water environments. Middle Jurassic (Bajocian-Bathonian; Saraorschi The Munteana-Dumbravita section is one Formation), which is overlain by strictly pelagic, of the best profiles of the Southern Carpathians fully marine carbonate-siliceous sediments. The in Romania, comprising the whole Jurassic and first sequence is represented by red marls and the earliest Cretaceous strata of the Danubian red nodular limestones of Ammonitico Rosso­ Units. From a paleogeographic point ofview , this type (5; 8.5 m) (?Bathonian - Lower Callovian; succession documents very well the opening Toplita Formation), more similar to typical of a new oceanic domain and, according to the Mediterranean Ammonitico Rosso marneux. geotectonic sketch, it represents the passive The deepest episode of sedimentation took margin of a continent, in this case the Moesian place during the original complex (6) of green, Plate. variegated and red siliceous limestones with References cherts, or thin-bedded radiolarites, almost 55- IANCU, V., BERZA T., SEGHEDI A., GHEUCA I. & HANN H.-P. m-thick (Middle Callovian; Seretina Formation). 2005. Alpine polyphase tectono-metamorphic The first massive limestone bed without cherts evolution of the South Carpathians: A new overview. - marks the base of a new part of the succession Tectonophysics 410: 337-365. (7; almost 45 m) still strictly pelagic, but its KRA.UTNER, H.G. & KRSTIC, B. 2002. Alpine and pre-Alpine structural units within the Southern Carpathians middle and upper parts yielding cherts yet and Western Balkanides. - Geologica Carpathica again. The colors of these beds are variable, 53, Special Issue, Proceedings of XVII Congress of from variegated to reddish, while in the middle Carpathian-Balkan Geological Association, Bratislava. part, the first allodapic (calcareous turbidites) RAILEANU, G. 1960. Recherches geologiques dans la region Svini�a-Fa�a Mare. - Ann. Corn. Geol. 26-28: 347-383. limestones occur. These beds exhibit typical SA.NDULESCU, M. 1994. Overview on Romanian geology. - turbidite features with sharp, erosional base, Romanian Journal of Tectonics and Regional Geology fractionation of grainsfclasts, and cross- 75: 3-15. 9th International Congress on the Jurassic System - Abstracts 107

Jurassic ammonitefaunas ofnor thern Iran and their palaeobiogeographic significance

MAHMOUD REZA MAJIDIFARD

Research Institute fo r Earth Sciences, Geological Survey of Iran, Te hran, Iran; E-mail: m_maj idifard@ yahoo. corn

The UpperBajocian-Tithonianammonitefaunas preferences of the groups, because in central of NNE Iran are mostly of Submediterranean and northern Iran very shallowwaterconditions affinity, but elements of Subboreal, prevailed during the Aalenian to Early Bajocian Mediterranean, and Ethiopian (Madagascar, (Shemshak Sea). As a result of the Late Bajocian eastern Africa, Ethiopia, Somaliland, and sea level rise fo llowing the Mid-Cimmerian Kachchh) provinces are occasionally tectonic event fairly deep marine environments intermingled.Amongthe 30 genera only a few can were established especially in the Alborz and be regarded as belonging to one ofthe Subboreal, Koppeh Dagh basins (Dalichai and Chaman­ Mediterranean or Ethiopian provinces. In order Bid formations, respectively).The dominating to unravel the origin of the faunal elements and ammonites inhabiting these basins show a their migration routes, the relationship of the clear relationship to the Submediterranean ammonite fauna of Iran to that of other regions province. This is supported by the occurrence was analysed. On the whole, at the species level of Submediterranean ammonites such as the Aalenian to early Bajocian ammonite faunas Garantiana, Macrocephalites, Morphoceras, of northern and central Iran show a very close Pachyceras, Larcheria, Orthosphinctes, relationship to that of northwestern Europe, A Dichotomoceras, and Richterella and some characteristic feature of this fauna is the scarcity cosmopolitan taxa such as Cadomites, Oxycerites, of Phylloceratidae (accounting for less than 1% Ta ramelliceras, Hecticoceras, and Reineckeia. to up to 3%) and the lack of Lithoceratidae. In Moreover, palaeogeographic reconstructions contrast, from the Late Bajocian to Oxfordian place the Iranian platform at a latitude of 30° Phylloceratidae account for more than 50°/o N during the Jurassic, which is equivalent to of the ammonites in the studied sections. This European areas situated at the southern margin feature can be explained by differing depth of Eurasia. 108 9th International Congress on the Jurassic System - Abstracts

Middle Jurassic ostracod fauna from Jaisalmer, Rajasthan;'"lndia

KUMARI MANISHA*, MANISH M. LAL & S. VIDHYA

Department of Earth Sciences, SPCAS, Pondicherry University, Puducherry 605014, India; E-mail: drmku mari@g mail. corn

*Corresponding author

The Mesozoic beds of the Jaisalmer Basin, localities, covering all five members of the Rajasthan, have long been known to Jaisalmer Formation, have been systematically geoscientists. These beds cover a large area of sampled. All members yielded a rich and about 4200 km2, attain a maximum thickness of well preserved ostracod fauna which is 1085 m on the surface and range in age from represented by 151 species. These belong to the Lias to Aptian (DAS GUPTA 1975). The beds 38 genera (excluding 8 indeterminate taxa). are predominantly marine and are rich in both Seventy species are new records from the macro- and microfaunas. In the present work, basin: Acanthocythere sp. cf. A. sphaerulata, the author has followed DAs GUPTA (1975) for Acrocythere khoslai, Anchistrocheles sp. A, A. the stratigraphic classification of the Jurassic sp. B, Bairdopillata sp. A, B. sp. B, Bhatina sp., succession of the basin. The Hamira Member By thoceratina sp., By thocypris jaisalmerensis, B. comprises a succession of yellow, buff-coloured sp. A, B. sp. B, By thoceratina reticulata, Cy therella arenaceous limestones, yellowish shales, and jurassica, C. sp., Cy therelloidea reticulata, C. sp. marly limestone and contains gastropods, A, C. sp. B, Cy theropteron badabagensis, C. sp. brachiopods, and bivalves. The Joyan Member A, C. sp. B, C. sp. C, C. sp. D, C. sp. E, Darwinula consistsoflight-yellowshale,yellowfossiliferous sp., Eocytheridea elongata, Eucytherura sandstone and hard, buff-coloured limestone badabagensis, E. nagorii, E. sp. B, Fabanella with corals, well exposed around J oyan, along paradimorpha, F. minaae, F. badabagensis, the Jaisalmer-Polji-ki-Deri Road to Kanodh, F. parasarda, F. cy lindrica, F. rectangulata, F. and along the Mohangarh road. Bivalves and sp.', Fastigatocythere sp. cf. F.? spinisulcata, F. corals occur in this member. The Fort Member (Amicytheridea) triangulata jaisalmerensis, is divisible into a lower unit of white to off­ F. (A.) sp. A, F. (A.) sp. B, F. (Habocythere) white sandstone with minor intercalations of sp., F.? (Batella) sp., Galliaecytheridea sp., calcareous shales, and an upper unit of yellow Glabellacythere parahussaini, Leiria sp., and greyish yellow limestone with or without Lophocythere sp., Macrodentina jaisalmerensis, fossils, along with marl and shale; the member Mandelstamia jakhari, M.? jaisalmerensis, contains foraminifers, ostracods, bivalves, Micropneumatocythere joyanensis, M. gastropods, echinoids, and brachiopods. The paramasurdiensis, M. sp., Monoceratina Badabag Member comprises soft,yellow , cross­ jajiyaensis, M. sp., Morkhovenicythereis bedded sandstone, fo ssiliferous marl, a flat jaisalmerensis, Paracypris jaisalmerensis, pebble conglomerate, buff and golden yellow P. trapizea, Paradoxorhyncha punctata, limestone, both with and without fossils, and P. jaisalmerensis, Paranotacythere sp., P. yellow and greenish shales. Brachiopods, sp. A, Procytheridea jaisalmerensis, P. sp., bivalves, ostracods, and fo raminifers are well Progonocythere ovata, P: �p�; Protobuntonia sp., preserved in this member. The Kuldhar Member Theriosynoecum sp. A, T. sp. B, Trichordis minuta comprises golden yellow-brown limestone with and T. sp. Seventy-five species are assigned to or without fo ssils, marl, greenish shales, oolitic already known taxa. Six species - Genus A-F are limestone beds, and cross-bedded sandstone. indeterminate. The rich fossil assemblage consists of Based on the stratigraphic distribution of brachiopods, bivalves, cephalopods, ostracods the ostracods, five zones are proposed. They are, and fo raminifers. in ascending order, the Micropneumatocythere In all twenty-two sections at different joyanensis Range Zone (Bajocian), Trichordis 9th International Congress on the Jurassic System -Abstracts 109 hadibhadangensis Range Zone (late Bajocian - The paper is based on the fieldwork carried out under the early Bathonian), Cy theropteron micropunctata DST sponsored Research project no. SR/FTP /ES-04/2003. The first author is highly thankful to the Department of Macrodentina Range Zone (Bathonian), Science and Technology, Government of India, New Delhi, jaisa lmerensis Range Zone (late Bathonian-early for the grant of financial assistance to take up the study. Callovian), Majungael/a perforata kachchhensis Grateful thanks are due to Prof. S.P. MoHAN, Dr. S.M. Range Zone (middle - late Callovian). The HussAIN, and Dr. S. GANDHI (all are from Department of M. perforata kachchhensis Range Zone has Geology, University of Madras, Chennai) for their kind help rendered during the first author's visit to Chennai fo r been further subdivided into the following taking SEM photography. three subzones: the Majungael/a perforata kachchhensis Fastigatocythere (Bate/la) References fa lcula Concurrent Range Subzone, Majungael/a DAs GUPTA, S.K. 1975. A revision ofthe Mesozoic - Tertiary stratigraphy of the Jaisalmer basin, Rajasthan. - Indian perforata kachchhensis - Gal/iaecytheridea Journal of Earth Sciences 2: 77-94. remota Concurrent Range Subzone, and }ONES, T. R. & SHERBORN, C.D. 1888. On some Ostracoda the Majungael/a perforata kachchhensis - from the Fuller's Earth, Oolite and Bradford Clay. - Galliaecytheridea remota Interval Subzone. Proceedings of the Bath Natural History Field Club 6: Of these, two zones, the Trichordis 249-278. KHOSLA, S.C., jAKHAR, S.R. & MOHAMMED, M.H. 1997. hadibhadangensis and Cy theropteron Ostracodes from the Jurassic of Habo Hill, Kachchh, micropunctata Range zones, were originally Gujarat. - Micropaleontology 43: 1-39. described from Kachchh by KHOSLAet al. (1997, KHOSLA, S.C., MANISHA, K, DARWIN F.A., jAKHAR, S.R. & 2005). NAGORI, M.L. 2005. Middle Jurassic Ostracoda from the Northern Island Belt, Rann of Kachchh, Gujarat, India. - journal of Palaeontological Society of India 17-64. SO: 110 9th International Congress on the Jurassic System - Abstracts

Recent progress in ecological studies on living radiolarians and its application to the Jurassic ecosystem - End-Triassic mass extinction and early Jurassic recovery in the pelagic realm

ATSUSHI MATSUOKA

Department of Geology, Niigata University, Niigata 950 2181, japan; E-mail: matsuoka@geo. se. n iig a ta -u. ac.jp

Research on living radiolarians has been extinction event and early jurassic recovery by carried out at the Sesoko Marine Station of the applying our knowledge of living radiolarian University of Ryukyus and the Sado Marine studies. The end-Triassic mass extinction is Biological Station of Niigata University for more characterized by an abrupt collapse of the than 20 years. This research has provided us marine ecoystem, represented by a drastic with fundamental data on radiolarian ecology decline of Triassic radiolarians. Only a limited including fe eding behavior (MATSUOKA 2007; number of radiolarian taxa could survive SUGIYAMA et al. 2008), symbiosis (TAKAHASHI et this event. These taxa include Canoptum, al. 2003; YuASA et al. 2012), possible parasitism Pantanellium, and Bipedis. The early jurassic (SuzuKI et al. 2009), and other aspects of recovery was gradual and stepwise. Full radiolarian biol�gy. recovery of the marine ecosystem, represented Detailed observations on the feeding by re-entry of multi-segmented nassellarians behavior of laboratory-cultured radiolarian such as Parahsuum, Droltus, and Bagotum, took specimens make it possible to understand the place in the Sinemurian. relationship between skeletal morphology and fe eding behavior. Four types offe eding strategies well correspond to skeletal morphology in References extant radiolarian taxa (MATSUOKA 2007). High MATSUOKA,A 2007. Livingradiolarian fe eding mechanisms: diversity of radiolarian skeletal morphology is • new light on past marine ecosystems. - Swiss Journal partly related to variations in feeding strategies. of Geoscience 100: 273-279. SUGIYAMA, K., HORI, R.S., KUSUNOKI, Y. & MATSUOKA, 2008. A The wide variation in feeding behavior means Pseudopodia) features and fe eding behavior of living that radiolarians occupy several kinds of nassellarians Eucyrtidium hexagonatum HAECKEL, ecological niches in marine environments. Pterocorys zanc/eus (MULLER) and Dictyocodon We can infer feeding behavior of extinct prometheus HAECKEL. - Paleontological Research 12: 209-222. radiolarian groups based on their skeletal SUZUKI, N., KURIHARA, T. & MATSUOKA, 2009. Sporogenesis A morphology. Once we recognise the role of of an extracellular cell chain from the spheroidal radiolarians in the food web of modern ocean radiolarian host Haliommilla capillaceum (HAECKEL), environments, we can apply it to reconstruct Polycystina, Protista. - Marine Micropaleontology 72: marine ecosystems in the past. Fluctuation in 157-164. TAKAHASHI, 0., MAYAMA, S. & MATSUOKA, 2003. Host­ A morphological diversity of radiolarian skeletons symbiont associations of polycystine Radiolaria: is well documented in the fossil record. This epifluorescence microscopic observation of living fluctuation can be interpreted as changes in Radiolaria. - Marine Micropaleontology 49: 187-194. YUASA, T., HORIGUCHI, T., MAYAMA, S., MATSUOKA, & the number of ecological niches in the marine A TAKAHASHI, 0. 2012. Ultrastructural and molecular ecosystem through time. characterization of cyanobacterial symbionts in We try to reconstruct the ecosystem Dictyocoryne profunda (polycystine Radiolaria). - evolution during the end-Triassic mass Symbiosis 57: 51-55. 9th International Congress on the Jurassic System -Abstracts 111

On the Oxfordian-Kimmeridgian (Upper Jurassic) boundary - current state of knowledge

BRONISt.AW A. MATYJA 1 & ANDRZEJ WIERZBOWSKI2 *

1/nstitute of Geolog� University of Wa rsaw, iwirki i Wigwy 93� 02-089 Wa rszawa� Poland; E-mail: [email protected] 2Po/ish Geological Institute - National Research Institute� Rakowiecka 4� 00-975 Wa rszawa� Poland; E-mail: andrzej. [email protected]

*Corresponding author

The Kimmeridgian Stage was named by runs about two ammonite zones higher (about o'ORBIGNY in the first half of the 19th century 1.3 myr) than the Subboreal standard (OGG et after the village of Kimmeridge at the Dorset al. 2012). Coast, but it was SALFELD (1913) at the The Flodigarry section at Staffi n Bay in beginning of 20th century,who first defined the Skye, northern Scotland, has been recently base of the Stage at the base of the Kimmeridge proposed as the primary standard for the base Clay corresponding to a marked change in the of the Kimmeridgian Stage by the Kimmeridgian Aulacostephanidae ammonite family lineage - Working Group, and the International from the genus Ringsteadia to the genus Pictonia. Subcommission on Jurassic Stratigraphy. According to that definition the older genus The continuous succession of Subboreal Ringsteadia was indicative of the Pseudocordata ammonites of the family Aulacostephanidae Zone of the uppermost Oxfordian, whereas (from Ringsteadia to Pictonia) recognized the appearance of the genu·s Pictonia defined here makes it possible to distinguish both the the base of the Baylei Zone of the lowermost Pseudocordata Zone and the Baylei Zone, with Kimmeridgian. Although the definition seems the lowest recognized ammonite horizon - the perfect, it has born some inconveniences: (1) Pictonia flodigarriensis horizon (absent in the Ammonites of the family Aulacostephanidae Dorset sections) which marks the real base of show limited palaeogeographic distribution the Kimmeridgian Stage. The Boreal ammonites being known mostly from the fairly small of the family Cardioceratidae show also a Subboreal Province of NW Europe; (2) the continuous succession, from Amoeboceras to transition between the genera Ringsteadia and Plasmatites, corresponding to the transition Pictonia at the Dorset Coast is not continuous from the Rosenkrantzi Zone to the Bauhini Zone, because of a stratigraphical gap at the base thew boundary of which is also coeval with the of the Kimmeridge Clay - hence a part of the base of the Kimmeridgian Stage (MATYJA et al. succession at the Oxfordian-Kimmeridgian 2006; WIERZBOWSKI 2010). boundary is not represented in these sections. The SubmediterraneanfMediterranean Marked differences between the coeval subdivisions of the stratigraphical interval ammonite faunas between the Subboreal in question corresponding to the so-called ammonite succession in northwestern Europe "Submediterranean Upper Oxfordian" includes and the Submediterranean and Mediterranean the Bimammatum Zonesensu lato and the Planula ammonite successions in middle and southern Zone; fo r correlation reasons (see also below) it Europe resulted also in erroneous correlation is better, however, to split the fo rmer into two of the Oxfordian-Kimmeridgian boundary independent zones: the Hypselum Zone below standard in the past, which additionally and the Bimammatum Zone sensu stricte above. complicated the problem. It should be The stratigraphical interval corresponding to remembered that the currently accepted the Hypselum Zone ( = Semiarmatum Zone) Oxfordian-Kimmeridgian boundary in the includes the Semimammatum Subzone, the Submediterranean-Mediterranean successions Semiarmatum Subzone, and the Berrense (base of the Platynota Zone or Silenum Zone) Subzone (cf. BONNOT et al. 2009), whereas that 112 9thInternational Congress on the Jurassic System -Abstracts

of the Bimammatum Zone. the Bimammatum 0. marantianum). Marked changes occurred Subzone and the Hauffianum Subzone. The bulk also in the Aspidoceratidae as shown by the of these chronostratigraphic units is defined on decline of Euaspidoceras, and appearance of the basis of Submediterranean-Mediterranean Aspidoceras and Physodoceras, as well as the ammonites having wide correlation potential occurrence of the "transitional" forms of the in the World, especially of the families Neaspidoceras - Clambites type. As the studies Aspidoceratidae and Oppeliidae. of the section crucial for the correlations are The Subboreal and Boreal ammonites ongoing we hope that soon the detailed position occurring in the Submediterranean succession of the Oxfordian/Kimmeridgian boundary in Europe (Poland and Germany) indicate that in the Submediterranean succession will be the whole Planula Zone, and at least the bulk of established. the Bimammatum Zone correlates with a lower part of the Subboreal Baylei Zone and a lower The study was financed by the National Science Centre (grant 2012/05/B/ST 10/02121). part of the Boreal Bauhini Zone. It results from the occurrence, in this stratigraphical interval, References of such ammonites as the Boreal Amoeboceras BONNOT, A., MARCHAND, D., COURVILLE, P., FERCHAUD, P., (Plasmatites), as well as of the Subboreal QUEREILHAC, P. & BouRSICO,T P.-Y. 2009. Le genre Prorasenia and Pictonia (MATYJA et al. 1997; Epipe/toceras (Ammonitina, Perisphinctaceae, Aspidoceratidae) sur le versant parisien du WIERZBOWSKI et al. 2010). In contrast, the seuil du Poitou (France): fa unes ammonitiques, newly undertaken studies in the Hypselum Zone biostratigraphie et biozonation de la zone a reveal the presence of the Boreal Amoeboceras Bimammatum pars (Oxfordien superieur).- Revue de rosenkrantzi Spath and the Subboreal Paleobiologie 28: 371-411. 0GG, ).G., HINNOV, L.A. & HUANG, C. 2012. jurassic. In: Ringsteadia and Microbiplices indicative of GRADSTEIN, F.M., 0GG, j.G., SCHMITZ, M. & 0GG, G; The the Pseudocordata Zone. Although a precise Geologic Time Scale: 731-791, Elsevier, Amsterdam. position of the boundary between the Subboreal MATYJA, B.A., WIERZBOWSKI, A. & WRIGHT, j.K. 2006. The Pseudocordata Zone and the Baylei Zone, as Sub-BorealfBoreal ammonite succession at the well as that of the coeval boundary between the Oxfordian/Kimmeridgian boundary at Flodigarry, Staffin Bay (Isle of Skye), Scotland. - Transactions of Boreal Rosenkrantzi and the Bauhini Zone, both , the Royal Society of Edinburgh, Earth Sciences 96: corresponding to the base of the Kimmeridgian 387-405. Stage, cannot be so fa r precisely recognized in SALFELD, H. 1913. Certain Upper jurassic strata of England. the Submediterranean succession, this should - Quarterly journal of the Geological Society, London 69: 423-432. be drawn not fa r from the boundary between WIERZBOWSKI, A. 2010. On the Oxfordian/Kimmeridgian the Hypselum (Semiarmatum) Zone and the boundary and its GSSP - current state of knowledge. - Bimammatum Zone. It should be remembered Vo lumina jurassica 8: 177-182. that the stratigraphical level at the transition MATYJA, B.A. & WIERZBOWSKI, A. 1997. The quest for unified between the Hypselum and the Bimammatum Oxfordian/Kimmeridgian Bondary: implications of the ammonite succession at the turn of the Bimammatum zones in the Submediterranean succession and Planula zones in the Wielun Upland, central is very prospecting fo r wider stratigraphic Poland. - Acta Geologica Polonica 46: 77-105. correlations because of marked changes in WIERZBOWSKI, A., GtOWNIAK, E. & PIETRAS, K. 2010. ammonite faunas - in the Oppeliidae - in Ammonites and ammonite stratigraphy of the the Ta ramel/iceras lineage (transition from Bimammatum Zone and lowermost Planula Zone (Submediterranean Upper Oxfordian) at Bobrowniki T. externnodosum to T. costatum), as well as and Raciszyn in the Wielun Upland, central Poland. - in the Ochetoceras lineage (appearance of Volumina Jurassica 8: 49-102. 9th International Congress on the Jurassic System - Abstracts 113

Ammonite distribution in late Middle-Upper Jurassic deposits of epicratonic Poland: the key to ecology, biogeography, palaeogeography and geotectonic events

* 2 BRONISt.AW A. MATYJA1 & ANDRZEJ WIERZBOWSKI

1/nstitute of Geology, University of Wa rsaw,i wirki i Wig ury93, 02-089 Wa rszawa, Poland; E-mail.· [email protected] 2Polish Geological Institute - National Research Institute, Rakowiecka 4, 00-975 Wa rszawa, Poland; E-mail: andrzej. [email protected]

*Corresponding author

Late Middle and Late Jurassic deposits rich in several sections of epicratonic Poland for a in ammonites are widely distributed in the distance of over 500 km from the land areas epicratonic areas of Poland. The epicratonic in the north and the Tethys Ocean in the marine basin of Poland was that time bordered south. The ammonites studied represent the by land areas from the north and the east, and stratigraphical interval from the Callovian to the widely open towards the south, the Tethys Tithonian. The percentage shares ofthe different Ocean. ammonite groups (families and subfamilies) Northern and central Poland was dominated are presented. The detailed biostratigraphy and by siliciclastic deposits from the Callovian to the fades patterns related to the evolution of the Tithonian. The northern area was characterized epicratonic basin of Poland make it possible to also by several phases of development o0f recognize the changes in ammonite spectra in shallow-water carbonate platforms, whereas space and time. in central Poland patchy spongy bioherms The Boreal Province was firmly established and coral reefs developed on domal structures in the area of northern Poland at least from formed by halokinetic movements of Permian the Lamberti Chron of the latest Callovian up salts. In contrast, the siliciclastic sediments to the Te nuicostatum Subchron of the Middle which prevailed in the Callovian in southern Oxfordian. The ammonite spectra show the Poland were replaced by the sponge megafacies dominance of the fa mily Cardioceratidae, the during Oxfordian times, and these were representatives of which account fo r about followed by widely distributed shallow-water 90°/o of the whole number of specimens. The carbonate platform deposits during the Early Submediterranean ammonites dominated in Kimmeridgian. Flooding of the carbonate central and northern Poland from the Plicatilis platform took place at the end of the Early Chron (well afterits earliest time) of the Middle Kimmeridgian and this resulted in appearance Oxfordian up to the end of the Bifurcatus Chron of siliciclastic fa cies which were uniformly of the Late Oxfordian. The Boreal ammonites developed over wide areas of the epicratonic (Cardioceratidae) reappeared in the Hypselum Poland during the Late Kimmeridgian and Chron (Late Oxfordian) along with the first Early Tithonian. The shallow-water carbonate appearance of the Subboreal ammonites deposits fo rmed in environments of variable (Aulacostephanidae) . Both these groups salinity appeared at the beginning of the continued successively their occurrence with Late Tithonian. These resulted in the total minor fl uctuations and declined close to the disappearance of the ammonite faunas, and in end of Kimmeridgian, but another group of consequence were followed by the deposition Subboreal ammonites (Virgatitidae) appeared of evaporates during the Berriasian. in the Early Tithonian (Early Volgian) and Changes in ammonite spectra were traced existed until the total ecologically controlled in relation to sedimentation history. These disappearance of ammonites at the beginning are based on published and unpublished data of the Late Tithonian. giving the detailed distribution of ammonites The area of southern Poland, corresponding 114 9th International Congress on the Jurassic System - Abstracts to the south-western Mesozoic border of the Kimmeridgian and markedly-- dominated Holy Cross Mts and the whole Polish Jura Chain over the Submediterranean Oppeliidae from the beginning of the Callovian (MATYJA & and Aspidoceratidae. Beginning from the GI:ZEJEWSKA 1979; DEMBICZ & PRASZKIER 2003) Pseudoscythica Chron (Early Tithonian - up to the Planula Chron of the latest Oxfordian Early Volgian) the representatives of the in Submediterranean subdivision or of the family Virgatitidae accounted for 100% in Early Kimmeridgian in the BorealfSubboreal the ammonite spectra both in northern and subdivisions (MATYJA 1977; WIERZBOWSKI 1978; southern Poland thus closely linking the Polish MATYJA & GtOWNIAK 2003), belonged to the Sub­ basin with the seas of the Russian Platform. mediterranean Province. Such interpretation is a consequence of the common occurrence of The study was financed by the National Science Centre representatives of the families Perisphinctidae, (grant 2012/05/B/ST 10/02121). Aspidoceratidae, Ataxioceratidae, Reineckei­ idae, Macrocephalitidae, Oppeliidae, and References Lissoceratoidae which constitute together ARKELL, W.J. 1956. Jurassic Geology of the World. 806 p., Oliver and Boyd, Edinburgh. over 50% of the whole number of specimens, DEMBICZ, K. & PRASZKIER, T. 2003. Stratygrafia, mikrofacje occasionally along with the admixture i srodowisko sedymentacji osad6w keloweju z profilu ofseveral percentages of Phylloceratidae. The Wlodowic kolo Zawiercia. - Tomy Jurajskie I: 35-52. representatives ofBoreal and Subboreal families MATYJA, B.A. 1977. The Oxfordian of the south-western (Cardioceratidae and Aulacostephanidae) margin of the Holy Cross Mts. - Acta Geologica Polonica 27: 41-64. constituted, however, up to 30% of the MATYJA, B.A. & GIZEJEWSKA, M. 1979. Distribution of specimens, both in the Callovian and in the Callovian and Lower Oxfordian ammonite fa unas in Early and the earliest Middle Oxfordian (Boreal Poland. - Acta Geologica Polonica 29: 177-185. Spread of ARKELL 1956). Later on, the Boreal MATYJA, B.A. & GtOWNIAK, E. 2003. Nast�pstwo amonit6w dolnego i srodkowego oksfordu w profilu ammonites appeared at least twice: in the kamieniolomu w Ogrodziencu i ich znaczenie Semimammatum Subchron of the Hypselum biogeograficzne. - Tomy Jurajskie 53-58. 1: Chron (MATYJA & WIERZBOWSKI 1988), and MATYJA, B.A. & WIERZBOWSKI, A. 1998. The stratigraphical in the litocerum horizon of the Hauffianum and palaeogeographical importance of the Oxfordian Subchron of the Bimammatum Chron (MATYJA • and - Lower Kimmeridgian succession in the Kcynia IG IV Borehole. - Biul. Panstw. Inst. Geol. 382: 35-70. & WIERZBOWSKI 1997) - both appearances MATYJA, B.A. & WIERZBOWSKI, A. 1988. The two representing short-time invasions in which the Amoeboceras invasions in Submediterranean Late Oxfordian of Central Poland. In: Rocha, R.B. Soares, number of Boreal Cardioceratidae exceeded & 60% of the whole ammonite spectra. A.F. (eds.), 2nd International Symposium on Jurassic Stratigraphy 1: 421-432, Lisboa. Due to the small number of data it is still MATYJA, B.A. & WIERZBOWSKI, A. 1996. Biogeographic not clear when the Subboreal Province reached differentiation of the Oxfordian and Early the southern epicratonic Poland. The area of Kimmeridgian ammonite fa unas of Europe and its central Poland along with the adjoining part stratigraphic consequences. - Acta Geologica Polonica of southern Poland belonged to the Subboreal 45: 1-8. MATYJA, B.A. & WIERZBOWSKI, A. 1997. The quest fo r Province already from the latest Hypselocyclum a unified Oxfordian/Kimmeridgian boundary: Chron at the junction of the Early and Late implications of the ammonite succession at the turn Kimmeridgian (MATYJA & WIERZBOWSKI 1998) ofthe Bimammatum and Planula zones in the Wielun onwards. Upland, Central Poland. - Acta Geologica Polonica 47: 77-105. The ammonites of the Subboreal family WIERZBOWSKI, A. 1978. Ammonites and stratigraphy of Virgatitidae appeared in northern and central the Upper Oxfordian of the Wielun Upland, central Poland in the Fallax Subchron of the latest Poland. - Acta Geologica Polonica 28: 299-333. 9th International Congress on the Jurassic System - Abstracts 115

Phricodoceratinae SPATH, 1938 (Mollusca, Cephalopoda): ontogeny, evolution & paleobiogeography

CHRISTIAN MEISTER1 * & JEAN-LOUIS 00MMERGUES2

1Natural History Museum of Geneva, Department of Geology and Paleontology, CH-1211 Geneva, Switzerland; E-mail: [email protected] 2UFR Sciences Vie, Universite de Bourgogne, CNRSjuB, UMR 5561, Biogeosciences Dijon, F-21000 Dijon,Fra nce; E-mail: [email protected]

*Corresponding author

Phricodoceratidae is an original and rare P. cantaluppii FA NTINI SESTINI, 1978. It ranges Lower Jurassic family represented by the genus from the Upper Sinemurian (Raricostatum Phricodoceras HYATT, 1900 which contains ten Zone) to the Upper Pliensbachian (Spinatum species: P. taylori (J. DE C. SOWERBY, 1826), P. Zone) corresponding to a range of about 6 to lamellosum (o'ORBIGNY, 1844), P. urkuticum 7 millions years. Exhaustive results, based on (GECZY, 1959), P. paronai (BETTONI, 1900), P. the revision of the different species with their bettonii GECZY, 1976, P. venzoi FANTINI SESTINI, complete synonymy and on morphological, 1978, P. cornutum (SIMPSON, 1843), P. oistoides stratigraphic and paleogeographic approaches, GECZY,19 76, P. imbricatum (BETTONI, 1900), and allow proposing an evolutive history of Phricodoceras (MEISTER 2007). A hypothesis of sexual dimorphism where P. taylori => P. bettonii => P. venzoi may represent the microconchs and P. lamellosum => P. urkuticum => P. paronai the macroconchs are also given. The discovery, by MEISTER et al. (2010), of a key taxon (i.e., Angulaticeras spinosus MEISTER, SCHLOGL & RAiills, 2010) allows with certainty to understand the origin of Phricodoceras and to place it among the Schlotheimiidae (Fig. 1). It shows that the discovery of intermediate fo rms is often the key to phyletic reconstructions in ammonites.

References DOMMERGUES, J.-L. & MEISTER, C. in press. Significance of intermediate fo rms in phyletic reconstruction of ammonites: Early Jurassic Phricodoceras case study. - Acta Palaeontologica Polonica. http:/ jdx.doi. org/10.4202japp.2011.0148. MEISTER, C. 2007. Les Phricodoceratidae SPATH, 1938 (Mollusca, Cephalopoda): ontogenese, evolution et paleobiogeographie. - Geodiversitas 29: 87-117. MEISTER, C., 00MMERGUES, J.-L., OOMMERGUES, C., LACHKAR, N. & EL HARIRI, K. 2011. Les ammonites du Pliensbachien du jebel Bou Rharraf (Haut Atlas oriental, Maroc). - Geobios 44: 117.e1-117.e60. MEISTER, C., SCHLOGL, J. & RAKUS, M. 2011. Sinemurian ammonites from Male Karpaty Mts., Western Carpathians, Slovakia. Part 1: Phylloceratoidea, Lytoceratoidea, Schlotheimiidae. - Neues Jahrbuch fiir Geologie und Palaontologie Abhandlungen 259: 1. a, b, c: Angu/aticeras spinosus MEISTER, SCHLOGL & 25-88. Fig. RAKUS. Phricodoceras taylori (SowERBY). d: 116 9th International Congress on the Jurassic System -Abstracts

Microfacies of the Bathonian sediments of the Jumara Dom'e, Kachchh, western India: Inference of depositional environments

ARPAN MISRA

AMD, Department of Atomic Energy, W.R.,]ai pur 302 033, India; E-mail: [email protected]

The Kachchh Basin is a pericratonic rift basin quartz-bearing angular to su bangular intraclasts situated at the western margin of the Indian and fe rruginous ooids) higher up in the section. plate and fo rms a classic area for Jurassic rocks Bioclastic limestones containing a diverse and in India. The Jumara Dome fo rms a prominent abundant fauna indicate a productivity and is exposure of the Bathonian sediments in the in accordance with such depositional settings. basin. A rigorous fa cies analysis based on The Sponge Limestone member of the Patcham microfacies towards reconstruction of the Formation is represented by this association. depositional environment and setting of The microfacies association (2) contains carbonate sedimentation with correlation of bioclastic mudstones, bioclastic wackestones, basin components had been lacking. Thus an bivalve packstones, and bivalve float- to important Kachchh Mainland outcrop of the rudstones. The association forms well-bedded Bathonian sediments viz. the Jumara Dome limestone-marlfmarlstone alternations and was taken up for the present study. Detailed represents a largely low-energy depositional stratigraphic sections of the Bathonian rocks environment which had seen phases of slight have been measured fo r the purpose. Macrofacies influence of storm events. Tempestitic shell beds have been recorded for corroborating the which show ferruginization and an increased microfacies data. Microfacies analysis has been content of terrigens (sand-sized quartz grains) carried out by studying thin-sections of rock and ooids (including broken ones) represent samples under the microscope with the aim episodes of higher energy conditions. The to interpret the depositional environment and Jumara Coral Lime�tone member of the Jhurio setting during Bathonian times. Fo,rmation is represented by this association. The Bathonian sediments at the Jumara The microfacies association (3) contains Dome are characterized by well-bedded ferruginous echinoderm/bioclastic packstones, limestone-marlfmarlstone alternations with ferruginous intraclastic packstones, and tempestite beds and massive limestones echinoderm grainstones. In this association (packstones and grainstones), and have been the well-bedded limestone-marlfmarlstone classified as Patcham and Jhurio fo rmations in intercalations are absent. The association descending order. The section has several units represents reworked sediments of the where the limestones show a nodular fabric. transgressive phase in a higher-energy setting. The microfacies types can be grouped into three Sorting of grains is variable. High degree of associations. Association (1) contains bioclastic ferruginization, appreciable terrigenous (sand­ mud- to wackestones, peloidal grainstones, and sized quartz grains) influx, presence of ooids bioclastic floatstones. Fine-grained peloidal (including a few broken ones) and oncoids, grainstones and packstones have appreciable and a relatively high percentage of intraclasts percentages of peloids and contain small-sized almost throughout the unit are characteristic bioclasts. The association fo rms well-bedded features. The Echinoderm Packstone belonging limestone-marlfmarlstone alternations. This to the Jhurio Formation is represented by this indicates a marine, open sea, mid to outer association. The presence of granular sparite (deep) carbonate ramp environment. Bioclastic cement along with fibrous cement and syntaxial wackestones, especially in the lower part of rim cement, the sorting, and the bioclastic the section represent a low-energy, setting content of the sediment support the prevalence below the storm wave-base which gave way to of such environments. a higher energy setting as indicated by peloidal A carbonate ramp setting seems to have packstonesand bioclasticfloatstones (containing been prevalent at the time of sedimentation 9th International Congress on the Jurassic System - Abstracts 117 of the carbonates during Bathonian times. In of storm events, shiftingoccasio nally adjacent general, the depositional environment seems to to the storm wave-base. Reworked sediments of have been an open marine, mid to outer (deep) the transgressive phase witnessed a relatively ramp. It was largely low energy, just below the high-energy depositional environment. storm wave-base with phases of slight influence 118 9thInternational Congress on the Jurassic System - Abstracts

Ammonite zonation of the Boreal Bathonian Stage of Greenland

VASILY MITTA1 * & PETER ALSEN2

1Borissiak Paleontological Institute RAS, Profs oyuznaya 123, Moscow 117997, Russia; E-mail: mitta@ paleo.ru 2Geological Survey of Denmark and Greenland (GEUSJ Oster Vo ldgade 10, DK-1350 Copenhagen K, Denmark; Email: [email protected]

*Corresponding author

The report presents the first results of the relatively high sub-oval section and narrow revision of the Middle Jurassic ammonite umbilicus (Arctocephalites ex gr. arcticusf collections from East Greenland, stored at the greenlandicus, Arcticoceras ex gr. ishmaef Museum of Natural History of Copenhagen, and cranocephaloide). The second morphotype collected by J. Callomon, T. Birkelund, and many includes shells more or less inflated, with other researchers. thick whorls, a wider umbilicus, and generally The Boreal Bathonian is characterized, first of with a more coarsely ribbed sculpture all, by ammonites of the Family Cardioceratidae, ("Arctocephalites" ex gr. sphaericusffr eboldi, belonging to the genera Cranocephalites, "Arcticoceras" ex gr. harlandifishmae var.). Arctocephalites, Arcticoceras (Subfamily Transitional forms between these Arctocephalitinae), and Cadoceras (Subfam. morphotypes are observed only in the lower Cadoceratinae) forming a phyletic evolutionary part of the Arcticus zone. Apparently, at this lineage (CALLOMON 1985). According to time, there was a phylogenetic divergence CALLOMON (1993, etc.) the first appearance of within the Arctocephalitinae. The most suitable Arctocephalites is in the Arcticus Zone, replacing valid generic name from the literature fo r the ancestral Cranocephalites. All ammonites fo und inflated species is Greencephalites REPIN, 2007, in the Arcticus and Greenlandicus zones, were with the type species Cadoceras freboldi SPATH. referred to various species of Arctocephalites. ' During the revision of the collections we The succeeding Ishmae Zone is dominated have tried to take into account definitions of by the genus Arcticoceras, the descendants of the late J.H. CALLOMON, whom we honor as a Arctocephalites; in that zone a single Oxycerites fellow elder and a teacher. Accordingly, the (Fam. Oppeliidae) appears also. The genus Arcticus zone as a whole is characterized by Kepplerites (Fam. Kosmoceratidae) has its Greencephalites sphaericus (SPATH); the lower first appearance in the Cranocephaloide Zone part of the Greenlandicus zone by G. crassus and the cardioceratids are still referred to the (MADSEN), its upper part by G. freboldi (SPATH). Arcticoceras. The Variabile Zone sees the first In the Ishmae Zone the genus Greencepha/ites appearance of Cadoceras which occurs together is represented by a new species that is yet to with Arcticoceras and Kepplerites. Higher, in be described. In the Cranocephaloide zone the Calyx, Apertum, and N ordenskoeldi zones, of East Greenland ammonite shells have various Ca doceras and Kepplerites are indicated. usually been subject to varying degrees of According to CALLOMON (1993), the Bathonian­ compaction, and it is commonly impossible, Callovian boundary presumably lies at the to determine the original width of whorls; base of Apertum Zone; the Bajocian-Bathonian however, the zone appears to be dominated by boundary is not defined. the last representatives of Arcticoceras. Recent A re-study of the collections shows that the collections (Alsen Coli.) from this zone in North­ entire range of the Arcticus-Cranocephaloide East Greenland include a specimen with wide zones of East Greenland contains two umbilicus of early whorls. This finding represent morphotypes of cardioceratid shells, and can a lowermost occurrence of the genus Cadoceras almost be proven for all zones. One general in the Middle Bathonian. In the Variabile Zone morphology includes flattened shells with a and above the cardioceratids are presented 9th International Congress on the Jurassic System - Abstracts 119

Zonation extended to its original definition. The Variabile Proposed Ammonite genera ZonaUon afterCellomon, 1993 I and Calyx zones are referred to the Upper 11 notflen8kJoeld'p Bathonian. n a I Jl � nonlenskjoeldl Representatives of Kepplerites from the dJaff.brew i Cadoceras apertum- range interval CALLOMON E tenulfasclcu/atus � & BIRKELUND have marked nodes at the rib 1: E i t sperlum T t 1 bifurcations resembling Early Callovian J I apertum p Kepplerites keppleri (OPPEL) and Late Bathonian & epertum a K. dietli ScHAIRER. However, occurring above Q. - � vardeldoeltMisls are shells of K. tenuifasciculatus CALLOMON ! pwamplus ! with thick ribs which undoubtedly belong to - I .5! I the Upper Bathonian. Accordingly, the entire J5 rosenkrantz/ I Cll I -.::: Apertum Zone is here assigned to the Upper � I lnflatus J I Bathonian. The proposed changes in the scale I tyr;hon/s ca.i u of the Bathonian Stage are shown in Fig. 1. �� 0{�� CfFitJOC8phslol j ::E.! CI8SSipllcatum j Supported by the Program of the Presidium RAS no. 28 j p tl /shmse � and by grant RFBR no. 11-05-01122. 1: � 0 s: /shmaea .!! J .!! j t harlendl References i r-.- � CALLOMON, J.H. 1985. The evolution of the Jurassic .a frebold/ J ammonite family Cardioceratidae. - Palaeontology, 1 "2 i � (!) .!! I gl8e(l/andlcus .!1 Special Paper 33: 49-90. I mlctumblllcatus I CALLOMON, J.H. 1993. The ammonite succession in the �c (!) (!) Middle Jurassic of East Greenland. - Bulletin of the T J dellcatus Geological Society of Denmark 40: 83-113. . � I � arr:tJcus I MELEDINA, S.V. 1987. Ammonites and zonal stratigraphy 1. Subdivision of the Bathonian Stage of East of the Callovian of subboreal regions of USSR. 182 p., Fig. Greenland. Moscow (Nauka). [In Russian] MITTA, V.V., BARSKOV, I.S., GRUNDEL, f., ZAKHAROV, V.A., mainly by species of this genus, which is most SELTZER, V. B., IVANOV, A.V., ROSTOVTCEVA, J.A. & likely a direct descendant of Greencepha/ites. TA RASOVA, L.O. 2004. - The Upper Bajocian and Lower Bathonian in the section near Saratov. - Vernadsky The Ishmae zone has been shown to belong Museum Novitates 12: 1-39. [In Russian] to the upper half of the Lower Bathonian (e.g., MITTA, V.V. & SELTZER, V. B. 2002. First finds of MITTA & SELTZER 2002) and this was confirmed Arctocephalitinae (Ammonoidea) in the Jurassic ofthe by MITTA et al (2004, 2012). The Greenlandicus south-eastern Russian Platform, and the correlation of the Boreal Bathonian Stage with the standard scale. Zone is correlated with the lower half of - Transactions Sci. Research Geological Institute, the Lower Bathonian of the West-European Saratov State University N.S. 10: 12-39. [In Russian] standard, and the Arcticus Zone presumably MITTA, V.V., SHURYGIN, B.N., 0ZYUBA, O.S., KOSTYLEVA, V.V., belongs to the Upper Bajocian. We propose to GLINSKIKH, L.A., SELTZER, V. B., IVANOV, A.V. & URMAN, limit the Ishmae Zone to the range ofAr cticoceras O.S. 2012. Preliminary results of study the Bathonian (Middle Jurassic) rocks in the vicinity of Saratov in harlandi RA.wsoN and A. ishmae (KEYSERLING), year 2012. - Problems of paleoecology and historical as is customary in other boreal regions such geoecology: 151-163. Saratov, State Technical as Arctic Canada, Northern Siberia and the University. [In Russian] Petshora Basin (MELEDINA 1987; POULTON PouLTON, T.P. 1987. Zonation and correlation of Middle Boreal Bathonian to Lower Callovian (JurassicJ crassip/icatum, 1987). Three faunal horizons: ammonites, Salmon Cache Canyon, Porcupine River, cranocephaloide, and tychonis represent the northern Yukon. - Bulletin of the Geological Survey of Middle Bathonian Cranocephaloide zone, thus ·Canada 358: VII + 155 p. 120 9thInternational Congress on the Jurassic System - Abstracts

Boreai-Tethyan correlation of the Bajocian-Bathonian boundary beds in the Sokur section (Central Russia): new insights into an old story

VA SILY MITTA1 *, VIKTORIA KOSTYLEVA2, 0XANA S. DZYUBA3, LARIS GLINSKIKH3, 80RIS N. SHURYGIN3, VLADIMIR SELTZER4 & ALEXEY IVANOV5

1Borissiak Paleontological Institute RAS, Profs oyuznaya 123, Moscow 117997,Russia; E-mail: mitta@ paleo.ru 2Geological Institute RAS, Pyzhevsky lane 7, Moscow 11901 7; E-mail: kovicto@yandex. ru 3Trofimuk Institute of Petroleum Geology and Geophysics SB RAS; Novosibirsk, Russia; E-mail: [email protected], [email protected] 4Saratov State University,Astr ahanskaya 83, Saratov 410012, Russia; E-mail: [email protected] 5Saratov State Te chnical University,Polit ehnicheskaya 77, Saratov41 0054, Russia; E-mail: Ya shkovia@ mail.ru

*Corresponding author

The Boreal-Tethyan correlation of the Bajocian­ recognized in the lower part of this section, Bathonian boundary beds is one of the most Pseudocosmoceras michalskii and Oraniceras complex problems of Mesozoic biostratigraphy. besnosovi. These beds are conformably overlain The standard zonal scales of the Upper Bajocian by beds withArcticoceras harlandi and A. ishmae and lower Bathonian are based on the West and hence assigned to the namesake zones of European (Submediterranean) successions the Boreal Jurassic zonation. At the same time, of parkinsoniids. The zonal scales of the the section contains beds with Retroceramus "Boreal Bathonian" (CALLOMON 1993), which bulunensis and R. vagt, reliably correlated in crops out over a vast area (East Greenland, the Boreal succession with ammonite zones northern Pechora, North Siberia, Arctic Canada, (Fig. 1). Furthermore, the highest occurrences North Alaska) are based on the succession of Oraniceras in the section are associated with of arctocephalitines and until recently their th'e earliest record of Arcticoceras harlandi. correlation with the primary standard scale The age of beds with Arcticoceras ishmae was only tentative. and closely related species has been a subject Direct Boreal-Tethyan correlation of the of discussion for some time. In the Boreal Bajocian-Bathonian boundary beds has only succession, the Harlandi and lshmae zones become possible recently. Deposits in the same until now were provisionally dated as Middle geological section (Sokur Quarry near Saratov) Bathonian (ZAKHAROV et al. 1997; SHURYGIN contain both ammonites of the Peri-Tethyan et al. 2011). Considering that the interval of family Parkinsoniidae (Parkinsonia, Oraniceras), distribution of the genus Oraniceras in the Peri­ typical of the Bajocian-Bathonian boundary Tethyan regions is restricted to the two lowest beds, and m em hers ofthe boreal Cardioceratidae subzones of the Zigzag Zone, in the Sokur (subfamily Arctocephalitinae: Arcticoceras section the association of Oraniceras and first and Arctocephalites), characteristic of the Arcticoceras suggests an Early Bathonian age of Arcticoceras "Boreal Bathonian" (MITTA & SELTZER 2002). A the lower beds containing species of subsequent integrated study has revealed here and Retroceramus, which define zones of the not only the Boreal ammonite zone, but also Boreal (secondary) standard succession. Thus, associated "Boreal" Bathonian zones based on the study of the Sokur section, which is a unique bivalves, foraminifers, and belemnites. These succession of Bajocian-Bathonian boundary data allow adequate correlation of the Boreal beds in the Boreal-Tethyan ecotone, provides zonation with Tethyan scales in the boundary a solution to the hotly debated problem of the interval of the Upper Bajocian and Lower Boreal-Tethyan correlation. Bathonian (MITTA et al. 2012). Supported by RASPrograms 23 and 28 and RFBR grants Two zones based on Parkinsoniidae are 11-05-01122, 12-05-00453, 13-05-00423. 9th International Congress on the Jurassic System -Abstracts 121

Zones M Lithology ber en (1) Moscow .:t= en c (1) 0 0 > E ro Ryazan IV E > 0 CO :c >- >- .0 .0

0 ? 300 km o W W e::=- Boreal zonation w 15> by ammonites by bivalves w v-- CO ? > w Praebuchia 0:: anabarensis

cranocephaloide Retroceramus Ill vagt We::=- ' <@ ishmae

harlandi w� R. bulunensis ? greenlandicus

<@ W R. polaris o en arcticus WC::W � · R. retrorsus <@ cu; (1) w� c � ::J Submediterranean "S .<@ .0 ammonite zonation

<@ Middle 0:: Progracilis <@ w Bathonian ·:;: 0 ? Te nuiplicatus <@ en 0 <@ c roc en ·c: (1) 0 ea .s:::. -ro w en <@ Zigzag (i) 0;: _. � en ro 11 <@ ..c Bomfordi Upper (.) Parkinsoni � Bajocian w Truellei

1. The Bajocian-Bathonian boundary beds ofthe Sokur section (Central Russia) and Boreal-Tethyan correlation. Fig.

References year 2012. - Problems of paleoecology and historical CALLOMON, J.H. 1993. The ammonite succession in the geoecology: 151-163, Saratov. [In Russian] Middle Jurassic of East Greenland. - Bulletin of the SHURYGIN, B.N., NIKITENKO, B.L., MELEDINA, S.V., DZYUBA, geological Society of Denmark 40: 83-113. O.S. & KNYAZEV, V. G. 2011. Comprehensive zonal MITTA, V.V. & SELTZER, V. B. 2002. First finds of subdivisions of Siberian Jurassic and their significance Arctocephalitinae (Ammonoidea) in the Jurassic of the for Circum-Arctic correlations. - Russian Geology and south-eastern Russian Platform, and the correlation Geophysics 52: 825-844. of the Boreal Bathonian Stage with the standard scale. ZAKHAROV, V.A., BOGOMOLOV, IL'INA, V. l., KONSTANTINOV, Yu.l., - Transactions Sci. Research Geological Institute, A.G., KURUSHIN, N.l., LEBEDEVA, N.K., MELEDINA, S.V., Saratov State University N.S. 10: 12-39. [In Russian] NIKITENKO, B.L., SOBOLEV, E.S. & SHURYGIN, B N. 1997. . MITTA, V.V., SHURYGIN, B.N., DZYUBA, O.S., KOSTYLEVA, V.V., Boreal zonal standard and biostratigraphy of the GLINSKIKH, L.A., SELTZER, V. B., IVANOV, AV. & URMAN, Siberian Mesozoic. - Russian Geology and Geophysics O.S. 2012. Preliminary results of study the Bathonian 38: 965-993. (Middle Jurassic) rocks in the vicinity of Saratov in 122 9th International Congress on the Jurassic System - Abstracts

Brachiopod diversity in the Jurassic of the Kutch and Jaisalmer basins, western India

DEBAHUTI MUKHE�EE

Palaeontology Division 1, CHQ Geological Survey of India, Ko lkata

The Jaisalmer and Kutch basins in the western occupying a shallower position, shows a part of India started to form as a result of proliferation of brachiopods, particularly of the intense tectonic activity associated with the terebratulid Ku tchithyris, of which six species fragmentation ofGondwanaland (BISWAS 1991) are abundant in the uppermost Callovian and and became inundated by the sea during the Oxfordian. Early /Middle Jurassic. The newly formed basins In Kutch, Ku tchithyris is the lone terebratulid provided a virgin area for faunal invasion and but in the Jaisalmer Basin alongwithKu tchithyris rapid speciation of some groups of organisms two other terebratulid genera, the cosmopolitan and thus have a spectacular fossil record, of Plectoidothyris and Bihenithyris, are also which brachiopods are a major component. In dominating. In the Kimmeridgian-Tithonian, Kutch, the sedimentary fill consists ofcarbonates Somalithy ris has been recorded in both basins in the Middle and Late Bathonian and then (Fig. 1). The brachiopod distribution in both the dominantly siliciclastics and records a general basins can be summarized as follows. deepening which culminates in the Oxfordian In Jaisalmer, the two dominant genera and was followed by a regression (FORS ICH et al., in the Bathonian are Plectoidothyris and 2003). Brachiopods apparently thrived nearly Cryptorhynchia, and in the Callovian. the throughout, but the number and diversity varied predominant taxa are Ku tchithyris breviplicata, widely depending on the lithofacies. In some K. mitra, K. ingluviosa, K. dhosaensis, K. horizons, such as the Upper Bathonian coral bed jooraensis, Bihenithy ris, Aulacothyris sp. and of the Jumara Dome, brachiopods are prolific A. pala, Bihendulirhynchia, Gibbirhynchia, and diverse (5 rhynchonellid species belonging Rhynchonel/oidel/ci, Sphenorhy nch ia to three genera, 4 terebratulid species and a'symmetrica, and Ku tchirhynchia. In the two zeilleriid genera). Another example is the Oxfordian, the dominant genera are Bihenithyris, argillaceous siltstone bed in the Middle Callovian K. jooraensis, G. nobi/is, Sphenorhy nchia, and of the Jumara Dome where the terebratulid Rhynchonel/oidel/a. In the Kimmeridgian, Ku tchithyris breviplicata largely outnumbers terebratulids are absent but the large other brachiopods, which are sparse specimens rhynchonellid Gibbirhy nchia nobilis is sparsely of K. ingluviosa and Aulacothyris. In contrast, in present. the shale-concretionary limestone units of the In Kutch, Bathonian strata contain Upper Callovian of the Jumara and Jara domes Ku tchithyris acutip/icata, K. propinqua, K. brachiopods are much fewer in number. euryptycha, K. planiconvexa, K. katametopa, In the Bathonian and Callovian, brachiopods C. karuna, C. jooraensis, C. pu/cherrima, C. are much diverse and abundant in the Jumara rugosa, Flabel/othyris dichotoma, Eudesia and Keera domes, whereas in the Jhura Dome multicostata, Ku tchirhynchia kutchensis, and they become prolific and diverse only during Rhactorhynchia pseudoinconstans. In the Late Callovian and Oxfordian. The Jara and Callovian, Ku tchithyris breviplicata, K. mitra, Jumara domes occupied a more offshoreposi tion K. ingluviosa, K. dhosaensis, K. pyroidea, K. whereas the Jhura Dome was much closer to the propinqua, K. euryptycha, Aulacothyris sp., coast in the Middle Jurassic. Therefore, during Gibbirhynchia nobilis, Rhynchonel/oidel/a, the Late Callovian sea-level highstand, the Jara, Sp henorhynchia asymmetrica, Ku tchirhynchia Jumara and Keera domes probably represent and Rhactorhynchia occur. The Oxfordian deeper parts of the basin, in which a fine­ brachiopod fauna of Kutch is dominated by grained and probably soupy substrate inhibited five species of Ku tchithyris i.e., K. py roidea, K. colonisation by brachiopods. The Jhura Dome, jooraensis, K. ingluviosa, K. dhosaensis, and K. 9th International Congress on the Jurassic System - Abstracts 123

1. Distribution ofPlectoido thyris (circle), Bihenithyris (triangle), Somalithyris (sphere) and Ku tchithyris (small ellipse), Fig. Cryptorhynchia (cross) in the Middle-Upper Jurassic. euryptycha,as well as by Rhynchonel/oidel/a and C. pu/cherrima and C. rugosa (MuKHERJEE et al. Sp henorhynchia. In the Kimmeridgian-Tithonian 2002). The genus had a very quick dispersal Somalithy ris and Acanthorhynchia are present and has a wide biogeographic distribution, C. in Kutch and Jaisalmer in a chocolate brown pu/cherrima is present in the Upper Bathonian oolitic limestone. of Burma, the Pamirs, and New Zealand, and Interestingly, the brachiopod distribution another species, C. bearensis, has been recorded shows that though Kutch and Jaisalmer in the Upper Bathonian of Mexico. The genus were adjacent basins the brachiopod faunas has also been recorded in the Bathonian strata considerably differed in the Bathonian but of J aisalmer (Fig. 1). became similar from the Callovian onwards. The terebratulide fauna ofJaisalmer consists This may indicate a separation of the basins of cosmopolitan taxa that have come from during Bathonian times, which due to the rise other parts of the Indo-Madagascan Province in sea level at the end of the Bathonian probably (Bihenithyris and Somalithy ris) or even the became connected in the Callovian. European Province (Plectoidothyris).

The brachiopod genera in Kutch are more References endemic. Ku tchithyris appeared in the Middle BISWAS, S. K. 1991. Stratigraphy and sedimentary evolution Bathonian ofKutch withoutany obvious ancestor of the Mesozoic basin of Kutch, western India, and speciated quickly to monopolize the space of p.74-103, In Sedimentary basins of India: tectonic context, S. K. TAN DON, C. C. PANT & S. M. CASSHYAP, eds. the newly emerging basin with its 12 species for Gyanodaya Prakashan, Nainital. a span of 13.5 m.y., continuing to the Oxfordian FiiRSICH, F.T., CALLOMON, J. H., PAND.EY, D.K. & }AITLY, A. (MUKHERJEE 2007). In the Jaisalmer Basin some K. 2004. Environments and fauna] patterns in the of these species are present in the Callovian. Kachchh riftbasin, western India, during the Jurassic. - Rivista ltaliana di Paleontologia e Stratigrafia, 110: Ku tchithyris has also been recorded from Pamir, 181-190. England, New Zealand, Madagascar, and Israel MUKHERJEE, D. 2007. A taxonomic and phylogenetic study - all from the Middle Jurassic. Cryptorhynchia, of Kutchithyris - a Jurassic terebratulide from Kutch, a Middle Jurassic rhynchonellid brachiopod, is India. - Journal of Asian Earth Sciences 30 (2007): abundant in the Bathonian sediments of Kutch. 213-237. MUKHERJEE, D.,BARDHAN,S.&GHOSH,D.N.2002.Significance The oldest species, C. karuna and C. jhooraensis, of new species of Cryptorhynchia (Brachiopoda) from are known from the Middle Bathonian of Kutch the Middle Jurassic of Kutch, India. - Alcheringa 26: and gave rise to two Upper Bathonian species, 209-231. 124 9th International Congress on the Jurassic System - Abstracts

Life in a Jurassic shelf lagoon: The Kamar-e-Mehdi Formation of east­ central Iran

YA NHONG PAN1 * & FRANZ T. F0RSICH2

1Nanjing Institute of Geology and Palaeontology, Chinese Academy of Sciences, East Beijing Road 39, 210008 Nanjing, China; E-mail: [email protected] 2Fachgruppe Paliioumwelt, GeoZentrum Nordbayern, Friedrich-Alexander University Erlangen, Loewenichstrasse 28, D 91054 Erlangen, Germany; E-mail: fra [email protected]

*Corresponding author

The Callovian-Oxfordian Kamar-e-Mehdi and a 40-m-thick package of gypsum with Formation of east-central Iran is an extensive mudstone and dolostone intercalations occur. carbonate shelf lagoon, up to 100 km wide and The formation is overlain by evaporites of the about 500 km long, that formed behind a large Magu Gypsum Formation. carbonate platform, the Esfandiar Limestone The Kamar-e Mehdi Formation contains a Formation (WILMSEN et al. 2010). The carbonate rich, moderately diverse macrofauna, strongly system developed on a tilted fault block, the dominated by bivalves, which are represented

Tabas Block, which is sandwiched between by around 70 taxa (FURSICH & PAN 2014). the Yazd Block in the west and the Lut Block The remaining fossils groups (gastropods, in the east. The three blocks together form the brachiopods, crinoids, calcisponges, serpulids, Central-East Iranian Microcontinent (CEIM) and corals) are comparatively rare, except which, during the Jurassic, was situated at the where they form elements of patch reefs. These southern margin of Eurasia and experienced patch reefs are usually1-5 m across and up to extensional tectonics due to subduction of the 1.5 m high. Frame-builders are either the oyster Neotethys. Sediments of the shelf lagoon, the Nanogyra, calcisponges and Nanogyra, the carbonate platform, and of the slope fo rming O¥Ster Actinostreon, the sclerosponge Neuropora the eastern flank of the fault block (Qal-eh and branching corals, corals, or microbialites Dokhtar Formation) are lithostratigraphically with some corals. The latter variety is locally grouped in the Esfandiar Subgroup of the Late common in the lower part of the formation, Bajocian - Tithonian Magu Group (WILMSEN et which has been singled out as the Echellon al. 2003). Limestone Member. In this member, patch The sediments of the shelf lagoon are reefs may reach up to 12 m in height. Within mainly low-energy, fine-grained carbonates the microbial crusts Tubiphytes is a common (mudstones, wackestones, floatstones) with element. rare intercalations of grainstones and rudstones Ammonites (perisphinctids) are extremely and contain several levels with meter-sized rare and belemnites are absent. Up-section, the patch reefs. Occasional thin intercalations of diversity and abundance of the faunal elements fine-grained sandstones are derived from the decreases drastically. uplifted Yazd Block in the west and exhibit The benthic macrofauna is dominated signs of storm-induced sedimentation such as a by small shallow-infaunal bivalves such as sharp erosional base, parallel lamination often Nicaniella, Corbulomima, and Protocardia and fo llowed by oscillation ripples, current ripple by rarer, large deep-burrowing bivalves such lamination, and hummocky cross-stratification. as Pholadomya, Ceratomya, and Homomya, Parts ofthe carbonates are organised in several­ which occasionally are preserved in growth meter-thick cycles which are characterised position. Occasionally, the small bivalves form by an upward decrease of clay content and shell pavements, in which the disarticulated an increase in the degree of cementation and valves are generally convex-up oriented. benthic macrofauna. Towards the top of the More conspicuous are shell concentrations formation, mudstones with gypsum needles (pavements and thin shell beds) of epibyssate 9th International Congress on the Jurassic System - Abstracts 125

(Pseudopecten, Camptonectes, Eligmus), substrate consistency, which was soft to soupy endobyssate ( Gervillella ), and cementing taxa throughout much of the sedimentary record of (Actinostreon, Nanogyra ), which typically the formation. occur at the top of the carbonate cycles. As Palaeobiogeographically, the overwhelming both, byssate and cementing taxa require some majority of the bivalves are known also hard substrate for anchorage they apparently from other areas of the northern shelf of colonised the lagoonal floor when a certain the Neotethys such as the epicontinental amount of secondary hard substrates in form seas of Europe. Exceptions are the bivalves of shell debris or complete shells of infaunal Agrawalimya, so far known only from the elements were available. Callovian of Kachchh, western India, Eligmus, Individual carbonate cycles start with marl an element of tropical areas such as the Arabian or silty marl followed by calcareous marlstonesI Peninsula and Sinai but occasionally spreading silty marlstones which contain a softground south to Kachchh and north to southern and fauna composed of small shallow- and large western Europe (Sardinia, Normandy), and deep-infaunal bivalves. Towards the top the Neoburmesia, hitherto known only from Japan. clay and silt content decreases as apparently Two of the most common taxa thriving in the did the sedimentation rate. Winnowing by waters of the shelf lagoon, Pseudopecten tipperi currents produced autochthonous shell and Camptonectes sp. nov., are the only endemic pavements. Pauci- to monospecific pavements elements of the bivalve fauna. indicate some degree of sorting and lateral transport (parautochthonous shell pavements). References The secondary hard substrates were colonised FURSICH, F.T. & PAN, Y. -H. 2014. Callovian-Oxfordian by epifaunal taxa. Most conspicuous are two (Jurassic) bivalves from the Kamar-e-Mehdi Formation large pectinids, Pseudopecten tipperi and a new of east-central Iran. Beringeria (in press). , WILMSEN, M., FURSICH, F.T. & SEYED-EMAMI, K. 2003. species of Camptonectes, whi�h afterwinno wing Revised lithostratigraphy of the Middle and Upper formed laterally extensive thin shell beds on top Jurassic Magu Group of the northwestern Tabas Block, of the cycles. east-central Iran. - Newsletters on Stratigraphy 39: Environmental factors governing 143-156. t. · r WILMSEN, M., FURSICH, F.T., SEYED-EMAMI, K., MAJIDIFARD, distribution of the benthic fauna were salinitJ, M.R. & ZAMANI PF )RAM, M. 2010. Facies analysis of a which in the upper part of the formation led large-scale Juras� : shelf-lagoon: the Kamar-e-Mehdi to increasing environmental stress, and the Formation of eas :entral Iran. - Facies 56: 59-87. 126 9th International Congress on the Jurassic System - Abstracts

A review of Virgatosphinctes densiplicatus (WAAGEN) from the Tithonian beds of Kachchh Basin, west India

DHIRENDRA K. PANDEY & SNEHA BHAUMIK*

Department of Geolog� Universityof Rajasthan, ]aipur 302 004, India; E-mail: dhirendrap@hotmail. corn

*Corresponding author

The variability in the ornamentation of Early the closest comparable species. However, V. Tithonian Virgatosphinctes densip/icatus communis differs from densiplicatus in having (WAAGEN, 1875) from the Umia Ammonite longer primary ribs. Additionally, V. communis bed (SPATH 1933: 865) of the Kateswar and exhibits oblique folds on the smooth lateral Lakhapar sections has been analysed. All these surface near the aperture, whereas such oblique ammonites exhibit biplicate ribbing on the folds are absent in V. densip/icatus. inner whorls (ribs branching at mid lateral References height) and virgatotome ribbing on the outer SPATH, L.F.1927-1933. Revision of the Jurassic cephalopod whorls. Occasionally, one of the secondaries fauna of Kachh (Cutch). Parts I-VI. - Memoirs of the ris in virgatotome ribs appears free, but close Geological Survey of India, Palaeontologia Indica, new series 9, 2: part I, 1-71, pis. 1-7 [1927]; part 72- examination of the virgatotome ribbing revealed 11, that ribs initially bifurcate at one-third oflateral 161, pls. 8-19 [1928a]; part Ill, 162-278, pis. 20-47 [1928b]; part IV, 279-550, pls. 48-102 [1931a]; part height and subsequently at mid lateral height. V, 551-658, pis. 103-124 [1931b]; part VI, 659-945, The primary ribs are thin and closely spaced on pls. 125-130 [1933]. the inner whorls and gradually become thicker WAAGEN, W. 1873-1875. Jurassic fa una of Kutch. The and sparser. The maximum diameter of the Cephalopoda. - Memoirs of the Geological Survey of investigated specimens measured 126 mm. India, Palaeontologia Indica, series 9, 1: part I, 1-22, pis. 1-4 [1873]; part 11, 23-76, pis. 5-14 [1875a]; part Virgatosphinctes densiplicatus (WAAGEN) •Ill, 77-106, pls. 15-24 [1875b]; part IV, 107-247, pis. and Virgatosphinctes communis SPATH are 25-60 [1875c]. 9rh International Congress on the Jurassic System - Abstracts 127

Sequence stratigraphic framework of the Oxfordian to Tithonian sediments (Baisakhi Formation) in the Jaisalmer Basin

DHIRENDRA K. PANDEY & DHARAMVEER POONIYA*

Department of Geo/og� Universityof Rajasthan, ]aipur 302 004, India; E-mail: dhirendrap@hotmail. eo m

*Corresponding author

Seven sections through the Oxfordian - Thechronologicalorderoftheparasequences Tithonian Baisakhi Formation in the jaisalmer has been established on the basis of ammonites Basin have been interpreted for construction ofa (Oxfordian Dichotomosphinctes sp. and sequence stratigraphic framework. In all, within Kimmeridgian To rquatisphinctes a/terniplicatus these sections 35 parasequences grouped into (WAAGEN) or To rquatisphinctes n.sp.) and the three depositional sequences (TST-HST /FSST) most logical facies correlation. Unfortunately, have been recognized. At least in two cases the no marker bed has been recognized. However, maximum flooding surface (MFS) has found the record of at least two brackish-water phases superimposed on the transgressive surface. helped in understanding depositional settings These parasequences belong to a continuous along onshore - offshoretransec ts during these sequence representing shoreface, the deepest time intervals. part of the basin, to fo reshore, shallower parts In general, the Kimmeridgian - Tithonian of the basin. During deposition of the Tithonian part of Baisakhi Formation exhibits a general part of the sequence the southern part . of coarsening-upward trend and a change from the basin witnessed shallow, nearshore or lower shoreface to fluvialenvironments. The at fo reshore to fluvial depositional environments least three sequence cycles that are represented and, consequently, several depositional gaps by the succession correspond to a still higher, and less distinct parasequences. i.e. second-order sequence cycle. 128 9th International Congress on the Jurassic System - Abstracts

Record of a condensed late Early to Middle Callovian horizon (Rehmanni­ Obtusicostites zones) from the eastern part of the Jaisalmer Basin, western India

DHIRENDRA K. PANDEY & NARENDRA SWAMI*

Department of Geology, Universityof Rajasthan, ]aipur 302 004, India; E-mail: dhirendrap@hotmail. eo m

*Corresponding author

Condensed horizon recorded in the Oxfordian Callovian Athleta Zone). Based on ammonite of the neighbouring Kachchh Basin has association, consisting ammonite assemblages been fo und quite useful in the intrabasinal of"Rehmanni zone" sensu SPATH (1933), Anceps stratigraphic correlation (ALBERTI et al. 2013). and Obtusicostites zones sensu KRISHNA & Bioturbation, concentration of high diversity 0JHA (1996, 200), this condensed horizon has of biotic elements, reworking and mixing of been assigned to late Early Callovian to Middle fauna are common features observed in the Callovian age. condensed horizons. Condensed successions The coeval sediment recorded from are commonly deposited during transgressions the Kuldhar river section is much thicker and are associated with ,maximum flooding (measured > 15 m) from where at least surfaces" and therefore may form important Macrocephalites transitorius assemblage (Early sequence stratigraphic markers. The condensed Callovian), Subkossmatia opis assemblage (late horizon recorded in the present work from Early Callovian), Reineckeia anceps assemblage the eastern part of the Jaisalmer Basin (1km (early Middle Callovian) and Cal/otia gigantea west of the Kanod village) lithostrtigraphically assemblage (late Middle Callovian) have been belongs to Kuldhar Member of the Jaisalmer recorded by KRISH�A (1987). This implies that Formation. It is characterized by bioturbated thEt eastern margin of the basin presents more calcareous highly fo ssiliferous siltstone with erosional and reworking events. reworked ammonites (Eucycloceras eucyclum (WAAGEN), Jdiocycloceras periophinetoides Obtusicostites obtusicosta References (SPATH), (WAAGEN), ALBERTI, M., FORSICH, F. T. & PANDEY, D.K. 2013. Kinkeliniceras kinkelini (DACQUE), Hubertoceras Deciphering condensed sequences: A case study from aff. mu tans (WAAGEN), Sivajiceras paramorphum the Oxfordian (Upper Jurassic) Dhosa Oolite member (WAAGEN), S. aureum SPATH, S. besairiei of the Kachchh Basin, western India. - Sedimentology COLLIGNON). The other biotic elements recorded 60 (2): 574-598. KRISHNA. I. 1987. An overview ofthe Mesozoic stratigraphy from this horizon are bivalves (P/agiostoma, of Kachchh and Jaisalmer basins. - Journal of the Lopha-marshi, Oysters), brachiopods Palaeontological Society of India, 3 2: 13 6-149. (Terebratulids, large Rhynchonellids ), KRISHNA, J. & 0JHA, J.R. 1996. The Callovian ammonoid belemnites and trace fossils. The reworking is chronology in Kachchhh (India). In: Advances in Jurassic Research (Ed., Riccardi, A.C.). GeoResearch evident from bored and encrusted concretions, Forum, 1-2: 151-166. weathered ammonite fragments encrusted with KRISHNA, J. & 0JHA, J.R. 2000. The lntrabasinal Correlation oysters and serpulids. in the Middle Jurassic Callovian Stage of Kachchh This 65 cm thick condensed horizon is (Gujarat) and Ammonoid-Foraminifer Integration. - underlain by 12 cm thick bioclastic mud- to Geophytology 28 (1&2): 101-120. PANDEY, D.K. CHOUDHARY, S, TEJ BAHADUR, SWAMI, N. & packstone bed with hardground surface, which SHA, J. 2012b. A review of the Lower - lowermost may correspond to Late Bathonian upper Upper Jurassic lithostratigraphy of the Jaisalmer part of the Bada Bag Member at the Kuldhar Basin, western Rajasthan, India - an implication on section (PANDEY et al. 2012) and is overlain biostratigraphy. - Volumina Jurassica 10: 61-82. SPATH, L.F.1927-1933. Revision of the Jurassic cephalopod by 100 cm thick gypsiferous shale yielding fauna of Kachh (Cutch). Parts I-VI. - Memoirs of the hecticoceratids (upper part of Callovian Geological Survey of India, Palaeontologia lndica, new Kuldhar Member, probably representing Upper series 9 (2): 1-945. 9th International Congress on the Jurassic System - Abstracts 129

Sedimentological and palaeoecological significance of trace fossils from the Jurassic succession of the Jhura Dome, Mainland Kachchh, Western India

SATISH J. PATEL 1 * & NIRALJ. PATEL2

1Department of Geo/ogJ" The Maharaj Sayajirao University of Baroda, Va dodara-390 002, India; E-mail: sjpgeo/ogy @gmail.com 2GSPC Bhavan, Sector -11, Gandhinagar - 382 011, India

*Corresponding author

Kachchh is a famous region amongst geologists differentplac es and mapped for their lateral and for its rich fossil content and spectacular vertical continuity and a composite litholog was outcrops of Jurassic-Tertiary successions in prepared; systematic stratigraphic sampling has various domes, highlands, streams, and rivers. been done; physical and biological sedimentary The Jhura Dome, containing the oldest exposed structures (trace fossils) have been observed, Jurassic sediments of Kachchh Mainland, recorded and examined. Sedimentary fa des provides vital information to understand and ichnofades analysis were attempted for the stratigraphy, configuration, and lateral fades Jurassic sequence (Bajodan to Oxfordian) of the changes within the basin. The study area (Fig. 1) Jhura Dome to determine the palaeoecological is situated in the northern part of the Mainland parameters and to interpret the depositional stretching from 23° 30' to 23° 40' N and 69° environment fo r the bioturbated carbonate­ 30' to 69° 40' E and falls in the Survey of India dominated succession. Topographic Sheet No. 41 E/11 Lithostratigraphically, the succession of The objective of the paper is to study and the Jhura Dome consists of two fo rmations, the understand the sedimentological characteristics Jhurio and the overlying Jumara Formation. The and trace fossil content ofthe J urassic succession core part ofthe Jhura dome, consists ofthe oldest of the Jhura Dome. For these purposes, rocks, the Jhurio Formation fo rming a big inlier. stratigraphic logs have been measured at Both formations have further been divided into

169° GREAT

1. Location map of the study area. Fig. 130 9th International Congress on the Jurassic System - Abstracts

Ta ble 1. Lithostratigraphic divisions of the Jhura Dome Ta ble 2. Ethology and toponomy of trace fossils from the section (BISWAS 1980). Jhura Dome.

Formation Member Description

IV Dhosa Oolite Member: Green oolite of various fa des such as DO SF,RM CSSF etc. are (20 m) marlstone bands alternating with rich in ammonites, belemnites, brachiopods, beds of green shale and topped by conglomeratic band and bivalves while CF and GGSF, and some part

Ill Green, gypsiferous shale with of the RMCSSL and DOSF are found to be devoid (106 m) fossiliferous marl, ferruginous and of trace fossils. white marlstone bands A total of 71 ichnospecies and 3 7 Green, gypsiferous shale with Jumara 11 ichnogenera were identified with some (50 m) fossiliferous white marlstone and red ferruginous bands. Green, indistinct forms. All identified ichnospecies hard, sandy fossiliferous marlstone have been tabulated (Table 2) and grouped I Thick, greenish to yellow-grey, into different ethological and toponomical (90 m) laminated, gypsiferous, argillaceous shale with thin red nodular hematite categories based on their behavioural and bands and numerous grey marlstone preservational patterns. Trace fossils such a and yellowish white limestone bands Rhizocorallium uraliense, Parahaentzschelinia Member G Well bedded and jointed white, grey, ardelia, Phoebichnus trochoides, Pilichnus 72 m) or cream-coloured limestone ( dichotomus, Phymatoderma isp., Cosmorhaphe Member Thick Golden oolite bands are F (20 m) intercalated with thinly bedded carpathica, Chondrites recurvus, and a number yellow limestone of Zoophycus species are reported for the first Member E Golden oolite-thick beds time from the sedimentary succession of the m) (45 Jhura Dome. Zoophycus is the most conspicuous Member D Khaki-coloured laminated Jhurio feature of the Dhosa Oolite subfacies. (40 m) calcareous shale with lenses of crystalline calcite The analysis of trace fossils revealed six Member C Golden oolite-thick beds, when ichno-assemblages, eighteen ichno-guilds m) weathered brick-red (15 and three ichnofacies. Six ichno-assemblages Member B Grey, khaki-coloured, calcareous, (Protovirgularia lA, Zoophycos-Chondrites lA, (25 m) laminated silty shales Member A Limestone and minor shale Rhizocorallium-Pilichnus lA, Ophiomorpha (19 m) lA,· Thalassinoides-Palaeophycus lA, and Ta enidium-Keckia lA) have been distinguished informal members (Table 1) by BISWAS (1991). on the basis of their occurrence and association The Middle Jurassic succession of the Jhura with other ichnotaxa which provided important Dome (Jhurio and Jumara fo rmations) consist information on palaeoenvironment, bathymetry, of carbonate and mixed siliciclastic-carbonate wave and current energy, fo od availability, sediments and attain thickness is about 600 m. oxygen conditions and substrate consistency. Clastic (oolitic) carbonate rocks are present Eighteen ichnoguilds are recognized, which at four different stratigraphic levels in the indicate similar feeding behaviour and occupy succession; based on lithological characteristics, a similar tier or location within the substrate associated physical and biogenic structures, (BROMLEY 1990). They include the Arenico/ites textures, body fo ssil content, and type of bed IG, CalycraterionIG , Chondrites IG, Diplocraterion contact, the succession exhibits six sedimentary IG, Gy rochorte IG, Ke ckia IG, Margaritichnus fa des and four subfacies namely, (1) Limestone IG, Ophiomorpha IG, Palaeophycus IG, Fades - (LF); (Badi Limestone Subfacies - BLSF, Parahaentzschelinia ·-J.G;· Phoebichnus IG, White Nodular Well Bedded Limestone Subfacies Planolites IG, Protovirgularia IG, Rhizocorallium - NWWLSF); (2) Conglomerate Fades - CF, (3) IG, Skolithos IG, Ta enidium IG, Thalassinoides IG, Calcareous Silty Shale Fades - CSSLF, ( 4) Oolitic and Zoophycus IG. Each ichno-guilds provides Limestone Fades - OLF (Golden Oolite Subfacies details on the substrate condition, level of - GOSF and Dhosa Oolite Subfacies - DOSF), (5) tiering, diversity, density, degree ofbioturbation, Rippled Calcareous Sandstone•Shale Fades associated ichnotaxa, ichnofacies, lithofacies - RMCSSF, and (6) Greenish-grey Shale Fades ,and probable depositional environment. - GGSF. The majority of the fades are highly Three Seilacherian ichnofacies have been fossiliferous and bioturbated ; certain bands identified: Skolithos Ichnofacies ( shoreface); 9rh International Congress on the Jurassic System - Abstracts 131

lchnogenera / lchnospecies Ethology Toponomy 1. Ancorichnus ancorichnus Crawling (Repichnia) Endichnial 2. Arenico/ites carbonarius Dwelling (Domichnia) Endichnial 3. Beaconites antarcticus Grazing (Pascichnia) Epichnial 4. Beaconites coronus Grazing (Pascichnia) Epichnial 5. Bergaueria isp. Dwelling (Domichnia) Epichnial 6. Bifonnites isp. Dwelling and feeding Endichnial 7. Chondrites intricatus Feeding (Fodinichnia) Endichnial 8. Chondrites isp. Feeding (Fodinichnia) Endichnial 9. Chondrites patulus Feeding (Fodinichnia) Endichnial 10. Chondrites recurvus Feeding (Fodinichnia) Endichnial 11. Chondrites targionii. Feeding (Fodinichnia) Endichnial 12. Cochlichnus anguineus Crawling (Repichnia) Epichnial 13. Cosmorhaphe carpathica Grazing (Pascichnia) Epichnial 14. Ca/ycraterion isp. Dwelling (Domichnia) Epichnial 15. Ca/ycraterion samsonowiczi Dwelling (Domichnia) Epichnial 16. Didymaulichnus isp. Crawling (Repichnia) Epichnial 17. Diplocraterion habichi Dwelling and feeding Endichnial 18. Gordia marina Crawling (Repichnia) Epichnial 19. Gyrochorte comosa Grazing (Pascichnia) Epichnial 20. Gyrolithes polonicus Feeding (Fodinichnia) Endichnial 21. Keckia annulata Grazing (Pascichnia) Epichnial 22. Laevicyc/us mongraensis Dwelling (Domichnia) Endichnial 23. Lockeia omata Resting (Cubichnia) Epichnial 24. Lockeia siliquaria Resting (Cubichnia) Epichnial 25. Margaritichnus reptilis Dwelling (Domichnia) Endichnial 26. Monocraterion tentaculatum Dwelling (Domichnia) Endichnial 27. Ophiomorpha nodosa Dwelling (Domichnia) Endichnial 28. Ophiomorpha recta Dwelling (Domichnia) Endichnial 29. Palaeophycus annu/atus Crawling and feeding Endichnial 30. Palaeophycus heberti Crawling and feeding Endichnial 31. Palaeophycus striatus Crawling and feeding Endichnial 32. Palaeophycus tubularis Crawling and feeding Endichnial 33. Parahaentzschelinia ardelia Feeding (Fodinichnia) Endichnial Endichnial 34. Phoebichnus trochoides Feeding (Fodinichnia) 35. Phycodes circinnatum Feeding (Fodinichnia) Endichnial 36. Phycodes curvipalmatum Feeding (Fodinichnia) Endichnial 37. Phycodes pa/matum Feeding (Fodinichnia) Endichnial 38. Phycodes pedum Feeding (Fodinichnia) Endichnial 39. Phymatoderma isp. Feeding (Fodinichnia) Endichnial 40. Pilichnus dichotomus Feeding (Fodinichnia) Epichnial 41. Planolites annularis Crawling and feeding Endichnial 42. Planolites beverleyensis Crawling and feeding Endichnial 43. Planolites isp. Crawling and feeding Endichnial Crawling and feed ing Endichnial 44. Planolites montanus 45. Protovirgularia dichotoma Crawling (Repichnia) Epichnial 46. Rhizocorallium irregulare Dwelling and feeding Endichnial 47. Rhizocorallium jenense Dwelling and feeding Endichnial 48. Rhizocorallium uraliense Dwelling and feeding Endichnial 49. Sabularia ramosa Feeding (Fodinichnia) Epichnial 50. Scolicia strozzii Crawling (Repichnia) Hypichnial 51. Sko/ithos /inearis Dwelling (Domichnia) Endichnial 52. Skolithos vertica/is Dwelling (Domichnia) Endichnial 53. Ta enidium J;Bmeronensis Crawling and feeding Endichnial Crawling and feeding Endichnial 54. Ta enidium satanassi 55. Ta enidium serpentinum Crawling and feeding Endichnial 56. Th alassinoides foedus Dwelling and feeding Hypichnial and epichnial 57. Th alassinoides horizonta/is Dwelling and feeding Hypichnial and epichnial 58. Thalassinoides paradoxicus Dwelling and feeding Hypichnial and epichnial 59. Th alassinoides suevicus Dwelling and feeding Hypichnial and epichnial 60. Urohelminthoida dertonensis Grazing (Pascichnia) Hypichnial 61. Zoophycus brianteus Feeding (Fodinichnia) Endichnial 62. Zoophycus caudagalli Feeding (Fodinichnia) Endichnial 63. Zoophycus circinnatus Feeding (Fodinichnia) Endichnial Feeding (Fodinichnia) Endichnial 64. Zoophycus insignis 65. Zoophycus laminatus Feeding (Fodinichnia) Endichnial 66. Zoophycus villae Feeding (Fodinichnia) Endichnial Type Feeding (Fodinichnia) Endichnial 67. Zoophycus A 68. Zoophycus Type B Feeding (Fodinichnia) Endichnial 69. Zoophycus Type C Feeding (Fodinichnia) Endichnial 70. Zoophycus Type D Feeding (Fodinichnia) Endichnial Type Feeding (Fodinichnia) Endichnial 71. Zoophycus -E 132 9th International Congress on the Jurassic System - Abstracts

Cruziana Ichnofades (lower shoreface carbonate fades, respectiwy.. Trace fossils offshore) and Zoophycus Ichnofades (shelf). have also produced similar response and their An idealized shoreface model of ichnofades diversity and abundance was controlled by the was applied fo r better understanding of various differentdep· ositional settings. The sedimentary depositional environments corresponding to fades and their corresponding sedimentary different ichnofades (PEMBERTON et al. 1992). structures, trace fossils, body fossils and The collected information has been integrated in depositional environment is given in Table 3 for working out the depositional environments for a better understanding of the relationship of the sedimentary succession of the Jhura Dome trace fossil assemblages with the depositional which revealed seven distinctive depositional environment. settings; Shelfal below SWWB, Transition to Lower Shoreface, Upper Offshore to Lower Offshore,Lower Shoreface above FWWB,Lower References BISWAS, S.K. 1980. Mesozoic rock stratigraphy of Kutch, Offshore to Shelf, Lower Shoreface to Middle Gujarat. - Quarterly Journal of the Geological, Mining Shoreface, and Upper Offshore. and Metallurgical Society of India 49:1-52 (for The presence of intraformational 1977). conglomerates is typical of storm-generated BISWAS, S.K. 1991. Stratigraphy and sedimentary fa des; DOSF and GOSF (=clastic limestones) evolution of the Mesozoic basin of Kutch, western India. In: TANDON, S.K., PANT, C.C. & CASSHYAP, S.M. suggest extensive sediment reworking, agitated, ( eds), Proceedings of Seminar on Sedimentary Basins moderate to high energy conditions in shallow of India, Nainital: 74-103, Gyanodaya Prakashan, marine ( shoreface-offshore) environments and Nainital. occasionally witnessed storm conditions (wave PEMBERTON, S.G., MACEACHERN, J.A. & FREY, R.W. 1992. Trace fo ssil facies models: environmental and ripples). A sudden increase or decrease in allostratigraphic significance. In: WA LKER, R.G., & terrigenous influx (silidclastic sedimentation) jAMES, N. (eds), Facies Models: Responses to Sea Level is responsible fo r kick-off or development of Change, Geological Association of Canada: 4 7-72

Table 3. Sedimentary facies and their corresponding sedimentary structures, trace fo ssils, body fossils, and depositional environment.

.

Phytlcal sedimentary Deposltional Litbofades Trace-fossils Body fossils structures Environment Highly iliferous;foss Conglomeratictowards Zo, Th,Pa, Ch, Sk, top; Condensedsection; DOl Oolites Rh,Gy Ammonoids; UpperOffs hore Belcmnites;

Wave ripples; Th, Rh, PI, Py, Highly fossiliferous; , Pi. OpPa, Par, Mo, Lamellibranchia; Lower Shoreface to Crossstratification Ma, Le, RMCSSL Coarsegnmules to Gy, Gyl, Brachiopods Middle Shoreface and Go, Di, ea, pebbles Cb, Ar,An Belemnites Gastropods Be Ch, parallel , Lamcllibranchia; Thin lamination; An,Lo, Pa, Ph,Co,Pr, Se,Cos, BI'Khiopods Lower Offshore to Well Ke, NWWLs bedded Th, Zo Belemnite Shelf Crinoids Mega leripp marks; Ta, Rh, Ch, Lamellibranchia; Lowangle Ke, Op,Sk, Brachiopods cross stratification; PI, Pa, Pi, Di, Dy, Lower Shoreface GOa Parallel lamination Go, Belemnite Ar,Be, Sa, Mo, Py Oolites;pebbly Ma, Crinoids, towards Corals above FWWB top Th

Rh, Ur, Th, Sa,Se, PI, Belemnite; Pi, Py,Mo , Pa, Upper to Parallel Ma, Le. ds 01fahel:e CSSL lamination; Gy, Di, Ca, Ch, Bi, Ammonoi LowerOffshore Be, Ar Lamelh'branchia; Brachiopods; Parallel BLa lamination; Zo, Ur, Rh, Shelfal SWWB Th, Op SmallGastropoda; Bedded ammonoids; below Bryozoans '----� . ------·-·------·-�··---- 9th International Congress on the Jurassic System - Abstracts 133

Discovery of Early Bathonian ammonites from Kachchh, western India and their biostratigraphic implications

DEO BRAT PATHAK & BINDHYACHAL PANDEY

Department of Geology, Banaras Hindu University, Va ranasi 221005, India; E-mail: dbpathak@yahoo. cam, [email protected]

The ammonite genera Parkinsonia and The new ammonoid assemblage includes Siemiradzkia are reported for the first time the genera Parkinsonia, Siemiradzkia, from the Indian subcontinent including the Prohecticoceras, Procerites, and Wag nericeras Himalayas. These genera are recorded here in with a few other endemic fo rms. This association with Prohecticoceras, Procerites, assemblage is dominated by cosmopolitan and Wag nericeras from the famous ammonite­ genera well known from the Submediterranean bearing J urassic locality of Kachchh, western province which enables to date the present India. This finding represent the oldest section in context of the Submediterranean ammonite-bearing levels in the Kachchh standard ammonoid zonal scheme and in turn Mainland. allows its correlation with the Macrescens The present contribution is based on a fresh Subzone (Zizag Zone) to Recinctus Subzone ammonoid collection from part of the Patcham (Aurigerus Zone) interval of Early Bathonian Formation, exposed in the northwest sector age. It is also the first definite record of the of Nara dome (23Q 38' 30" N, 69Q 07' SS" E), presence of Early Bathonian sediments in the about 1 km south of the village Nara, situated Kachchh Basin. The presence of two zones in in the western part of Mainland Kachchh. The a single bed (l.S-m-thick) suggests a relatively investigated stratigraphic section is -16-m­ slow rate of sedimentation and stratigraphic thick comprising whitish grey limestone, sandy condensation. The sudden appearance of these limestone with shalefsiltfmarl interbeds and Submediterranean ammonoid faunal elements is underlain and overlain by volcanic rock. The in the Indian subcontinent is probably due to an ammonites have been collected in-situ from a expansion event during the eustatic rise in sea -l.S-m-thick highly fossiliferous, ammonoid­ level at the end of the Early Bathonian, already rich limestone bed lying -3.S m above the recognized on the northern margin of the Tethys base. In contrast, all other hard bands of the in southern Europe. succession are relatively poorly fossiliferous. 134 9th International Congress on the Jurassic System - Abstracts

Parkinsoniids and garantianids (Late Bajocian Ammonoidea) as guide fossils and biostratigraphic indices

GIULIO PAVIA1 * & SIXTO R. FERNANDEZ-LOPEZ2

1Dipartimento di Scienze del/a Te rra, Universita deg/i Studi di To rino, 10125 To rino, Italy; E-mail: [email protected] 2Departamento Paleontologia, Facultad Ciencias Geo/6gicas, ea/leJose Antonio Novais,2, Universidad Complutense de Madrid, 28040-Madrid, Spain; E-mai/: [email protected]

Taphonomic, palaeobiological and appearances of innovative biota in several areas biochronological data are relevant in (then fossils in the stratigraphic record) may be interpreting time-space relationships of interpreted as synchronous events if they are the fossiliferous rock bodies, and in understanding effects of synchronous geographic dispersions the palaeoenvironmental changes taking from a common external source area. However, place on Earth' surface. It is assumed that the they are diachronous towards the source bed-by-bed order of succession shown by area. The appearances of innovative biota can fossils in the stratigraphic record represents be complementarily calibrated through the the chronological order of the producer taxa. synchroneity of the transgressive/regressive However,a particular feature of the fossil record changes an�ysed in sequence stratigraphy, too can condition the validity ofthe palaeontological (SANDOVAL et al. 2001). interpretations. In diverse cases it cannot be Since the latest decades of the past century, assured that fossils and rocks of the same the International Subcommission on Jurassic stratigraphic interval represent the same time Stratigraphy (ISJS) promoted activities to get interval or the same palaeoenvironment. In this definitions for the Global Boundary Stratotype sense, it must be stressed that the fossil record Section and Point (GSSP) of each stage of the can supply information on palaeoenvironments Jurassic System, and more recently (MORTON and processes that have left no traces in the 2003) asserted the opportunity to locate stratigraphic record (FERNANDEZ-LOPEZ 2000). settions that could be proposed as reference Consequently, palaeontological successions fo r the basal boundary of substages. The can display higher biochronological and definition of the base of each chronozone is geochronological completeness than also an aspect to be pursued. Such formal lithostratigraphic and biostratigraphic definitions are feasible where successions successions. Taphonomic analyses are display high chronostratigraphic completeness fundamental,astheirresultscanfurnishevidence and stratigraphic parameters do permit this of diachroneity within the facies and the fo ssil (FERNANDEZ-LOPEZ et al. 2009; PAVIA & ZUNINO assemblages of the studied stratigraphic unit. 2012). It becomes hard if the succession is The characterization of palaeontological units affected by stratigraphic and/ or taphonomic (such as the taphorecords) in a stratigraphic condensation (FERNANDEZ-LOPEZ 2011). That succession and their arrangement according is a common case in the Parkinsoni Zone, which to the time interval of the palaeobiological represents the latest Chron of the Bajocian entities, which produced the recorded fo ssils, Stage. The ammonite groups involved in the allow defining the palaeontological successions. topic are basically: the microconch Parkinsonia The palaeontological succession can show with the macroconch partner Durotrigensia, a higher number of palaeoenvironmental, and the macroconch Garantiana with many depositional, and palaeobiological events than allied taxa among them the microconch Pseudogarantiana. the stratigraphic succession (PAVIA & MARTIRE 1997; PAVIA et al. 2013). Parkinsonia l.s. - The first occurrence of Also the palaeobiogeographic parkinsoniids in the West Tethyan areas looks constrains have an effect on the potential as sudden, and it is the diagnostic criterion to of biochronostratigraphic interpretations: define the base of the Parkinsoni Zone (RIOULT 9th International Congress on the Jurassic System - Abstracts 135 et al. 1997) according to the record of the gradients between the Submediterranean group of Parkinsonia acris as the index of the and NW European provinces. New continuous basal subzone. Citations of "parkinsoniids" biostratigraphic and palaeontological recur in the literature (e.g., ScHWEIGERT et al. successions are needed to define the subzonal 2002) but their meaning need to be clarified and zonal Garantiana-Parkinsoni boundary. for effective taxonomic relationships and Garantiana I.s. - This early and middle biostratigraphic pertinence, as they commonly Late Bajocian taxon developed in the derive from condensed stratigraphic sections Submediterranean Province and repeatedly affected by taphonomic condensation with diversified during the Garantiana Chron re-elaborated fossils. Personal data from the with largest dispersion in the NW European Basque-Cantabrian Basin assure the presence Province. Taxa of the dimorphic couple of re-sedimented specimens (contemporaneous Garantiana-Pseudogarantiana are zonal and to the encasing sediments) in the middle part subzonal indexes for the Garantiana Zone of the Garantiana Zone (FERNANDEZ-LOPEZ throughout most of the Mediterranean­ 1988). Such specimens show intermediate Caucasian Subrealm. Garantianids developed morphological features between the genus through evolutionary lineages according to Caumontisphinctes of the uppermost Niortense palingenetic processes and peramorphic Zone, and the Parkinsonia of the basal Parkinsoni modifications, interrupted by paedomorphic Zone. This new biochronostratigraphic changes. This iterative evolutionary pattern information means that the origin of Parkinsonia produced numerous and brief phyletic has to be found in a still unknown place within lineages with common homeomorphs that the Submediterranean Province, and that the make it difficult to unravel their taxonomic first occurrence of Parkinsonia is not a valid "strapwork". Moreover, the type specimens criterion to recognize the basal boundary of of most garantianids were elected on fo ssils the Acris Subzone as it may be affected by deriving from the condensed sections of the diachroneity in terms of palaeobiogeographic NW European Province (e.g., DIETZE et al. 2002,

Biochronostratigraphy Biostratigraphy Biochronology BATHONIAN stratigraphic registratic succession of intervals ammonite taphorecords BOMFORDI

PARKINSONI DENSICOSTA Ysed 12: ... 1RS-12/61

...... ------IRL-12/161 ACRIS ---1Bed 11 ------IRL-11/151 z HBed 1o <( TETRAGONA ...... -10/141 (.) ------IRL 0 HBed9�.... -, GARANTIANA SUBGARANTI \ ' \ ' <( I ' \ - - -IRL-9/131 ea I - -- \ w I DICHOTOMA \ I \ � I I RL-9/121 HBed 8 I ------BACULATA , - 1_ .... -I RL-8/10 I ' I ----- '\, -1 RL-8/9 I NIORTENSE POLYGYRALIS I ----- I _ I RS-7/5 ----iBed 7l ,- � I BAN SKI ' ' ------� Bed 61 ' ----- HUMPHRIE- BLAGDENI ----- SIANUM 1. The biochronological and palaeontologic succession of the Upper Bajocian of Maizet. The left column lists the Fig. geochronological divisions and the standard (sub)chronozones for the Bajocian Stage of the West Tethyan Subrealm (modified from PAVIA et al. 2013: fig. 7). 136 9thInternational Congress on the Jurassic System - Abstracts and references therein). Only the latest genus FERNANDEZ-LOPEZ, S. 1988. El Bajociense superior y Paragarantiana is unambiguously recorded, as Bathoniense inferior en Mataporquera (Santander). Ciencias de la Tierra. - Geologia 11: 73-84. contemporaneous with the sedimentary rock FERNANDEZ-LOPEZ, S. 2000. Ammonite taphocycles in bodies, from the lowermost Parkinsoni Zone carbonate epicontinental platforms. In: HALL, R.L. & Paragarantiana is largely documented in SMITH, P. L. (eds.), Advances in Jurassic Research 2000. the central sector of the jurassic Anglo-Paris - GeoResearch Forum 6: 293-300. FERNANDEZ-LOPEZ, S.R. 2011. Taphonomic analysis and Basin, and on it we concentrated our research. sequence stratigraphy of the Albarracinites beds Although the Bajocian sections of Calvados (lower Bajocian, Iberian Range, Spain). An example are condensed, repeated taphonomic analyses of shallow condensed section. - Bulletin de la Societe (PAVIA et al. 2013, and references therein) Geologique de France 182: 405-415. allowed aligning successive palaeontological FERNANDEZ-LOPEZ, S.R., PAVIA, G., ERBA, E., GUIOMAR, M, HENRIQUES M.H., LANZA, R., MANGOLD, MORTON, N., units with biochronological meaning (Fig. 1 ) . 0LIVERO, D. & TIRABOSCHI, D. 2009. Formal proposal Our study delineates the following conclusions: for the Bathonian GSSP (Middle Jurassic) in the Ravin (1) Paragarantiana derived by a proterogenetic du Bes Section (Bas-Auran, SE France). - Swiss Journal process with paedomorphic result from of Geosciences 102: 271-295. MoRTON, N. 2003. Meeting of Jurassic Subcommission garantianids, during the transition between the Mondello, Sicily. 19th September 2002.- International Garantiana and Parkinsoni zones, displaying Subcommission on Jurassic Stratigraphy, Newsletter the first occurrence in layers of the first record 30: 3-4. of Parkinsonia gr. acris; (2) such a new phyletic PAVIA, G. & MARTIRE, L. 1997. The importance of lineage seems to be driven by a sea-level change taphonomic studies on biochronology: examples from the European Middle Jurassic. - Cuadernos de at the passage between the Garantiana and Geologia lberica: 153-181 Parkinsoni biochrons; (3) this evolutionary PAVIA, G. & ZUNINO, M. 2012. Ammonite assemblages event of Paragarantiana origination has an and biostratigraphy at the Lower to Upper Bajocian unequivocal and singular biochronological boundary in the Digne area (SE France). Implications meaning that may be used to define the base for the definition of the Late Bajocian GSSP.- Revue de Paleobiologie, vol. spec. 11: 205-227. of the Parkinsoni Zone, possibly paired with PAVIA, G., DEFAVERI, A., MAERTEN, L., PAVIA, M. & ZUNINO, the first appearance of the P. acris group M. 2013. Ammonite taphonomy and stratigraphy of when its chronostratigraphic value would be the Bajocian at Ma�zet, South of Caen (Calvados, NW ascertained. France). - C.R. Palevol 12: 137-148. RI

A first Upper Jurassic 40Ar /39 Ar date from Oxfordian ammonite-calibrated volcanic layers (bentonites) from the Rosso Ammonitico Veronese, Italy

*, PIERRE PELLENARD1 SEBASTIEN NOMADE2, LUCA MARTIRE3, FABRICE MONNA4 & HERVE GUILLOU2

1Biogeosciences, CNRS- UMR 6282, Universite de Bourgogne, F-21000 Dijon, France; E-mail: Pierre. [email protected] 2LSCE-IPSL, CNRS-UMR 8212, CEA Orme, F- 91191 Gif-sur-Yvette, France; E-Mail: Sebastien.nomade@ lsce.ipsl.fr; [email protected] 3Dipartimento di Scienze del/a Te rra, Universityo[ To rino, via Va lperga Caluso 35 10125 To rino, Italy; E-mail: [email protected] 4ARTeHIS, CNRS-UMR 6298, Universite de Bourgogne, F-21000 Dijon, France; E-Mail: Fabrice. [email protected]

*Corresponding author

The scarcity of interbedded volcanic units in the Upper Callovian to the Middle Oxfordian ammonite-bearing marine successions hinders (G. transversarium Biozone). As ammonites the accurate numerical calibration of the Late diagnostic of the G. transversarium Biozone J urassic Time Scale, even with the progress made were fo und just below the thickest bentonite at in GTS2012, including improved numerical ages Kaberlaba and just above at Echar, this bentonite for stage boundaries, obtained by selecting only clearly belongs to the G. transversarium Biozone single-zircon U- Pb ages, recalculating 40Ar /39 Ar (Middle Oxfordian). dates, and more precise magnetostratigraphy The laser-fusion step-heating 40Ar/39Ar and cyclostratigraphy (GRADSTEIN et al. 2012). method was performed on 30 small ( <100 In this study we fo cus on eight volcanic ash 11m) transparent sanidines, carefully hand­ layers weathered into bentonites, identified picked under a binocular microscope after by their fi eld characteristics, mineralogy, and several treatments from the thickest bentonite. geochemical features that occurred in pelagic The apparent age spectrum obtained fo r cherty limestones, the Rosso Ammonitico sanidines is 100o/o concordant; all steps Veronese, from the Trento Plateau domain, yield indistinguishable ages, with a well­ north-eastern Italy, at the Serrada, Echar, defined plateau age of 156.1 ± 0.89 Ma (2cr and Kaberlaba sections (PELLENARD et al. full uncertainty propagation) using the 2013). In the Rosso Ammonitico Veronese, optimisation model ofRENNE et al. (2010, 2011) bentonites appear as continuous, centimetre­ fo r estimating the partial decay constants of 4°K thick red or white plastic day-rich horizons, and 40 Ar* /4°K ratio of Fish Canyon sanidine. interbedded with limestones and cherts. The plateau age we obtain can be directly Mineralogical and elemental analyses were compared to U-Pb ages available fo r the jurassic performed ·on all powdered samples to Time Scale. Nevertheless, there are no well­ confirm their volcanic nature. At Kaberlaba, constrained radiometric dates, closely tied to five bentonites are recognised. The ammonite ammonite biostratigraphy, currently available assemblage, characteristic of the Gregoryceras for the whole of the Upper jurassic. Some Upper transversarium Biozone, indicates a Middle jurassic Ar/ Ar dates are integrated as secondary Oxfordian age fo r the top of the unit where the guides into GTS2012: (1) A suite of dates from thickest bentonite has been identified (CLARI et the almost totally non-marine Morrison Fm in al. 1990; MARTIRE etal. 2006).At Echar, the same the USA (GRADSTEIN et al. 2004; OGG et al. 2008); five bentonites are recognised and are overlain (2) dates from Oxfordian tuffs intercalated with by three stromatolitic beds, the first of which terrestrial sediments in China (CHANG et al. belongs to the G. transversarium Biozone, with 2009); (3) dates from ocean-floor basaltveins the same taxa as at Kaberlaba. At Serrada, six in the Pacific (GRADSTEIN et al. 2012). A single bentonites are recognised and are dated from Re/Os date is available from ammonite-bearing 138 9rh International Congress on the Jurassic System - Abstracts marine sedimentary successions in the Lower GRADSTEIN, F.M., 0GG, J.G. & SMITH, A.G. 2004. A Geologic Kimmeridgian (SELBY 2007). As a consequence, Time Scale 2004. 589 pp., Cambridge University Press, Cambridge. the Late Jurassic Time Scale derives mainly from GRADSTEIN, F.M., 0GG, J.G., SCHMITZ, M.D. & OGG, G.M. 2012. the Pacific seafloor-spreading numerical model The Geologic Time Scale 2012. 1144 pp., Elsevier, ofthe M -sequence magnetic polarity pattern and Amsterdam. from limited recent cyclostratigraphic studies MARTIRE, L., CLARI, P., LOZAR, F. & PAVIA, G. 2006. The Rosso Ammonitico Veronese (Middle-Upper Jurassic (GRADSTEIN et al. 2012). The age proposed of the Trento Plateau): a proposal oflithostratigraphic here, well constrained within the standard ordering and fo rmalization. - Rivista ltaliana di Jurassic biostratigraphic zonation, provides Paleontologia e Stratigrafia 112: 227-250. the first accurate and reliable numerical age 0GG, J.G., 0GG, G. & GRADSTEIN, F M. 2008. The concise currently available for the Late Jurassic Time Geological Time Scale. 177 pp., Cambridge University Press, Cambridge. Scale (PELLENARD et al. 2013). This Middle PELLENARD, P., NOMADE, S., MARTIRE, L., DE 0LIVEIRA Oxfordian date is in better agreement with RAMALHO, F., MONNA, F. & GUILLOU, H. 2013. The first GTS2004 boundaries than with the current 40Ar/39Ar date from Oxfordian ammonite-calibrated GTS2012. This precise new tie-point can be volcanic layers (bentonites) as a tie-point fo r the Late Jurassic. - Geological Magazine, in press. used to anchor floating cyclostratigraphy and RENNE, P. R., MUNDIL, R., BALCO, G., MIN, K. & MUDWIG, K.R. magnetostratigraphy, thus contributing to the 2011. Response to the comment by W. H. ScHWARZ et improvement of seafloor-spreading models al. on ,Joint determination of4°K decay constants and and, above all, will aid in the calibration of the 40Ar+ /4°K fo r the Fish Canyon sanidine standard, and Late Jurassic time scale. improved accuracy for Ar-40/Ar -39 geochronology" by P. R. RENNE et al. (2010). - Geochimica et References Cosmochimica Acta 75: 5097-5100. (HANG, S., ZHANG, H., RENNE, P. & FA NG, Y. 2009. High­ RENNE, P. R., MUNDIL, R., 8ALCO, G., MIN, K. & MUDWIG, K.R. precision 40Ar/39Ar age constraints on the basal 2010. Joint determination of 4°K decay constants and Lanqi Formation and its implications fo r the origin 40Arf4°K fo r the Fish Canyon sanidine standard, and of angiosperm plants. - Earth and Planetary Science improved accuracy fo r Ar-40/ Ar-39 geochronology. ­ Letters 279: 212-221. Geochimica et Cosmochimica Acta 74: 5349-5367. CLARI, P.A., MARTIRE, L. & PAVIA, G. 1990. L'unita Selcifera SELBY, D. 2007. Direct Rhenium-Osmium age of the del Rosso Ammonitico Veronese (Alpi Meridionali). Oxfordian-Kimmeridgian boundary, Staffin Bay, - In: PALLINI, G. et al. (eds.), Atti Convegno "Fossili, Isle of Skye, U.K., and the Late Jurassic time scale. -

Evoluzione, Ambiente": Pergola 11 1987: 151-162. • Norwegian Journal of Geology 47: 291-299. 139 9th International Congress on the Jurassic System - Abstracts

Integrated stratigraphy of the potential candidate Oxfordian GSSP at Thuoux and Saint-Pierre dl\rgen�on (France)

PIERRE PELLENARD1 *, ANNACHIARA BARTOLINI2, SLAH BOULILA3, PIERRE-YVES COLLIN1, DOMINIQUE FORTWENGLER1, BRUNO GALBRUN3, SILVIA GARDIN4, VINCENT HUAULT5, EMILIA HURET6, DIDIER

MARCHAND7 & )ACQUES THIERRY1

1UMR CNRS 6282 Biogeosciences, Universite de Bourgogne, 6 Bd Gabriel, 21000 Dijon, France; E-mail: [email protected]; [email protected]; dominique.fortwengler@ wanadoo.fr; [email protected] 2Museum National d'Histoire Nature/le, UMR 7207 CR2P ,Centre de recherche sur la Pa/eobiodiversite et les Pa/eoenvironnements'; Fra nce; E-mail: [email protected] 3Universite Paris 6, UMR 71 93 /STeP ,Institut des Sciences de la Te rre-Paris'; Paris, France; E-mail: [email protected]; [email protected] 4Universite Paris 6, UMR 7207 CR2P ,Centre de recherche sur la Pa/eobiodiversite et les Pa/eoenvironnements'; Paris, France; E-mail: [email protected] 5UMR CNRS 7359 Georessources, Universite de Lorraine, BP 239, 54506 Va ndceuvre-Ies-Nancy Cedex, France; E-mail: vincent. [email protected] 6ANDRA, Pare de la Croix-Blanche, 1-7 rue jean Monnet, 92298 Chatenay-Malabry, Fra nce; E-mail: [email protected] 78a, avenue Ste Claire, 06100 Nice, France; E-mail: [email protected]

*Corresponding author

In Western European . basins, the an accurate biostratigraphy (FORTWENGLERetal. Callovian-Oxfordian transition is commonly 2012). The Thuoux and Saint-Pierre d'Argen<;:on marked by hiatuses or condensed levels. sections consist of several tens of metres of The scarcity of available ammonite-rich shales and calcareous shales, with occasional continuous sedimentary successions, nodular rusty or buff-coloured carbonate beds, allowing precise ammonite biostratigraphy characteristic of the "Terres Noires" Formation. and integrating ammonite taxa from various The Callovian-Oxfordian boundary is well palaeobiogeographical provinces, renders exposed in both sections and all ammonite difficult the choice of a reliable section to define biohorizons and subzones of the uppermost a Global boundary Stratotype Section and Point Callovian Lamberti and basal Oxfordian Mariae (GSSP) fo r the Middle-Late jurassic transition. In Zones can be clearly identified. this context, the RedcliffPoint- Ham Cliffsec tion At Thuoux, the biostratigraphic framework (Weymouth, UK) was proposed as a candidate is precisely based on the fo llowing succession for the Callovian-Oxfo rdian boundary GSSP, of different ammonite species and genera. while the Savournon section (Subalpine Basin, Within the Lamberti Zone Lamberti SE France) was selected as an alternative (PAGE subzone and the Mariae Zone - Scarburgense et al. 2008). Here we propose other potential Subzone, which bracket the boundary, the sections as a candidate GSSP for the Callovian­ corresponding biohorizons are clearly Oxfordian boundary at Thuoux and Saint-Pierre identified: (1) The upper part of the Callovian d'Argen<;:on(Subalpine Basin, SE France). (lamberti horizon) is characterised by scarce Numerous well-exposed outcrops in the Kosmoceras and Distichoceras and always the Diois, Baronnies, and the Buech valley have clear presence of Quenstedtoceras lamberti been studied over several decades for the (SOWERBY), Hecticoceras punctatum LAHUSEN Middle-Late jurassic transition, including and Poculisphinctes poculum (LECKENBY). biostratigraphic, sedimentological, and tectonic (2) The uppermost part of the Callovian aspects. In many sections of this domain, (paucicostatum horizon) is characterised by numerous well-preserved ammonites provide the total disappearance of Kosmoceratidae and 140 9th International Congress on the Jurassic System - Abstracts the eo-occurrence of the latest Quenstedtoceras curve does not correlate with carbonate content cf. lamberti (Sow.) with the first Cardioceras and oxygen-isotope values, therefore mirroring, paucicostatum LANGE. In the upper part of at least in part, the primary environmental that horizon, we notice abundant Hecticoceras signal. The "- 1,5 %o increasing li13Ccarb trend pau/owi (DE TSYTOVITCH) and the first around the Callovian/Oxfordian boundary has appearance of Peltoceratoides eugenii (RASPAIL). already been documented in other sections and (3) The basal Oxfordian is characterised by the boreholes in France, Switzerland and elsewhere isochronous first appearance of true Cardioceras (PELLENARD et al., 2013). The positive li13Ccarb scarburgense Hecticoceras (YOUNG & BIRD), shiftto maximal values can thus be used as an (Brightia) th uouxensis FoRTWENGLER et al. and auxiliary marker of the CallovianfOxfordian Peltoceratoides eugenii morphe eugenii. This (and MLJ) boundary. fauna characterises the thuouxensis horizon, the High-resolution analysis of magnetic first biohorizon of the Scarburgense Subzone. susceptibility and field spectral gamma ray ( 4) Above, several shell ornamentation changes measurements were performed on 700-m-thick are used to characterise the basal Oxfordian: Early-Middle Oxfordian marine marls of the the secondary ribs of Peltoceratoides eugenii Terres Noires Formation. Sub-Milankovitch to suddenly bifurcate lower on the flanks, and Milankovitch cycles are clearly identified, with Hecticoceratinae macroconchs have softer the long-term eccentricity ( 405 kyr and 2 myr) ornamentation. (5) The first morphs close to C. being the most prominent. The 405 kyr cycle woodhamense ARKELL appear at the top of the was used as a high-resolution geochronometer Scarburgense Subzone. This species never co­ for astronomical calibration of this poorly exists with C.scarb urgense. constrained interval of Late Jurassic time. The The potential of nannofossil biohorizons to astronomical calibration of the Mariae Zone be useful proxies fo r the Callovian-Oxfordian indicates a duration of -2.2 myr in this basin boundary has been tested by a quantitative (BOULILA et al. 2010). New high-resolution analysis and biometric measurements of key magnetic susceptibility analysis (every 8 cm) and taxa. Results indicate that the marker species spectral gamma ray measurements (every 12 Stephanolithion bigoti maximum, defined as cm) of the Thuoux and Saint-Pierre d'Arge"';on having "measurements exceeding 6x31J.m", is sections spanning the Callovian-Oxfordian not present in the boundary interval, although transition will allow astronomical calibration an increase in size reaching 5.50/5.60 11mof rim of the associated ammonite sub-zones and length occurs from the Paucicostatum Subzone, horizons, and assessment of variations in in coincidence with a positive carbon isotope sedimentation rate. excursion. Thus, the recognition and utility of S. bigoti maximum as a marker for dating and References correlating the Callovian-Oxfordian boundary BOULILA, S., GALBRUN, B., HINNOV, L.A., COLLIN, P.-Y., 0GG, J.G., FORTWENGLER, D. & MARCHAND, D. 2010. Milankovitch interval depends only on accurate biometric and sub-Milankovitch forcing of the Oxfordian (Late measurements. The Callovian-Oxfordian Jurassic) Terres Noires Formation (SE France) and boundary is well defined in palynology by global implications. - Basin Research 22: 717-732. the occurrence of Wa naea fi mbriata. Ongoing FORTWENGLER, D., MARCHAND, D., BONNOT, A., }ARDAT, R. & investigations of dinoflagellate cyst assemblages RAYNAUD, D. 2012. Proposal for the Thuoux section as a candidate for the GSSP of the base of the Oxfordian in the Thuoux and Saint-Pierre d'Arge"';on stage. - Carnets de Geologie (Notebooks on Geology), sections should provide deciding factors in CG2012A06: 117-136. the placement of the GSSP fo r the Middle-Late PAGE, K.N., MELENDEZ, G., HART, M.B., PRICE, G.D., Jurassic transition. WRIGHT, J.K., BOWN, P. & BELLO, J. 2009. Integrated stratigraphical study of the candidate Oxfordian The marlstone bulk-carbonate li13C­ Global Stratotype Section and Point (GSSP) at Redcliff record at the Thuoux section shows marked Point, Weymouth, Dorset, UK. - Volumina Jurassica 7: fluctuations, with values from 0 °/o o to 2 %o. 101-111. Although the values are quite scattered in some PELLENARD, P., TRAMOY, R., PUCEAT, E., HURET, H., MARTINEZ, intervals, significant trends across the MLJ M., BRUNEAU, L. & THIERRY, J. 2013. Carbon cycle and palaeoenvironmental changes at the Middle-Late (Middle-Late Jurassic) boundary are still well Jurassic transition from the Paris Basin (France). - discernable. This general pattern of the Marine and Petroleum Geology, in press. li13Ccarb 9th International Congress on the Jurassic System - Abstracts 141

Evolution of Volgian-Valanginian microphytoplankton communities in the Olenyok River region, North Siberia

E. B. PESTCHEVITSKAYA

Institute of Petroleum Geology and Geophysics, Novosibirsk 630090; E-mail: paleodinocyst@gmail. eo m

A palynological study of the Volgian-Valanginian the Russian Platform (PESTCHEVITSKAYA et al. section from the Olenyok River basin provides 2011; HARDING et al. 2011); the appearance of new data on the evolution of Siberian Bourkidinium has also been identified in the dinoflagellate communities in Late Jurassic Late Tithonian of Western Europe (BOOROVA and Early Cretaceous times. Ammonite and et al. 1999) and the Middle Volgian of the foraminiferal zones in the Volgian and Berriasian Russian Platform (RIDING et al. 1999). ( 4) The give us additional stratigraphic control of the Batioladinium varigranosum - Circulodinium dinoflagellate succession (NIKITENKO et al. distinctum - Circulodinium colliveri Zone 2012). (uppermost Volgian - Lower Berriasian). First Taxonomic changes in dinoflagellate fi nds of Circulodinium col/iveri are also reported assemblages allow the definition of five from the Berriasian of Canada and Antarctica; dinoflagellate zones. All assemblages include the appearance of Circulodinium distinctum some taxa, which provide interregional has been defined in the Berriasian of Siberia, correlation. The correlative events are as Canada, Greenland and England; the appearance fo llows: (1) The Athigmatocysta glabra - of Te hamadinium dodekovae is defined in France Circulodinium compta Cometodini11m as Berriasian (PESTCHEVITSKAYA et al. 2011). habibii Zone (Lower Volgian). Occisucysta (5) The Pareodinioideae - Cassiculosphaeridia ?monoheuriskos, Leptodinium subtile, L. reticulata Cyclonephelium cuculliforme simplex, and L. mirabile are common in the Zone. The diversity of pareodinioid Late Tithonian of North America; Occisucysta forms, Barbatacysta - Sentusidinium and ba/ios and Scriniodinium inritibile disappear in Escharisphaeridia - Batiacasphaera groups the Late Kimmeridgian of Western Europe. (2) are also typical of other regions of Siberia; the The Scriniodinium campanula - Trichodinium appearance of Cassiculosphaeridia reticulata ciliatu m-Occisucysta wiersbowskii Zone (upper has also been defined as Late Berriasian in part of the Lower Volgian - lower part of the Siberia and the Subpolar Urals; the appearance Middle Volgian). the appearance of Occisucysta of Cy clonephelium cuculliforme has also been wierzbowskii and Scriniodinium campanula reported from the Late Berriasian of North has also been defined in the Early Volgian of Siberia and Arctic Canada. Dinoflagellates Poland; the disappearance of Scriniodinium become rare in the Valanginian. An important inritibile and Occisucysta balios has also been feature is the appearance of Muderongia crucis, identified in the Late Kimmeridgian of Western as its first occurrence has been defined in other Europe and the Middle Volgian of the Russian regions of Siberia in the upper part of the Lower Platform (PESTCHEVITSKAYA et al. 2011). (3) The Valanginian (PESTCHEVITSKAYA 2010). Gochteodinia villosa -Dingodinium ?spinosum The established biostratigraphic succession - Bourkidinium sp. Zone (upper part of the and biofacies analysis of dinoflagellate Middle Volgian - lower part of the Late Volgian). communities allow the reconstruction of The extinction of Gonyaulacysta dualis has transgressive-regressive (T-R) changes of the also been recognised in the middle part of the North Siberian palaeo-basin in the Olenyok Middle Volgian in the Nordvik section of North River region during the Volgian, Berriasian, Siberia (NIKITENKO et al. 2008); the appearance and Valanginian. Essential taxonomic changes of Dingodinium ?spinosum and Gochteodinia in dinoflagellate communities and quantitative vil/osa, has been correlated with the Portlandian fluctuations of the microphytoplankton in of Western Europe and the Middle Volgian of general indicate that Volgian-Valangianian 142 9th International Congress on the Jurassic System - Abstracts deposits were fo rmed in the marginal zone are also recognised in different regions of of the palaeo-basin influenced by frequent Europe, Canada, and Antarctica and can be T- R events. Shallow water environments in regarded as reliable correlative markers. The the Early Vo lgian are confirmed by the lower established biostratigraphic succession of quantity of microphytoplankton (8% in relation dinoflagellate zones provides the stratigraphic to the terrestrial palynomorphs ). However, the basis for the analysis of local T- R events in the diversity of dinoflagellates suggests normal Volgian-Valanginian and the reconstruction of marine conditions. The transgression occurred the dynamic of the North Siberian palaeobasin at the end of the Early Volgian. Dinoflagellate in the Olenyok River region. associations became very rich and diverse. They contained numerous taxa of the families Gonyaulacaceae and Pareodiniaceae (56°/o), a Projects RAS 23, 28 and IGSP 608. feature that is often regarded as an indicator References of the neritic zone. The Middle to Late Volgian BOOROVA, D., LOBITZER, H., S PIEN, P. & VA SICEK, 1999. KU z. and the beginning of the Berriasian were Biostratigraphy and facies of Upper Jurassic-Lower characterized by unstable environments Cretaceous pelagic carbonate sediments (Oberalm-, leading to frequent changes in the taxonomic Schrambach- and Ro8feld-Formation) in the Northern composition of dinoflagellate communities Calcareous Alps, South of Salzburg. - Abhandlungen der Geologischen Bundesanstalt 56: 273-318. and quantitative fluctuations of different HARDING, I.C., SMITH, G.A., RIDING, J.B. & WIMBLEDON, groups of microphytoplankton. The percentage W.A.P. 2011. Inter-regional correlation of Jurassic/ of microphytoplankton varied to a great Cretaceous boundary strata based on the Tithonian­ extent (12-57% in relation to the terrestrial Valanginian dinoflagellate cyst biostratigraphy of the Volga Basin, western Russia. - Review ofPalaeobotany palynomorphs). The diversity of dinoflagellates and Palynology16 7: 82-116. was reduced, but remained rather high which is HUNT, C.O. 2004. Palynostratigraphy of the classic typical for shallower areas of the neritic zone. Portland and Purbeck sequences of Dorset, southern The increased percentage of dinoflagellates England, and the correlation of Jurassic-Cretaceous with simple morphology and of the fa mily boundary beds in the Tethyan and Boreal realms. In: BEAUDOIN, A.B. & HEAD, M.J. ( eds.), The palynology Pareodiniaceae possibly point to climate and micropalaeontology of boundaries. - Geological cooling. During that time, microphytoplankton •Society of London Special Publication 230: 175-187. associations were periodically dominated by NIKITENKO, B.L., PESTCHEVITSKAYA, E.B., LEBEDEVA, prasinophytes of the genera Leiosphaeridia and N.K. & ILYINA, V. l. 2008. Micropalaeontological and palynological analyses across the Jurassic-Cretaceous Ta smanites that is ofteninterpreted as evidence boundary on Nordvik Peninsular, Northeast Siberia. ­ of stagnant, anoxic conditions. The regression Newsletters on Stratigraphy 42: 181-222. began in the Late Berriasian and became stronger NIKITENKO, B.L., PESTCHEVITSKAYA, E.B., KHAFAEVA, in the Early Valanginian. It is confirmed by S.N. & KNYAZEV, V.G. 2012. Preliminary data on the taxonomic changes of the microphytoplankton. biostratigraphy and biofacies of Volgian-Valanginian section from the Olenyok river region (North Its quantity was reduced in the Late Berriasian, Siberia). In: VISHNEVSKAYA, V. S. (ed.), Contemporary but dinoflagellate diversity remained rather micropalaeontology. - Proceeding of XV Russian high indicating stable, fully marine conditions. micropalaeontological conference: 19-22, Gelendzhik, Sharp reduction of the microphytoplankton Kuban University [in Russian]. PESTCHEVITSKAYA, E.B. 2010. Dinocysts and percentage (3-9°/o) occurred in the Early palynostratigraphyof the Lower Cretaceous in Siberia: Valanginian. The prasinophyte Leiosphaeridia is 230 p., Novosibirsk, Geo. the most abundant taxon here. Dinoflagellates PESTCHEVITSKAYA, E.B. 2007. Dinocyst biostratigraphy of are rare, including Sentusidinium, Apteodinium, the Lower Cretaceous in North Siberia. - Stratigraphy Cribroperidinium, Circulodinium, and and GeologicalCorrelation 15: 577-609. PESTCHEVITSKAYA, E., LEBEDEVA, N. & RYBOKON, A. 2011. Batioladinium. Uppermost Jurassic and lowermost Cretaceous Thus, the palynological study of the dinocyst successions of Siberia, Subarctic Urals and Volgian-Valanginian succession in the section Russian Platform and their interregional correlation. from the Olenyok River region shows that - Geologica Carpathica 62: 189-202. RIDING, J.B., FEDOROVA, V.A. & ILYINA, V. l. 1999. Jurassic taxonomic changes in the microphytoplankton and lowermost Cretaceous dinoflagellate cyst communities depend on both local biostratigraphyvoftheRussian Platform and Northern environments and evolutionary events, which Siberia, Russia. - AAPSContribution series 36: 1-184. 9th International Congress on the Jurassic System - Abstracts 143

Marine (black) and marginal-marine (green) Toarcian shales in Europe - carbon isotope consistency,TOC inconsistency

GRZEGORZ PIENKOWSKI1 * & MARTA HODBOD2

1Po/ish Geological Institute - National State Institute, Rakowiecka 4, PL-00-975 Wa rszawa, Poland; E-mail: [email protected] 2Polish Geological Institute - National State Institute, Rakowiecka 4, PL-00-975 Wa rszawa, Poland; E-mail: [email protected]

*Corresponding author

A black shale is a black/dark grey mudstone rich whereas there is a perfect correlation between in total organic carbon - TOC (>5% by weight) CIE steps in marine and marginal-marine/ generally formed in anoxic marine bottom non-marine settings, the correlation is directly waters, usually connected with Oceanic Anoxic opposite when the TOC content is compared. Events (OAE), including the well-documented Contrary to the epicontinental open marine Toarcian Oceanic Anoxic Event (T-OAE), one basins, where more negative 613C values mean of the largest ( --6%o) in Phanerozoic times. higher TOC content, in the Polish Basin there They were fo rmed when a high rate of organic is an opposite correlation: the more positive burial globally over a brief interval of time has the 613C values, the higher the TOC content. In led to the deposition of organic-rich sediments. the Polish Basin, strata richest in TOC predate Many parts of Europe contain prime targets the T- OAE. Palynofacies reflect the sea-level fo r shale gas exploration, one of these is the changes (shore proximity) and climate changes Posidonia Shale (Early Toardan, -183 M a ago) inferred from kaolinite content, megaspore of northern Germany and approximately coeval frequency and CIE steps. Of particular note black shales from the Paris Basin (France) and is the dinoflagellate peak associated with a Cleveland Basin (England). At the same time, flooding surface, slightly preceding the T- OAE in the Polish Basin, poorly consolidated green/ onset, which reflects a bloom of plankton, grey mudstones, claystones and siltstones most probably associated with major climate­ ("verdine" facies) with subordinate sandstone oceanographic change. Each 100-kyr cycle in intercalations (Ciechocinek Formation) were carbon-isotope values was characterized by deposited in a large embaymentflagoon. increasingly severe palaeoclimatic changes, Deposition ofboth black and green shales in early culminating in extremely hot and humid Toarcian times is associated with abrupt and conditions (high abundance of megaspores and large-magnitude changes in the global carbon fungal spores), co-incident with the peak of the cycle (Carbon Isotope Excursions - CIE), which final-most negative carbon-isotope excursion appear to be a recurrent phenomenon during and TOC-rich, black shale deposition in West greenhouse periods of Earth' history. Early Europe. In the marginal-marine Polish Basin Toarcian carbon-isotope data from terrestrial these extreme greenhouse conditions are organic matter of the Polish Basin (phytoclast related to the lowest values of TO C. Productivity separates) show that the shift to light carbon in this brackish-marine waters (inferred from isotope values in the woody organic matter,and P 0 content) was only slightly diminishing 2 5 therefore also in atmospheric carbon dioxide, during the T-OAE, mostly due to increasing occurred in major steps, similarly as in the freshwater influx (gradual disappearance of oceans. The steps identified in green shales in dinoflagellates) and shallowing of the basin. Poland were correlated with those identified Depletion ofTOC in green shales should be then from marine organic matter (black shales), explained by preservational conditions, related where they have previously been attributed to to an intensified hydrolic cycle and runoff, 100 kyr eccentricity forcing of climate. However, resulting in shallowing, destruction of the 144 9th International Congress on the Jurassic System - Abstracts halocline and a well-oxygenated bottom. Of note References is a very sensitive reaction of these processes to HESSELBO, S.P. & PIENKOWSKI, G. 2011. Stepwise atmospheric carbon isotope excursion during the changes in o13C values. Early Jurassic Oceanic Anoxic Event. - Earth and Planetary Science Letters 301: 365-372. 9th International Congress on the Jurassic System - Abstracts 145

End-Triassic biota crisis and earliest Jurassic recovery in continental strata of Poland in relation to rapid climatic reversals associated with CAMP volcanism

*, 2 GRZEGORZ PIENKOWSKI1 GRZEGORZ NIEDZWIEDZKI & PAWEt.BR ANSKI3

1Polish Geological Institute - National State Institute, Rakowiecka 4, PL-00-975 Wa rszawa, Poland; E-mail: [email protected] 2Subdepartment of Evolution and Development, Department of Organismal Biology, Evolutionary Biology Centre, Uppsala University, Norbyviigen 18A, 752 36 Uppsala, Sweden; E-mail: grzegorz. [email protected] 3Polish Geological Institute - National State Institute, Rakowiecka 4, PL-00-975 Wa rszawa, Poland; E-mail: [email protected]

*Corresponding author

Eight climatic events indicated by the kaolinite/ sulphate aerosols, and toxic compounds is illite ratio, Chemical Alteration Index, colour inferred to have caused this series of rapid of sediments, and palynomorphs can be climatic reversals and resulting extinction of distinguished in the transitional Triassic - many less adapted fo rms. Our conclusion is that Jurassic (T-J, c. 201 mya) continental strata the extinction period is more prolonged than of Poland. The first climatic humidification the some 20,000 years duration of the 'initial' turnover, evidenced by shift from smectite to CIE. Just above the palynofloral extinction level, kaolinite-dominated mudrocks, coincides with appearance of new fo rms started the Jurassic the earlier ('precusor') Rhaetian negative cS13C palynofloral recovery. Tetrapod evolution excursion, which means that the beginningorg events at the end Triassicfearliest Jurassic were of climate perturbations predated the oldest related with extinction of the Pseudosuchia, known CAMP flood basalts by some 100-200 Dicynodontia, Capitosauroidae, Plagiosauridae, kyr. The global, late Rhaetian 'initial' negative and Rhynchosauria, while appearance of a cS13C excursion is divided into two 'sub-peaks' highly-diversified tetrapod ichnofauna in the org (KoRTE & KozuR 2011) corresponding to hot earliest}urassic strata indicates a rapid recovery and humid events, separated by a cooler/ drier and refill of ecological niches. event. Based on calculation of the duration Obtained values of initial 1870sjl860s of the whole 'initial' bi-partite CIE (10,000 to between 2.905 and 4.873 and very low iridium 20,000 years; RUHL et al. 2011), our study shows content lend no support fo r an asteroid impact that these changes are of too high a frequency at the T-J boundary event, although one cannot to be linked with astronomical forcing, but exclude a hypothetical comet impact or 'comet they could be easily associated with episodes shower', which would not leave any geochemical of CAMP eruptions. This is further supported traces behind. However, CAMP-related volcanic by differences of certain geochemical and volatiles causing frequent climate disturbances palynological properties (Os isotope system and influencing in many ways the ecosystem disturbances as well as darkening of miospores seem to be a much more substantiated cause and, circumstantially, PAHs content. Between for the end-Triassic extinction, while relative the 'initial' excursion and the T-J boundary stabilization of climate in Hettangian times zone, next five climatic fluctuations are inferred allowed the biota recovery (PIENKOWSKI et al. from the changing kaolinite-illite ratio, the last 2012). two are also associated with Os isotope system perturbations, polycyclic aromatic hydrocarbon This paper is part of a project, which has been financed by the Polish National Science Centre, granted on the (PAH) releases, 'spore peak' and darkened basis of decision no. DEC-2012/06/M/STl0/00478. G.N. miospores. A series of periodic atmospheric is currently funded by a Wallenberg Scholarship grant loading by C0 , CH or, alternatively, by S0 , awarded to P. E. Ahlberg (Uppsala University). 2 4 2 146 9th International Congress on the Jurassic System - Abstracts

References M. 2012. Sedimentologicat · palynological, and KORTE, C. & Ko R, W. 2011. Bio- and chemostratigraphic geochemical studies ofthe terrestrial Triassic-jurassic zu assessment of carbon isotope records across boundary in north-western Poland. - Geological the Triassic-jurassic boundary at Csovar quarry Magazine 149: 308-332. (Hungary) and Kendlbachgraben(Austria) and RUHL, M., BONIS, R.N., REICHART, G.J., SINNINGHE DAMSTE, implications for global correlations. - Bulletin of the j.S. & KORSCHNER, W. M. 2011. Atmospheric carbon Geological Society of Denmark 59: 101-115 injection linked to end-Triassic mass extinction. - PIENKOWSKI, G., NIEDZWIEDZKI, G. & WAKSMUNDZKA, Science 333: 430-434. 9th International Congress on the jurassic System - Abstracts 147

New high-resolution geochemistry of Sinemurian marine sections in British Columbia and Nevada

2 l SARAH J. PORTER1• *, PAUL L. SMITH1, ANDREW H. CARUTHERS1, PENGFEI Hau , DARREN R. GR{kKE2 & DAVID SELBY2

1Department of Earth, Ocean and Atmospheric Sciences, University of British Columbia, Va ncouver V6T 1Z4, Canada; E-mail: [email protected]; [email protected]; [email protected]; [email protected] 2Department of Earth Sciences, Durham University, Sciences Laboratories, Durham DH1 3LE, UK; E-mail: d. [email protected]; [email protected]

*Corresponding author

Understanding marine depositional values at FCDI remaining relatively continuous environments throughout geological time at - -25 to -26 per mil, contrasting with those allows us to evaluate past changes in ocean at LCII that shiftgradually from - -27 per mil to chemistry. Using powerful geochemical tools -24 per mil. Further, the gradual positive trend such as carbon and osmium (Os) isotopes, observed at LCII corresponds to a comparable we are able to trace temporal alterations in and coeval positive shiftseen in shales in Dorset, . the balance of inputs to the global oceans. As UK (JENKYNS & WEEDON 2013) This suggests such, significant input from meteorite impact, that the LCII sediments record a potentially continental weathering and mantle-derived global carbon isotope signal at this time that fluxes can be identified and distinguished (e.g., may reflect an increase in global ocean primary

COHEN et al. 1999; PEUCKER-EHRENBRINK & productivity. Why, then, is this signal not also RAVIZZA 2000). observed at FCD? Using Os isotopes we are able This study focuses on two Sinemurian to quantitatively demonstrate that both sections

( -199.8 - 190.3 Ma; GRADSTEIN et al. 2012) were deposited under contrasting depositional marine sites from North America: Five Card conditions (open ocean vs. partially restricted Draw (FCD), Nevada, USA and Last Creek (LC), with significant input from continental British Columbia, Canada. At each location, weathering), and further, that this is what is two stratigraphic sections were sampled and likely to have dictated the differences observed analysed. Our first Five Card Draw section between the two carbon isotope profiles. (FCDI) spans -110 m of the Sinemurian from the

Involutum Zone through to the Harbledownense References Zone. Five Card Draw is the type section for the COHEN, A.S., COE, A.L., BARTLETT, J.M. & HAWKESWORTH, C.J. North American Sinemurian zonation scheme 1999. Precise Re-Os ages of organic-rich mudrocks (TAYLOR et al. 2001), and following thorough and the Os isotope composition ofJurassic seawater.­ Earth and Planetary Science Letters 167: 159-173. biostratigraphic correlation with this site, GRADSTEIN, F.M., 0GG, J.G., SCHMITZ, M.D. & 0GG, G.M. the chosen study areas are ideally suited for 2012. The Geological Time Scale 2012. Elsevier BV. geochemical analysis and comparison. Amsterdam. Herein we present high-resolution carbon jENKYNS, H.C. & WEEDON, G.P. 2013. Chemostratigraphy (CaC0 , TOC, 613C ) of Sinemurian (Lower Jurassh.:) isotope data and rhenium-osmium (Re­ 3 org black shales from the Wessex Basin, Dorset and Os) data from these sections, with a view palaeoenvironmental implications. - Newsletters on to understanding seawater chemistry and Stratigraphy 46: 1-21. environments of deposition during this stage of PEUCKER-EHRENBRINK, B. & RAVIZZA, G. 2000. The marine the Jurassic. Of particular interest are sections osmium isotope record. - Terra Nova 12: 205-219. TAYLOR, D.G., GUEX, J. & RAKUS, M. 2001. Hettangian and FCDI and LCII within the upper Leslei Zone. At Sinemurian ammonoid zonation for the Western this level, both sections exhibit significantly Cordillera of North America. - Bulletin de la Societe different carbon isotope profiles, with li13C vaudoise des sciences naturelles 87: 381-421. 148 9th International Congress on the Jurassic System - Abstracts

An overview of Upper Gondwana fossil floral assemblages of the Kachchh Basin, India

NEERU PRAKASH

Birbal Sahni Institute ofPalaeobotan� 53, UniversityRoad , Lucknow,In dia; E-mail: neerup_in@yahoo. eo m

Kachchh is a pericratonic and pericontinental Bryophytes: Represented by sterile thallus e.g., rift basin. The Mesozoic sedimentary horizons Thallites, Hepaticites. owe their formation to riftingalong the major Pteridophytes: Represented by Isoetites, Precambrian lineaments in the western India Sellaginellites, Phlebopteris, Matonidium, - East Africa divergent plate region prior to Coniopteris, Cladophlebis, Gleichenites, fragmentation of the Gondwana Superplate Hausmannia, and Dictyophyllum. (KRISHNA 1987). The thick stratigraphic Pteridosperms: Sterile leafs of Pachypteris and succession is well developed and floristically Sagenopteris; the fruit Caytonia. rich. These successions have been categorized Bennettitales: Sterile leaves; e.g., Ptilophyllum, on the basis of lithology, stratigraphy, and Pterophyllum, Anomozamites, Ctenozamites, palaeontological records into the Jhurio, Pseudoctenis, Nilssoniopteris, Otozamites, ? Jumara, Jhuran, and Bhuj fo rmations, their Bucklandia, as well as Williamsonia flower age ranging from Bathonian to Albian (BISWAS and bract scale, Cy cadolepis. 1971, 1999). Cycads: Sterile leaves showing variations in The complete Upper Gondwana succession shape and size are recorded by genera such is exposed in the Mainland, whereas the older as Cy cadites and Ta eniopteris. Mesozoic succession (Bathonian to Callovian) Conifers: Represented by abundant sterile is exposed in the northern 'Island belt' as well twigs of Pagiophyllum, Brachyphyllum, as in eastern Kachchh (Washtawa/Khandir Elatocladus, Allo.cladus and cone scales of Formation and Wagad sandstone; BISWAS & Araucarites. DESPANDE 1983). The Bhuj Formation lies Cone: Conites. directly on the Katrol beds with apparent conformity and is exposed near Bhuj. It In addition to these, some unclassified comprises ferruginous coarse sandstone, white forms such as Ka chchhia, Rajmahalia, and sandstone with interlaminated sandy shale, Lorumfo rmophyllum are reported. while fi nely mottled pink, red, white, and yellow The fossil flora from Kachchh exhibit two coloured beds are cross-bedded and friable. types of floral assemblages within the basin: The extraordinarily well preserved, rich and Ty pe-1 flora is dominated by a number of diversified palaeofloral assemblage is recorded species ofthe genus Pachypteris along with other from strata exposed in various localities around plant groups: the Pteridophytes Cladophlebis, Linguifolium, Sagenopteris colpodes, Bhuj and the Bhuj-Lakhpat road (BasE & cf. species BANERJI 1984) . The fossils are preserved in of Ta eniopteris (Pentoxylalae), Nilssoniopteris, form of impressions and compressionsand Pterophyllum, Otozamites, Ptilophyllum, show excellent morphological and anatomical (Bennettitales), Elatocladus, Pagiophyllum, and details. The presentation illustrates a typical Brachyphyllum (conifers). (The taxa have been Upper Gondwana flora consisting of various recorded from Rudra Mata dam site, Chawad, plant groups such as bryophytes, pteridophytes, Gadsisa, and Kakadbhit, representing the Jhuran pteridosperms, cycads, Bennettitales, and Formation). conifers. Its diversity and composition is Ty pe-2 flora is dominated by Ptilophyllum compared with contemporaneous deposits of along with conifer remains such as India and other Gondwana continents. The flora Brachyphyllum, Pagiophyllum, and Allocladus. comprises thalli, fronds, leafy twigs, and cone The genus Isoetites is also commonly recorded scales. The following floral elements have been from here (forms recorded from Trambau, fo und: Sukhpur, Bhajodi, and Dharesi represent the 9th International Congress on the Jurassic System -Abstracts 1 49

Bhuj Formation). during Jurassic times, the floralsimilar ities are The overall fossil floral assemblage is strong mostly at the generic and in some cases dominated by Cycadales and conifers and shows even at the species level (McLoUGHLIN & POTT close affiliation with the flora reportedfrom the 2009).

Jabalpur Formation. However, Bennettitales References are commonly known and dominant in one of BISWAS, S.K. 1971 Note on Geology of Kutch. Quarterly the two types of floral assemblage reported Journal of the Geological. - Mining and Metallurgical from the Rajmahal Formation of Rajmahal Hills Society of India 43: 223-235. BISWAS, S.K. 1999. Review on the evolution of rift basins with rare conifers, while the other type of flora in India during Gondwana with special reference represented by dominant conifers followed by to western Indian basins and their hydrocarbon pteridophytes and Pentoxylales with extremely prospects. - Proceedings of the Indian National rare bennettitalean remains has been reported Science Academy 65: 261-283. from Nipania of the Rajmahal Hills, Jharkhand. BISWAS, S.K. & DESPANDE, S.V. 1983 Geology and hydrocarbon prospects of Kutch, Saurashtra and The phytogeographical correlation with Narmada basins. In: BHANDARI, L.L. et al. (eds.), contemporaneous floral assemblages of Petroliferous basins of India: 111-126. Western Australia and Antarctica suggests its KRISHNA, J. 1987. An overview of the Mesozoic stratigraphy floral affinity at the generic level. Due to close of Kachchh and Jaisalmer Basins. - Journal of the Palaeontological Society of India 32: 136-149. the juxtaposition and contiguous position of McLouGHLIN, S. & Porr, C. 2009. The Jurassic flora Western Australia with the northern extension of Western Australia. - Geologiska Foreningen of the Indian subcontinent or greater India Stockholm Forhandlingar 131: 113-136. 150 9th International Congress on the Jurassic System - Abstracts

When did the twain meet? The epeiric Ethiopian Gulf with the Western Indian era ton; Coccoliths, the beacon of light!

}YOTSANA RAI

Birbal Sahni Institute ofPalaeobotany,53 UniversityRoad , 226007, Luckno""India; E-mail:]yotsana@ yahoo.com

The Kachchh Basin is a sedimentary basin tentatively suggests an upward extension of situated on the southwestern fringe of India the age into the latest Toarcian ( -175.6 Ma) for and is fo rmed during Early-Middle Jurassic these earliest Kachchh sediments. Reworked times by the southern extension of the N eo­ nannofossils of Early Jurassic age (Pliensbachian Tethys at a palaeolatitude of 33°S. Aftera phase - Toarcian ) are consistently fo und in Callovian of terrestrial sedimentation in the Late Triassic, - Oxfordian age nannofossil assemblages marine sedimentation started during Early at Jara, Jumara, and Habo domes and in the

Jurassic time. The oldest marine sedimentary Wagad Uplift (RAI & }AIN submitted). Though rocks called Kaladongar Formation are exposed the provenance has not yet been recovered, it in Kuar Bet of the Pachchham Island. The lowest is envisaged that both the global eustatic sea­ unit of the Kaladongar Formation, called Dingi level rise and local tectonics are responsible for Hill Member,has for the first time been precisely this Pliensbachian-Toarcian boundary interval dated by a moderately diversified and well inundation of the Kachchh Basin (RAI & }AIN preserved calcareous nannofossil assemblage. 2012). The assemblage includes marker species of Biscutum fi nchii, Bussonius prinsii, Crucirhabdus primulus and Discorhabdus criotus straddling References PANDEY, D.K., LATHUILIERE, B., FURSICH, F.T. & KULDEEP, S. the Pliensbachian-Toarcian interval boundary 2002. The oldest cyathophorid coral (Scleractinia) (NJS to NJ7). This nannofossil find suggests from siliciclastic environments of the Kachchh Basin, that after the rifting of the western margin of .western India. - PaHiontologische Zeitschrift 76: 347- the Indian plate, the first epeiric transgressive 356. PANDEY, B., PATHAK, D.B. & KRISHNA, ). 2013. Ca/liphyl/oceras event via an arm of the southern Tethys known heterophylloides (Oppel, 1856) from the basal most as the Ethiopian Gulf in the Kachchh Basin )urassic succession of Sadhara Dome, Kachchh, India. occurred during the Pliensbachian-Toarcian - Journal of the Palaeontological Society of India 58: boundary interval (at 183 Ma), ea. -11.4million 61-65. ). & )AIN, S. 2012. Early Jurassic Gondwanaland breakup years earlier than the ammonite-based RA.I, - a nannofossil story. National Level Field based (Calliphylloceras heterophylloides) Early Workshop on GeologyofKachchh Basin, western India: Bajocian or older ( -171.6 Ma) record by PANDEY Present status and Future perspectives. Abstracts: 84- et al. (2013) and the ?Early Bajocian ( -171.6 85, Department of Earth and Environmental Science, Ma) coral-based record (the Amphiastraea­ KSKV Kachchh University, Bhuj. RAI, J. & )AIN, S. submitted. Pliensbachian nannofossil Isastraea assemblage) by PANDEY et al. (2002). assemblage from Kachchh: Implications on the The record of Lotharingius sp. and Triscutum earliest Jurassic transgressive event on the western sullivanii within the present assemblage also Indian margin. - Zitteliana. 9th International Congress on the Jurassic System - Abstracts 151

Integrated nannofossil-dinoflagellate cyst - ammonoid biostratigraphy from Wagad area, Kachchh, Western India

}YOTSANA RAI\ SURABHI GARG\ MRIDUL GUPTA\ ABHA SINGH\ DHIRENDRA K. PANDEY2 & RA.HUL GARG1

1Birbal Sahni Institute of Palaeobotany, 53, UniversityRoad , Lucknow, India 2Geology Department, Universityof Rajasthan, ]aipur,India

The entire Kachchh Basin is marked by six Diazomatolithus lehmanii, Discorhabdus major uplifts one of them being Wagad. The corollatus, D. criotus, D. striatus, D. ig notus, Wagad upliftis bounded by a high angle normal Ethmorhabdus gallicus, Hexapodorhabdus fault to its south, while all the other uplifts are cuvilleri, Lotharingius vellatus, L. crucicentralis, bounded by either high angle faults or flexure L. barozii, L. haufi i, Octopodorhabdus zones to their north. decussatus, 0. praevisus, Podorhabdus grassei, The Wagad region is stratigraphically Retecapsa octofenestrata, Staurolithites lumina, divided into the Washtawa, Kanthkot, and Stephanolithion bigotii, S. speciosum octum, S. Gamdau formations in ascending order. The hexum, Triscutum beaminsterense, T. sulliviani, Kanthkot Formation is further dividedinto three T. tiziense, T. expansum, Tubirhabdus patulus, members, the lower Patasar Shale Member, the Umbria granulosa, Wa tznaueria britannica, W. middle Fort Sandstone Member,and the upper barnesae, W. manivitiae, and Zeugorhabdotus Adhoi Member.The type section of the Patasar erectus. Crucirhabdus primulus, Magaganella Shale Member is exposed near the Patasar tank protensa, Diductiusconstans, and Parhabdolithus in western Wagad. It is from this locality that liasicus recorded with the assemblage are calcareous nannofossil and dinoflagellate data considered as reworked Early Jurassic are presented herein. The shales occur above nannofossils. the datable fossiliferous Kantkote Ammonite The presence of L. velatus in older PTS-2 Beds of the upper Washtawa Formation and and PTS-3, L. crucicentralis in PTS-3, and C. below the unfossiliferous sandstones of the Fort perforata in PTS-5 suggests a Late Oxfordian - Sandstone Member. There is a gradual increase Early Kimmeridgian age for the assemblage, the in the thickness of the Patasar Shale Member boundary between the two stages lying most from East to West (DESAI & MERH 1975). likely in sample PTS-4. Stephanolithion bigotii At Patasar tank apparently barren exposures bigotii is found throughout the section. Patasar of Patasar shales are exposed as cliff section Shale samples have also yielded a rich and well comprising more than 50 m. They are grey to preserved dinoflagellate cyst assemblage. The dark grey in colour,soft , gypsiferous in the lower occurrence of Aldorfi a dictyota, Dingodinium part and greenish grey to khaki, silty in the upper jurassicum, D. tuberosum, Endoscrinium luridum, part. The upper part is often marked by flaggy, Gonyaulacysta jurassica, Prolixosphaeridium yellowish brown siltstone alternations. These capitatum, Rigaudella aemula, Scriniodinium shales are continuously exposed eastward crystallinum and Tubotuberella apatela attests a towards Nara, where the upper part gradually Late Oxfordian- Early Kimmeridgian age fo r the grades into friable sandstones. Patasar shales at Patasar tank. The assemblage In all, 12 representative samples (denoted shows affinity with both Boreal and Austral as PTS) were collected, out of which six (PTS-2, dinoflagellate cyst assemblages. However, PTS-3, PTS-4, PTS-5, PTS-11, and PTS-12) the ammonite data suggests that the Patasar were productive and contain a highly diverse, Shale Member questionably belongs to the moderately preserved nannofossil assemblage. ?Grossouvrei Subzone of the Upper Bifurcatus The assemblage contains Axopodorhabdus Zone of Middle Oxfordian age on the basis of cy lindratus, Biscutum dubium, B. dorsetensis, a single specimen of Perisphinctes cf. besairiei B. novum, Cretarhabdus conicus, Crepidolithus (PANDEY et al. 2012). perforata, Cy clagelosphaera margerelli, 152 9thInternational Congress on the Jurassic System - Abstracts

References 322. DESAI, G. & MERH, S.S. 1975. Western Wagad Mesozoic PANDEY, D.K., ALBERTI, M. & FURSICH,F.T. 2012. Ammonites sediments and their depositional environments. of the genus Perisphinctes W GEN, 1869 from the AA - Symposium on Sediment, Sedimentation & Oxfordian of Kachchh, western India. - Revue de Sedimentary Environment, University of Delhi: 313- Pah�obiologie 31: 483-587. 153 9th International Congress on the Jurassic System - Abstracts

Nannofossil biostratigraphy of the Chari Formation, Jumara Dome, Kachchh, western India

RAI1, 2 }YOTSANA MRIDUL GUPTA1, SURABHI GARG\ ABHA SINGH\ SREEPAT }AIN & DHIRENDRA K. PANDEY3

1Birbal Sahni Institute ofPalaeobota� 53, UniversityRoad , Lucknow- 226007, India; E-mail:]yotsana_ [email protected] 2DG-2, Flat no. 51[, SFS Flats, Vikaspuri, New Delhi-110018 3 Department of Geology, University of Rajasthan, ]aipur

The Kachchh Basin, situated on the western sandy shales underlying the Dhosa Oolite. margin of the Indian plate, was formed in the The Bathonian assemblage recovered Late Triassic following the rifting between from the Jhurio Formation is represented by India and Africa. Lithostratigraphically, the Axopodorhabdus cy lindratus, Cy clagelosphaera Jurassic rocks of the basin are classified into margerelii, Calyculus sp., Diazomatolithus Patcham, Chari, Katrol, and Umia fo rmations (in lehmanii, Discorhabdus criotus, Ethmorhabdus ascending order; WAAGEN 1873-75) and were gal/icus, Ca rinolithus magharensis, Lotharingius subsequently redesignated by BISWAS (1977) haufi i, L. crucicentra/is, L. sigil/atus, L. velatus, as Jhurio, Jumara, Jhuran, and Bhuj fo rmations, Octopodorhabdus deccusatus, Staurolithites respectively, with details of stratigraphic type sp., Wa tznaueria barnesae, W. britannica, W. sections. The boundaries between these two manivitae, and Zeugorhabdotus erectus. The lithostratigrahic schemes are the same fo r the presence of W. manivitae (FAD marks the base first three formations but the boundaries bf of NJ 10= Lower Bajocian) and Ca rinolithus the Katrol-Umia and Jhuran-Bhuj formations magharensis [LAD marks Middle Bathonian= differ. Among different domal exposures in the NJ 11 (part)] suggests an age of the upper part Kachchh mainland, the Jumara Dome (N 23°40', of the Jhurio Formation straddling between E 69°06') is the type section of the Jumara the Lower Bajocian and Middle Bathonian

Formation of BISWAS (1977), located nearly (MATTIOLI & ERBA 1999). Ammonite data have 80 km NW of Bhuj. The Jurassic succession also suggested a Middle Bathonian age fo r the exposed at the Jumara Dome belongs mainly to lowest sediments exposed in the Jumara Dome the Jhurio, Patcham, Chari (Jumara) and Katrol (JAIN 1995, 2002; }AIN & PANDEY 2000). (Jhuran) fo rmations (FURSICH et al 2001). The Callovian-age nannofossil assemblage The Middle Jurassic marine succession of includes Anfra ctus harrisonii, Ansulasphaera Kachchh is globally known for its abundant helvetica,Axopodorhabdus atavus,A. cy lindratus, datable macro- as well as microfossils. In this Biscutum depravatus, B. dorsentensis, B. study an attempt is made to date the Jhurio, dubium, B. fi nchii, B. grande, B. novum, B. Patcham and Chari fo rmations rocks in the profundum, B. striatum, Bussonius leufensis, Jumara Dome by their calcareous nannofossil Carinolithus magharensis, Crepidolithus crassus, assemblages. In all, 17 samples were collected C. granulatus, C. perforata, C. pleinsbachensis, out of which 15 (nine from the Jumara and Cretarhabdus conicus, Crucirhabdus primulus, six from the Jhurio and Patcham fo rmations) Cy clagelosphaera margerelii, · Diazomatolithus were found productive. The Chari Formation lehmanii, Discorhabdus criotus, Discorhabdus is capped by the Dhosa Oolite Member corollatus, D. ig notus, D. striatus, Diductius (constituting several bands), an important constans, Ethmorhabdus gal/icus, Fa viconus marker bed. The calcareous nannofossil multicolumnatus, Hexapodorhabdus cuvillieri, assemblage at Jumara is well diversified and Lotharingiuscontractus,L.crucicentralis,L.haufi i, moderately preserved with pronounced etching L. sigillatus, L. velatus, Magaganella protensa, in Bathonian-age nannofossils of the Jhurio and Mitrolithuselegans,Octopodorhabdusdeccusatus, Patcham formations as well as the Oxfordian­ 0. praevisus, Podorhabdus grassei, Pseudoconus age nannofossils recovered from calcareous enigma, Parhabdolithus liasicus, Perissocydus 154 9th International Congress on the Jurassic System - Abstracts noeliae, Retecapsa incompta, R. schizobrachiata, Mesozoic. Newsletters on Stratigraphy 20: 91-114. Rhagodiscus nebulosus, Schizosphaeralla FURSICH, F. T., PANDEY, D.K., CALLOMON, J. H. JAITLY, A. K. & SINGH, I. B. 2001. Marker beds in the Jurassic of the punctulata, Stephanolithion bigotii bigotii, Kachchh Basin, western India: their depositional S. hexum, S. speciosum octum, Staurolithites environment and sequence-stratigraphic significance. lumina, S. quadriarculla, S. stradneri, - Journal of The Palaeontological Society of India 46: Similiscutum orbiculus, Th urmannolithion 176-198. c/aratum, Triscutum beaminsterensis, T. JAIN, S. 1995. Biostratigraphical and paleoecological studies of Middle Jurassic (Upper Bathonian-Lower sullivanii, T. tiziense, Tubirhabdus patulus, Callovian) beds exposed in Jumara Dome, Kachchh, Umbria granulosa, Wa tznaueria barnesae, Western India. - Unpublished Thesis, 202 pp. W. britannica, W. contractu, W. manivitae, W. JAIN, S. 2002. Middle Jurassic ammonite biozonation ovata, Zeugorhabdotus erectus, and Z. fluxus. in western India: Global implications. - Geological Society of America, Annual Meeting, Colorado. Paper The presence of Ansulasphaera helvetica, C. No. 141-10, 34. perforata, Cretarhabdus conicus, D. striatus, )AIN, S. & PANDEY, D.K. 2000. Middle Jurassic ammonite Faviconus multicolumnatus, L. crucicentralis, biozonation in Kachchh, western India. - Bulletin of Stephanolithion bigotii bigotii, S. hexum, and the Indian Geologists Association 33: 1-12. MATTIOLI, E. & ERBA, E. 1999. Synthesis of calcareous S. speciosum octum constricts the Jumara nannofossil events in Tethyan Lower and Middle Formation up to the first band of the Dhosa Jurassic successions. - Rivista Italiana di Paleontologia Oolite to the NJ13 NF Zone ofBowN et al. (1988) et Stratigrafia 105: 343-376. of the Middle to latest Callovian. RAI, j. 2006. Reworked Pliensbachian-Aalenian Additionally, as elsewhere (RAJ 2006, 2007; nannofossils from Jara Dome, Kutch: Early Jurassic palaeobiogeography of western India. - In: Xlth RAI & }AIN 2012), some Early Jurassic reworked International Nannoplankton Association, Nebraska, forms of Crepidolithus pliensbachensis, U.S.A.: 84-85. Mitrolithus elegans, Parhabdolithus /iasicus, RAI, J. 2007. Early Jurassic calcareous nannofossils from Triscutum sullivanii, and T. tiziense are also Patcham Island, Kutch, western India. - In: XXIth Indian Colloquium on Micropalaeontology and recorded in the Bathonian-Oxfordian succession Stratigraphy, Nov. 16-17, 2007, B.S.I.P., Lucknow: 143. ofJumara. RAI, J. & JAIN S. 2012. Early Jurassic Gondwanaland breakup - a nannofossil story. - DST Sponsored Field Workshop and Brainstorming Session on 'Geology References , of Kachchh Basin, Western India: Present Status and BISWAS, S.K. 1977. Mesozoic rock-stratigraphy of Kutch, Future Perspectives', 26th to 29th January 2012, Gujarat. - Quarterly Journal of the Geological Kachchh University, Bhuj, Kachchh (Abstract). Mineralogical and Metallurgical Society of India 49 WAAGEN, W. 1873-75. Jurassic fa una of Kutch. The (3-4): 1-51. Cephalopoda. - Memoirs of the Geological Survey BOWN, P. R., COOPER, M.K.E & LORD, A.R. 1988. A calcareous of India. Palaeontologica Indica, New Series 9 (1-4): nannofossil biozonation scheme for the Early to Mid 1-247. 9th International Congress on the Jurassic System - Abstracts 155

Middle-Jurassic age calcareous nannofossils from Habo Dome, Kachchh, western India

RAil, *, }YOTSANA S. J. PATEL2, ABHA SINGH1 MRIDUL GUPTA\ SURABHI GARG1, BISWAJEET THAKUR1 & HITENDRA SHUKLA3

1Department of Microplankton, Birbal Sahni Institute of Palaeobotany, 53, UniversityRoad , Lucknow- 226007, India; E-mail: jy [email protected] 2Department of Geology, M.S. Universityof Baroda, vadodara- 390 002, India 3 Department of Geology, Bundelkhand University,]hansi , India

*Corresponding author

Habo Dome, the biggest inlier domal structure fo ssils. At certain levels conglomerates, shell (ea. 320 m in height) is situated in the northern beds, and coral fragments are seen. Abundant Mainland of Kachchh. The geographical extent traces (Laevicyclus, Fucopsis, Sponge/iomorpha, of the Habo Hill is roughly elliptical (E-W 16 Ophiomorpha, Rhizocorallium, Halymenidium km, N-S 6 km). The rugged topography with its etc.) are observed (PATEL et al. 2008). Above the highest peaks is situated roughly on the longer sandstone thick grey shale is capped by thin, axis of the hill. The southern slopes are flat, prominent, hard, fo ssiliferous oolitic limestone gentle, extensive and monotonous, whereas the bands (sandy oo-micrites), called 'Dhosa northern ones are steep and short. Oolite member; it is the best marker bed in the The Mesozoic rocks exposed in Habo Dome Kachchh Basin. The member consists of three to are Bathonian to Kimmeridgian in age and fo ur hard bands, rich in megafossils especially have been divided into Patcham, Jumara, and ammonoids (Perisphinctes (Arisphinctes) cf. Jhuran fo rmations (BISWAS 1977; FURSICH colei, Perisphinctes (A.) aff. cotovuiformis, et al. 2001). In Habo Dome the upper part of Perisphinctes (A.) kheraensis, Perisphinctes (A.) cf. the Patcham Formation crops out only at one trifidus), belemnites, brachiopods, gastropods, place in the northern flank of the hill, south and bivalves. The topmost layer of the Dhosa of Dhrang Village. In Habo hill the maximum Oolite is an intraformational conglomerate and thickness of the exposed upper part of Pateham contains both reworked pebbles and boulders Formation is ea. 16.6 m, and it consists of thinly of oolitic limestone with abundant large-sized bedded yellowish brown, black and dirty white reworked ammonites and belemnites (ALBERTI limestone interbedded with thin calcareous et al. 2011, 2013). shales. The black limestone is bioturbated and The samples collected from the Patcham, contains abundant Chondrites and resting traces Jumara and Jhuran fo mations of the Habo (Lockeia; PATEL et al. 2008). Dome were analysed fo r calcareous nannofossil The Patcham Formation is conformably productivity. The nannofossil assemblages are overlain by the thick argillaceous J umara ( Chari) well diversified and moderately preserved. Formation. The fo rmation is exposed on the Samples from the Patcham Formation in the core periphery of inliers. Being soft, it usually gives of the Dome have yielded Wa tznaueria barnesae, rise to a greenish-grey undulating landscape of W. britannica, Cy clagelosphaera margerelii, low relief and hard bands occasionally fo rming Lothringuis contractus, Discorhabdus striatus, cuestas. The fo rmation is characterized by and L. velatus. The assemblage is dated Upper monotonous olive-grey, gypsiferous, laminated Bathonian-Lower Callovian in age (Fig.1). shales with thin, red fe rruginous bands, The Jumara Formation has yielded alternating beds of limestone, and occasional well preserved and moderately diversified sandstone inter-beds. The middle part ofJumara nannofossil assemblages. The assemblage Formation consists of three to four thick bands contains Crepidolithus perforata, Cretarhabdus ofsand stone. This unit is characterized by planar conicus, Cy clagelosphaera margerelii, and trough cross -lamination withabundanttrace Diazmatolithus lehmanni, Discorhabdus 156 9th International Congress on the Jurassic System - Abstracts

� C') m

z D) :::J :::J Sample 0 0' en I riV;> 0 ''""'"'"""

0 ga/1/cus 0 ;tJ )> r::. I Genus sp. indet Lotharinglus contractus

n I I Lotharingius 0 0 !i )> 0 0 ..,.. ·� ,. I

:sp. nlnntll hinniU

Triscutum

Trlscutum expansus

Trl scutum sp. Trl scutum su/1/vani/

;tJ 0 0 )> 0 )> )> )> )> )>

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,3:I :I: CALLOVIAN OXFORDIAN � 0 I ::0 Z ! � �

Fig.1. Composite chart showing litholog, nannofossil assemblage and nannofossil events recorded in Habo dome. 9th International Congress on the Jurassic System - Abstracts 157 striatus, Ethmorhabdus gallicus, Fa viconus serve as standard fo r the Indo-Pacific province. multicolumnatus, Lotharinguis contractus, Identification ofmarker taxa (both cosmopolitan L. crucicentralis, L. sigillatus, Stradnarlithus and substitute) and assignment to nanno-zones sp., Stephanolothion bigotii, Stephanolithion due to diachronous nature of some markers in sp., Triscutum expanses, Tubirhabdus patulus, various zonal schemes are taken into account Wa tznaueria barnesae, W. britannica, (BRALOWER et al. 1989; DE KAENEL & BERGEN Zegrhabdutus erectus, Z. fluxus. & and In various 1996; BOWN COOPER 1998; MATTIOLI & ERBA zonation schemes the presence of Lotharinguis 1999). crucicentralis (LAD indicates base ofNJ 15a of the

Middle Oxfordian (DE KAENEL & BERGEN 1996) References to NJ 15b of Late Oxfordian (BowN et al. 1988), ALBERTI, MATTHIAS, FURSICH, FRANZ T. & PANDEY, Stephanolothion bigotii bigotii (FAD is from the DHIRENDRA K. 2013. Deciphering condensed upper part of the Lower Callovian), Crepidolithus sequences: A case study from the Oxfordian (Upper Jurassic) Dhosa Oolite member of the Kachchh Basin, perforata (range Lower Callovian to Lower western India. - Sedimentology 60 (2): 574-598 Volgian fide BowN 1998) and Discorhabdus ALBERTI, M., PANDEY, DHIRENDRA .K. & FURSICH, F.T. 2011. striatus (LAD NJ 15a Middle Oxfordian; BowN Ammonites of the genus Peltoceratoides SPATH, 1924 1998) and FAD of F. multicolumnatus (= base of from the Oxfordian ofKachchh, western India. - Neues NJ 15b of Upper Oxfordian; BowN 1998). Thus Jahrbuch fiir Geologie und PaHiontologie 262: 1-18. BISWAS, S.K. 1977. Mesozoic rock-stratigraphy of Kutch, the samples from Upper Jumara Formation Gujarat. - Quarterly Journal of the Geological, underlying the Dhosa Oolite are dated Late Mineralogical and Metallurgical Society of India 49 Callovian-Oxfordian (Fig.1). (3-4): 1-51. Samples from the Jhuran Formation contain BowN, P. R. 1998. Calcareous nannofossil biostratigraphy., Staurolithites quadriarculla, Cretarhabdus British Micropalaeontological Society Publication Series: 315 pp., Chapman and Hall, Dordrecht. conicus, C. margerelii, W. britannica, W. BOWN, P. R. & COOPER, M.E.K. 1998. Jurassic. In: BOWN, P. R. barnesae, L. sigillatus, S. bigotii bigotii (LAD ( ed.), Calcareous nannofossil biostratigraphy. - British in NJ 16 of BowN et al. 1988 coinciding with Micropalaeontological Society Publication Series: 38- NJ 20A of BRALOWER et al. 1989 of Middle 85, Chapman and Hall, Dordrecht. BOWN, P. R., COOPER, M.K.E & LORD, A.R. 1988. A calcareous Tithonian age), and Triscutum beaminsterensis nannofossil biozonation scheme for the Early to Mid (LAD indicates upper Lower Kimmeridgian). Mesozoic. - Newsletters on Stratigraphy 20: 91-114. The age of the base of the Jhuran Formation BRALOWER, T., MONECHI, S. & THIERSTEIN, H.R. 1989. is thus constrained from the Divisum (NJ 15, Calcareous nannofossil zonation of the Jurassic­ Cretaceous boundary interval and correlations Upper Lower Kimmeridgian) to the Lower with the Geomagnetic Polarity Timescale. - Marine Fallauxi Tethyan ammonite Zone (NJ 20A Zone Micropalaeontology 14: 153-235. of BRALOWER et al. 1989, corresponding to the DE KAENEL, E. & BERGEN, J.A. 1996. Mesozoic calcareous Middle Upper Volgian NJ 16 Zone of BowN et al. nannofossil biostratigraphy from sites 897,899, 1988) (Fig.1). and 901, Iberia abyssal plain: new biostratigraphic evidence. - Proceedings of the Ocean Drilling Program, The abundance of Zegrhabdotus spp. (5 �m) Scientific Results 149: 27-59. usually increases in upwelling zones and is thus FURSICH, F. T., PANDEY, D.K., CALLOMON, J. H. JAITLY, A. K. & considered as a good palaeo-fertility indicator SINGH, I. B. 2001. Marker beds in the Jurassic of the (STREET & BowN 2000). These authors also Kachchh Basin, western India: their depositional environment and sequence-stratigraphic significance. suggested W. barnesae is abundant during - Journal of The Palaeontological Society of India 46: periods of more muddy deposition, while 176-198. Zegrhabdotus spp. is more common during MATTIOLI, E. & ERBA, E. 1999. Synthesis of calcareous carbonate deposition. nannofossil events in Tethyan Lower and Middle On the basis of limited nannofossil marker Jurassic successions. - Rivista italiana di Paleontologia e Stratigrafia 105: 343-376. taxa the Bathonian-Callovian, Callovian­ PATEL, S.J., DESAI, B.G., VA IDYA, A.D. & SHUKLA, R. 2008. Oxfordian, and the Oxfordian-Kimmeridgian Middle Jurassic trace fo ssils from Habo Dome, boundaries are delineated from the upper Mainland Kachchh, Western India. - Journal of the Patcham, Jumara, and lower Jhuran formations Geological Society of India 71: 345-362. STREET, C. & BOWN, P. R. 2000. Palaeobiogeography of exposed in Habo Dome. This nannofossil data is Early Cretaceous (Berriasian-Barremian) calcareous tagged with known ammonite data. Integrated nannoplankton. - Marine Micropaleontology 39: calcareous nannofossil-ammonite studies may 265-291. 158 9th International Congress on the Jurassic System - Abstracts

Continental Jurassic of peninsular India - A floristic and stratigraphic riddle

ANNAMRAJU RAJANIKANTH* & CHOPPARAPU CHINNAPPA

Birbal Sahni Institute ofPalaeobotany,53 UniversityRoad , Lucknow 226 007, India; E-mail: annamraj u [email protected]; [email protected]

*Corresponding author

Terrigenous facies of peninsular India, initiated Jharkhand/West Bengal) (see Figs 1 and 2) litho­ by a glacigenic episode and culminating units provide stratigraphic, phytogeographic, in a lithologic hiatus, is grouped under the and phytoevolutionary inferences. Gondwana Supergroup (VENKATACHAL et The present communication aims to re­ al. 1993). Post-Gondwana deposits, often evaluate plant fossil data and their limitations associated with Ptilophyllum Flora and at times for inferring an unequivocal age. An analysis of with marine intercalations, have been variously the macro-palaeobotanical evidence in the Kota assigned Early, Middle or Late Jurassic or Early succession reflects preponderance of conifers Cretaceous ages (FEISTMANTEL 1887; Fox 1931; fo llowed by pteridophytes and Bennettitales. SPATH 1933; ARKELL 1956; SASTRY et al. 1979; Pteridospermales, Cycadales, and Ginkgoales DATTA et al. 1983; BANERJI 1990; MITRA 1993; are poorly represented. These floral cornponen ts SEN GUPTA 1994; RAJANIKANTH et al. 2000; are closely comparable with floralevi dence from

LAKSHMINARAYANA 2002; VIJAYA & PRASAD Rajmahal (Early Cretaceous), which may suggest 2001; PANDEY & CHOUDHARY 2007; DUTTA the reassessment of its Jurassic age based on 2002; MUKHOPADHYAY et al. 2010). Subsequent Kota macro-plant evidence (RAJANIKANTH researches separated coastal 'Gondwana' & SUKH-DEV 1989). Micro-palaeobotanical litho-units from the purview of Gondwana evidence shows a dominance of pteridophytes n (PRASAD & PUNDIR 1999; RAJANIKANTH 2010). fo llowed by gym osperms and bryophytes. Age reassignments of the Rajmahal basalt (Me Moreover the age assignment ranges from

OOUGALL & McELHINNY 1970) opened a new early Jurassic to early Cretaceous (VIJAYA & paradigm of early Cretaceous floristics and PRASAD 2001).This long-ranging chronological litho-units comprising the Ptilophyllum Flora in both intra- and pericratonic sedimentary basins. DIS1'RIB1JnON OfNON-MARINE Thus the traditional Jurassic age connotation JURASSICLITHO tiNITS of the Ptilophyllum Flora (Upper Gondwana) shifted to the Early Cretaceous. This view is supported by a non-deposition phase (hiatus/ erosion) of Jurassic sediments in peninsular

India (VENKATACHALA & MAHESHWARI 1991). This created an uncertainty over the placing of non-marine Jurassic litho-units distributed in the Pranhita-GodavarijKrishna-Godavari, South Rewa, Jaisalmer, and Rajmahal basins. A reassessment of the floristic and stratigraphic evidence is required to understand the status of continental Jurassic in peninsular India. Macro­ and micro-palaeobotany of Kota (Pranhita­ Godavari/Krishna- Godavari, Maharashtra, Andhra Pradesh), Hartala/Bandhogarh (South Rewa, Madhya Pradesh), Lathi (Jaisalmer, Fig. 1. Showing geographic distribution of non marine Rajashtan) and Dubrajpur (Rajmahal, Bihar/ Jurassic litho-units in India. 9th International Congress on the Jurassic System - Abstracts 159

30 40 25 • PTP 30 20 • PTS •BRY • cvo 20 15 •BEN •PTP 10 • GNG 10 •GYM d • CON 0 5 ' ' .i ! Jl• 0 KOTA lATHI HARTALA>UBRAJPUR I MACROPALAEOBOTANY MICROPALAEOBOTANY Fig. 2. Distribution of macro-and micro-plant relics in non-marine Jurassic litho-units of India; Legend: BRY: Bryophytes, BEN: Bennettitales, CON: Coniferales, CYD: Cycadales, GNG: Ginkgoales, GYM: Gymnosperms, PTP: Pteridophytes, PTS: Pteridospermales.

inference negates the exact stratigraphic status Jurassic to early Cretaceous age (VIJAYA & Rov of the Kota succession. A critical reassessment 2000; TRIPATHI 2000). The later age connotation of lithologic and faunal data is suggested. seems rational since the assemblage zones are Moreover the extent of the Kota succession has comparable with other micro-palaeobotanical been extended from the intra-cratonic Pranhita­ evidence from various intra- and peri­ Godavari Basin to the peri-cratonic (coastal cratonic early Cretaceous basins. Macro- and 'Gondwana') Krishna-Godavari Basin, and an micropalaeobotanical evidencs found in J urassic unconformity with the overlying Gangapur "nd strata of continents adjoining India (Antarctica, Raghavapuram (Early Cretaceous) succession Australia, Africa), too, are subjected to age has been suggested. Both macro- and micro­ reassignments (JEFFERSON 1982; GEE 1987; HILL palaeobotanical evidence of these two units 1994; BOSE et al. 2000; PHILIPPE et al. 2004). are dated as early Cretaceous and the Kota The problem of continental Jurassic in India evidence, too, may signal an early Cretaceous should be reassessed in the light of occurrence age connotation. of cosmopolitan taxa (plant relicts) and wide Macro- and micro-palaeobotanical historical geographic distribution of faunal information of Hartala/Bandhogarh (South evidence and the possibility of facies variations Rewa) is poorly/hardly known and its age given a different chronological limitation. assessment is questionable (PAL 1984; SUKH­ DEV 1988). The Lathi Formation (Jaisalmer References Basin), represented by conifer wood taxa ARKELL, W.J. 1956. Jurassic Geology of the World. 806 p., Oliver and Byod Ltd., London. and Bennettitales, bears no stratigraphic BANERJI, J. 1990. Plant fossils from Dubrajpur Formation, affinity (BONDE 2010; SHARAM et al. 2002). Bihar and their significance in stratigraphy. - Micro-palaeobotanical data is suggestive of Palaeobotanist 38: 122-130. a dominance of gymnosperms followed by BoNDE, S.D. 2010. A new genus of podocarpaceous wood from the Lathi Formation (Early Jurassic) ofRajasthan, pteridophytes (SRIVASTAVA 1966). Further data India. - Geophytology 38:19-24. is needed for stratigraphic and age conclusions BOSE, M.N., TAYLOR, E.L. & TAYLOR, T. N. 1990. Gondwana (PANDEY & CHOWDHURY 2007). florasof India and Antarctica- a survey and appraisal. The Dubrajpur macro-palaeobotanical In: TAYLOR, T. N & TAYLOR, E.L. (eds.), Antarctic data consist of pteridophytes, Bennettitales, palaeobiology: its role in the reconstruction of Gondwana: 18-148, Springer, New York. Cycadales, pteridosperms, and conifers in DATTA, N.R., MITRA, N.D. & BANDYOPADHYAY, S.K. 1983. order of decreasing abundance (BANERJI Recent trends in the study of Gondwana basins of 1990). Significant floral components suggest peninsula and extra peninsula, India. - Petroleum an early Cretaceous affinity. Sub-surface micro­ Asia Journal 6: 9-169. DUTTA, P. 2002. Gondwana lithostratigraphy of peninsular palaeobotanical data, in contrast, exhibit India. Gondwana Research 5: 540-553. a dominance of pteridophytes followed by FEISTMANTEL, 0. 1879. Upper Gondwana flora of the gymnosperms and bryophytes and suggest a outliers on the Madras coast. - Palaentologia lndica 160 9th International Congress on the Jurassic System - Abstracts

1: 202-234. RAJANIKANTH, A. 2010. Status of coastal Gondwana - A Fox, C.S. 1931. The Gondwana system and its related fl oristic perspective. In: JAYAPPA, K.S. & NARAYANA, fo rmations. - Memoirs, Geological Survey of India 58: A. C. ( eds.), Coastal environments problems and 1-241. perspectives: 264-276, IK International Publishing GEE, C.T. 1987. Revision of the early Cretaceous flora from House. Hope Bay, Antarctica. XIV International Botanical RAJANIKANTH, A., VENKATACHALA, B.S. & ASHOK, K. 2000. Congress, Berlin, West Germany, Abstracts: 333. Geological age of the Ptilophyllum Flora - A critical HILL, R.S. ( ed.) 1994. History of the Australian vegetation: reassessment. - Memoirs of the Geological Society of Cretaceous to Recent. 433 p., Cambridge University India 46: 245-256. Press, Cambridge. SASTRY, M.V.A., ACHARYA, S.K., SHAH, S.C., SATSANGI, P. P., JEFFERSON, T. H. 1982. Fossil fo rests from the lower GHOSH, S.C. & SINGH, G. 1979. Classification of Indian Cretaceous of Alexander Island, Antarctica. - Gondwaa sequence: A reappraisal. - IV International Palaeontology 30: 233-249. Gondwana Symposium, India, Geological Survey of LAKSHMINARAYANA, G. 2002. Evolution in basin fill style India 2: 502-507. during the Mesozoic Gondwana continental breakup SEN GUPTA. 1994. Does continental Jurassic sequence occur in the Godavari Triple Junction- SE India. - Gondwana in India. - Proceedings, 9th Gondwana Symposium, Research 5: 227-244. Hyderabad 1: 299-309 Me DOUGALL, I. & Me ELHINNY, M.W. 1970. The Rajmahal SHARMA, B.O. & TRIPATHI, R.P. 2002. Petrified conifer traps of India - K-Ar ages and palaeomagnetism. - woods from Lathi Formation (Jurassic), Rajasthan, Earth and Planetary Science Letters 9: 371-378. India. - Geophytology 30: 27-30. MUKHOPADHYAY, G., MUKHOPADHYAY, S.K., ROYCHOWDHURY, SPATH, L.F. 1933. Revisions of the Jurassic cephalopod M. & PARUI, P. K. 2010. Stratigraphic correlation fauna of Kutch. - Memoir of the Geological Survey of between different Gondwana basins of India. - Journal India, Palaeontologia lndica 9: 659-945. ofthe Geological Society of India 76: 251-266. SRIVASTAVA, S.K. 1966. Jurassic microflorafro m Rajasthan, PAL, P. K. 1984. Fragmentary plant remains from the India. - Micropalaeontology 12: 87-103. Hartala Hill, South Rewa Gondwana Basin, India. - SUKH-DEv 1988. Floristic zones in the Mesozoic fo rmations Palaeobotanist 32: 126-129. and their relative age. - Palaeobotanist 36:161-167. PANDEY, D.K. & CHOWDHARY,S. 2007. Sequence stratigraphic TRIPATHI, A. 2000. Palynological events during . late framework of Lower to Lower Middle Jurassic Triassic-Early Jurassic time in India. - Palaeobotanist sediments of the Jaisalmer Basin, India. - Beringeria 49: 309-408. 37: 121-131. VENKATACHALA, B.S. & MAHEWHWARI, H.K. 1991. Indian PHILIPPE, M., BAMFORD, M., Me LOUGHLIN, S., ALVES, L.S.R., Gondwana redefined. In: Indian Gondwana. - FA LCON LANG. H.J., GNAEDINGER, S., 0TTONE, E.G., Geological Society of India, Bangalore, Special POLE, M., RAJANIKANTH, A., SHOEMAKER, R.E., TORRES, Publication: 81-87. T. & ZAMUNER, A. 2004. Biogeographic analysis of VENKATACHALA, B.S., MAHESHWARI, H.K. & RAJANIKANTH, Jurassic-early Cretaceous wood assemblages from A. 1993. The Gondwana Supergroup. - Gondwana Gondwana. - Review of Palaeobotany and Palynology Geological Magazine, Special Volume: 80-92. 129: 141-173. VIJAYA & PRASAD, G.V.R. 2001. Age of the Kota Formation, PRASAD, B. & PUNDIR, B.S. 1999. Biostratigraphy of the Pranhita Godavari Valley, India. A palynological exposed Gondwana and Cretaceous rocks of Krishna­ approach. -Journal of the Palaeontological Society of Godavari Basin, India. - Journal ofthe Paleontological India 46:77-93. Society of India 44: 91-117. VIJAYA & Rov, A. 2000. Late hour Jurassic palynomorph RAJANIKANTH, A. & SUKH-DEv 1989. The Kota Formation: assemblage in the Dubrajpur sediments, Birbhum Fossil flora and stratigraphy. - Geophytology 19: 52- district, West Bengal, India. - Palaeobotanist 49: 41- 64. 49. 9th International Congress on the Jurassic System - Abstracts 161

An overview of yellow Limestone deposit ofJaisalmer Basin ofRajasthan, India

T. S. RA.NAWAT1 & NEERAJ SRIVASTAVE2 *

1Additional Director (Geology), Department of Mine & Geology, Udaipur,India 2Sr. Manager (Geology & Environment), ASDCP Ltd., Udaipur, India; E-mail: neeraj.shrivastava@ golcha.com

*Corresponding author

The Mesozoic rocks are well exposed in the times its use has increased manifold mainly in Jaisalmer basin of Rajasthan. It is classified as interior flooring, wall claddings, monuments, Lathi, Jaisalmer, Baisakhi, Bhadasar, Pariwar cobble stones and for decorative purpose. and Habur fo rmations (DAs GUPTA 1975; With the increasing demand of this decorative KRISHNA 1987; PANDEY et al. 2012). The rocks stone in the world market the deposit of yellow of these fo rmations are mainly represented by limestone is precious for us and it should be limestone, sandstone and shale. Out of these scientifically mine to get maximum recovery formations Lathi, Jaisalmer, Baisakhi and because this deposit is having tremendous Badasar formations belong to J urassic age. scope to earn fo reign exchange and emerged as The yellow limestone is mainly confined in the a valuable asset fo r ornamental stone industry. Jaisalmer Formation (AGARWAL et al. 1988; References DMG 2004; IBM 2011). The yellow limestone AGARWAL, S.C., BHATNAGAR P. & KHABYA, N. 1988. Limestone is occurring in Jaisalmer, Bada Bag, Moolsagar, deposit of Rajasthan. Publication of Department of Mines and Geology, Udaipur. Kanod, Amarsagar,Chundi , Bhagata, Manria, etc. DASHORA, R.S. & BHARGAVA, K.D. 1971. Investigation areas and widespread in more then 5.4 million of yellow limestone and other economic minerals sq. meters. It contains 42 to 51 °/o calcium oxide in Jaisalmer area. Report of field season 1970-71, and having thickness of hardly about 3 mts. The Department of Mines and Geology, Udaipur. strike of the bed is N15°E and dipping at an DAs GUPTA S.K. 1975. A revision of the Mesozoic-Tertiary Stratigraphy of the Jaisalmer Basin, Rajasthan. - angle of 4° to so in north western direction. The Indian Journal of Earth Sciences, 2 (1): 77-94. total estimated resource of yellow limestone is DMG. 2004. Mineral directory of Rajasthan. Publication of about 8.2 million tons. The yellow limestone is Department of Mines and Geology, Udaipur. massive and partly crystalline with pink colour IBM. 2011. Indian Mineral Yearbook. Publication of Indian Bureau of Mines, Nagpur. bands at some places. Fossiliferous bands are KRISHNA, J. 1987. An overview ofthe Mesozoic stratigraphy also very common (MuoE et al. 2012). Under of Kachchh and Jaisalmer basin. - Journal of the microscope it shows presence of well rounded Paleontological society of India 32: 136-149. quartz grains in the calcareous cement. PANDEY, D.K. CHOUDHARY, S., TEJ BAHADUR, SWAMI, N. & The mining of the yellow limestone is SHA, J. 2012b. A review of the Lower - lowermost Upper Jurassic lithostratigraphy of the Jaisalmer continuing from last several decades. It is Basin, western Rajasthan, India - an implication on quarried in blocks of 50 to 60 ems length, 30 biostratigraphy. - Volumina Jurassica 10: 61-82 to 40 ems in width and thickness of about 30 MUDE, S.N., JAGTAP, S.A., KUNDAL, P., SARKAR, P. K. & ems is sawed into tiles and used as yellow KUNDAL, M.P. 2012. Paleoenvironmental significance of ichnofossils from the Mesozoic Jaisalmer Basin, marble after polishing. It has been used since Rajasthan, north western India. - Proceedings of the ancient time fo r construction of fort, temples International Academy of Ecology and Environmental and various other building purposes. In recent Sciences. 162 9th International Congress on the Jurassic System - Abstracts

Limit of Upper Bathonian-Lower Callovian in -Anktlizato region (Morondava Basin)

HASINA NIRINA RANDRIANALY & ARMAND RASOAMIARAMANANA

DepartmentofPaleontologyand BiologicAnthropolog� Fa cultyofSciences, Universityof Antananarivo, Madagascar; E-mail: [email protected]

In the Ankilizato area of the Morondava bioclastic limestones containing a rich benthic Basin Bathonian-:-Callovian strata are well macrofauna. A transgressive phase started in exposed and richly fo ssiliferous. Studies of the Early Callovian which is indicated by Bathonian macro- and microfacies have been carried out sediments fo und reworked in the Lower in order to characterize more precisely the Callovian strata, marked by a combination of Upper Bathonian-Lower Callovian succession. Bathonian and Callovian faunas, and marly clay According to this work, the Bathonian is deposits with abundant macrocephalitids and characterized by thin-bedded oolitic and phylloceratids. 9th International Congress on the Jurassic System - Abstracts 163

Stable isotopes of foraminifera and ostracods for interpreting the Toarcian Oceanic Anoxic Event at the South Iberian palaeomargin

MATIAS REOLID

Departamento de Geologia, Universidad de]a en, 2307 Spain; Email: mreo/[email protected]

The EarlyToarcian Oceanic Anoxic Event (T-OAE) oceanic influences. is recognized as one of the most important In the FV section, a bed-by-bed geochemical environmental changes during the Mesozoic, analysis was conducted in the 30-m-thick with a dramatic impact on marine biota rhythmic succession of softand hard marlstones revealed by a significant mass extinction event with a total of 24 sample levels selected fo r a in benthic and pelagic groups. The sedimentary detailed analysis of stable isotopes (oxygen record of the T- OAE is characterized by organic­ and carbon). Analyses of o13C and 8180 (at rich sediments ("black shales") associated with the University of Michigan) were applied on a distinct negative excursion in o13C recorded in bulk samples and shells of different genera organic matter, marine carbonates, brachiopods, of foraminifera (Lenticulina and Dentalina) belemnites, and fo ssil wood (e.g. jENKYNS & and ostracods. A total of 364 specimens were CLAYTON 1997; HESSELBO et al. 2007; SUAN et investigated in 140 analyses. al. 2008). Several environmental changes may The analysis of the abundance and diversity have been involved in the mass extinction of fo raminiferal assemblages troughout the event, mainly affecting benthic organisms, section indicates an important diminution in such as general anoxia, the enhancement of the number of fo raminifera per gram and of the greenhouse conditions and a warming trend, pr a-diversity at the base of Serpentinum Zone. sea-level changes (e.g., HALLAM 1986; WIGNALL The o13C and 8180 values obtained from whole o13C et al. 2005; G6MEZ & GoY 2011). The of samples do not exhibit a clear trend or isotopic foraminiferal shells reflects the carbon isotopic excursion. composition of the dissolved inorganic carbon The o13C of Dentalina, Lenticu/ina, and (DIC) in sea-water in which the shell calcified. ostracods show a negative isotopic excursion It is, however, not in isotopic equilibrium with at the base of the Serpentinum Zone, more sea-water, because biogenic calcification is accentuated in the case of Lenticulina. The o13C relatively rapid resulting in kinetic isotope values subsequently recovered. In general, fractionation. Still, the stratigraphic trends of l)B(Lenticulina values are lower than l)B(Dentalina o13C composition of calcitic fo raminifera do values and no clear pattern is observed according reflect the o13C fluctuationsof the ambient DIC. to test size. Values of 013CLenticulina and 013CDentalina This work fo cuses on the analysis of o13C are usually lower than o13C from bulk samples. and 8180 from whole rock and tests of selected With respect to 8180, values of both Denta/ina foraminifera (Lenticulina and Denta/ina) and and Lenticulina show minor fluctuations, ostracods from Lower Toarcian marls and marly 0180Dentalina being lower than °180Lenticulina' No limestones of the South Iberian Palaeomargin relationship is observed with the test size of the (Western Tethys ), as well as on the comparison foraminifera. Redox (CrIAI, N if AI, VI AI, and U I with geochemical redox and palaeoproductivity Th) and palaeoproductivity proxies (SrI AI, U I proxies with the aim to improve knowledge of AI, P ITi and TOC) show a peak at the base of the the processes and the environmental effects Serpentinum Zone. of the Toarcian Oceanic Anoxic Event. The This data allow the interpretation of selected outcrop is a pelagic section called environmental conditions during the Early Fuente Vidriera (FV). It is of special interest fo r Toarcian and the characterization of redox interpreting the Early Toarcian Oceanic Anoxic and paleoproductivity conditions in the water Event at the westernmost end of the Tethys, column and pore-water of shallow to deep characterized by a complex palaeogeography infaunal microhabitats, with special attention and by being relatively isolated from open to the T- OAE. Microhabitat affected the o13C 164 9rh International Congress on the Jurassic System - Abstracts

values, cS13C . being generally lower than Oceanic Anoxic Event this part of the L entiCu 1.ma -in cS13C due the more depleted 13C values of palaeomargin. 0ent a 1.ma the pore-water in deep infaunal microhabitats. The lowest values of cS13C (lower part of the References Serpentinum Zone) occurred during suboxic G6MEZ, J.J. & Gov, A. 2011. Warming-driven mass extinction in the Early Toarcian (Early Jurassic) of northern conditions indicated by redox proxies, low and central Spain. Correlation with other time­ diversity and abundance of foraminifera, and equivalent European sections. - Palaeogeography, higher TOC values. The fine-grained, organic­ Palaeoclimatology, Palaeoecology 306: 176-195. rich sediments favoured depletion in 13C of pore­ HALLAM, A. 1986. The Pliensbachian and Tithonian water-dissolved inorganic carbon compared extinction events. - Nature 319: 765-768. HESSELBO, S.P., }ENKYNS, H.C., DUARTE, L.Y. & 0LIVEIRA, to that of the bottom water, a feature more L.C.Y. 2007. Carbon isotope record of the Early Jurassic accentuated during suboxic conditions. The cS13C (Toarcian) Oceanic Anoxic Event from fossil wood values of potential deep infauna (Lenticulina) and marine carbonate (Lusitanian Basin, Portugal). - reflect the oxygen restricted conditions better Earth and Planetary Science Letters 253: 455-470. jENKYNS, H.C. & CLAYTON, C.K. 1997. Lower Jurassic than the shallow infauna (Dentalina) and the epicontinental carbonates and mudstones from whole sediment. With respect to cS180, values England and Wales: chemostratigraphic signals and from bulk samples fluctuate more strongly the early Toarcian anoxic event. - Sedimentology 44: cS180 687-706. and exhibit lower values than en ta 1.ma and 0 SUAN, G., PITTET, BOUR, MATTIOLI, E., DUARTE, L.Y. cS180 en . • The stratigraphic differences 8., 1., L t1cu 1.ma & MAILLIOT, S. 2008. Duration of the Early Toarcian between cSlBQDenta/ina and cSlBQLenticulina COrrespond carbon isotope excursion deduced from spectral to vital effectsbecause no important fluctuations analysis: Consequence for its possible causes. - Earth in temperature occurred in the bottom waters and Planetary Science Letters 267: 666-679. as deduced from the absence of peaks and WIGNALL, P. B., NEWTON, R.J. & LITTLE, C.T.S. 2005. The timing of paleoenvironmental change and cause-and­ stratigraphic trends in the studied interval. effect relationships during the Early Jurassic mass The cS180 values do not allow interpretation of extinction in Europe. - American Journal of Science temperature changes related to the Toarcian 305: 1014-1032. 9th International Congress on the Jurassic System - Abstracts 165

Ecostratigraphy of foraminiferal assemblages and geochemistry for approaching the incidence of Early Toarcian environmental changes at the North Gondwana palaeomargin (Traras Mountains, Algeria)

MATIAS REOLID1 *, ABBAS MAROK2 & ABBES SEBANE3

1Departamento de Geologfa, Universidad de]a en, 23071 ]aen, Spain; E-mail: [email protected] 2Departement des Sciences de la Te rre et de l'Univers, Universite Abou-Bekr Belkaid, 13000 Tlemcen, Algeria 3Departement des Sciences de la Te rre, Universite d'Es-Senia, 31000 Oran, Algeria

*Corresponding author

The Early Toarcian was characterised by analysed from 16 samples. important environmental changes and a The observed benthic fo raminiferal mass extinction event usually interpreted assemblages are dominated by the suborder as a global Toarcian Oceanic Anoxic Event Lagenina, with minor content of Textulariina, (T-OAE). This mass extinction event had a Miliolina, and Spirillinina, comprising 17 genera significant impact on many marine organisms and 26 species. The ecostratigraphic analysis of (bivalves, brachiopods, foraminifera, ostracods, the foraminiferal assemblages along the studied ammonites and dinoflagellates ). The stronger succession reveals four well differentiated incidence of the T- OAE is documented at the stratigraphic intervals: boundary of the subboreal Tenuicostatum­ The end ofthe Pliensbachian is characterised Falciferum zones and the Submediterranean by a foraminiferal assemblage dominated and Mediterranean Polymorphum-Serpentinum by potentially deep infaunal fo rms (mainly zones and Polymorphum-Levisoni zones. Lenticu/ina gottingensis). The presence of In the Traras Mountains (Tlemcen Domain, epifauna and shallow infauna as well as the Northern Algeria), the T- OAE remains scarcely number of species and the a-diversity (> 3.0) studied. The selected Mellala section is one suggest good oxygen and nutrient availability of the very few examples of continuous and in the infaunal microhabitats. The high monotonous hemipelagic sedimentation (marls number of calcareous species corresponding to and marly limestones, SO m thick) through the K-strategists (Dentalina, Lingulina, Marginulina, Pliensbachian-Toarcian boundary (ELMI et al. Vaginulina, Saracenaria, Fa lsopalmula, 2009). Marginulinopsis, and Planularia and Spiril/ina) The aim of this research involves the and the presence of agglutinated fo rms point to ecostratigraphic analyses of foraminiferal a stable and constant benthic environment. assemblages for determining the response to The beginning of the Toarcian shows ecosedimentary dynamics during the Early significant changes in foraminiferal assemblages Toarcian, complemented with the analyses with respect to the uppermost Pliensbachian. of geochemical proxies and C and 0 stable At the Pliensbachian-Toarcian boundary six isotopes. species disappear (Saracenaria sublaevis, This research uses the ammonoid Falsopalmula insignis and Marginulinopsis biozonation proposed by ELMI et al. (2009) speciosa, Sp irillina infima, Ammobaculites for the Mellala section. The fo raminiferal agglutinans, and A. fo ntinensis). The general assemblages were analysed from 43 marly trend is the decrease of the proportion of sample levels. The ecostratigraphic analysis epifauna indicating more adverse conditions was fo cused on the stratigraphic fluctuationsof compared with the end of the Pliensbachian. the composition of foraminiferal assemblages. The Polymorphum Zone reveals a decrease of roe, geochemical proxies (redox proxies CoI AI, shallow infauna and epifauna, and an increase CuiAI, CrIAI, and V I AI; and palaeoproductivity in the proportions of potentially deep infauna. proxies Bal AI, and P ITi) and cS13C and cS180were The last record of agglutinated foraminifera is in 166 9thInternational Congress on the Jurassic System - Abstracts the Mirabile Subzone pointing to environmental forms, probably related to increasing stress changes in the epifaunal microhabitat. In the conditions. The proportions of the opportunist epifauna only Ophthalmidium appears as a new Lenticulina toarcense increase in the Levisoni genus in the Polymorphum Zone. Lingulina Zone (mean value of 58%) being the dominant tenera and L. pupa are especially abundant. species. The most significant information is the Three new species of nodosariids appear at reduced diversity ( 4 species and a-diversity < 1). the base of the Toarcian; Lenticu/ina toarcense, At 1.30 m above the PolymorphumiLevisoni Planularia preobonensis, and Ichtyolaria zonal boundary microfossils are almost absent su/cata. The most abundant foraminifer is and only two species where found (Lenticulina Lenticulina toarcense ( 43°/o of the assemblage). toarcense and Lingulina tenera). These data The dominance of Lenticulina toarcense and suggest more unfavourable conditions at the its inferred opportunist behaviour confirm a sea floor. Probably the PolymorphumiLevisoni perturbation in the palaeoecological parameters zonal boundary constitutes an episode of at the sea-bottom. The presence of Planularia restricting conditions resulting in suboxic preobonensis marks the late normal phase of waters at the sea floor as indicated by the the fo raminiferal development (SEBANE et al. maximum values of redox proxies (Col AI, Cui 2007) that immediately preceded the crisis AI, CrIAI, and V IAI) . However, it was not an related to the anoxic event that occurred during anoxic event as has been describeq-from other the early Levisoni Chron. The Polymorphum localities fo r this time interval due the values Zone is characterised by an initial decrease of these ratios, the low values of TOC and the in the diversity of benthic foraminifera and absence of an azoic interval with respect to the subsequent irregular fluctuationsin the values, benthic assemblages. which could be interpreted as changes in the The upper part of the Levisoni Zone is more palaeoenvironmental conditions resulting calcareous with an increasing shallow infauna in instability. Redox and palaeo-productivity and decreasing potentially deep infauna. The proxies in the Polymorphum Zone exhibit a-diversity index and the increasing number of important fluctuations in the Semicelatum species indicate more favorable conditions. Subzone with local maximum values of Col AI, CrI AI, and V I AI suggesting a decrease in the degree of oxygenation and an increase in the References precipitation of these redox-sensitive elements. ELMI, S., MAROK, A., SEBANE, A. & ALMERAS, Y. 2009. Importance of the Mellala section (Traras Mountains, Local increase of P ITi could be correlated with northwestern Algeria) for the correlation of the an increase in productivity; however, Bal AI Pliensbachian-Toarcian boundary. Vo lumina does not corroborate this interpretation. jurassica 7: 37-45. A negative excursion of cS13C is recorded in SEBANE, A., MAROK, A. & ELMI, S. 2007. Evolution des peuplements de foraminiferes pendant la crise the PolymorphumiLevisoni zonal boundary. toarcienne l'exemple des donnees des Monts des a The beginning of the Levisoni Zone is Ksour (Atlas Saharien Occidental, Algerie). - Comptes characterised by the disappearance of epifaunal Rendus Palevolution 6: 189-196. 9th International Congress on the jurassic System -Abstracts 167

The Early Toarcian Oceanic Anoxic Event in the External Subbetic (South Iberian Palaeomargin, westernmost Tethys): geochemistry, nannofossils, and ichnology of the La Cerradura section

MATIAS REOLID1 *, EMANUELA MATTIOLI2, LUIS M. NIET01 & FRANCISCO J. RODRIGUEZ-TOVAR3

1Departamento de Geologfa and CEAC1; Universidad de jaen, 23071 ]aen, Spain; Email: mreolid@ ujaen.es 2Laboratoire de Geologie de Ly on, UMR 5276 CNRS, Universite Ly on 1, ENS Ly on, 69622 Villeurbanne, France 3Departamento de Estratigrafia y Paleontologfa, Universidad de Granada, 18071 Granada, Spain

*Corresponding author

The Toarcian Oceanic Anoxic Event (T-OAE) Chondrites (small and large), Palaeophycus, is one of the most important environmental Planolites, Teichichnus, Thalassinoides, and changes during the Mesozoic with a dramatic Trichichnus. The fill oftrace fossils is occasionally impact on the marine assemblages. The record rich in organic matter. Foramininifera (mainly ofT-OAE is characterized by a crisis of carbonate Lagenina suborder) and ostracods are production, an increase of organic matter common. content of sediments, and a negative excursion The marly interval is characterized by of 013( (e.g. jENKYNS & CLAYTON 1997; HERMOSO the absence of ammonoids. The fo raminifera et al. 2009). There is a great geographic and ostracods are very scarce or absent in variability of the T- OAE concerning the organic the first two meters of these marls. The trace matter content and degree of oxygenation of the fossil assemblage reveals a drastic decrease sea-bottom. The aim of this work is the analysis in diversity just above the top of the marl­ of geochemical data, calcareous nannofossils, limestone rhythmites where the C0 Ca content 3 and ichnofossils in the very well exposed La decreases to minimum values in the section Cerradura section (Subbetic, South Iberian (19%), followed by a gradual recovery showing Palaeomargin, westernmost Tethys) that allow an increase in diversity from 3 m above the top to interpret the environmental conditions at of the marl-limestone rhythmites. the sea-bottom and in the water column. The nannofossil assemblage of La Cerradura The La Cerradura section is located at a is of Tethyan affinity with a dominance of slope of the motorway A-44, km 57. The studied Mitrolithus jansae and Schizosphaerella mainly interval consists of 27 m of marl-limestone in the marl-limestone rhythmites of the rhythmites ranging from the Algovianum Zone Pliensbachian, whilst Crepidolithus crassus that (Upper Pliensbachian) to the Polymorphum has a N Tethyan affinity is very scarce. The First Zone (Lower Toarcian) and 11 m of dark marls Occurrence of Carinolithus superbus occurs 60 of the Serpentinum Zone (Lower Toarcian). cm over the last surface of the marl-limestone The marl-limestone rhythmites are very rich rhythmites and defines the NJT 6 that normally in belemnites and ammonoids with Canavaria, contains the T- OAE (MATTIOLI et al. 2009). As Emaciaticeras, Fo ntanelliceras, Lioceratoides, ammonites are lacking in the interval, we are Neolioceratoides, Protogrammoceras, and able to precisely date the base of the T- OAE Ta uromeniceras (Upper Pliensbachian) and negative excursion by means of the NJT 6 Dactylioceras (Polymorphum Zone; Lower nannofossil zone. We can thus demonstrate Toarcian), rendering a fine biostratigraphy that the T- OAE is synchronous with many possible. The top of the marl-limestone other Tethyan settings (MATTIOLI et al. 2009). rhythmites is an ammonite-rich horizon Absolute abundances are very high, comprising (Dactylioceras commune and D. polymorphum). between 0.5 E9 and 1.5 E9 specimens per gram The limestone layers are mudstones with an of rock. However, abundances dramatically diverse trace-fossil assemblage consisting of drop in the interval between samples 31 and 168 9thInternational Congress on the Jurassic System - Abstracts

27, where the relative abundance of M. jansae the Serpentinum Zone confirm the adverse also decreases. A similar trend is observed in conditions at the sea floor probably related several western Tethyan sections (MATTIOLI et to anoxic-suboxic conditions. Environmental al. 2008, 2009). Orthogonoides hamiltoniae, an conditions were unfavourable fo r the incertae sedis that normally is recorded during development of calcareous nannoplankton also the levels enriched in organic matter,is common in the surface waters, as attested by the drop in in the interval between 4 and 5 m above the top absolute abundances. Furthermore, the deep of the marl-limestone rhythmites. photic zone seemed to have been particularly Geochemical data indicates an abrupt change hostile to phytoplankton, as shown by the main related to the beginning of the marly interval. decrease in the relative abundance of the deep­ The CaC0 (0/o) dramatically decreases with dwelling M. jansae, probably related to the 3 lowest values at the base of the marls (1 m over sporadic upward migration of the anoxic zone the marl-limestone rhythmites) in coincidence in the water column (further attested by the with relatively higher values of total organic presence of small pyrite framboids). Increasing carbon (TOC, 0.4 wt.o/o). However, this value is values of Cu, U, Th, TS, TOC, and U aut., as well low compared with central and north Europe as the record of pyrite framboids < 5 �m size records. The values of o13C in the rhythmites confirm anoxia (probably affecting the water (Upper Pliensbachian to Polymorphum Zone) column at any time). The First Occurrence of are around 1.20°/o o, and a negative excursion Ca rinolithus superbus in this section is recorded of o13C (0.8%o) occurs from the top to 1 m in the interval where geochemical signals above the rhythmite (0.21 %o). From this level indicate restricted oxygen conditions. This onwards o13C increases to the top of the marls event also permits effective correlations with (reaching 2.47°/oo). The authigenic U and the other Tethyan settings where the T- OAE has Total Sulphur (TS) exhibit the highest values been recorded. just above the marl-limestone rhythmites. The content of Cu, U, and Th also increases in the same interval. In SEM, small pyrite framboids References ( -4 �m) are also recorded in the lower part of HERMOSO, M., MINOLETTI, F., LE CALLONNEC, L., }ENKYNS, the marl interval. .H.C., HESSELBO, S.P., RICKABY, R.E.M., RENARD, M., DE RAFAELIS, M. & EMMANUEL, L. 2009. Global and The carbon cycle perturbation related to the local fo rcing of Early Toarcian seawater chemistry: T- OAE is clearly recorded in the La Cerradura A comparative study of different paleoceanographic section by the decrease in C0 Ca and the negative settings (Paris and Lusitanian basins). 3 excursion of 013C at the base of the Serpentinum Paleoceanography 24: PA4208. Zone, NJT 6 nannofossil zone. The trace }ENKYNS, H.C. & CLAYTON, C.J. 1997. Lower Jurassic epicontinental carbonates and mudstones from fossil assemblage from the marl-limestones England and Wales: chemostratigraphic signals and rhythmites (Upper Pliensbachian Algovianum the early Toarcian anoxic event. - Sedimentology 44: Zone to Lower Toarcian Polymorphum Zone) 687-706. reflects favourable oxygen conditions ( oxic MATTIOLI, E., PITTET, B., PETITPIERRE, L. & MAILLIOT, S. 2009. Dramatic decrease of the pelagic carbonate to slightly disoxic) fo r macrobenthic trace­ production by nannoplankton across the Early makers. A decrease in diversity or absence of Toarcian Anoxic Event (T-OAE). - Global and Planetary fo raminifera and trace fossils at the base of Changes 65: 134-145. 9th International Congress on the Jurassic System - Abstracts 169

Preliminary report on the ammonite fauna and stratigraphy of the Beckeri Zone (Upper Kimmeridgian) of the southern Crimea (Ukraine)

MIKHAIL A. ROGOV

Geological Institute of RAS, Moscow, 11901 7, Russia; E-mail: [email protected]

Upper Jurassic strata of Crimea (Ukraine) are a latest Beckeri Zone age ( - rebou/etianum mainly represented by shallow-water reef horizon or closeby level). fades, characterized by significant thickness ( 4) A rich ammonite assemblage has (up to few kilometers), complex tectonics, and been collected from bed 59. It includes, along rare ammonite records. Only recently Upper with phylloceratids (Pseudophylloceras and Kimmeridgian ammonite-bearing beds were Sowerbyceras), a few Ochetoceras semimutatum discovered in the eastern Crimea (ARKADIEV & (FoNT.) and small-sized ataxioceratids RoGov 2006), while new records ofmicrofossils resembling Virgataxioceras minutum (BERCKH.) suggested that this substage also could be This assemblage could be dated as belonging to recognized in the southern Crimea (ANIKEYEVA the Seta tu m Subzone of the Beckeri Zone. & ZHABINA 2009). A new section, containing (5) Ammonites were most abundant (more rich ammonite assemblages of the uppermost than 100 specimens were collected) in bed Kimmeridgian, has been discovered recently 66. The ammonite assemblage is dominated between Chelebi and Foros mountains near to by Ta ramelliceras cf. compsum (OPP.), which Foros settlement, southernmost Crimea by the includes more than 70% ofall ammonite records. amateur palaeontologist Aleksei Kudryavtsev. In addition to this species Sowerbyceras are This section is represented by a fo lded relatively common here, while other ammonites marlstone succession with ·a total thickness (Euvirga/ithacoceras (?) tantalus (HERBICH) and ea. 30 m. Ammonites occur in abundance in indeterminable ataxioceratids,Aulacostephanus the lowermost part of this section and become (A ulacostephanoceras) cf. jasonoides (PAVL.), relatively uncommon upwards. Belemnites and Pseudophylloceras sp., Sutneria sp. etc.) are rare. bivalves are very rare. Terebratulid brachiopods This assemblage could belong to the uppermost are relatively numerous in the lowermost part Subeumela or Setetum Subzone of the Beckeri of the section only (beds 59-66), but were not Zone. fo und above. (6) Beds 72-73 in the lowermost part of The fo llowing assemblages could be the succession are characterized by a nearly recognized, from youngest to oldest: homogeneous ammonite assemblage dominated (1) Ataxioceratid ammonite, resembling by Sowerbyceras and including also Haploceras Lithacoceras, and Berckhemeria sp. were (?) sp. and Pseudophylloceras consanguineum collected from bed 15, suggesting an earliest (GEMM.) Tithonian age. The studied succession is characterized by (2) Beds 26-41 are characterized by unique ammonite assemblages of the Beckeri ammonite assemblages consisting mainly of Zone, which strongly differ from assemblages of Subplanites-like microconchiate ataxioceratids this age known from other areas. Aspidoceratid orleiostracanammonites,belongingtothegenera ammonites are here absent or extremely rare Sowerbyceras, Haploceras, and Protetragonites. (only one small-sized Sutneria was recorded), At least two ataxioceratid-dominated and two while Ta ramel/iceras from bed 66 is more leiostracan-dominated assemblages could be numerous compared with any other described recognized here. The age of these assemblages Kimmeridgian assemblage. could not yet be determined precisely, but lies close to the Kimmeridgian-Tithonian boundary. This study has been supported by RFBR grant 12-05- 00380 and Program of the Presidium of RASno.28. I am (3) Slightly below, in bed 44, Neochetoceras also wish to thank ALEKSEI KUDRYAVTSEV and YURI ZHUKOV, ex gr. rebouletianum (FONT.) and Silicisphinctes who showed me the section, provided some specimens, sp. were collected. These ammonites indicate and helped collecting the ammonites. 170 9th International Congress on the Jurassic System - Abstracts

References of Geological Sciences·ofth� NAS of Ukraine: 99-103, ANIKEYEVA, O.V. & ZHABINA, N.M. 2009. Sedimentation Kyiv [in Ukrainian]. conditions of the Upper Jurassic deposits in the ARKADEV, V.V. & RoGOV, M.A. 2006. New data on Upper Mountain Crimea, Yalta amphitheater. In: Fossil Kimmeridgian-Tithonian biostratigraphy and flora and fauna of Ukraine: paleoecological and ammonites of the Eastern Crimea. - Stratigraphy and stratigraphic aspects. - Proceedings of the Institute Geological Correlation 14: 185-199. 9th International Congress on the Jurassic System -Abstracts 171

Quantitative and qualitative aspects of changes in shell size through the evolution of Volgian ammonites in the Russian Sea: Cope's rule, Lilliput effect, dimorphism, and polymorphism

MIKHAIL A. ROGOV

Geological Institute of RA� Moscow, 11901 "' Russia; E-mail: [email protected]

Recent advances in studies of biodiversity reduction in size of dorsoplanitid ammonites changes and evolution of fossil lineages through across the Arctic and extinction of nearly all time rarely considered quantitative changes in genera. First craspeditid ammonites, belonging fossil populations. Investigations of changes in to three geographically separated subfamilies, size through evolution are relatively common, all show a very small size at the end ofthe Middle but mainly focus on mass-extinction time­ Volgian and at the very beginning of the Late intervals and usually do not include observations Volgian (RoGov 2013). During the Late Volgian on dimorphism and polymorphism. Here I these ammonites show different patterns in am presenting a few examples of evolution of shell-size evolution, and only their Valanginian Volgian ammonite faunas in the Russian Sea, and especially Hauterivian descendants show showing quantitative and qualitative aspects of a size of macroconchs comparable with that of changes in shell size. the Middle Vo lgian age. (1) Cope's rule in the evolution of Volgian (2) Miniaturisation in response to stress ammonites environments and Lilliput effect as post­ The Volgian Stage is well-known as a time extinction phenomenon when giant ammonites were common, but rate Vo lgian ammonite faunas show few and time of size increase ·differ significantly miniaturization events of different nature. In within lineages. Members of the Virgatitidae the beginning of the Early Volgian, invasion family, endemic to the Subboreal Russian of ammonites of Submediterranean origin and Polish seas, show a gradual increase in (Paralingulaticeras) led to appearance of the size of macroconchs during the Early and endemic species, which are characterized by Middle Volgian, while · the size of microco nchs smaller size ( -1/2 the size of this genus in remains nearly constant (see also below). Submediterranean faunas) and absence of Larger virgatitids ( megaconchs Virgatites ventrolateral nodes, which are typical fo r late giganteus and V. rosanovi, attaining more growth stages in typical Paralingulaticeras. than 0.5 m in diameter) are known from the Such a size decrease was accompanied by a high Virgatus Zone o(the Middle Volgian just before abundance of these ammonites (up to -60o/o of the extinction of this fa mily. Nearly the same all ammonite records; see RoGOV 2010). Other pattern in shell-size changes characterized Submediterranean ammonites in the Lower the dorsoplanitid lineage, but it started later, Volgian are also usually relatively small-sized because Lower Volgian dorsoplanitids were (Neochetoceras) or represented mainly by uncommon on the Russian Platform and only small-sized morphotypes (dwarf macroconchs since the beginning of the Middle Vo lgian these of Schaireria). The miniaturization event ammonites became abundant. Occasionally, in Paralingulaticeras and partially in other the same gradual increase in shell size was Submediterranean taxa strongly resembles recognized within successive populations the response of cardioceratid populations in of the species ( Lomonossovel/a lomonossovi; untypical environments aftertheir southwards see MITTA 1993). The maximum diameter of immigration (MATYJA & WIERZBOWSKI 2000) megaconchs of Epivirgatites at the beginning and could be considered as stress-related of the Nikitini Chron was slightly less than 1 m, phenomenon. Another type of miniaturization well comparable with the size of Portlandian event occurred in the latest Middle Vo lgian just giants of the same age. But the upper subzone of after extinction of giant megaconchs. At this the Nikitini Zone was characterized by a strong time the oldest Ka chpurites, dwarf descendants 172 9th International Congress on the Jurassic System - Abstracts of Laugeites (with shell diameter of mainly are here used as morphological terms only. -3 cm compared with at least 8-10 cm in Lower and Middle Volgian dorsoplanitids and microconchs of Laugeites) are blooming. At all virgatitids usually show two or three separate known localities their shells form coquinas, size groups, while specimens of intermediate consisting of hundreds of specimens, while size are absent or very uncommon. Virgatitid other ammonites (the last relatively small­ microconchs have a shell diameter of usually sized Epivirgatites) remain uncommon. These between 8 and 15 cm and are characterized Ka chpurites are also characterized by evolute by nearly constant type of ribbing at the body coiling and relatively simple ribbing (mainly chamber and phragmocone or by changes in the fine biplicate ribs and intercalatories) and do rib ratio. Macroconchs show biplicate ribbing or not reveal significant size dimorphism. It should smoothing of sculpture on the outer whorls; they be noted that miniaturization occurred within are usually less numerous than microconchs. all Boreal lineages near to the Middle/Late Macroconchs are also uncommon within Volgian transition, but it was not simultaneous dorsoplanitids from the Panderi Zone, while in in the various taxa. Such a remarkable post­ the overlying Virgatus Zone macroconchs of the extinction event is easily comparable with other genus Dorsoplanites dominate. Dorsoplanitids simplification and dwarfism in ammonites, from the Middle Volgian Nikitin Zone are described by GuEx (2001) as special response mainly characterized by three size morpho­ to enormous stress (for review see NEVO 2011), groups ( microconchs, macroconchs, and big and as "Lilliput effect"( URBANEK 1993), because macroconchs (megaconchs)). Three size groups these small species also show high abundance are also very typical of the latest Middle to Late but very low diversity. Significantly, just after its Volgian Garniericeratinae. It should be noted appearance the genus Ka chpurites shows very that early garniericeratins (Kachpurites) are fast evolution accompanied at some levels by a represented by microconchs ( -3-4 cm), small very high variability. During all the time when macroconchs ( 6-7 cm) and relatively rare large evolution of this genus (and of the descendant macroconchs (up to 20-25 cm); the small­ genus Garniericeras) was rapid, these ammonites large macroconch ratio changed significantly dominated in all studied populations of the within different populations. Garniericeras, a Russian Sea, usually accounting fo r up to 80- late member of this subfamily, shows two size 90% of all records. Nevertheless members groups in nearly all assemblages (microconchs of Ka chpurites mainly remained small-sized and small or large macroconchs). Interpretation during the early part of the Fulgens Chron of the discussed polymorphism in shell size and even among full-grown macroconchs includes developmental polymorphism sensu commonly attained only 5-6 cm in diameter, MATYJA (1986) and/or discrete adaptive norms while big macroconchs (20-25 cm) were very (see NIGMATULLIN 2012 for example of DAN in uncommon. In the latest part of the Late Volgian modern cephalopods) coupled with possible (Nodiger Chron) a higher evolutionary speed sexual dimorphism. was typical of members of the other craspeditid subfamily (Craspeditinae) , also accompanied This study has been supported by RFBR grant 12-05- by size decrease at the beginning. Late Volgian 00380 and Program ofthe Presidium of RAS no. 28. ammonite faunas of all Boreal regions with a References rare exception (large-sized Chetaites at the end GUEX, J. 2001. Environmental stress and atavism in of the Vo lgian in Northern Siberia) consisted ammonoid evolution. - E£logae Geologicae Helvetiae of ammonites which were much smaller than 94: 321-328. MATYJA, B.A. 1986. Developmental polymorphism in Middle Volgian ones (RoGov 2013). Oxfordian ammonites. - Acta Geologica Polonica 36: (3) Dimorphism and polymorphism in shell 37-68. size of Volgian ammonites MATYJA, B.A. & WIERZBOWSKI, A. 2000. Biological response Recognition of dimorphism and of ammonites to changing environmental conditions: polymorphism as well as their interpretation an example of Boreal Amoeboceras invasions into Submediterranean Province during Late Oxfordian. - met some problems in the Volgian ammonites, Acta geologica Polonica 45-54. SO: as they are mainly lacking any mature MITTA, V.V. 1993 Ammonites and zonal stratigraphy of modifications. Thus micro- and macroconchs the Middle Volgian deposits of Central Russia. 132 p., 9th International Congress on the Jurassic System -Abstracts 173

Geoprognoz, Kiev. [in Russian] RoGOV, M.A. 2010. A precise ammonite biostratigraphy NEVO, E. 2011. Evolution under environmental stress through the Kimmeridgian-Volgian boundary beds at macro- and microscales. - Genome Biology and in the Gorodischi section (Middle Volga area, Russia), Evolution 3: 1039-1052. and the base of the Volgian Stage in its type area. - NIGMATULLIN, CH.M. 2012. Discrete adaptive norms of Volumina jurassica 8: 103-130. cephalopods: On an example of giant squid Dosidiscus RoGOV, M.A. 2013. The end-jurassic extinction. Extinction. gigas (Ommastrephidae) from the eastern Pacific Grzimek's Animal Life Encyciopedia: 487-495, Ocean. In: LEONOVA, T.B., BARSKOV, I.S. & MITTA, V.V. Cengage. ( eds.), Contributions to current cephalopod research: URBANEK, A. 1993. Biotic crises in the history of Upper Morphology, systematics, evolution, ecology and Silurian graptoloids: a palaeobiological model. - biostratigraphy: 42-44, PIN RAS, Moscow. [in Russian Historical Biology 7: 29-50. with English summary] 174 9th International Congress on the Jurassic System -Abstracts

New data on the Lower-Upper Kimmeridgian boundary beds of southern Tatarstan, Central Russia

MIKHAIL A. ROGOV1 *, ANDRZEJ WIERZBOWSKI2, ELENA V. SHCHEPETOVA1 & HUBERT WIERZBOWSKI3

1Geological Institute of RAS, Moscow, 11901 7, Russia; E-mail: [email protected] 2Polish Geological Institute-National Research Institute, Wa rsaw, 00-975, Poland; E-mail: andrzej. [email protected] 3Geological Institute of Polish Academy of Sciences, Wa rsaw, Poland; E-mail: [email protected]. pi

*Corresponding author

The lowermost and uppermost Kimmeridgian the presence of the Mutabilis Zone has been deposits of Central Russia are relatively widely suggested based on a single historical record Aspidoceras liparum A. distributed and fairly well known, while Lower­ of the ammonite ( = Upper Kimmeridgian boundary beds are missing lallierianum (o'ORB.) in PAVLOW 1886: pl. 9, fig. or strongly condensed in nearly all sections 3). and were not investigated in detail so far. It During fieldwork in 2010 and 2011 we should be noted that the position of the Lower­ studied key sections of the Lower-Upper­ Upper Kimmeridgian boundary (the base of the Kimmeridgian boundary beds, located at the Mutabilis Zone) in the Subboreal succession Volga river bank close to the border between the remains the matter of discussion during the last Ulyanovsk Region and the Tatarstan Province of decades. Traditional definition of this boundary Russia. High cliffs at the right bank of the Volga by FAD ofAu lacostephanoides is widely accepted river,loc ated along a few kilometers from Mimei (MESEZHNIKOV 1984; HANTZPERGUE et al. 1997, to Tarkhanovskaya Pristan (HANTZPERGUE et al. 1998). Since the transition from Rasenioides to 1998), are consist mainly of the Kimmeridgian Aulacostephanoides (Aulacostephanites) is very and only occasionally of underlying Middle gradual with co-occurences of specimens with Jurassic deposits. The Kimmeridgian succession

or without ventral rib interruption (cf. ARKELL & is mainly represented by grey to light-grey CALLOMON 1963; BIRKELUND etal. l978), English calcareous silty clay with a total thickness of ea. authors have proposed the FAD of Rasenioides 15 m with a well visible band of dark-grey to (i.e., the base of the Askepta Subzone) as brown oil shales having roe contents of up to the marker of the base of the M utabilis Zone 12.4%. (BIRKELUND et al. 1983). The latter definition The fo llowing ammonite succession could of the Lower-Upper Kimmeridgian boundary be recognized here: is, however, unclear in those regions, where (1) Crussoliceras spp., Rasenioides spp., Rasenioides is rare or absent (i.e. the whole Amoebites cf. modestum (MESEZHN. & ROMM). Arctic, Russian Platform etc.), whereas in the Remains of the same assemblage with Submediterranean succession the boundary in Crussoliceras are known also from other question lies within the Hypselocyclum Zone areas of the Russian Platfo rm (Kostroma,

(MATYJA & WIERZBOWKSI 2000). Here we follow Kaluga, and Moscow regions). In the Tver the older definition of the Mutabilis Zone and its region (BUEV 2012) Amoebites kitchini (SALF.), lower boundary by FAD of Aulacostephanoides. Rasenioides (Semirasenia) discoides HANTZ. Ammonites from the boundary of the and Aspidoceras binodum (OPP.) are also fo und Cymodoce and Mutabilis zones of the Russian in this assemblage. The assemblage could be Platfo rm are generally poorly known. Only distinguished as the lacertosum horizon after a few specimens of such ammonites were the most common microconchiate species figured or mentioned since the end of the 19th of Crussoliceras. eo-occurrence of Boreal, century and the position of all these records Subboreal, and Submediterranean ammonites within succession remains unclear. Moreover, allows correlation of this unit with the Divisum 9th International Congress on the Jurassic System -Abstracts 175

Zone of the Submediterranean succession, the This study has been supported by RFBR grant 12-05- discoides horizon of the Subboreal Cymodoce 00380, the Program of the Presidium of RASno.2 8., and the Polish Ministryof Science and Higher Education (grant Zone, and the Boreal Kitchini Subzone. no. N N307 036537). (2) Amoebites sp. nov. (beaugrandi auct. non SAUVAGE, 1871), Aulacostephanoides References spp., dominated by small-sized coarsely­ ARKELL, W.J. & CALLOMON, J.H. 1963. Lower Kimeridgian ribbed Amoebites. It roughly corresponds to ammonites from the drift of Lincolnshire. - Paleontology6: 216-245. "faunas" with Amoebites aff. beaugrandi of East BIRKELUND, T. & CALLOMON, J.H. 1985. The Kimmeridgian Greenland and Spitsbergen in the Modestum ammonite faunas of Milne Land, central East Subzone of the Kitchini Zone. Unfortunately, Greenland. - Gnmlands Geologiske Unders0gelse aulacostephanid ammonites collected along Bulletin 153: 5-56. BIRKELUND, T., CALLOMON, J.H., CLAUSEN, C.K., N0HR Amoebites with are mainly represented by HANSEN, H. & SALINAS, I. 1983. The Lower Kimmeridge fragmentary preserved juveniles and their Clay at Westbury, Wiltshire, England. - Proceedings of precise identification is difficult. Nevertheless, the Geologists' Association 94: 289-309. the presence of a well developed smooth band BIRKELUND, T., THUSU, B. & VIRGAN, J. 1978. Jurassic­ at the venter of these ammonites confirms their Cretaceous biostratigraphy of Norway, with comments of the British Rasenia cymodoce Zone. - Palaeontology identification as Aulacostephanoides, typical of 21: 32-63. the Mutabilis Subzone of the Mutabilis Zone. BuEv, D.V. 2012. Rare Kimmeridgian ammonites from (3) Slightly above the unit with coarse­ the poorly studied section located in Tver region. In: ribbed Amoebites, a single specimen of Palaeontologyand evolution of the biodiversityin the Earth history (in museum context). - Collection of Zenostephanus sachsi (MESEZHNIKOV) has been scientific articles: 119-124, GEOS, Moscow. found. This species is typical of the sachsi HANTZPERGUE, P.,ATROPS, F. &ENAY, R. 1997. Kimmeridgien. horizon of Spitsbergen and Franz-Josef Land In: Biostratigraphie du Jurassique Ouest-Europeen et and perhaps it occurs at nearly the same level Mediterraneen. - Bulletin du Centre de Recherche Elf in East Greenland (cf. SYKE� SURLYK 197 6: fig. Exploration Production 17: 87-96. & HANTZPERGUE, P., BAUDIN, F., MITTA, V., 0LFERIEV, A. & 7A). ZAKHAROV, V. 1998. The Upper Jurassic of the Volga ( 4) Overlying light-grey to grey clays basin: ammonite biostratigraphy and occurence of (uppermost 2.8 m of clayey unit) and brownish organic-carbon rich fa cies. Correlations between oil shales are characterized by a nearly boreal-subboreal and submediterranean provinces. In: CRASQUIN-SOLEAU, S. & BARRIER, E. (eds.), Peri­ homogeneous ammonite assemblage, consisting Tethys Memoir 4: Epicratonic basins of Peri-Tethyan of Aulacostephanoides sp. and aspidoceratids, platforms. - Memoires du Museum national d'histoire accompanied by poorly preserved cardioceratid naturelle 179: 9-33. microconchs. This assemblage also belongs to MATYJA, B.A. & WIERZBOWSKI, A. 2000. Biostratigraphical the Mutabilis Subzone. correlation between the Subboreal Mutabilis Zone, and the Submediterranean upper Hypselocyclum - (5) The presence of Orthaspidoceras liparum Divisum zones of the Kimmeridgian. In.: HALL, R.L. & (OPPEL) and 0. lallierianum (o'ORB.) above the SMITH, P. L. (eds.), Advances in Jurassic Research 2000. oil shales marks the base of the uppermost - GeoResearch Forum 6: 129-136. subzone of the Mutabilis Zone (Lallierianum MESEZHNIKOV, M.S. 1984. Kimmeridgian and Volgian stages ofthe North ofthe USSR. 224 p., Nedra, Leningrad [in Subzone) and its basal lallierianum horizon. Russian]. The uppermost horizon of this subzone PAVLOW, A.P. 1886. Les ammonites de la zone Aspidoceras a (schilleri horizon) is unknown from the Russian acanthicum de l'est de la Russie. - Memoires du Comite Geologique (3): 1-91. [in Russian] Platform. 11 SYKES, R.M. & SURLYK, F. 1976. .A revised ammonite zonation of the Boreal Oxfordian and its application in northeast Greenland. - Lethaia 9: 421-436. 176 9th International Congress on the Jurassic System - Abstracts

Distichoceras bicostatum (STAHL) (Ammonoidea) from Kutch, western India; its stratigraphic and palaeoecological significance

PINAKI ROY

Department of Geo/og� Durgapur Government College, Durgapur - 713214, West Bengal, India

Distichoceras bicostatum (STAHL) has been worldwide patterns as well as morphometric redescribed including SPATH's (1927-33) fo rm analysis imply a probable nektobenthic shallow­ and additional topotype. Following PALFRAMAN water mode of life of the present species. (196 7) the taxon has been designated as a macroconchiate fo rm. In Kutch, D. bicostatum References occurs in the Lamberti Zone, more precisely SPATH, L.F.1927-1933. Revision of the jurassic cephalopod in the uppermost white limestone bed of fa una of Kachh (Cutch). Parts I-VI. - Memoirs of the Upper Callovian age. Wide palaeogeographic Geological Survey of India, Palaeontologia Indica, occurrence and short temporal distribution of new series 9, Calcutta, 2: part I, 1-71, pis. 1-7 [1927]; part 11, 72-161, pis. 8-19 [1928a]; part Ill, 162-278, the species make it a useful tool fo r interregional pis. 20-47 [1928b]; part IV, 279-550, pis. 48-102 stratigraphic correlation. Comparing the [1931a]; part V, 551-658, pls. 103-124 [1931b]; part mode of occurrence of the Kutch species with VI, 659-945, pis. 125-130 [1933]. 9th International Congress on the Jurassic System - Abstracts 177

Integrated biostratigraphy across the AalenianfBajocian boundary of the Central High Atlas, Morocco

DRISS SADKI

Department of Geolog)/J Fa cultyof Science, BP. 11201 Zitoune, Meknes, Morocco; Email: driss.sadki@ gmail. com

The Rich area, situated in the center of the basin of zeilleriids that are comparatively close to of the High Moroccan Atlas, presents a thick Rugitela hughesi (DAVIDSON). This species is Aalenian-Bajocian succession with continuous accompanied in the Concavum Zone by only a few marine sedimentation, which offers a rich and specimens of Lophrothyris contractu BucKMAN, varied fauna. This section was proposed as Acanthothyris oligocantha BRANCO, A. tenuispina a submediterranean auxiliary stratotype for WAAGEN, and a shell of the genus Loboidothyris the boundary between Aalenian and Bajocian BuCKMAN. Apart from Rugitela cf. hughesi, also (SADKI 1994). An integrated biostratigraphic very rare in the basal part of the Bajocian, and analysis of this section is proposed from the a Zeilleria sp., no other brachiopods have been distribution of the main palaeontological collected from the Discites Zone. groups: ammonites, belemnites, brachiopods, Bivalves. - The bivalve taxa, identified bivalves, gastropods, calcareous nannofossils, by ISTVAN SZENTE (University of Budapest, foraminifera, and ostracods. This integrated Hungaria) from the Rich section, are dominated biostratigraphy enables us to establish parallel by Pa/aeonucu/a, indicating soft substrate and scales, to serve as a comparison tool, but mostly poorly oxygenated waters. Other burrowing it is an element of dating when ammonites are fo rms such as Trigonia, Astarte, and Nicaniel/a rare or absent. occur only sporadically, appearing mainly Ammonites. - The succession of ammonite in the Concavum Zone together with the faunas of the Aalenean-Bajocian boundary supposedly pseudo-planktonic Bositra. These interval shows six successive assemblages are remarkably abundant at the top of the

(SADKI & ELMI 1991), occasionally dominated Concavum Zone. In the Discites zone, a rare by NW European graphoceratids, occasionally Palaeneilo sp. and Grammatodon sp. occur. by taxa of the Mediterranean Province which Gastropods.- Gastropods, analysed by CaNT I N also enables good correlations. This succession & Mo ARI (2001), show an inverse distribution allows to identify different biohorizons that to that of bivalves. Their density and their characterize the transition between the Aalenian diversity gradually increase up-section. In and Bajocian in the Moroccan Central High the Graphoceras concavum Biozone, we can Atlas (SADKI 1994). The boundary between the identify Amphitrochus abbas (HUDLESTON), two stages is marked by the first appearance ?Discohe/ix subaequa/is (o'ORBIGNY), Eucyc/us of Hy per/ioceras together with numerous ornatus (SOWERBY), Eucyc/oidea (Pseudalaria)? mediterranean elements. cf. etheridgii (TAWNEY), and Sadkia richens

Belemnites. - Belemnites are very rare, (CONTI & MONARI). In the Hyperlioceras occasionally absent in the Concavum Zone and discites Biozone, we find Amphitrochus abbas at the base of the Discites Zone. They become (HUDLESTON), Eucyc/us ornatus (SowERBY), abundant and diverse from the top of the Eucyc/oidea (Pseudalaria)? subangulata Discites Zone onwards where we can identify (MuNSTER), Eucyc/oidea (Pseudalaria)? cf. Holcobelus. etheridgii ( NE Sadkia richens TAW Y), (CONTI & Brachiopods. - The Rich area has yielded MoNARI) and Rhynchocerithium? sp. Aaleno-Bajocian brachiopods, mainlyzeilleriids, Calcareous nannofossils. - Several bio­ in marly layers. The biostratigraphic succession horizons of calcareous nannofossils at the RA (SADKI & ALME S 1992), shows a fa unal break Aalenian-Bajocian boundary were identified between the Con cavum and Discites zones. Both by DE KAENEL (1990) and were correlated with zones are characterized by the predominance the ammonite zones established by SADKI et 178 9thInternational Congress on the Jurassic System - Abstracts al. (1986). The most striking pattern of events Gourrama (Haut Atlas c-eRtral; Maroc). - Miscellanea is the great number of first occurrences in the del Servizio Geologico Nationale de Roma 5: 243- 248. vicinity of the Aalenian-Bajocian boundary. CONTI, M.A. & MoNARI, S. 2001. Middle Jurassic gastropods The new occurrences are mainly species of the from the Central High Atlas, Morocco. - Geobios 34: genus Wa tznaueria, which experienced a major 183-2 14. diversification at that time. In this interval, DE KAENEL, E. 1990. Etudes biostratigraphiques fondees several new species of Wa tznaueria make their sur les nannofossiles calcaires. Deuxieme partie: Nannofossiles calcaires du Jurassique des marges appearance: W. manivitae, W. fr equens at the Sud et Nord de la Tethys (marge Sud: Haut-Atlas, base of Concavum zone and W. barnesae, and Maroc; marge Nord: Jura, Suisse). These Universite de W. britannica in the Discites zone. Neuchatel, 318 p. Foraminifera and ostracods. - Foraminifera SADKI, D. 1994. Proposition de la region de Rich (Haut­ Atlas central marocain) comme stratotype auxiliaire and ostracods consist of associations, generally submediterraneen pour la limite Aalenien-Bajocien. ­ known from the Toarcian. The major micro fauna Geobios M.S. 17: 431-440. renewal is located at the Aalenian-Bajocian SADKI, D. & ALMERAS, S. 1992. Les brachiopodes aaleno­ boundary with the disappearance of Lenticulina bajociens de la region de Rich (Haut-Atlas central, orbigny, L. chicheryi, Nodosaria pu/chra and the Maroc): implications biostratigraphiques et paleoecologiques. - Cahiers Universite Catholique appearance of Lenticulina quenstedti, L. ga/eata, Lyon, Serie Sciences 5: 93-105. and Garantella stel/ata. This association marks SADKI, D. & ELMI, S. 1991. Fluctuations de la composition des peuplements d'Ammonoides en relation avec the Biozone 81 of the Discites Zone (AMHOUD & 80UTAKIOUT 1994) . la dynamique sedimentaire au passage Aalenien­ Bajocien dans le Haut-Atlas central marocain. In: Kinkelinel/a Ostracods abound with gr. MoRTON, N. (ed.), Proeedings of Conference on sermoisensis which disappears at the end of the Aalenian and Bajocian Stratigraphy, Isle of Skye, Aalenian. Scotland: 113-122. SADKI, D., IBNOUSSINA, M. & MOUTERDE, R. 1986. Biostratigraphie des ammonites de 11\alenien et du References Bajocien inferieur dans le Haut-Atlas central (Maroc). AMHOUD, H. & BOUTAKIOUT, M. 1994. Les foraminiferes de PICG-UNESCO, 185, Marrakech 1985. - Revue de la 11\alenien-Bajocien inferieur dans la localite Rich- Faculte des Sciences de Marrakech, N.S. 2: 443-462. 9th International Congress on the Jurassic System - Abstracts 179

Middle Jurassic coral biohermal limestones from pelagic carbonate platforms (Pieniny Klippen Basin, Western Carpathians)

}AN SCHLOGL1 *, ADAM TOMASOvYCH2 5 , DARIA IVANOVA3, BERNARD LATHUILIERE\ LOIC VILLIER & MARIAN GOLEJ2

1Department of Geology and Paleontology, Fa cultyof Natural Sciences, Comenius University, Mlynska dolina, 842 1S Bratislava, Slovakia; E-mail: [email protected] 2Geological Institute, Slovak Academy of Sciences, Dubravskci cesta 9, SK-840 OS Bratislava, Slovakia; E-mail: [email protected], [email protected] 3Department of Paleontology,Stra tigraphy & Sedimentology, Geological Institute, Bulgarian Academy of Sciences 24, Acad. G. Bonchev Str., 1113 Sofi a, Bulgaria; E-mail: dariaiv@geology. bas.bg 4UMR Georessources n°73S9 Universite de Lorraine, Campus Aiguil/ettes- BP 70239, F S4S06 Va ndoeuvre Jes Nancy Cedex, France; E-mail: bernard. [email protected] 5UMR CNRS 72 07, Centre de recherche sur la paleobiodiversite et les paleoenvironnements, Universite Pierre et Marie Curie, T.46-S6, Se etage, case 104, 4, place ]ussieu, 7S2S2 Paris cedex OS, France; E-mail: laic. [email protected]

*Corresponding author

Unique, several decametres-thick coral reefs Central Western Carpathians, and Easterm Alps (Vrsatec Formation) that developed on the record the maximum relative sea-level rise. Czorsztyn pelagic carbonate platform (eastern Radiolarites were deposited in troughs, and part of the Pieniny Klippen Belt - PKB, Western sedimentation was condensed on the shallow Carpathians) in the Penninic Ocean were elevations: all Oxfordian fa cies indicate aphotic assigned to the Oxfordian by MISIK (1979), conditions. KOCHANOVA (1979), SIBLIK (1979), and The Vrsatec Formation is fo rmed by white

MoRYCOWA & MisiK (2005) on the basis of their and pinkish biohermal coral framestones, bivalve and coral fauna. SCHLOGL et al. (2006) bindstones, and rudstones, locally with bivalves, revised the local stratigraphic succession and gastropods, nautiloids, brachiopods, decapods, argued that these reefs are of Bajocian age on holothurians, crinoid, ophiuroid, and echinoid the basis of ammonites and on the basis of a ossicles, and calcareous sponges. In addition complete re-interpretation of the stratigraphic to reef constructors, the benthic communities superposition. MORYCOWA & 0LXZEWSKA (2013) are clearly dominated by species-rich bivalve recently suggested that fo raminifera point to a assemblages. Brachiopods are rather rare and of Late Jurassic age. Here, we integrate our own low diversity (mainly represented by the genus field data and focus on multiple taxa to shed Parvirhynchia). Coral reefs were horizontally more light on the age controversy and to assess replaced by (1) breccias that accumulate at depositional conditions and the palaeoecology footwall margins of fa ulted blocks (with clasts of the coral-reef communities. fo rmed by biohermal limestones) and by (2) Both Bajocian and Oxfordian coral reefs crinoidal limestones. Peri-biohermal breccias were widespread in epicontinental seas do not represent fore reef wave-exposed rubble rimming the northern and southern margins of but are comparable to scarp breccia (AUBRECHT the Tethys (LEINFELDER et al. 2002). However, & SzuLc 2006). The deposition of biohermal the development of coral reefs on the Czorsztyn limestones was replaced by crinoidal-spiculitic Ridge either during the Bajocian or during the limestones on shallow pelagic carbonate Oxfordian is rather surprising. First, Bajocian platforms. The thickness of the Vrsatec coral reefs were not reported from pelagic Formation varies from few metres to more than carbonate platforms in the Tethys, and any new 70 m. occurrences will thus be informative about The Bajocian age ofthe biohermal limestones coral-reefecology in such environments. Second, is supported by ammonites, brachiopods, and Oxfordian deposits in the Pieniny Klippen Belt, benthic fo raminifers that occur within and 180 9th International Congress on the Jurassic System - Abstracts above the Vrsatec Formation. Dykes and breccia genera are Isastrea,,. Periseris, Thecosmilia, interspaces within the biohermal limestones are C/adophyl/ia, Dendraraea, and Thamnasteria. locally filled with Bositra buchi concentrations Such a coral assemblage is quite typical of the and contain common specimens ofthe ammonite Lower Bajoeian reefs of France, Luxembourg, Nannolytoceras tripartitum, with a stratigraphic and Switzerland (LATHUILIERE 2000a, b). Five of range from the Late Bajocian (G. garantiana and these genera are also common in the Oxfordian, P. parkinsoni zones) to the Early Bathonian especially from higher-latitude reefs, but they and early Middle Bathonian. Stratigraphic are represented by morphologically similar but termination of coral-reef limestones is marked differentspecies in the Bajocian and Oxfordian. by abundant borings and ferrigenous coatings Periseris does not occur in the Upper jurassic. that imply condensation and by abrupt MoRYCOWA & MisiK (2005) also describe the replacement with cross-bedded crinoidal­ genusAtelophyllia on the basis oftwo fragments. spiculitic limestones. These crinoidal-spiculitic We confirm the identification of this genus that limestones contain unequivocal Middle jurassic was known from the Lower Bajocian of France brachiopods (Apringia, Stolmorhynchia). only. Dendraraea dendroidea also implies a The upper boundary of crinoidal limestones Bajocian age (LATHUILIERE & GILL 1998). The never extends beyond the Late Bajocian (G. Bajocian age also explains the absence of some garantiana Zone) in the Pieniny Klippen Belt. coral taxa that are generally very abundant in The Vrsatec Limestone thus clearly pre-dates Oxfordian reefs. the G. garantiana Zone. This research was supported by grants APW 0644-10, The lower boundary of the Vrsatec APW 0248-07 and VEGA 2/0068/11. Formation is poorly constrained but it should post-date the termination of siliciclastic-rich References AUBRECHT, R. & SZULC, J. 2006. Deciphering of the complex sedimentation on the Czorsztyn Ridge during depositional and diagenetic history of a scarp the H. discites Zone. It can be either coeval limestone breccia (Middle Jurassic Krasin Breccia, with a significant hiatus at the basis of the Pieniny Klippen Belt, Western Carpathians). - crinoidal limestones (lowermost Bajocian - W. Sedimentary Geology 186: 265-281. laeviuscula and S. propinquans zones) or with KocHANovA, M. 1979. Die Bivalven des Jura der Vrsatec­ Klippe. Zapadne Karpaty, Paleontol6gia 4: 7-34. the lowermost part of the crinoidal limestones LATHUILIERE, B. 2000a. Coraux constructeurs du Bajocien (S. propinquans Zone). inferieur de France, lE�repartie. - Geobios 33: 51-72. Assemblages of benthic fo raminifera fo und LATHUILIERE, B. 2000b. Coraux constructeurs du Bajocien in the Vrsatec Formation are diverse and inferieur de France, 2eme partie. - Geobios 33: 153- 181. contain species of genera with hyaline wall LATHUILIERE, B. & GILL, G.A. 1998. Dendraraea corail (Spirillina, Te thysiel/a, Paalzowel/a, Hungarillina, scleractiniaire branchu jurassique: structure, Radiospirillina, Lenticulina, and Nodosariidae) , systematique, ecologie. - Palaeontographica A 248: dark microgranular wall (Troglogtel/a, 145-162. Earlandia, Glomospira, Planiinvoluta), LEINFELDER, R.R., SCHMID, D.U., NOSE, M. & WERNER, W. 2002. Jurassic reef patterns. The expression of a porcelanous wall (Nubecularia, Labalina, changing globe. - Society of Economic Paleontologists Ophthalmidium, Cornuspira), agglutinated wall and Moneralogists, Special Publication 72: 465-520. (Trochammina, Ve rneuilinoides, Textularia, MISIK, M. 1979. Sedimentological and mikrofacial study in Va lvulina, Ammobaculites) and aragonitic wall the Jurassic of the Vrsatec (castle) klippe (neptunic (Epistomina Trocho/ina). dykes, Oxfordian bioherm limestones). Zapadne and Such taxonomic Karpaty, Geol6gia 5: 7-56. [in Slovak with English composition and diversity is comparable to summary] assemblages from the Bajocian of the jura MoRYCOWA, E. & MISIK, M. 2005. Upper Jurassic shallow­ Mountains and Burgundy only. Ophthalmidium water scleractinian corals from the Pieniny Klippen obscurum, terquemi, Labalina rawiensis, and Belt (Western Carpathians, Slovakia). - Geologica 0. Carpathica 56: 415-432. Hungarillina media appear fo r the first time MORYCOWA, E. & OLSZEWSKA, B. 2013. Foraminiferal in the Bajocian, and the first three species are assemblage in the coral-bearing limestones of restricted to the Bajocian-Bathonian. the Vrsatec area (Pieniny Klippen Belt, Western The coral assemblages were described by Carpathians, Slovakia). - Geologica Carpathica 64: 63-69. MORYCOWA MI K (2005). We re-assess the & SI SIBLiK, M. 1979. Brachiopods ofthe Vrsatec Castle Klippen composition of coral assemblages on the basis of (Bajocian - ?Berriasian) near Ilava (Slovakia). Zapadne new and extensive sampling. The most abundant Karpaty, Paleontol6gia 4: 35-64. 9th International Congress on the Jurassic System - Abstracts 181

Distribution of the Jurassic Pectinoida and Ostreoida from the Tanggula Mountains, China: Biogeographic relations and importance of trans­ Pacific migration and the Hispanic Corridor

* 2 }INGENG SHA1 & PAUL L. SMITH

1Nanjing Institute of Geology and Palaeontology, Academia Sinica, 39 East Beijing Road, Nanjing 210008, China; E-mail: [email protected] 2Department of Earth, Ocean and Atmospheric Sciences, the Universityof British Columbia, 2207 Main Mall, Va ncouver, B. C. V6T 1Z4, Canada; E-mail: [email protected]

*Corresponding author

During the Jurassic, the wedge-shaped Tethys related to that of Tanggula's neighbour, the Ocean opened eastward to the west Pacific, northwest Pacific; (2) some species crossed the connecting to the northwest and southwest Pacific from east to west and the Tethys ocean Pacific faunal provinces. At various times from north to south; (3) the Hispanic Corridor beginning in the Early Jurassic it also connected played an important role in connecting Pacific westwards to the east Pacific through the with Tethyan bivalve faunal provinces from the Hispanic Corridor, an equatorial seaway along earliest Jurassic onwards. the junction of North and South America (SMITH

& TIPPER 1986; DAMBORENEA 2000; ABERHAN 2001; SHA 2001/2002). To the northwest, the References ABERHAN, M. 2001. Bivalve palaeobiogeography and the Tethys also was linked to the epicontinental s�as Hispanic Corridor: time of opening and effectiveness of northwestern Europe which in turn connected of a proto-Atlantic seaway. - Palaeogeography, to the Arctic sea via the Viking Corridor, again Palaeoclimatology, Palaeoecology 165: 375-394. beginning in the Early Jurassic (HALLAM 1977, DAMBORENEA, S.E. 2000. Hispanic Corridor: Its evolution 1994). Towards the southeast, beginning in and biogeography of bivalve molluscs. - GeoResearch Forum 6: 369-380. the Tithonian, it communicated with the south HALLAM, 1977. Biogeographic evidence bearing on A Pacific through the Southern Andes-East Africa the creation of Atlantic seaways in the Jurassic. - seaway (HALLAM 1983, 1994). The Tanggula Milwaukee Public Museum Special Publication, Mountains were situated at the northern margin Biology and Geology 2: 23-34. HALLAM, 1983. Early and Mid-Jurassic molluscan A of the eastern Tethys near the junction of the biogeography and the establishment of the central northern Tethys and northwestern Pacific. This Atlantic seaway. - Palaeogeography, Palaeoclimatology, is a key position, critical to our understanding Palaeoecology 43: 181-193. HALLAM, 1994. An outline of Phanerozoic biogeography. of dispersal between the major oceans of the A Jurassic globe. 246 p., Oxford University Press, Oxford. SHA, }INGENG 2001/2002. Hispanic Corridor fo rmed as In the main ridge of the Tanggula Mountains early as Hettangian: On the basis of bivalve fo ssils. - of west China, there are abundant Bajocian­ Science Bulletin 46: 1821-1824 (2001, in Chinese); Tithonian Pectinoida (SHA et al. 1 998) and 47: 414-417 (2002, in English). Ostreoida (SHA et al. 2002) consisting of 12 SHA, }INGENG, FURSICH, F.T., SMITH, P. L. & WANG, LIJUN 1998. Jurassic Palaeotaxodonta, Pteriomorphia and genera and 21 species. The temporal and spatial Isofilibranchia (Bivalvia) of the main ridge of the distribution of these freely migrating bivalves Tanggula Mountains. - Beringeria 21: 3-55. demonstrates that (1) the Mid-Late Jurassic SHA, }INGENG, SMITH, P. L. & F ICH, F.T. 2002. New Jurassic URS pectinid and ostreid fauna in northeastern Ostreoida (Bivalvia) from China (Tanggula Mountains, Tethys is most similar to that of northwestern Qinghai-Xizang Plateau) and their paleobiogeographic context. - Journal of Paleontology 76: 431-446. Europe and similar to that of the Indian Plate. SMITH, P. L. & TIPPER, H.W. 1986. Plate tectonics and Some species originated in the east Pacific paleobiogeography: Early Jurassic (Pliensbachian) during the Early Jurassic. The fauna is little endemism and diversity. - Palaios 1: 1-14 182 9thInternational Congress on the Jurassic System - Abstracts

Palaeobiogeography and evolution of Kutch Virgatosphinctinae

SABYASACHI SHOME1 * & SUBHENDU 8ARDHAN2

1Palaeontology Division -I, Geological Survey of India, Central Headquarters, Ko lkata 70001 6, India; E-mail: [email protected] 2DepartmentofGeological Sciences,jadavpur University,Ko lkata 700032, 1ndia; £-mail: sbardhan12@ gmai/.com

*Corresponding author

Due to regional uplift sincethe Late Oxfordian­ During Kimmeridgian time, the eastern Early Kimmeridgian the Kutch Basin became sea of Kutch became shallower (BISWAS 1977; progressively shallow and the palaeo-shoreline DESHPANDE & MERH 1980; RUDRA et al. 2007). showed rapid fl uctuation and steadily receded This posed a problem fo r the survival of the towards west. During Oxfordian time the stenohaline ammonites. The only Bharodia mainland represented the deeper part of the genus which successfully invaded the mainland basin while the palaeo-shoreline went up to of Kutch is To rquatisphinctes. The first the Kantkote region of eastern Kutch. Dhosa occurrence of To rquatisphinctes in the mainland oolite was the dominant motif of the off-shore comes from the Lower Katrol horizons at Jurun mainland, while nearshore the Kantkote (Jawahar Nagar) area which were assigned as sandstone dominated the shallow waters of Lower Kimmeridgian on the basis of belemnites eastern Kutch. (SPATH 1931). Two To rquatisphinctes species Ammonite distribution was more or less i.e., T. jurunensis and T. alterniplicatus, have homogeneous. Within the perisphinctiins, been reported from here. Discosphinctes was dominant in both region, During the Middle Kimmeridgian the but Ataxioceras appeared first in the Kantkote shoreline further shifted towards west. sandstone of eastern Kutch. Next ammonite­ To rquatisphinctes community not only migrated ' bearing horizons were encountered at Bharodia but also quickly speciated to produce different - west of Kantkote of Upper Oxfordian age genera such as Ka troliceras and Pachysphinctes To rq uatisphinctes (FORSICH & PANDEY 2003). in a restricted locality on Kutch mainland, made its first appearance along with older i.e. in Ler and adjoining areas. Although Ataxioceras and Discosphinctes in Upper To rquatisphinctes lived side by side with these Oxfordian to Upper Kimmeridgian Bharodia fo rms for a considerable stratigraphic span, the beds (SPATH 1931; FORSICH & PANDEY 2003) but Middle Kimmeridgian is actually dominated by the typical Kimmeridgian fauna of mainland, i.e. both Ka trolicerasandPachysphinctes. Thereafter the Ka tro/iceras-Pachysphinctes group is totally To rquatisphinctes was excluded from Kutch or absent. The typical Lower to Middle Oxfordian rather Indo-Madagascar areas. mayatiins, present in the Kantkote sandstone Ka troliceras and Pachysphinctes, although and throughout the mainland of Kutch also did morphologically quite distinct, overlapped not continue here. Thus the age of the Bharodia both temporally and spatially in Kutch. So, ammonite bed may be locally assigned only it is very difficult to establish the correct to the Late to latest Oxfordian. It appears that evolutionary plexous. The ontogenetic study of the origin of To rquatisphinctes is very cryptic adult Pachysphinctes reveals that Ka tro/iceras and that the genus evolved in a restricted area is nothing but a form which retained the (nearshore eastern Kutch). In Bharodia, the intermediate stage of it in its genetic spectrum. only specimen recorded is fragmentary and It appears, therefore, that To rquatisphinctes first incomplete. It is very difficult to identify the gave rise to Ka tro/iceras which soon produced evolved To rquatisphinctes in septate specimens. Pachysphinctes. Evolution took place within the The evolutionary novelties i.e., virgatatome Early Kimmeridgian Alterneplicatus Zone of trifurcation, longer secondaries, etc. only appear KRISHNA & PATHAK (1993), which according to on the later part of the chamber. them is equivalent to the Divisum Zone ofEurope. 9th International Congress on the Jurassic System -Abstracts 183

The evolution is very much compatible with the place of origin are not very clear. Within the punctuation model involving macroevolution. Virgatosphinctinae, Virgatosphinctes is not only The Ka troliceras-Pachysphinctes association the end member of the spectrum, it is the largest lasted throughout the Middle and Late and most complex in terms of ornamentation. Kimmeridgian in Kutch. Both are represented by Virgatotome, fasciculate ribbing pattern, single species (SHOME 2009) which fa ced steep which appeared in the late phragmocone stage inter-specific competition. The great intra­ of Pachysphinctes, has been recapitulated specific variability of each species might be due in the early ontogeny of Virgatosphinctes. to ecological displacement. One of the most Nowhere these two taxa stratigraphically and dominant trends of character displacement is geographically intergrade, but in many places the contrast in body size. Pachysphinctes is the Virgatosphinctes appears in horizons overlying hypermorphic giant, while Ka troliceras shows a Pachysphinctes-bearing beds. Once originated declining body size up-section. Pachysphinctes, Virgatosphinctes immediately spread to however,went extinct perhaps at the end of the many places. In most of the areas the genus is Kimmeridgian while the ancestral Ka troliceras represented by Virgatosphinctes denseplicatus speciesgave riseto thestillsmallerdescendantK. which shows less intraspecific variation than pottingeri. KRISHNA & PATHAK (1993) indicated the Kutch population. In Kutch and some that it continued up to the Early Tithonian. The adjoining areas it continued up to the Late subsequent history of Ka troliceras is obscured Tithonian. At the Jurassic-Cretaceous boundary in the eastern part of the mainland since the the Virgatosphinctes lineage was terminated younger sediments are sparsely fossiliferous. similar to many other ammonites that went The Tithonian succession is well exposed extinct arguably during a mass extinction at at the western fringe of the mainland of Kutch. the Jurassic-Cretaceous boundary. Appearance Lower Cretaceous sediments with occasional of virgatatome ribbing, which CALLOMON ' fossiliferous (mostly bivalve) bands overlying (1981) described as evolutionary innovation the Tithonian strata are restricted to this region. per excellence, lost its genetic uniqueness and It is evident that the sea further receded and never appeared in the Cretaceous ammonites. the shoreline existed only in this part of Kutch before final withdrawal from the Kutch Basin References during Aptian time (BISWAS 1991; RUDRA & BISWAS, S.K. 1977. Mesozoic rock-stratigraphy of Kutch. BARDHAN 2006). - Quarterly Journal of the Geological Mining and Metallurgical Society of India 49 (3 & 4): 1-52. The most dominant Tithonian ammonite BISWAS, S.K. 1991. Stratigraphy and sedimentary evolution assemblage is characterized by Virgatosphinctes of the Mesozoic basin of Kutch, Western India, pp. denseplicatus. It occurs in two distinct In: TAN DON, S.K., PANT, C.C. & CASSHYAP, S.M. ( eds.), associations found at different localities. The Sedimentary Basins of India: Tectonic Context: 74- Sahera-Moondan area, which is stratigraphically 103, Gyanodaya Prakashan. CALLOMON, J.H. 1981. Superfa mily Perisphinctaceae. In: older than the Lakhapar section, contains only DONOVAN, D.T., CALLOMON, j.H. & HOWARTH, M.K. Virgatosphinctes denseplicatus. Virgatosphinctes Classification ofjurassic ammonoidea. In: HousE, M.R. denseplicatus in the Lakhapar section has the & SENIOR, J.R. (eds.), The Ammonoidea. - Systematics same population structure as in typical Late Association, Special Volume 18: 101-155. DESHPANDE, S.V., & MERH, S.S. 1980. Mesozoic sedimentary Tithonian assemblages (SHOME et al. 2004; model ofWagad hills, Kutch, Western India. - journal SHOME & ROY 2006; SHOME & BARDHAN 2009). of the Geological Society of India 21: 75-83. Virgatosphinctes has an almost circumglobal FiiRSICH, F.T. & PANDEY, D.K. 2003. Sequence stratigraphic distribution and is found in many places significance of sedimentary cycles and shell spanning the entire Tithonian (VERMA concentrations in the Upper jurassic-Lower & Cretaceous ofKutch, western India.- Palaeogeography WESTERMANN 1972). Many workers described Palaeoclimatology, Palaeoecology 193: 285-309. Virgatosphinctes denseplicatus even from KRISHNA, J. & PATHAK, B. 1993. Late Lower Kimmeridgian Lower Tithonian horizons of different region. - Lower Tithonian virgatosphinctins of India: Therefore, it appears that the monotypic evolutionary succession and biogeographic implications. - Geobios, Memoire special 15: 227- assemblage of the Sahera-Mooildan section 136. belongs to the Lower Tithonian. However, RUDRA, P. & BARDHAN, S. 2006. Status of "Trigonia " the evolution of Virgatosphinctes and its ventricosa (Bivalvia) from the Upper jurassic - 184 9th International Congress on the Jurassic System -Abstracts

Lower Cretaceous of Kutch, western India: Kitchin's of Kutch, Gujarat. - Current Science 86: 197-202. unfinished synthesis. - Cretaceous Research 27: 611- SHOME, S. & Rov, P. 2006. New record of Pterolytoceras 628. SPATH, 1927 from the Upper jurassic (Late Tithonian) RUDRA, P., BARDHAN, S. & SHOME, S. 2007. Phylogeny of Kutch, we.stern India and its palaeobiogeographic of the Late jurassic-Early Cretaceous subgenus significance. - Indian Minerals 59: 57-64. Eselevitrigonia (Bivalvia) of Kutch, India, and SHOME, S. & BARDHAN, S. 2009. A new Late Tithonian paleobiogeographic constraints. journal of ammonite assemblage from Kutch, western India. - Paleontology 81: 1066-1079. journal of Palaeontological Society of India 54: 1-18. SHOME, S. 2009. Systematics, palaeobiogeography SPATH, L.F. 1931.Revision of the jurassic cephalopod fauna and evolution of the Upper jurassic of Kachh (Cutch). - Palaeontologia lndica, Geological (Kimmeridgian-Tithonian) ammonites of Kutch, Survey of India, New Series 9(2): 1-945. Western India. Unpublished PhD thesis, jadavpur VERMA, H.M. & WESTERMANN, G.E.G. 1972. The Tithonian University, 168 p., Kolkata. (Jurassic) ammonite fauna and stratigraphy of Sierra SHOME, S., DE, S., RAY, P. & DAS, S.S. 2004. Ammonites as Cartoce, Sar Luis Potosi, Mexico. - Bulletin of American biological stopwatch and biogeographical black box - Paleontology 63 (277): 107-320. a case study from the jurassic-Cretaceous boundary 9th International Congress on the Jurassic System - Abstracts 185

Jurassic Boreal zonal standard: Possibilities of Boreal-Tethyan correlation based on an integrated bio-, magneto-and chemostratigraphic approach

BORIS N. SHURYGIN* & 0XANA S. DZYUBA

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

*Corresponding author

In early studies, the Boreal Jurassic stratigraphy Boundary Stratotype Section and Point (GSSP) was based on data on ammonite occurrences aggravates the problem in the case when the in the numerous sections of the northern GSSP is defined at the first appearance datum territories of Russia, Northern America, of a taxon. Extremely different points of view of and East Greenland. The biostratigraphic ammonite experts on taxonomic affiliation of studies were based on the assumption that the same specimens (in part caused by a lack biostratigraphic scales were applicable only of monographic research) and the intention within palaeobiogeographic provinces (SAKS to produce a super-detailed zonation (up to et al. 1980). Regional zonal scales comprised biohorizons) complicate strongly the solution provincial zones with different index species of long-distance correlation problems. for synchronous biostratons. In these scales, In addition to Jurassic ammonite ammonite zones with a wide geographic biostratigraphy, great importance has recently range correspond to time intervals when the been placed on using integrated parallel zonal taxonomic composition of faunal assemblages scales from different Boreal groups of fo ssils was geographically levelled (they are usually (ammonites, belemnites, bivalves, micro fauna, associated with significant transgressive microflora) to provide more detailed and reliable events). As was stated (SAKS et al. 1980), such correlations (ZAKHAROV et al. 1997; SHURYGIN et zones form a system ofbiostratigraphic markers al. 2011; NIKITENKO et al. 2013). If one considers with rather isochronous boundaries. Ten widely the Boreal standard as a combination of these recognised markers were mentioned fo r the scales, it can be regarded as a combination, in Jurassic sediments, namely, theP. planor bis Zone which the reference intervals are characterised (Hettangian), A. stokesi Zone (Pliensbachian), D. by a unique succession of the results of athleticum Zone, Z. monestieri Zone (Toarcian), bioevents of different (independent) nature 0. jugatus Zone (Bathonian), C. elatmae Zone (phylogenetic, chorologic, ecological). A fixed (Callovian), C. cordatum Zone (Oxfordian), A. succession of independent events, apparently, eudoxus Zone (Kimmeridgian), P. pectinatus has the highest probability of isochroneity when Zone, and the D. maximus Zone (Volgian). identified in different regions. The boundaries Long-distance correlations based solely of biostratigraphic units distinguished fo r on ammonite biostratigraphy have some different fo ssil groups often do not coincide restrictions.Asarule,ammonitezonalboundaries with each other. When sections are correlated are postulated as based on evolutionary events. with the help of the entire set of parallel zonal However, the phenotype well distinguished scales, the discrepancy of boundaries permits from its ancestor is not formed immediately identifying and tracing very narrow intrazonal close to the point of divergence. Therefore, the intervals (eo-intervals, i.e., zone overlapping uncertainty interval of position of a phylo- or intervals between parallel scales). phenazone boundary will always exist near The Boreal standard should reflect as much the point of divergence, even if one does not as possible the specificity of the Boreal (Arctic) take into account the time fo r the geographic domain. The stratotype region for this standard distribution of a new phenotype. Internationally must have a typical Boreal (Arctic rather than accepted practice of definition of Global mixed) fa una. Correspondingly, a possible 186 9th International Congress on the Jurassic System - Abstracts

Boreal composite carbon-isotope curve Calpionellid Belemnite oi !!! �1 3C zonation zonation lc:trtinr�nhirl � .2 2 (/)-C/) :::I

otopeta

curvulus a/pil/ensis D picteti c analogus ea ·c: parami- -Cl)� eaN mounum Q)c:: ea >. � 0:::: )( dalmasi 0 c � privasensis -� E sibiricus .E :0:::: subalpina (J M17r � 0 Q.. -�Cl) ·s· c:: Q) B Cl)0 Een grandis EQ) en chetae ..c:: .9Cl) � ::;, c Ol ea ·a, g jacobi ------Q) c. taimyrensis c. .� t :::::1 Cl)c. ea A c::Q) .... enQ) Q.. C. -� -� --:- enc. (/) Cl) C. C:: 2. okensis 2 Q)C:: ::i .._.. - Normal polarity c=J Reversed polarity � No data

Fig. 1. Boreal (Siberian) ammonite-, belemnite-, magneto- and C-isotope stratigraphy across the J-K boundary calibrated against Tethyan (Mediterranean) standard afterBRA G IN et al. (2013) and DZYUBA et al. (2013).

candidate is Siberia (and the Arctic biochorema), trace the GSSP boundary globally. Obviously, which is located in the centre of the Panboreal precise position of Tethyan biostratigraphic Superrealm, where the set of interrelated scales boundaries will be never defined in Boreal for various fo ssil groups is most complete sections. There will always be a small or large (SHURYGIN et al. 2011; NIKITENKO et al. 2013). uncertainty interval, even if GSSP is based on Note that the regional scales for the marginal geomagnetic or isotopic event. Here we show biochoremas of the Panboreal Superrealm that the uncertainty interval can be sufficiently (like a zonal scheme for the Jurassic of Russian narrowed by using an integrated approach, on Platform), which reflect features of mixed an example of the Jurassic-Cretaceous (J-K) faunas, remain crucial in correlating between boundary interval,.,.which is one of the most Boreal and Tethyan successions. problematic intervals of the Phanerozoic (Fig. In many instances, the integrated bio-, 1). magneto- and chemostratigraphic approach is Two most widely used 'Tethyan' J-K necessary to solve problems of Boreal-Tethyan boundary markers (the base of the B. jacobi correlation, and this approach is especially ammonite Zone and the base of the calpionellid important fo r defining GSSPs. In our opinion, it Zone B) in Boreal regions correspond to is acceptable to use any event (palaeontological, different levels within the Upper Volgian C. geomagnetic reversal, isotopic excursion) as the taimyrensis ammonite Zone (HousA et al. 2007; marker fo r defining the GSSP. The problem is to BRAGIN et al. 2013). The uncertainty interval 187 9th International Congress on the Jurassic System - Abstracts of their position in the Boreal standard is the boundary sections and their correlation potential. - whole C. taimyrensis Zone. If the base of the Palaeogeography, Palaeoclimatology, Palaeoecology 381-382: 33-46. magnetozone M18r (GRADSTEIN et al. 2012) or GRADSTEIN, F.M.,0GG, J.G., SCHMITZ, M.D. & 0GG, G.M. (eds.) the base of the P. grandis Subzone will be used 2012. The geologic time scale 2012.- 1144 p., Elsevier, as the J-K boundary marker the uncertainty Amsterdam. interval can be narrowed to the eo-interval of HousA, V., PRUNER, P., ZAKHAROV, V.A., et al. 2007. Boreal­ the C. taimyrensis ammonite Zone and the C. Tethyan correlation of the jurassic-Cretaceous boundary interval by magneto- and biostratigraphy. - tehamaensis belemnite Zone. This eo-interval Stratigraphy and Geological Correlation 15: 297-309. also includes a narrow zone of reversed polarity NIKITENKO, B.L., SHURYGIN, B.N., KNYAZEV, V. G., et al. 2013. interpreted as the Brodno Subzone (M19n.1r) Jurassic and Cretaceous stratigraphy ofAnabar region and a distinct positive carbon isotope excursion (Arctic Siberia, Laptev Sea coast) and Boreal zonal standard. - Russian Geology and Geophysics 54 (in (BRAGIN et al. 2013; DZYUBA et al. 2013). press). SAKS, V. N., ZAKHAROV, V.A., MELEDINA, S.V., et al. 1980. Modern theories about the development of fa una and This is a contribution to the RAS Programs 23 and 28 and the zonal stratigraphy of the Jurassic and Neocomian the RFBR project 12-05-00453. of the Boreal Belt. - Soviet Geology and Geophysics 21: 6-18. References SHURYGIN, B.N., NIKITENKO, B.L., MELEDINA, S.V., et al. 2011. BRAGIN, V.YU., DZYUBA, O.S., KAZANSKY, & SHURYGIN, Comprehensive zonal subdivisions of Siberian Jurassic A.Yu. B.N. 2013. New data on the magnetostratigraphy of and their significance for Circum-Arctic correlations. the Jurassic-Cretaceous boundary interval, Nordvik - Russian Geology and Geophysics 52: 825-844. Peninsula (northern East Siberia).- Russian Geology ZAKHAROV, V.A., BoGOMOLOV, IL'INA, V. l., et al. 1997. Yu.l., and Geophysics 54: 329-342. Boreal zonal standard and biostratigraphy of the DZYUBA, O.S., IZOKH, O.P. & SHURYGIN, B.N. 2013. Carbon Siberian Mesozoic. - Russian Geology and Geophysics isotope excursions in Boreal Jurassic-Cretaceous 38: 965-993. 188 9th International Congress on the jurassic System - Abstracts

Ammonite biostratigraphy of the Pliensbachian-Tear-E·ian transition at Westgate, Nevada, USA

PAUL L. SMITH* & ANDREW H. CARUTHERS

Department of Earth, Ocean and Atmospheric Sciences, Universityof British Columbia, Va ncouver V6T 1Z4, Ca nada; Email: psmith@eos. ubc.ca, [email protected]

*Corresponding author

The Pliensbachian-Toarcian interval is currently dealing with the geochemistry of the succession of significant interest because it appears to at Westgate in the Clan Alpine Mountains of record a multi-phased, global, second-order west-central Nevada. mass extinction that may be linked to the The Jurassic succession exposed at environmental stresses imposed by eruptions Westgate was first mapped in detail by within the Karoo-Ferrar large igneous CoRVALAN (1962). The lithostratigraphic units province (PALFY & SMITH 2000; CARUTHERS et he recognized that subsequently yielded the al. 2013). This poster and its accompanying Pliensbachian-Toarcian ammonites described paper contribute to our understanding of the here are now assigned to the Mina Peak Member Pliensbachian-Toarcian time scale, an important of the Sunrise Formation (TAYLOR et al. 1983). tool fo r comparing geochemical data sets from The Sunrise Formation is part of a regressive across the globe and fo r developing hypotheses sequence that in the Shoshone and Gabbs Valley to explore and explain the extinction event. ranges to the south ofWestgate is capped by the The work presented here accompanies and terrestrial deposits of the Pliensbachian Dunlap complements the poster by Caruthers et al. Formation. At Westgate, however, marine deposition continues into the Toarcian and probably into the Middle Jurassic. Radiometric Northwest Western Age The Pliensbachlan ammonite zonation for North America Europe error North America has been described by SMITH a Va riabilis Crassicosta M (2a) et al. (1988) and the Toarcian zonation by Q) }AKOBS et al. (1994). There have been numerous =o "0 ....._-----ll-181.4 (+1.2/-1.2) supporting publications describing in detail c:� Bifrons Planulata the Pliensbachian and Toarcian ammonites CO "(j �-----il-182.0 (+3.3/-4.9) of Canada (e.g., SMITH TIPPER 1996 and .... & CO }AKOBS 1997) but, apart fo r the work of IMLAY Serpentinum � (1968), little attention has been focused on 2:"'- ro Kanense the ammonites of the conterminous United UJ Ten u icostatum States. The Westgate succession is of particular significance in this context because, when the

t-----�183.6 (+1.7/-1.1) North American Pliensbachian zonation was Spinatum Carlottense established, part of the Mina Peak Member u;"- c: was designated as a reference section for the .! � �---t-184.1 (+1.2/-1.6) 0.: ::> Margaritatus Kunae uppermost Pliensbachian Carlottense Zone (Fig. 1). '-----1-.185.7 (+0.5/-0.6) The Pliensbachian-Toarcian ammonite Fig. 1. The Upper Pliensbachian to Middle Toarcian North succession at Westgate consists of fo ur American ammonite zones recognized at Westgate, west­ assemblages. In ascending stratigraphic order central Nevada. Approximate correlations of the North they consist of: American secondary standard zones with the primary standard zones of Europe are indicated (adapted from (1) An association of species of Fa nninoceras SMITH et al. 1988: fig. 9; jAKOBS et al. 1994: fig. 12). Pliens. and Arieticeras assigned to the Carlottense Zone

= Pliensbachian. of the Late Pliensbachian (Fig. 1 ). 9th International Congress on the Jurassic System - Abstracts 189

(2) An association of species of Lioceratoides, Palaeoclimatology, Palaeoecology, in press. Protogrammoceras, and Tiltoniceras. This IMLAY, R.W. 1968. Lower Jurassic (Pliensbachian and Toarcian) ammonites from eastern Oregon and association is also assigned to the Carlottense California. - United States Geological Survey Zone because it occurs below the first Professional Paper 593 C: 1-51. dactylioceratids and, in Canada, it includes JAKOBS, G. 1997. Toarcian ammonoids from North America. species of Fa nninoceras, Arieticeras, and - Geological Survey of Canada Bulletin 428: 1-137. Amaltheus. JAKOBS, G., SMITH, P. L. & TIPPER, H.W. 1994. An ammonite zonation for the Toarcian (Lower Jurassic) of the (3) An association of the hildoceratids seen North American Cordillera. - Canadian Journal of in assemblage 2 with species of Dactylioceras Earth Sciences 31: 919-942. and Nodicoeloceras?, assigned to the Early PALFY, J. & SMITH, P. L. 2000. Synchrony between Early Jurassic extinction, oceanic anoxic event, and the Toarcian Kanense Zone (Fig. 1 ). Karoo-Ferrar flood basalt volcanism. - Geology 28: (4) An association of depressed 747-750. dactylioceratids representing Peronoceras and SMITH, P. L. & TIPPER, H.W. 1996. Pliensbachian Catacoeloceras, assigned to the Planulata Zone biostratigraphy and ammonite fa una of the Queen of the Middle Toarcian (Fig. 1). Charlotte Islands, British Columbia. - Bulletins of American Paleontology 108: 1-122. SMITH, P. L., TIPPER, H.W., TAY LOR, D.G. & GUEX, J. 1988. A Lower Jurassic ammonite zonation for Canada and the References United States: the Pliensbachian. - Canadian Journal CORVALAN, J. 1962. Early Mesozoic stratigraphy of the of Earth Sciences 25: 1503-1523. Westgate area, Churchill County Nevada. Ph.D. thesis, TAY LOR, D.G., SMITH, P. L., LAWS, R.A. & GUEX, J. 1983. Stanford University, California, 224 p. The stratigraphy and biofacies trends of the Lower CARUTHERS, A.H., SMITH, P. L. & GROCKE, D. 2013. The Mesozoic Gabbs and Sunrise formations, west-central Pliensbachian-Toarcian (Early Jurassic) extinction, Nevada. - Canadian Journal of Earth Sciences 20: a global multi-phased event. - Palaeogeography, 1598-1608. 190 9thInternational Congress on the Jurassic System - Abstracts

Ichnology of the Callovian-Oxfordian of Katrol Hill Range, Southwest of Bhuj, Kachchh, western India

*, 2 PARAS M. SOLANKI1 NISHITH Y. BHATT\ SATISH ). PATEL & )AGDISH M. PATEL3

1Department of Geolog� M. G. Science Institute, Ahmedabad - 380 009, Gujarat, India; Email: parasso/[email protected], [email protected]

2Department of Geo/og� M. S. University of Baroda, Va dodara - 390 002, Gujarat, India; Email: sj pgeology @g mail.com 3Department of Geology, Shri R. R. La/an College, Bhuj, Gujarat, India; Email: [email protected]

*Corresponding author

Callovian to Oxfordian rocks are well exposed All fades types are highly bioturbated in the northern part of the Katrol Hill Range except the grey shale fa des, and the maximum abundance of trace fossils was observed in a of Mainland Kachchh (BHALLA & ABBAS 1978). The rocks are lithostratigraphically classified as succession of interbedded shale, siltstone, and jumara Formation and further divided into four sandstone. Apart from incomplete and collapse informal members, from I to IV in ascending structures, trace fossils include Acanthorhaphe order (BISWAS 1977, 1993). The studied incerta, Arenicolites carbonarius, A. isp., sections of the jumara Formation lie southwest Beaconites coronus, Bergaueria perata, B. isp., of Bhuj in the Katrol hill range, where except the Biformites insolitus, B. isp., Calycraterion lower part of the Member I all members are well samsonowiczi, Chondrites targionii, Circu/ichnus developed. Member I consist of shales, with thin isp., Dendrotichnium 1/arenai, Didymau/ichnus bands of greyish limestone containing small isp., Diplocraterion paral/elum, Dolopichnus bivalves and becoming cherty in the upper part. gulosus, Fustiglyphus annulatus, G/ockeria

The upper boundary of Member I is fixed at a glockeri, Gy rolithes . isp., Helminthopsis isp., fe rruginous sandstone band. The lower part of Impqnoglyphus torquendus, Lockeia siliquaria, Member 11 is characterised by highly bioturbated Megagrapton irregulare, Micatuba verso, shale-siltstone intercalations, while the upper Monocraterion isp., Nereites imbricata, part consists of thick, hard, medium to coarse Ophiomorpha nodosa, 0. annulata, Palaeophycus sandstone which marks the upper boundary of alternatus, P. annulatus, P. heberti, P. striatus, Member 11. Member Ill mainly consists of shale P. su/catus, P. tubularis, Paleomeandron isp. with thin bands of limestones and siltstones. aff. P. robustum, Parahaentzschelniia arde/ia, Member IV is dominated by shales in its lower Phoebichnus trochoides, Phycodes circinnatum, part, while the top part consists of oolitic P. curvipalmatum, P. palmatum, Phymatoderma limestones (Dhosa Oolite) forming a distinct isp.,Protovirgulariacf.dichotoma,Psammichnites marker horizon which separates the jumara plummeri, Rotamedusa roztocensis, Skolithos Formation from the Jhuran Formation (BISWAS linearis, Steigerwaldichnium heimi, Stel/ascolites 1977). radiatus, Ta enidium serpentinum, T. satanassi, The exposed succession has a thickness of Te ichichnus rectus, Tha/assinoides suevicus, T. about 234 m comprising various sedimentary horizonta/is, Zoophycus brianteus, Z. circinnatus, rock units which can be divided into six and Z. vi/le. litho fades based on sediment and bedding plane The rich and highly diversified trace fo ssils characteristics, grain size, and sedimentary revealed a wide range of animal behaviours structures. They are the Intercalated Calcareous represented by dwelling, feeding, crawling, and Shale Siltstone Fades (ICSSF), Limestone Fades resting structures. Horizontal feeding structures (LF), Ferruginous Sandstone Fades (FSF), are found abundantly in all lithofades indicating Massive Felspathic Sandstone Fades (MFSF), low wave and current energy for deposition Grey Shale Fades (GSF), and Oolitic Limestone of poorly sorted muddy to sandy sediments. Fades (OLF). However, a few coarse layers containing 9th International Congress on the jurassic System - Abstracts 191

Arenico/ites, Ophiomorpha,andSko/ithosindicate The high diversity and abundance of exploitation of the sediment by opportunistic deposit-feeding structures suggest availability animals under intermittently moderate wave of organic-rich and oxygenated substrates for and current energy or storm-wave conditions in colonization of endobenthic communities. the shoreface zone. Unlined backfill structures The sedimentological characteristics of the such as Ta enidium in ICSSF and MFSF of lithofacies and presence of trace fossils indicate Member I and 11 indicate more distal regions fluctuations of the sea level from the middle and record oxygenated quiet waters and stable, shoreface to offshore zone during deposition continuous, slow deposition and bioturbation of the Callovian to Oxfordian sediments of the yielding complex bioturbate textures (FREY et al. Jumara Formation. 1990). Thalassinoides burrows are dominating in intercalated sandstones and shales as well as in thick sandstone lithofacies (ICSSF,MFSF and References FSF) of Member and Ill. These large, semi­ BHALLA, S.N. & ABBAS, S.M. 1978. jurassic fo raminifera 11 from Kutch, India. - Micropaleontology 24: 160-209. permanent, mainly horizontal tunnel systems BISWAS, S.K. 1977. Mesozoic Rock-Stratigraphy of Kutch, suggest deposit-feeders as producers and Gujarat. - Quarterly Journal of the Geological, Mining probably represent the lowest energy levels and Metallurgical Society of India. 49 (3 & 4): 1-52. (FORSICH HEINBERG 1983) in the shoreface. BISWAS, S.K. 1993. Geology of Kutch: 52-98, K D. Malaviya & Institute of Petroleum Exploration, Dehradun. Zoophycus is characteristically found in BROMLEY, R.G. 1990. Trace fossils. Biology and taphonomy: OLF of Member IV and together with various - 280 pp., Unwin Hyman, ichnospecies of Chondrites, Rhizocorallium, FREY, R.W., PEMBERTON, S.G. & SAUNDER, T. D.A. 1990. Thalassinoides, Ophiomorpha etc. Zoophycus is Ichnofacies and bathymetry: a passive relationship. - an opportunistic ichnospecies which appears journal of Palaeontology 64: 155-158. FORSICH, F.T. & HEINBERG, C. 1983. Sedimentology, together with Chondrites in opportunistic biostratinomy and palaeoecology of an Upper jurassic situations of low-resource, inhospitable offshoresand bar complex. - Bulletin of the Geological oxygen-depleted environments (BROMLEY Society of Denmark 31: 6 7-9 5. 1990). Sediments thoroughly bioturbated by PATEL, S.J., DESAI, B.G. & SHUKLA, R. 2009. Paleoecological significance of the trace fossils of Dhosa Oolite the producer of Zoophycus indicates fairly low Member (Jumara Formation), Jhura Dome, Mainland sediment input below the storm wave-base in Kachchh, Western India. - journal of the Geological offshoreareas (PATEL et al. 2009). Society of India. 74: 601-614. 192 9rh International Congress on the Jurassic System - Abstracts

Response of Jurassic strata of Kachchh to Quaternary tectonics in an active intra-plate basin of Kachchh, western India

M. G. THAKKAR

Department of Earth and Environmental Science, KSKV Kachchh University, Bhuj-Kachchh-370001, India; E-mail: [email protected]

Kachchh is a peri-cratonic riftbasin generated Bhuj fo rmations cap the earlier rocks resisting in Late Triassic Period during the break-up them for erosion, while Jumara and Jhuran shale of Gondwanaland. The tectonic regime was fo rmations are exposed as bumpy grounds normal, hence the early basinal faults fo rmed against the scarps ..Kaladungar and Khadir half-graben basin. Post-Cretaceous Indo­ formations also preserve the neotectonic Eurasia collision along with plutonism and sub­ features in Pachchham, Khadir, Bela and Rapar aerial volcanism started reverse tectonics of uplifts. The response to Quaternary tectonics the Kachchh Basin, resulting into the uplift of is reflected as bedrock gorges, gullies, scarps all the Jurassic and Cretaceous strata exposing and triangular facets in the Jurassic strata. them on to the surface. Tertiary period, once The author has explored them critically and again, witnessed large scale transgressive and classified with respect to their cohesiveness. regressive deposits at the open end of the basin, The active fronts of KMF - Kachchh Mainland while fast upliftof Jurassic strata to the margin Fault, KHF - Katrol Hill Fault and IBF - Island of the craton on the landward side. Quaternary Belt Fault exhibit precipitous scarps where period shaped the present day landscape of hard limestone and sandstone caps, while the Kachchh exposing various features in jurassic core region of the domes along the master faults strata and revealed its complete stratigraphy. makes hummocky grounds where shale fades Depending on the nature of rocks, they form dominate. Southern slopes of all the uplifts peculiar geomorphic features. Jhuran (Katrol) are characterized by the bedrock gorges in Formation in Katrol Hill range fo rmed straight sandstones. The scarp recession is more where mountain fronts and ideal triangular fa cets along coh'esive and compact rocks are less and more the Katrol Hill Fault. In the dome dominated triangular fa cets, while the compact rocks show northern hill range of Kachchh Mainland, the straight mountain fronts. scarps have been developed where Jhuran and 9th International Congress on the Jurassic System - Abstracts 193

Untangling real from apparent seawater temperature variability during the Late Jurassic

ADAM TOMASOvYCH1 * DORRIT }ACOB2• 3, MICHAEL }OACHIMSKI4, MATTHIAS LOPEZ CORREA5, }AN SCHLOGL6

1Geological Institute, Slovak Academy of Sciences, Dubravska cesta 9, 84005 Bratislava, Slovakia; Em ail: [email protected] 2/nstitut fiirGeowis senschaften,]o hannes Gutenberg-UniversitiitMainz , 55099 Mainz, Germany 3 Department of Earth and PlanetaryScien ces, Macquarie University, Level 5, E7A Building, NSW 2109 Australia; Email:[email protected] 4GeoZentrum Nordbayern, UniversitiitErlan gen-Nilrnberg, Schlossgarten 5, 91054 Erlangen, Germany; Email: michael.joachimski@fa u.de 5GeoZentrum Nordbayern, Universitiit Erlangen-Nilrnberg, Loewenichstrasse 28, 91054 Erlangen, Germany; Email: [email protected] 6Department of Geology and Paleontology, Comenius University, Mlynska dolina G, 84215 Bratislava, Slovakia; Email: sch/og/@fn s. uniba.sk

*Corresponding author

Latitudinal and bathymetric variation in MS and micromill. We constrain the analyses temperature in present-day oceans is one of to two multicostate rhynchonellid genera that the major factors determining distribution have similar life habits and morphology. First, patterns and diversity of marine organiSIJlS, we compare the 6180 composition and Mg/Ca and estimating the temperature variability in brachiopods from shallow- and deep-shelf in past oceans is thus crucial in studies environments that lived during one ammonite that seek to explain major evolutionary, zone (Epipeltoceras bimammatum Zone), thus palaeobiogeographic, and palaeoecological effectivelyquantifying the bathymetric gradient patterns. However, palaeotemperature in temperature. Second, we assess the temporal estimates based on oxygen isotopes strongly change in 6180 and Mg/Ca of brachiopods suffer from uncertainties related to weak that inhabited deep-shelf environments over constraints on spatial variation in seawater -4 Myr during the Late Oxfordian to Early 6180 composition. Other geochemical proxies Kimmeridgian. are thus needed that can better constrain past During the Late Oxfordian Epipeltoceras seawater temperatures. bimammatum Zone, brachiopods from the One of such proxies that remain weakly used shallow shelf (coral reefs ofthe Swiss and French in analyses ofJurassic seawater temperatures is Jura Mts.) have a consistently higher Mg/Ca represented by the Mg/Ca ratio of brachiopod ratio (by 3-4 IJ.molfmol) and lower 6180 values shells. Our preliminary analyses of Recent (by -0.5 to -1 %o) than brachiopods from deep­ brachiopods imply that although temperature shelf habitats (sponge mounds of the Swabian sensitivity of Mg/Ca is rather low and Mg/ and Franconian Alb). These shallow and deep Ca values can differ among brachiopod taxa water habitats were located at similar latitudes sampled in the same habitat, brachiopod shells (25°-30°N) on the northern Tethys shelf (with do capture seasonal temperature variations and individual localities separated by no more than can detect large-scale temperature differences -500 km in longitudinal direction). The oxygen among different locations. isotope analyses imply a -4°-5°C temperature Here, we focus on temperature estimates difference between coral-reef habitats located derived from 6180 and Mg/Ca of Late Oxfordian above storm wave base and sponge habitats and Early Kimmeridgian brachiopod shells from located below storm wave base. Interestingly, the northern Tethys shelf analysed using high­ brachiopod communities show a marked shift resolution sampling of the shells with LA-ICP- in species and genus composition at this depth 194 9th International Congress on the Jurassic System - Abstracts level, indicating that temperature stratification precipitation ratio leading to salinity changes) could be a major driver of regional-scale rather than changes in temperature per se. brachiopod distribution. Importantly, brachiopod communities that Over the course of the Late Oxfordian occupied deep-shelf environments during to Early Kimmeridgian, brachiopods that this time interval were stable in terms of occupied deep-shelf environments with sponge their taxonomic composition and abundance mounds show remarkably stable Mg/Ca ratios patterns, and never grade into brachiopod (2-4 �molfmol). However, we observe also a communities that inhabited coral reefs in the trend towards more negative 8180 values with same region, supporting the hypothesis that Kimmeridgian shells showing similarly low trends based on 8180 composition ofbrachiopod 8180 values as Late Oxfordian shells from coral­ shells are decoupled from temporal changes in ( 8180 reefs = -1.5 to -1 %o). We hypothesize that temperature. 8180 the discrepancy in the Mg/Ca and trends This research was supported by the Slovak Research and largely imply temporal changes in seawater Development Agency (APVV 0644-10) and by the Scientific 8180 composition (e.g., change in evaporation/ Grant Agency (VEGA 0068/11). 9th International Congress on the Jurassic System - Abstracts 195

Ichnological record of food content change in Middle-Upper Jurassic pelagic sediments of the Fatricum domain in the Tatra Mountains, southern Poland

ALFRED UCHMAN* & RENATA }ACH

Institute of Geological Sciences, jagiellonian University, Oleandry2a, 30-063 Krak6w, Poland; Em ail: a/[email protected]; [email protected]

*Corresponding author

The general offshoredecrease in food content in shelf trough slope to basin plain in pelagic sediments is one of the basic ecological factors and hemipelagic sediments between phases of influencing benthic life. It is expected that this incidental sedimentation, mostly turbidites. paradigm influences burrowing organisms Abundance and diversity of trace fossils and hence it is reflected in the ichnological generally decrease stratigraphically up the record. This hypothesis is verified in the studied succession. In the lower part, most Jurassic sediments of the Fatricum domain beds of grey limestones and marls and the (Krizna Nappe) in the Tatra Mountains (West lowermost part of radiolarites display typical Carpathians, southern Poland) which show spotty structures, i.e. sections of beds are a gradual deepening from nearshore to deep characterized by relatively dense and diverse sea environments below CCD. The deepening cross-sections of trace fo ssils visible as variable was conditioned by opening of the Western spots. Chondrites, Planolites, Thalassinoides, and Tethys, further rifting, and the general Jura�sic Zoophycus are common. Other trace fo ssils are · transgression. rare or very rare in this and other parts of the During the latest Early Jurassic extensional studied interval. block tilting formed a horst and graben Up-section, in the upper part of radiolarites topography in the Western Carpathians, which and red nodular limestones, the spotty character persisted until the end of the Middle Jurassic. of sediments is less distinct and may nearly Subsiding basins were constantly filled with completely disappear, i.e. the spots decrease grey spotted limestones and marls, fo llowed in density, contrast, and diversity. In several by grey nodular limestones with Bositra, while beds any trace fo ssil can be seen; they display horsts acted as submarine palaeo-highs with bioturbational structures or are massive. condensed carbonates with glauconite and The commonest trace fo ssils are Chondrites Bositra-crinoidal limestones. Upper Jurassic and Planolites. Thalassinoides and Zoophycus rocks record a post-riftthermal subsidence and are rarer and trace fossils are generally less continuous deepening with sedimentation of compressed than in the lower part ofthe studied monotonous bio-siliceous-carbonate fa des. The interval. The changes are not ideally linear, but Upper Jurassic succession consists of pelagic fluctuations in these fe atures do not discard the sediments, mainly radiolarites, red nodular general trend. limestones, and platy micritic limestones. The changes are not related to grain size or These sediments are almost totally bioturbated. lithology of the sediment. Silicification can mask Primary lamination is rare and limited to a few primary structures in some beds. More regular thin horizons. diagenetic disturbance occurs in red nodular Ten recognized ichnogenera include limestones, in which trace fo ssils are preserved fo dinichnia (Zoophycus, Te ichichnus, Phycodes), only within the nodules. However, this process chemichnia ( Chondrites, Trich ich n us), pascichnia does not influence the general trend in the (Planolites, Phycosiphon), and domichnia­ distribution of trace fo ssils. fo dinichnia (Thalassinoides). They represent Primary lamination occurs only in a few the Zoophycus ichnofacies, which occurs in thin horizons in the studied deposits and is different marine settings from the deeper not associated with sediments darker than in 196 9thInternational Congress on the jurassic System - Abstracts other horizons. It can be referred to incidental organisms penetrated deeply in the sediment, rapid sedimentation, as is indicated by a subtle where distinct trace fossils were produced. The increase in grain size. This excludes changes thicker layer of nutritional sediments provided in oxygenation of pore water as the significant an ecospace fo r a higher diversity of burrowing factor controlling the ichnofauna. Instead, the organisms. changes of ichnological features in the studied In more oligotrophic conditions (higher interval are caused rather by a decrease in food part of the succession), the organic matter was content in the sediments. With deepening of concentrated in the soupy sediment near the the basin and decreasing sedimentation rate sediment-water interface, where preservation associated with generally advancing flooding of distinct trace fossils was impossible. Only of epicontinental areas, less and less fo od was in some beds, organisms penetrated deeper supplied to the basin from shallower areas. and produced trace fo ssils. Thus, diversityand Less and less organic matter was buried with abundance of trace fossils can be used as a proxy decreasing sedimentation rate and increasing of the trophic level in pelagic sediments. in distance from the shelf. In more eutrophic This research has been financed by the grant N N307 conditions (lower part of the interval), 016537. 9th International Congress on the Jurassic System - Abstracts 197

First contribution to precise biostratigraphy of Upper Tithonian rocks fromthe Ve racruz Basin (SE Mexico)

ANA BERTHA VILLASENOR1 FEDERICO 0L RI 2 & O Z

1Departamento de Paleontologia, Universidad Nacional Aut6noma de Mexico, 0451 0, Mexico, D.F. Mexico; Email: [email protected] 2Departamento de Estratigrafia y Paleontologia, Universidad de Granada, 18071 Granada, Spain; Email: fo [email protected]

Tithonian rocks are among those of greater Other authors working on the same precise potential fo r hydrocarbons sources in Mexico. ammonite-horizon-biostratigraphy approach The Pimienta Fm consists of more or less were Addate and collaborators (ADDATE et al. calcareous silt- and claystone with clayey to 1992 to 1996). Updated revisions based on this shaley intercalations and local development approach were provided by VILLASENOR et al. of concretions. These deposits are late (2000a, 2012). Tithonian in age and accumulated in low­ Since the earliest twentieth century up oxygenated sea bottoms across eastern Mexico to date, variable combinations of ammonite (outcrop and subsurface successions with genera such as Hap/oceras, Acevedites, reported thicknesses of 3.5 to 100 m and 20 Proniceras, Corongoceras, Micracanthoceras, m, respectively) and the western Gulf Rim Suarites, Wichmanniceras, Mazatepites, so­ (subsurface and offshore sites approximately20 called Kossmatia, Durangites, Substeueroceras, m in thickness.). Deposits of equivalent age in Paradontoceras, and Salinities have been central and northern Mexico belong to the interpreted to represent the Upper Tithonian in La Caja and La Casita formations (reported Mexico (for extended revision see VILLASENOR thicknesses between 10-15 and 200 m), which et al. 2012). However, information about represent a distal to proximal sedimentary bed-by-bed sampling and the corresponding succession under slightly more oxygenated reference to detailed stratigraphic columns sea bottom conditions, respectively. More of Upper Tithonian rocks is found in less than calcareous sediments correspond to the La 25% of the published papers, and no published Caja Fm. while sandy and silty limestones and information exists with precise Upper Tithonian siltstones correspond to the La Casita Fm. biostratigraphy from the Veracruz Basin in ESE Except fo r outcrops in north-central Mexico, Mexico. macro- and microfossil assemblages of late Following interpretations initially proposed Tithonian age have been largely collected from by OLORIZ (1987, 1992), a large part of the areas belonging to sedimentary basins with problems, or uncertainty, with Upper Jurassic economic interest (hydrocarbon sources). biostratigraphy and precise correlations in Since the earliest twentieth century,research Mexico relates to habitat patchiness in neritic on uppermost Jurassic deposits from Mexico environments with irregular, unstable bottom fo cused on biostratigraphy characterizing physiography that accentuated the differential ammonite assemblages, and less commonly influence of relative sea level fluctuations on calpionellid assemblages (Fig. 1). BURCKHARDT ecospace availability fo r ammonites. Resulting (1906, 1930),1MLAY(1939, 1980),BONET (1956), environmental heterogeneity, endemism, and R A CANTU-CHAPA (1963, 1967, 1976), VE M & dominant r-strategy in ammonites completed WESTERMANN (1973), and TREJO (1980) are the picture determining the difficulty representative examples of the "Capas de" or fo r reproducibility of precise homotaxial "Ammonite Beds" biostratigraphic approach. successions (e.g., VILLASENOR et al. 2012 fo r A turning point towards precise ammonite­ extended treatment). Potential, local hiatuses horizon-biostratigraphy was the Ph.D. thesis related to erosion or non-deposition are not of one of the authors (VILLASENOR 1991), then conclusively known yet. followed by later papers with collaborators. In such a context, the first precise, combined 198 9th International Congress on the Jurassic System - Abstracts information about Upper Tithonian deposits lines in pauci-specific ammonite assemblages. and fossil assemblages in SE Mexico (Veracruz Precise data about biostratigraphic ranges of State) is reported here on the basis of a bed­ ammonites such as Proniceras, Mazatepites, by-bed sampling during fi eld surveys in 2012 Durangites, and Salinites, together with other and 2013.The analysed section crops out 10 km inconclusively known ammonite taxa, have been southeastwards of the village of Tlapacoyan, collected. Additionally, microfacies analysis of within the so-called Veracruz Basin. The mainly peloidal rocks with silt-sized to fi ne­ ea. 20-m-thick section is well-bedded and and medium-grained bioclasts and common comprised of more or less calcareous siltstone recrystallization ( microsparite) provides and claystone with argillaceous to shaley information about the biostratigraphic ranges of intercalations (Pimienta Fm.) and a single tintinnoids such as Chitinoidella, Crassicol/aria, horizon with scarce calcareous concretions. and Ca lpionella. Macro-invertebrates other than ammonites are The obtained information provides a first bivalves (up to ea. 15°/o) and an insignificant step fo r providing precise biostratigraphy of number of gastropods, and rare brachiopods Upper Tithonian deposits outcropping in the occur in a condensed level at the top of the Veracruz Basin, but more research is needed section. Discontinuous ammonite horizons in other Mexican sections before its regional show commonly crushed inner moulds (leaf meaning and correlation potential within preservation) and no preservation of suture Mexico can be conclusively evaluated.

Fig. 1. Number of papers (PhD and undergraduate theses included) providing precise biostratigraphy based on bed­ by-bed sampling and reference to precise horizons in stratigraphic sections within the regions highlighted. Red star fo r location of the studied section. 9th International Congress on the Jurassic System - Abstracts 199

References 1-78. ADATTE, T., STINNESBECK, W., HUBBERTEN, H. & IMLAY, R.W. 1980. Jurassic paleobiogeography of the REMANE, J. 1992. The Jurassic-Cretaceous conterminous United States in its continental setting. boundary in Northeastern and Central Mexico - a - U.S. Geological Survey Professional Paper 1062: multistratigraphical approach. - VIII Congreso 1-134. Latinoamericano de Geologia, Salamanca, Aetas Tomo OLORIZ, F. 1987. El significado biogeogratico de las 4: 23-29. plataformas mexicanas en el Jurasico superior. ADATTE, T., STINNESBECK, W., REMANE, J. & HUBBERTEN, Consideraciones sobre un modelo eco-evolutivo. - H. 1996. Paleoceanographic changes at the Jurassic­ Revista de la Sociedad Mexicana de Paleontologia 1: Cretaceous boundary in the Western Tethys, 219-247. northeastern Mexico. - Cretaceous Research 17: 671- OLORIZ, F. 1992. North central and eastern Mexico. 689. In:. WESTERMANN, G.E.G. ( ed.). The Jurassic of the BONET, F. 1956. Zonificaci6n microfaunistica de las calizas Circum Pacific, part 4. - Biochronology 12: 100- cretacicas del Este de Mexico.- Boletin de la Asociaci6n 107,Cambridge University Press, New York. Mexicana de Ge6logos Petroleros 8: 389-488. TREJO, M. 1980. Distribuci6n estratigratica de Ios tintinidos BURCKHARDT, C. 1906. La faune Jurassique de Mazapil avec Mesozoicos Mexicanos. - Revista del Instituto un appendice sur les fossiles de Cretacique inferieur.­ Mexicano del Petr6leo 12(4): 4-13. Boletin del Instituto Geol6gico de Mexico 23: 1-217. VERMA, H.M. & WESTERMANN, G.E.G. 1973. The Tithonian Burckhardt, C. 1930. Etude systhematique sur le (Jurassic) ammonite fa una and stratigraphy of Sierra Mes6zoi'que mexicain. - Memoires de la Societe de Catorce, San Luis Potosi, Mexico. - Bulletin of the Paleontologique Suisse 49-50 : 1-279. American Paleontology 63(277): 107-320. CANTU-CHAPA, A. 1963. Etude biostratigraphique VILLASENOR, A.B. 1991. Aportaciones a la bioestratigrafia, des ammonites du centre et de l'Est du Mexique basada en fa una de ammonites, de la sucesi6n del (Jurassique superieur et Cretace). - Memoires de la Jurasico superior (Kimmeridgiano-Tithoniano) del Societe Geologique de France 42 (4): 1-102. area de Mazapil, Zacatecas, Mexico. Unpublished PhD. CANTU-CHAPA, A. 1967. El limite Jurasico-Cretacico en Thesis, Facultad de Ciencias, Universidad Nacional Mazatepec, Puebla (Mexico).-Instituto Mexicano del Aut6noma de Mexico: 154 p. Petr6leo, Secci6n Geologia, Monografia 1, Publicaci6n VILLASENOR, A.B., OLORIZ F. & GONZALEZ-ARREOLA, 2000. c. No. 7 AI-11: 3-24. Recent advances in Upper Jurassic (Kimmeridgian­ CANTU-CHAPA, A. 1976. El contacto Jurasico-Cretacico, la Tithonian) ammonite biostratigraphy from North­ estratigrafia del Neocomiano,.el hiato del Hauteriviano Central Mexico. Based in new collected ammonite superior-Eoceno inferior y las amonitas del pozo assemblages. - GeoResearchForum 6: 249-262. Bejuco. - Boletin de la Sociedad Geol6gica mexicana VILLASENOR, A.B., OLORIZ, F, LOPEZ PALOMINO, I. & L6PEZ­ 37: 68-83. CABALLERO,I.2012.Updatedammonitebiostratigraphy IMLAY, R.W. 1939. Upper Jurassic ammonites from Mexico. from Upper Jurassic deposits in Mexico. - Revue de - Bulletin of the Geological Society of America 50: Paleobiologie, Vol. spec. 11: 249-267. 200 9th International Congress on the Jurassic System - Abstracts

Foraminiferal zonation of the Jurassic of theCaucasus and Precaucasus

VA LERY JA. VUKS

Federal State Unitary Enterprise 'i1.P. Ka rpinsky Russian Geological Research Institute" (FGUP "VSEGEI''), Sredny pr. 74, St.-Petersburg 199106, Russia; E-mail: Va lery_ Vu [email protected]

The first fo raminiferal zonal schemes for the assemblages, these local zones can be traced Jurassic of the Caucasus were offeredin the 50s in the above mentioned zones of the Western of the last century. They partially are reflected Caucasus and Pre-Caucasus also that found in the regional stratigraphic schemes on the their reflection in the presented scheme. Jurassic of the Caucasus which were published Thus, all published foraminifer-based zonal in 1984 (ROSTOVTSEV & KRYMHOLTZ 1984). schemes can be compared with ammonite Recent geological research, including the zonations and the International Stratigraphic production of a new generation of geological scale (Figs 1, 2). It should be noted that zonal maps, allowed collecting of a large number divisions are not established for all structural­ of new data which not always fit well within fades zones of the Caucasus and Pre-Caucasus. mentioned schemes. Therefore improvement Besides, in a number of structural-fades zones, of the stratigraphical schemes of the Jurassic for which foraminifer-based scales exist, of the Caucasus becomes an important task. foraminifer divisions do not cover the whole Within this task it is necessary to be precise and Jurassic interval either because of absence of work in detail on the biozonal schemes which foraminifers in these deposits, or because of are known and published. lack of foraminifer research. Reliability of zonal During the Early and Middle Jurassic boundaries has not yet quite proved because of time the North Caucasian basins are usually the rare occurrence of ammonites and existence considered as palaeo-basins with more or less of data with different degree of detail on the similar living conditions. Therefore, correlation distribution of foraminifers in some deposits. of these deposits as a whole does not create Attempts have · been made to compare essential problems (Azbel & GRIGELIS 1991; divisions of the International Stratigraphic ROSTOVTSEV 1992). Thus, though there are three scale and the zonal ammonite standard with foraminiferal zonal schemes for the Russian regional ammonite and foraminifer scales of part of the Caucasus, it is possible to use as a the Caucasus (Figs 1, 2). These schemes can basis a foraminifer-based zonal scheme for the be considered as a basis for discussion and Western Caucasus and Pre-Caucasus (Fig. 1 ). improving of the regional stratigraphic schemes The Middle (Callovian) and Late Jurassic of the Jurassic of the Russian Caucasus. Caucasian basins are characterized by a high variety of fades and biotic assemblages that are References reflected in the large number of foraminifer­ AZBEL, A.Y. & GRIGELIS, A.A. (eds.) 1991. Prakticheskoe based zonal schemes which cannot be united rukovodstvo po microfaune SSSR. T. 5. Foraminifery mezozoya [Practical manual on microfauna of the in a single scale (Fig. 2). Four foraminiferal USSR. V. S. Mesozoic foraminifers]. 375 p., Nedra, zonal schemes are known in the mentioned Leningrad (In Russian). stratigraphic interval of the Western Caucasus GRIGELIS, A.A. ( ed.) 1982. Biostratigrafiya verkhneyurskikh and Pre-Caucasus (Laba, Lagonaki, Abino­ otlozhenii SSSR po foraminiferam [Upper Jurassic Gunajskaya, and Novorossijsko-Lazarevskaya biostratigraphy ofthe USSR according to foraminifera]. 173 p., Mokslas, Vilnius (In Russian). zones) and one such scheme exists for the RosTOVTSEV, K.O. (ed.) 1992. Yura Kavkaza [Jurassic of Central and Eastern Caucasus (GRIGELIS 1982; Caucasus]. 192 p., Nauka, St.Petersburg (In Russian). AZBEL & GRIGELIS 1991; VUKS 2004, 2007). The ROSTOVTSEV, K.O. & KRYMHOLTZ G.Y. (eds.) 1984. Haplophragmium coprolithiforme Local Zone Reshenie 2 Mezhvedomstvennogo regional'nogo stratigraficheskogo soveshchaniya po mezozoyu and the Labalina costata - Lenticulina tumida Kavkaza (Yura) 1977 g. [Decision of the Second Local Zone are established in the Laba Zone, but Interdepartmental Regional Stratigraphic Conference judging by composition of coeval foraminiferal on Mesozoic of the Caucasus (Jurassic) 1977]. 47 p., 9th International Congress on the Jurassic System - Abstracts 201

International Biozonal Regional biostratigraphic subdivisions and General ammonite Straigraphic standart scale (2006, 2012• . . 8.1ostrat1grap h1e d Foraminifers (local zones) lu Jurassique Quest E & Europeen et Medi- Ammonites tn "' CD CD terraneen, 1997; -In The Jurassic Western Caucasus Central and Calcareous >. -� m ! of Cl) and Precaucasus Eastern Dagestan � � � G�:�Taa:�. ���3 Caucasus

Q)... C/ydoniceras discus ? ? ? 1-- --1 c g �0�x-y-ce-n�1 �e s-- "' "2 ------orbis 0 �-rQ) �r ,...... , ..t: Procerites hodsoni !f.Aorrisiceras morrisi - :::0 "' � T. subcontractus m c Pr. proaracilis Aspnmctttes tenuip/icatus rvvv-vvvvv�v""V vvrv � vv Qutnqu�locullna lrO. il a lc m - - - Zigzagiceras Parkinsonia b c r u ---- -;..1.- - . . mtcra . �- pereg" na - ztgzag wurlembengtca -l\a to;i" 1i0ii11 - o�en ta �s -.R . l-- __ ----l l------l p n a r S. oer/ucida -+--+---___ im2fMO...f!lll1,�e:; c;onogtoDtgerma P. parkinsoni Parkinsonia parkinsont minima Recu ot es 1-----,------1 1----=----:-. ----t"""'SUbtamar Ciie1Ta -1 � dagestanica Garantiana Garan�tana caucastcu_s - H. \· K renko i _ _ J..eL'll!fl...ll11_ _ apto ella garantia garan ana . . _ '§JII.u..u 1 :::t� na tt htha 1 mt d t um M!gJU eoistominoides 1 :i Str. niorlense 0P 0. balcartcum ·c::; s Strenoceras niorlense caucasicum caucasica 0 _V tephanoceras "'\ S. G. Hyperammina humphnestanum \liirneu71inoiaasw; neumnoiaeS ... tchegemensis- tchegemensis- labaensis­ "Ci Otoites sauzei otoites sauzei Lenticulina m �::. J1f.Iaevtuscuta ' Ophthalmidium �p�, hthalmidium ::>onmma ovalts Wttchellia-- laeviuscula balcaricum auCJ!sfE.u mamillaris ..9 t---r,,....--.,.,,....-- ,.....-""l"l""""-1 \ _} rr.� !!!,'- H. discites Hyp erttocera� dtscttes ---- - .,u5Tamarckelrd 1-- - ? -- - --+--+----,"""__...,..__-r.-- -1 kaptorenkoae - ---- ... G!iaphoce as Graphoceras . _ _ _ - . Astacolus c Q) -lc�otn�c ar .IUL1Vw£L mL.L...- _d----"Q[Jj� '.JJJl.L ---4- _ _ _ tchegemica . "' c. l-- _ _ Nubeculinella btcostataeformts ·c: c. Brasilia - Sublamarckella CD :::t Ophthalmidium �infraoolithica 1 bradfordensis Brasilia bradfordensis kaptorenkoae -; infraoolithicum ... R.eth lielt a- Q) Ludwigia '! .'! kaptorenkoae c( � Ludwigia murchisonae ltdl}ae - ______0 murchisonae ...J Op hthifmTcliiim- Recurvoides Cornuspira orbicula Leioceras opalinun Leioceras opalinum mamontovae baksanicus • Lenticulina - , psekentchiensis ... 1 Ptevdellta aatensts Ptevdellta aatensts L;;,tkunn;t�r-: LentTCulina (.) Q) _ c. u. pseudoradtosa ...... uumomena toarcense ·u; c cense - Lenticulim ...... - - - / In "' c. t-'ntyseogrammo- Lenttcu1 ma "' :::t (.j_ rnouarsense orbignyi elongata ... ·c::; l'cerasdiso ansum/ habarovae ... rnouarsense Haugta va natJtlls ::;:, "' (.j_ 1 .., ... N-faugia variabilis/ Hildoceras bifrons Haplophragmoide� Haplophrag------.-- praeconvexus - moides prae- {2. r-...Hildoceras bifron:l' r- 0; sero�nrmum H!_fP!3._C e.!_a�a�t�ru� A. asper- convexus - ...J H. r-- \ 1 Dactyltoceras Dacty/ioceras Trochammina (tmmodiscusl tenwcostatum / '-.S.JI Uamataformi§/ c ... I' semicelatum .../ \...... !!S�r_ _J Q) PI. spinatum ...... -- "' c. - -?- C-;;;.n� l;;;ull na :c c. r-- -- (.) Amaltheus - Amalthe us bakhensis :::t ______"' margaritatus margaritatus ? .Q --- - In - ? --- Cornuloculina c ... -P. davoei-- - Q) 1-- ---::,...... ,-:- - - - - .:....- - - - - orbiculare .! � ---l ---- - ? 0 Tr. ibex Tragophx!J�_£e@_s_!E� r- - a: ? ...J Uptonia jamesoni - UjJfOma Jamesom, 1--c-+ --+-E--,--. -__----1 f;!f12P!s1.ogpr� IOPhlfialmiilium- ... "' ... . ancostatum �TJS1.ri.J:lj, . CD Q) 1---=., --:- --1 �chtoceras decltvus, concen tncum/ ·.:::: c. -- - 0 · I'-. ::;:, c. o. oxynotum xynot tceras cornwoculma �0 :::t E A. obtusum _oxynotum, I' c/ausa ...J CD ...... c ... Mtcroderoceras _ _ - -? - - _/ Q) Caenisites tumeri __ _ u; � ..J:Jia;hL 0 A. semicostatum ? ...J Arietites bucklandi """"=-c -t-:--+... ------1 /"'\ Q) �h.(":' 0 0 ..("_A/"'\/"'\//"' I"... A �'"'� /\ r. f'\/'\/ "' c. Schlotheimia ·a, c. c :::t angulata "' ... Alsatites liasicus :t:CD ::I: ;0 ...J Psiloceras planorbi5 �

Fig. 1. Biostratigraphic zonation of the Lower and Middle Jurassic of the Russian Caucasus. 202 9th International Congress on the Jurassic System - Abstracts

International Biozonal and General ammonite Regional biostratigraphic subdivisions Straigraphic standart scale (2006, 201 �) Biostratigraphie du Jurassique Quest - Q) Foraminifers C) Europeen et Medi- E fl) Q) ea G) G) C) terraneen, 1997; 'i: ea ...fl) Ammonites Western Central and ...fl) G) The Jurassic of ... .c Eastern >. ::::s Denmark and Caucasus UJ UJ UJ Caucasus UJ 2003 (' Durangites / ? Quinque oculina vulgaris ,______verbizhiensis - r - Trocholina e/ongata Cl) 1 � � • zone E Paraulaco- Parau/acosphinctes 1 o 0-eQ) ;::, sphinctes 10 � ...CP o ..... transitorius ,s s:: transitorius 1 111 �------CL t:: CO local zone CL 1§ :2 ? :::J COe 0 �o l�o;S::: ------Trocholina ex gr. - -� >------1� � �E solecensis - c: Simplisphinctes I CP Lithacoceras L � Textularia ea - densa local zone '20 albulus 1 = '�'Micracanthoceras" ponti \ I CP local zone ,______..! j:: Semiformiceras fa llauxi ;:; ? "C ------i S. semiforme Lithacoceras Virgatosimoceras �------ulmense Trocholina albertinum friburgensis ... - G/ochiceras � 1 , a e 0; Hybonoticeras nimbatum ,_ �� .!_�!! _ ..!1 ...J hybonotum local zone ------1------? Aulacostephanus 1 autissiodorensis I r------...CP ? c: Q, A. eudoxus I ea Q, r------I CP Aulacostephanus I c: CP ...Q) ·a,"C :::l mutabilis c: I a. 'i: Aspidoceras 0 2 Alveosepta a. CP Rasenia � E -ldoceras N : - jaccardi ­ cymodoce � ::::l E CP... local z�ne ii Mesoendothyra � . CJ I ..S! -CP i: 0 '------:e I izjumiana ..S! I1 ea ...J Pictonia baylei Sutneriaplatinota I 5 zone 1 I ,______local zone _ L g I N I . , � � Ringsteadia lI ea CP I J! o------u ... ,_ __ ? _ _ l e:: - 'Cii Q, pseudocordata _ _ _ _ _ 1 CPQ. f/1 Q, I I'!! E Perisphinctes Nubeculinella ea :::l Perisphinctes cauti- I�� .... cautisnigrae I � gigantocamerata - o z _ � a � ::l .!1!!.9!8!! .!_ � �� 1 1 c: I I� £:! Quinqueloculina .., ea CP Perisphinctes ? oq I 1:::::: - frumenta � ;:;"C pumilus CP ------1 I Cl) local zone .E Perisphinctes I a E )( i Perisphinctes 1 0 plicatilis l z I I Cl) .::! - f!. �B!jl���!_ �� �"Q- - - Cardioceras :� :§ - Marss on ena - ...CP Cardioceras : � cordatum S jurassica - 0 cordatum - C. verte­ 1 1 ...J Trocholina Quenstedtoceras bra/a local zone I1 1I g.c: transversarii mariae l c l! n ------..1 - - .1- -I', __� � � � , Quenstedtoceras Quenstedtoceras ./ ...CP lamberti Jamberti zone CL Lenticulina tumida CL Peltoceras athleta :::l Peltoceras ath/eta Labalina costata- zone zone Lenticulina tumida - - 1------l ------CP Erymnoceras local zone c: Erymnoceras Q) coronatum zone ;:;"C coronatu m ea Labalina costata :a'C ·:; Kosmoceras i Kosmoceras jason zone .2 jason zone i ii (J Stgaloceras 1------l------+------l? Sigaloceras cal/oviense Haplophragmium - - calloviense -:- Re eurvo lcles -. ... Proptanulttes coprolithiforme , , -Macrocephalites ventosus ­ ;0 koenigi local zone Macrocepnatttes macrocephalus Pseudonodosaria ...J herveyi zone terquemi zone Fig. 2. Biostratigraphic zonation ofthe Middle and Upper Jurassic ofthe Russian Caucasus. 9th International Congress on the Jurassic System - Abstracts 203

Leningrad (In Russian). Zapadnogo Kavkaza: foraminifery i ikh facial'nye VuKs, V.JA. 2004. Foraminiferal zonation of the Upper osobennosti [Biozonal scheme of the Upper Jurassic Jurassic of the Caucasus: comparison of schemes and of the Western Caucasus: fo raminifers and their new results. Abstract volume of the 32nd International facial features]. Jurassic System of Russia: Problems Geological Congress, Florence, Italy. August 20-28th, of stratigraphy and paleogeography. - Proceeding 2004. Part 1: 823. volume of the Russian meeting: 39-40, Yaroslavl 11. VUKS, V.JA. 2007. Biozonal'naya schema verkhnei yury State Pedagogical University, Yaroslavl (In Russian). 204 9rh International Congress on the Jurassic System - Abstracts

Syn- and post-tectonic palaeomagnetism of Jurassic sediments from the Velebit Mts (Karst Dinarides, Croatia)

2 * TOMASZ WERNER\ IGOR VLAHOVIC , MAGDALENA SIDORCZUK3 & MAREK LEWANDOWSKI4

1Institute of Geophysics, Polish Academy of Sciences, Wa rsaw,Po land; E-mail: [email protected] 2Facultyof Mining, Geology and Petroleum Engineering, Universityof Zagreb, Zagreb, Croatia; E-mail: ig or.vlahovic@ gmail.com 3Polish Geological Institute - National Research Institute, Wa rsaw, Poland; E-mail: [email protected] 4Institute of Geological Sciences, Polish Academy of Sciences, Wa rsaw,Pola nd; E-mail: lemar@twarda. pan.pl

*Corresponding author

The Early to Late Jurassic deposits along a Jurassic sites (345/30 in situ) correlates transect in Mali Halan in the southern part well with results of Marton (2008) fo r Early of the Velebit Mt. (Croatia) were studied Jurassic grainstones in the same area. The tilt­ using palaeomagnetic and rock magnetic corrected data for the "M" component fall close measurements. Magnetic susceptibility of to the Middle Jurassic segment for APWP for diamagnetic carbonates is not affected by Africa. However, site mean values for the "M" heating up to 400-500°C. SIRM(T) experiments component are distributed along the small revealed low temperature (Tub <400°C) Ti­ circle with subhorizontal WNW trending axis. poor magnetite and some hematite phase in This may be interpreted as pre- to syntectonic fresh samples. Magnetic carriers were also remanence recorded during regional folding. documented by electron microscope and SEM The "L'' component (of lower accuracy) for analyses. Heating in air results in excessive Early/M iddle Jurassic sites (in situ) falls close growth of a new magnetite phase above to APWP fo r Africa �nd also indicates its post­ 600°C, rendering NRM components analyses tectonic secondary origin. For Late Jurassic sites impossible above this temperature level. with lower NRM intensity the "I.:' component Thermal and AF treatment was performed seems to be post-tectonic but results fo r the "M" and was more successful fo r Early Jurassic sites component need to be yet discussed. Generally, with stronger NRM. It resulted in separation the origin of the characteristic NRM component of two ChRM components: "I.:' with Tub up to may be regarded as syntectonic, acquired during 200-250°C and "M" with Tub up to 400-475°C progressive uplifting and tilting, and in line with or two coercivity spectra (very softand harder) the model proposed for remagnetized Permian in most successfully demagnetized samples. In clastic sediments in the Velebit Mts. (Crne Grede some samples only the soft/LT component was and Kosna localities, LEWANDOWSKI et al. 2012, recorded. AGU Fall Meeting, GP21A-1136). The "M" component for Early and Middle 9th International Congress on the Jurassic System - Abstracts 205

Oxygen and carbon isotope records of uppermost Callovian-Lower Kimmeridgian belemnite rostra and bulk carbonates from the Polish Jura Chain (central Poland) : environmental changes in the Submediterranean Province of Europe

HUBERT WIERZBOWSKI

Institute of Geological Sciences, Polish Academy of Sciences, ul. Twarda 51/55, PL 00-818 Wa rszawa, Poland; E-mail: [email protected]

Oxygen and carbon isotope values of of the Submediterranean Province (Fig. 1 ) . mesohibolitid belemnite rostra from the Newly analysed data also show a short-lived Upper Callovian-Lower Kimmeridgian of the increase in the cS180 values and a decrease in Submediterean ammonite province (Polish bottom water temperatures at the Callovian­ Jura Chain in south-central Poland, Kujawy Oxfordian transition (in the uppermost part of area in north-central Poland and Swabian the Lamberti Subchron of the Lamberti Chron) Alb in southern Germany) were presented by in the Polish Jura Chain basin. WIERZBOWSKI (2002, 2004) and WIERZBOWSKI Carbon isotope trends derived from micritic et al. (2009). The data show relatively constant bulk carbonates and belemnite rostra from the temperatures of bottom waters, where studied Polish Jura Chain are partly dissimilar (Fig. 1). belemnites lived, throughout the Late Callovian­ This is likely caused by secular changes in the Middle Oxfordian and a temperature rise of ea. origin and the isotope composition of carbonate 2°C at the Middle-Late Oxfordian trans�tion micrite sedimented in the Polish Jura Chain (i.e. the transition of the .Transversarium and basin. Vast variations of the sedimentation Bifurcatus chrons). Belemnite cS13C valuespo int rate are observed in this area in the Oxfordian to the existence of the two positive carbon - a gradual rise in the calcium carbonate isotope excursions in the Upper Callovian sedimentation rate is observed starting from (Athleta and Lamberti zones) and the Middle the Plicatilis Zone of the Middle Oxfordian. The Oxfordian (Plicatilis and Transversarium rise is followed by an abrupt increase in the zones) of the Submediterranean Province (cf. deposition rate in the Planula Zone of the Upper WIERZBOWSKI 2002, 2004; WIERZBOWSKI et al. Oxfordian (in Submediterranean zonation) 2009). due to the flux of material from the prograded Belemnite rostra collected from the Middle­ carbonate platform (MATYJA & WIERZBOWSKI Upper Oxfordian of the Polish Jura Chain were 1994). previously screened fo r the state of preservation using the cathodoluminescence microscope The study was partly supported by the Polish National (WIERZBOWSKI 2002). As this method is Science Centre (grant no. 2012/0S/B/ST10/02121). considered insufficient by some authors (cf. References VEIZER 1974, 1983; MARSHALL 1992) the MATYJA, B.A., WIERZBOWSKI, A. 1994. Monografia g6rnej studied samples have been recently analysed fo r jury Pasma Krakowsko-Wielunskiego. Projekt iron, manganese and strontium contents. Only Badawczy KBN nr 600799101 (unpublished report): well-preserved rostra characterized by low Fe 1-39, Warszawa. ( < 200 ppm) and Mn (< SO ppm) concentrations MARSHALL, J.D. 1992. Climatic and oceanographic isotopic signals from the carbonate rock record and their as well as by high Sr (>800 pp m) contents were preservation. - Geological Magazine 129: 143-160. incorporated in revised stable isotope trends VEIZER, J. 1974. Chemical diagenesis of belemnite shells (Fig. 1). The revised belemnite data confirm and possible consequences for paleotemperature the timing of temperature variations and the determinations. - Neues Jahrbuch fiir Geologie und Palaontologie, Abhandlungen 147: 91-111. carbon isotope excursions in the Polish Jura VEIZER, J. 1983. Chemical diagenesis of carbonates: Chain. These variations are consistent with the theory and trace element technique. In: ARTHUR, palaeoenvironmental records of other areas M.A., ANDERSON, T. F., KAPLAN, I.R., VEIZER, J. & LAND, 206 9thInternational Congress on the Jurassic System - Abstracts

BOREAL SUBMEDITERRANEAN ...... Polygy- Platynota z ratus �� Kitchini Subki­ � tchini gi: lllI Galar 0 - ffi t----+------1 Planula :::E Planula :::E 0 :;;:: Bauhini Hauffia- z er <( w -nu m i5 +1 Bimam- Birnarn- er �....1 0 -malum rnaturn u.. Rosen- X Hypselum 0 z krantzi <( • • • er i5 • Grossou- w er Regula re D.. • • • vrei D.. u..0 - ::::l X Serraturn 1 Serratum Stenocy- Bifur- 0 Koldeweven • -cloides catus a: • Glosense Wartae � Glosense • D.. l ::::l llovaiskii Elizabe- Te nuiser- Blakei lhae Transver- z : . raturn sariurn � <( Lf • �Buckmani . . · i5 i5 � , er er Mal to- 0 0 nense u.. u.. �: . · Arkelli X X Densipli- � • 0 0 • 1-- ....1 turn . Ouatius Plicatilis w ....1 Verte- � w ea · brale • 0 0 • • 1--Pattura- 0 0 ( . . • tensis � � Cordatum • Cordatum z .. , z <( <( Corda- 1-- • • 1--Costi- Cord a- i5 Costi- i5 er turn cardia • ! • cardia turn er 0 r--- 0 u.. Bukowskii . • • 1--Bukowskii u.. X .....--'-----'-----', X 0 � Mesohibolitid 0 Praecor- · belemnites: Praecor- er . Chain er w datum � (Wierzbowski,Polish Jura datum w Mariae 2002; Mariae 3: Scarbur- Wierzbowskiet al. Scarbur- 3: ...J • 2009 ....1 0 gense and unpublished gense 0 . data) Kujawy area Lamberti • ..... • Lamberti • • (Wt erzbowski, • Larnberti - 2004) Larnberti ffi� ! f--- Henrici �W:':�.2004) Henrici �� I 0 &:l ' :::llS 0.5 0 -0.5 -1 -1.5b -1 0 1 3 0 1 2 18 17 16 6"0..,_ [%o VPDB) 6"C..._ _ VPDB)[%o 6"c..,_ [%o VPDB) _ Fig. 1. Uppermost Callovian-Oxfordian stratigraphy, 6180 and 613C values of well-preserved belemnite rostra and bulk carbonates from the Polish Jura Chain, Kujawy, and the Swabian Alb. 613C values of dully luminescent Upper Oxfordian belemnite samples from the Polish Jura Chain (marked with "1") are shown for comparison. Curves represent 5-point running averages for the isotope data.

L.S. ( eds.), Stable isotopes in sedimentary geology. - for Late Jurassic seas. Palaeogeography SEPM Short Course No. 10: 3-1-3-100. Palaeoclimatology Palaeoecology203: 153-168. WIERZBOWSKI, H. 2002. Detailed oxygen and carbon WIERZBOWSKI H., DEMBICZ, K. & PRASZKIER, T. 2009. Oxygen isotope stratigraphy of the Oxfordian in Central and carbon isotope composition of Callovian-Lower Poland. - International Journal of Earth Sciences Oxfordian (Middle-Upper Jurassic) belemnite rostra (Geologische Rundschau) 91: 304-314. from central Poland: A record of a Late Callovian global WIERZBOWSKI, H. 2004. Carbon and oxygen isotope sea-level rise? - Palaeogeography, Palaeoclimatology, composition of Oxfordian-Early Kimmeridgian Palaeoecology283: 182-194. belemnite rostra: palaeoenvironmental implications 9th International Congress on the Jurassic System - Abstracts 207

Revised seawater strontium isotope curve for the Late Bajocian­ Oxfordian (Middle-Late Jurassic)

*, HUBERT WIERZBOWSKI1 ROBERT ANCZKIEWICZ2, }AKUB BAZARNIK3 & }ACEK PAWLAK4

1/nstitute of Geological Sciences, Polish Academy of Sciences, ul. Twarda 51/55, PL 00-818 Wa rszawa, Poland; E-mail: [email protected] 2/nstitute of Geological Sciences, Polish Academy of Sciences, ul. Senacka 1, PL 31-002 Krak6w, Poland; E-mail: [email protected] 3/nstitute of Geological Sciences, Polish Academy of Sciences, ul. Senacka 1, PL 31-002 Krak6w, Poland; E-mail: [email protected] 4/nstitute of Geological Sciences, Polish Academy of Sciences, ul. Twarda 51/55, PL 00-818 Wa rszawa, Poland; E-mail: [email protected]

*Corresponding author

The seawater strontium-isotope curve is normalized to the recommended SRM 987 characterised by a broad and a deep trough at 87Sr/86Sr ratio of 0.710248 (cf. McARTHUR et the Middle-Late Jurassic transition (with the al. 2001). The strontium isotope curve was lowest 87Sr /86Sr ratio in the Phanerozoic). Due estimated using a LOWESS statistical model (cf. to the significant scatter or scarcity of strontium HERCMAN & PAWLAK 2012). The 95°/oconfidence isotope data in some stratigraphic intervals a interval was calculated with the Monte Carlo well-defined fit of the strontium isotope curve method taking account of measurement could not be produced for the Middle to Late uncertainties. Jurassic (cf. }ONES et al. 1994; )ENKYNS et al. The new strontium isotope data 2002). New data derived from well-preserved supplemented with published data by )ONES belemnite rostra have recently allowed the et al. (1994), CALLOMON & DIETL (2000), and presentation of the high-resolution strontium WIERZBOWSKI et al. (2012) allowed producing isotope curve for the Late Bajocian-Callovian a high resolution seawater strontium isotope period (WIERZBOWSKI et al. 2012). curve for the Late Bajocian-Oxfordian (Fig. 1). Well-dated stratigraphically and well­ The data show that the seawater 87Sr/86Sr ratio preserved belemnite rostra (non-luminescent, decreased gradually from the Late Bajocian to CFe < 150 ppm, CMn < SO ppm, C5r > 950 ppm) the Middle-Late Bathonian transition (from ea. from the Oxfordian of the Polish Jura Chain in 0. 707070 to ea. 0. 707000). An abrupt decrease central Poland and the Swabian Alb in southern of the 87Sr/86Sr ratio to ea. 0. 706875 occurred Germany have been newly analysed for their in the Late Bathonian-Early Callovian. The ratio strontium isotope composition. The samples fell slightly during the Middle Callovian and were dissolved in 2.5M HCI. The leachates were reached a quasi-constant value of ea. 0. 706850 evaporated to dryness. Strontium separation in the Late Callovian. A further decrease of the was perfo rmed in two steps with Bio-Rad 87Sr /86Sr ratio occurred in the Early Oxfordian, SOW-X8 and Eichrom Sr-spec resins. A blank and the Early-Middle Oxfordian transition is of chemical procedures was less than 20 pg characterized by the lowest ratio of ea. 0.706830. strontium. Isotope analyses of strontium were An stepwise increase of the 87Sr/86Sr ratio took conducted using a MC ICP-MS Neptune at the place starting from the latest Middle Oxfordian. Institute of Geological Sciences, Polish Academy The seawater 87Sr/86Sr ratio reached a value of of Sciences in Cracow, Poland. All isotope ratios ea. 0. 706880 at the Oxfordian-Kimmeridgian were corrected fo r fractionation effect using transition (according to the Submediterranean the 87Sr/86Sr value of 0.1194. Reproducibility ammonite zonation). of measured SRM 987 ratio over the course The Middle-Late Jurassic trough of the of the analyses was 0. 710262 ±6*10-6 (2a, seawater 87Sr/86Sr ratio is linked to a pulse of n=11). Measured sample 87Sr/86Sr ratios were hydrothermal activity of the seafloor, which 208 9th International Congress on the Jurassic System - Abstracts resulted in the influx of isotopically light, non­ construction algorithm. - Quaternary Geochronology radiogenic strontium to the oceans (cf.)ONE S et 12: 1-10. }ENKYNS H.C., }ONES, C.E., GROCKE, D.R., HESSELBO, S.P. al. 1994; )ONES & jENKYNS 2001). There is much & PARKINSON, D.N. 2002. Chemostratigraphy of evidence for the acceleration of the oceanic the Jurassic System: applications, limitations and crust spreading and the opening of new oceanic implications for palaeoceanography. - Journal of the basins at the Middle-Late Jurassic transition Geological Society, London 159: 351-378. }ONES, C.E. & }ENKYNS, H.C. 2001. Seawater strontium (cf. WIERZBOWSKI et al. 2012). isotopes, oceanic anoxic events, and seafloor The new data show that the seawater had hydrothermal activity in the Jurassic and Cretaceous. the lowest Phanerozoic 87Sr/86Sr ratio at the - American Journal of Science 301: 112-149. Early-Middle Oxfordian transition - a bit later }ONES, C.E., }ENKYNS, H.C., COE, A.L. & HESSELBO, S.P. than it was previously assumed (cf. jENKYNS et 1994. Strontium isotopic variations in Jurassic and Cretaceous seawater. - Geochimica et Cosmochimica al. 2002; WIERZBOWSKI 2012; see Fig. 1). The Acta 58: 3061-3074. presented data along with other published McARTHUR, J.M., HOWARTH, R.J. & BAILEY T. R. 2001. strontium isotope data may be used to obtain Strontium isotope stratigraphy: LOWESS version a best fit of the strontium isotope curve in the 3: best fit to the marine Sr-isotope curve for 0-509 Ma and accompanying look-up table for deriving Middle-Late Jurassic. numerical age. -Journal of Geology 109: 155-170. References WIERZBOWSKI, H., ANCZKIEWICZ, R., BAZARNIK, J. & PAWLAK, CALLOMON, J.H. & DIETL, G. 2000. On the proposed basal J. 2012. Strontium isotope variations in Middle Jurassic boundary stratotype (GSSP) of the Middle Jurassic (Late Bajocian-Callovian) seawater: Implications fo r Callovian Stage. - GeoResearch Forum 6: 41-54. Earth's tectonic activity and marine environments. - HERCMAN, H. & PAWLAK, J. 2012. An age-depth model Chemical Geology 334: 171-181.

168.3±1 .3 Ma 166.1±1.2 Ma 163.5±1 .1 Ma 157.3±1 .0 Ma

95% confidence limits

Lowess fit --- data fr m Jones et al.. ( 1994) 01 � data from Callomon and Dietl (2000) data from Wierzbowski • et al. (2012) present data • dating error 1------l

::u -i (/) i» OJ (I) -o c: � () () :::J 0" OJ 0 r () OJ 3" N a CJ I A � '-- Ql 0 31 en Ql IJ � a 0 ;e $; < <0" -· cc ()�Cil () Cl> 0 Ql a Ql c;· � Oo 0 (ii" Cl> :::J ::;,.- 3 Cl> 3 ill N :J ..... < en 0" a. :::J m · 3 en () < :::J Ql Ql � 0 Ql &T - c Cl> (i)" 0 [ Cl> ffi· eh Ql 3 c cc g ��· �- or en c (ii" Ql Ql Sl �- en a ::l. c ill c (ij" c: c 3 3 en c CJl CJl Cl> c 3 3 3 ro ro ro () () 0 0 0 ....ll) m � s: ll)..... r �m �s: �r g. m � s: S.r ::J"Il) ::J" ::J"Il) 0 -· -· 0 ,.... oo.: 0 ll) ..., ll) g::l. oc. �� ll)· '< ii)" CI> ii)" ii)" '< iir ro ll) w· ii)" (l) ll) :::J :::J :::J :::J :::J :::J :::J :::J :::J Fig. 1. Strontium isotope variations in Late Bajocian-Oxfordian seawater. The time scale of the diagram is based the on assumed equal duration of ammonite subchrons. Dating errors higher than one subchron are marked. 9th International Congress on the Jurassic System - Abstracts 209

Orbital cyclicity and its environmental response - a case study from the Upper Bathonian of Central Poland

*, PIOTR ZIOtKOWSKI1 TOMASZ WERNER2, ZOFIA DUBICKA3& LINDA A. HINN00

1Facultyof Geology, Universityof Wa rsaw, PL-02-089 Wa rsaw, Poland; E-mail: [email protected] 2/nstitute of Geophysics, Polish Academyof Sciences, PL-01-452 Wa rsa""Po land; E-mail: twerner@igf edu.pl 3Facultyof Geology, Universityof Wa rsa""PL-02-089 Wa rsaw, Poland; E-mail: [email protected] 4Department of Earth and PlanetaryScien ces, ]ohns Hopkins University, Baltimore, MD 21218, USA; E-mail: [email protected]

*Corresponding author

Upper Bajocian to Upper Bathonian black clays glycolated and heated samples have allowed and siltstones with ironstone concretions are to identifyill ite, kaolinite, chlorite, quartz, and known as the Ore Bearing Czestochowa Clay calcite as the rock fo rming minerals. XRD semi­ Formation which is famous due to the wealth quantitative analysis has shown that specimens of extraordinarily preserved ammonites. with the highest MS values contain relatively They have been known since the nineteenth more illite (paramagnetic) and less kaolinite century and are the basis fo r a very detailed (diamagnetic) than the specimens with the chronostratigraphic interpretation (MATYJA et lowest MS values which contain relatively less al. 2006). The Ore Bearing Czestochowa Clay illite and more kaolinite. Formation is currently well exposed in t,h e In the last step of our investigations we Czestochowa Region in several clay pits. studied fo raminifera from selected samples. The macroscopically monotonous rocks The analyses were carried out in the �75 �m were the fo cus of very detailed magnetic size fraction and an average number of 300 susceptibility (MS) investigations. The output specimens of fo raminifera per sample was MS signal was subjected to spectral analysis identified and counted. In general, the Bathonian (ZIOtKOWSKI & HINNOV 2009) that showed a clays yield rich and well-preserved fo raminiferal strong bundling pattern which corresponds assemblages dominated by benthic fo raminifera; to the ratio of orbital Milankovitch cyclicity. planktonic foraminifera occur only sporadically Samples fo r further investigations were (cf. SMOLEN 2012). More than 30 species of the collected from the MS extrema to answer the genera Ammobacu/ites, Astacolus, Epistomina, question, whether there is any more evidence Flabellinel/a, Frondicularia, Garantel/a, for environmental response to a changing Geinitzinita, Conoglobigerina, Ichthyolaria, insolation. Lagena, Lenticulina, Nodosaria, Ophthalmidium, Analysis of magnetic hysteresis parameters Palaeomiliolina, Paalzowel/a, Planularia, using the MicroMag™ magnetometer and a Pseudoglandulina, Reophax, Reinholdella, Spirillina, Saracenaria method described by BORRADAILE & WERNER and were recorded (Fig. (1994) allowed us to estimate the relative 1). This study reflects strong cyclic fluctuations content of diamagnetic, paramagnetic, and of the foraminiferal assemblages. Some samples ferromagnetic minerals in selected samples. are almost monospecific assemblages in which We found that only several percent of the MS 90% of the individuals belong to Epistomina depends on the presence of fe rromagnetic nuda TERQUEM. Other samples show very grains and their content varies only slightly high taxonomic diversity with a high content within particular samples. MS variations of Epistomina, Ophthalmidium, Lenticulina, are caused by the changing proportions of Palaeomi/io/ina, and Spirillina. paramagnetic and diamagnetic minerals in the The cyclic record of the foraminifers is well studied succession. correlated with the magnetic susceptibility X-ray diffraction analyses on sedimented, record and the illitejkaolinite content. Periods of 210 9th International Congress on the Jurassic System - Abstracts cooler climatic conditions are characterized by MATYJA, B., WIERZBOWSKI, A., GEDL, P., BOCZAROWSKI, A., the opportunistic fo raminifer Epistomina nuda KAIM, A., KEDZIERSKI, M., LEONOWICZ, P., SMOLEN, J., Sz­ CZEPANIK, P. & WITKOWSKA, M. Field trip B1 - Biostra­ TERQUEM and the prevalence of illite - a product tigraphical framework from Bajocian to Oxfordian. In: of weathering in a cool and dry climate. On the WIERZBOWSKI, A. et al. (eds.), Jurassic of Poland and contrary, during relatively warm conditions the adjacent Slovakian Carpathians. Field trip guidebook fo raminiferal assemblages were characterized of 7th International Congress on the Jurassic System; Poland, Krak6w, September 6-18, 2006: 149-152, Po­ by high diversity and the sediment by a higher lish Geological Institute, Warsaw. content of kaolinite, fo rmed in a humid and SMOLEN, J. 2012. Faunal dynamics of foraminiferal assem­ warm climate. blages in the Bathonian (Middle Jurassic) ore-bearing clays at Gnaszyn, Krak6w-Silesia Homocline, Poland. -Acta Geologica Polonica 62: 403-419. References Zt6tKOWSKI, P. & HINNOV, L.A. 2009. Cyclostratigraphy of BORRADAILE, G.J. & WERNER, T. 1994. Magnetic anisotropy Bathonian using magnetic susceptibility - prelimina­ of some phyllosilicates. - Tectonophysics 235: 223- report. In: KROBICKI, M. (ed.), Jurassica VIII, Vrsatec ry 248. 09-11.10.2009, Geologia, 35 3/1: 115 (in Polish).

1. Foraminifers from the Upper Bathonian ore-bearing Czestochowa Clay Formation. A. Paalzowel/a pazdroe Fig. BIELECKA; B. Epistomina nuda TERQUEM; C. Epistomina regularis TERQUEM; D. Lenticulina (Astacolus) argonauta (KoPI ); Lenticulina muensteri (ROEMER); F. Lenticulina he/ios (TERQUEM); G. Ophthalamidium sp.; H. Palaeomiliolina K E. czestochowiensis PAZDROWA; I, J. Ophthalmidium carinatum agglutinans PAZDROWA; K. Nodosaria pu/chra (FRANKE); L. Conoglobigerina bathoniana (PAZDROWA); M. Planularia prava (FRANKE); N. Flabellinella sp.; 0. Pseudoglandulina tenuis (BORN); P. Frondicularia cf. lingulaefo rmis ScHWAGER; Q. Lenticulina (Astacolus) dictyotes dictyotes (DEECKE); R. Sp irillina radiata TERQUEM; S. Lagena globosa (MONTAGU); T. Frondicularia sp.; U. Planularia cordiformis (TERQUEM); V. Planularia fi losa (TERQUEM); W. Ammobaculites coprolithiformis (SCHWAGER); scale bar: 100 11m. 9th International Congress on the Jurassic System - Abstracts 211

Index of Contributors

Agarwal, A. 11 Echevarria, J. 43 Alberti, M. 13 Al-Saad, H. 16 Fan, R. 45 Alsen, P. 32, 118 Farboodi, M. 96 Al-Suwaidi, A. H. 17 Feldman-Olszewska, A. 101 Anczkiewicz, R. 207 Felsch, T. 67 Angelozzi, G. N. 17 Fernandez-Lopez, S. R. 54, 134 Arabas, A. 19 Fortwengler, D. 139 Arai, M. so Frid, C. L. J. 57 Fiirsich,F. T. 13, 59, 67, 124 Bardhan, S. 182 Barski, M. 21 Galbrun, B. 139 Bartolini, A. 139 Gardin, S. 139 Baudin, F. 17 Garg, R. 151 Bayon, G. 48 Garg, S. 151, 153, 155 Bazarnik, J. 207 Gill, B. C. 34 Bhatt, N. Y. 23, 88, 190 Glinskikh, L. 120 Bhaumik, S. 126 Glowniak, E. 60 Biswas, S. K. 26 Golej, M. 179 Blau, J. 28 Gosling, W. D. 94 Blazejowski, B. 29 Gradinaru, M. 103, 105 Boulila, S. 139 Gregory, F. J. 92 Braham, B. 9.2 Grocke, D. R. 34, 147 Brahim, El Hadj Y. 31 Guillou, H. 137 Branski, P. 145 Gulyaev, D. 62 Budiel, C. C. 54 Gupta, M. 151, 153, 155 Gurav, S. S. 65 Caillaux, V. C. 54 Guzhov, A. 48 Callomon, J. H. 32 Caruthers, A. H. 34, 73, 147, 188 Haggart, J. 48 Caswell, B. A. 36, 57 Hammer, 0. 75 Chadi, M. 31 Hesselbo, S. P. 17, 66 Charbonnier,G. 48 Hethke, M. 13, 67 Chaudhari, A. 38 Hillebrandt, A. von 70 Chauhan, G. 39 Hinnov, L. A. 209 Chinnappa, C. 158 Hnylko, 0. 101 Coe, A. L. 36, 40, 94 Hodbod, M. 21, 143 Coimbra, R. 41 Hou, P. 34, 73, 147 Collin, P.-Y. 139 Hryniewicz, K. 75 Condon, D. 17 Huault, V. 139 Cuny, G. 48 Huret, E. 139

Damborenea, S. E. 17, 43 lppolitov, A. 62, 77, 79 Delsate, D. 48 lshida, N. 81 Deng, S. 45 lvanov,A. 120 Dera, G. 48 Ivanova, D. 179 Dommergues, J.-L. 115 Iwanczuk, J. 83, 101 Duarte, S. so Izumi, K. 93 Dubicka, Z. 209 Dzyuba, 0. S. 52, 120, 185 Jach, R. 195 212 9th International Congress on the Jurassic System - Abstracts

Jacob, D. 193 Mitta, V. 118, 120 Jadhav, P. B. 11 Manna, F. 137 Jain, R. L. 85 Mukherjee, D. 122 Jain, S. 153 Munsch, H. 59 Jaitly, A. K. 86 Jenkyns, H. C. 17 Nakrem, H. A. 75 Jha, N. 50, 87 Niedzwiedzki, G. 145 J oachimski, M. 193 Nieto, L. M. 167 J odhawat, R. L. 85 Nomade, S. 137 Joseph, J. K. 88 Joshi, H. 87 Olev, V. 75 016riz, F. 41, 197 Kachhara, R. P. 85 Kaim, A. 75 Pan, Y. 124 Kale, A. S. 11 Pandey, B. 133 Kelly, S. R. A. 92 Pandey, D. K. 13, 126, 127, 128, Kemp, D. 93 151, 153 Kennedy,A. E. 94 Patel, J. M. 190 Khaksar,A. 96 Patel, N. J. 129 Khaksar, K. 96 Patel, S. J. 23, 88, 129, 155, 190 Khosla, A. 98 Pathak, D. B. 133 Khosla, S. C. 100 Pavia, G. 134 Kimoto, K. 81 Pawlak, J. 207 Kiselev, D. 62 Pellenard, P. 137, 139 Kishimoto, N. 81 Pestchevitskaya, E. B. 141 Korte, C. 66 Pienkowski, G. 143, 145 Kostyleva, V. 120 Pooniya, D. 127 Krobicki, M. 101, 105 Popa, M. E. 105 Kulkarni, K. G. 65 Popov, E. 48 Kupriyanova, E. 77 Porter,S. J. 34, 73, 147 Kurihara, T. 81 Prakash, N. 87, 148 Prunier,J. 48 Lal, M. M. 108 Puceat, E. 48 Lathuiliere, B. 179 Lazar, I. 103, 105 Rai, J. 150, 151, 153, 155 Lewandowski, M. 204 Rajanikanth, A. 158 Li, X. 45 Ranawat, T. S. 161 Little, C. T. S. 75 Randrianaly, H. N. 162 L6pez Correa, M. 193 Rasoamiaramanana, A. 162 Lu, Y. 45 Reolid, M. 163, 165, 167 Riccardi, A. 17 Majidifard, M. R. 107 Riding, J. B. 94 Mancefiido, M. 17 Rodrfguez-Tovar, F. J.. 167 Manisha, K. 108 Rogov, M. A. 48, 169, 171, 174 Marchand, D. 139 Roy, P. 176 Marok, A. 165 Martire, L. 137 Sadki, D. 177 Matsuoka, A. 81, 110 Sadooni, F. 16 Mattioli, E. 167 Saldivar, E. G. 54 Matyja, B. A. 21, 29, 111, 113 Sandy, M. R. 75 Meister,C. 28, 115 Schlogl, J. 19, 79, 179, 193 Misra, A. 116 Sebane, A. 165 9th International Congress on the Jurassic System - Abstracts 213

Selby, D. 147 Seltzer, V. 120 Sha, J. 181 Shchepetova, E. V. 174 Shame, S. 182 Shukla, H. 155 Shurygin, B. N. 120, 185 Sidorczuk, M. 204 Singh, A. 151, 153, 155 Smith, P. L. 34, 48, 73, 147, 181, 188 Sobien, K. 83 Solanki, P. M. 190 Srivastave, N. 161 Strogen, D. P. 92 Surlyk, F. 32 Swami, N. 128

Thakkar, M. G. 39, 192 Thakur, B. 155 Thierry, J. 139 Thies, D. 48 Tomasorych,A. 179, 193

Uchman, A. 195 Ullmann, C. V. 66

Vidhya, S. 108 Villasefior, A. B. 197 Villier, L. 179 Vlahovic, I. 204 Vuks, V. J. 200

Werner,T. 204, 209 Whitham, A. G. 92 Wierzbowski, A. 19, 21, 29, 111, 113, 174 Wierzbowski, H. 29, 174, 205, 207 Wilmsen, M. 59

Yoshino, T. 81

Zi6lkowski, P. 209 Freunde der nordbayerischen Geowissenschaften e.V. Middle Oxfordian Passendorferiinae (Perisphinctidae, Ammonoidea) from Estepa (Seville, Betic Cordillera, S Spain): Evolution, biostratigraphy and biogeographic meaning.

Melendez Guillermoa *, Yaiiez-Jer6nimo, Juan de Diosb, Sequeiros, LeandroC, Affiliation and address including e-mail - Font size 12, italics a Departmento de Geologia, universidad de Zaragoza, c./ Pedro ·Cerbuna 12, E-50009 Zaragoza, (Spain, Emai/-gmelende@unizar. es b c./ La Roda de Anda lucia, 19, E-41560 Estepa, Sevilla Sp ain, E-mail- juyaje@hotmail. com c c./ Pintor El Greco 8, 50.E- 14004 Cordoba (Spain) Emai/- lsequeiros@probesi. org

* Corresponding author

References to the Jurassic of the surroundings of Estepa (Sevilla) in the so-called

"Subbetic Zone " of the Betic Cordillera (S Spain) are scarce and scattered. First detail studies and onite biostratigraphic data come from Sequeiros who studied the Callovian­ amm (1974) Oxfordian ammonite successions in the surroundings of Estepa, (the so-called: "Sierra de

Estepa") including such sections as Arroy� seco, Acebuchosa and Puente Genii, as well as some quarries around the town. Above the Callovian-Oxfordian boundary, within a 4-5 m thick nodular limestone interval (Rosso ammonitico fa cies) ammonite successions recognized in these localities have allowed characterising the middle and upper part of the

Transversarium Biozone (referred to by this author as the Riazi Biozone) the upper part of the Bifurcatus Biozone and the lower part of the upper Oxfordian, including the Hypselum and lower Bimammatum biozones. More recent samplings carried out by J.D. Yaiiez have allowed gathering an interesting collection of well preserved specimens adding new information to the existing data and confirming the good possibilities of the sections and of the studied interval (Melendez et al., 2013). Among the taxa recognized, it is worth mentioning the good collected specimens of oppeliids, (Taramelliceras) together with abundant representatives of Gregoryceras, Mirosphinctes, Euaspidoceras and most particularly, representatives (M and m) of Passendorferiinae. Among them, it is especially noteworthy the record of numerous specimens of Pass. (M & m) erycensis Melendez (= Per. regalmicensis Gemmellaro, 1877; non ·1874; Fig la) and Sequeirosia cf brochwiczi (Sequeiros, 1974). This association, together with common specimens of Gregoryceras of the group riazi (Grossouvre ), Mirosphinctes and Glochiceras of the group subclausum (Oppel)­ crenatum, allows characterizing the Luciaeformis-Schilli subbiozones of the Transversarium

Biozone (=Riazi Biozone, Sequeiros). A recorded specimen of Passendorferia, close to Pass. erycensis, (Fig. 1 b) holds a particular interest as it shows an early ontogenetic stage closely comparable to the innerwhorls of the original type of Per. regalmicensis Gemmellaro (1874,

PI XIV, fig 3a,b) a rather little known form, very rarely quoted besides the type specimen, which is a poorly preserved wholly septate inner whorl of a macroconch. This would suggest a close phylogenetic relationship between both forms and explain the possible origin of Pass. regalmicensis from its presumable ancestor Pass. erycensis, by means of a proterogenetic process. At the same time, this faunal similarity should reflectthe biogeographic connection

la lb Fig Fig

Figure (a) Passendorferia erycensis Melendez: adult microconch. (b) Sp ecimen (septate adult macroconch) 1. showing a ribbing similar to the type specimen of Pass. regalmicensis Gemmellaro 1874, in inner whorls. between both epioceanic areas (Betics and the Trapanese domain; Nw Sicily) during middle

Oxfordian. The general aspect of the type of Pass. regalmicensis Gemm, characterized by the evolute slow coiling and the thick ribbing sets it closer to the representatives of Bifurcatus Biozone than to those of middle-late Transversarium Biozone. It seems that the stratigraphic interval fo rmed by the subbiozones Rotoides, Stenocycloides and Grossouvrei, or the corresponding ammonite recorded associations, is well represented in the studied area, which might not always be the case in other regions of the Subbetic Zone or in Sicily (D' Arpaet al. 2004). All studied specimens (macro and microconch) from all subfamilies, are adult individuals, no specimens showing juvenile stage fe atures having been recorded. Among the microconch representatives of subfamilies Glochiceratinae, Taramelliceratinae and Peltoceratinae, specimens preserving the adult body chamber or even the peristome are not uncommon. Among the macroconchs instead, complete specimens are virtually absent, all studied specimens being incomplete phragmocones. They are generally fragmented or show a disarticulation surface along a septum, displaying a clear lithological, textural and structural discontinuity between the infilling (micritic limestone) and the surrounding matrix, more typically bioclastic or even including micritic fo ssil fragments. They, hence, constitute reelaborated elements, categorized as fragmented or disarticulated internal moulds. Specimens showing truncation facets are less common to absent. The more or less complete microconch specimens, although being preserved as peristomed shells, are also reelaborated elements, showing similar discontinuity between the micritic infilling and the surrounding bioclastic matrix. From the biochronological point of view the analysed recorded associations represent the late Transversarium (Schilli-Rotoides) and Bifurcatus (mainly Grossouvrei) taxorrecords. From the biostratigraphical point of view the reelaborated onite recorded amm associations are diachronic with (older than) the beds containing them. However, the homogeneity of the assemblages and the recognized general absence of diachronic specimens in the satne associations are criteria against a high diachrony between the recorded associations and the beds containing them. From the biogeographic point of view, the studied ammonite associations constitute taphonic populations of typ e 3, i.e. representing allochthonous and ademic elements. However, the taxonomic and biogeographic homogeneity of the associations, typically �ethyan (Passendorferiinae) with very scarce representatives of Perisphinctinae, suggests local (regional) drift of adult shells from near, deeper platform areas.

Acknowledgements:

Research project CLG 201 1-21947/BTE (MICIIN). Research team (consolidated Groups) E-17 from the Government of Arag6n (DGA) Spain.

References

D' Arpa, C. Melendez, G. 2004. Middle to early upper Oxfordian ammonite associations from West Sicily. & Rivista Italiana di Paleontologia, 110 (1), 255-267.

Gemmellaro, G.G. (1874) - Sui fo ssili della Zona con Peltoceras transversarium Quenst. sp. della Provincia di

Palermo e di Trapani. Atti Accad. di Sci., Left., ed Arti di Palermo. 4: 11 p., Palermo.

Gemmellaro, G.G. (1877) - Sopra alcuni fo ssili della zona con Pe/toceras transversarium, Quenstedt del Monte

Erice or San Giuliano. Giorn. Sci. Nat. Econ. XII: 82-98, Palermo.

Melendez, G., Yafiez, J.D., Sequeiros, L. 20 13. Las sucesiones de ammonites del Oxfordiense de Estepa

(Sevilla, cordilleras Beticas ): interes paleontol6gico y bioestratigrafico. In: Trending Top ics in

Paleontology. (Navas-Parejo, P., Martinez-Perez C., Pla-Pueyo, S. eds), 69-70. Atarfe, Granada.

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Department of Geology University of Rajasthan

&

Departmentof Science & Technology Government of Rajasthan Jaipur, India 36 The Jurassic Origin, Cretaceous Evolution and Diversification of Planktic Foraminifera and the need for search of its origin in India: Overview Raju Ve nkatachalapathy Department of Geology, Periyar Universi� Salem-63601t India Emai/-rvenkatachalapathy @gmail. com

The planktic fo raminifera appeared during the Jurassic period (Caron & Homewood, 1983) indicating that the planktic foraminifera evolved from pre-existing benthic ancestors, as is the case in a number of other groups of organisms (Tap pan & Loeblich, 1973). During the Jurassic the extent of the oceans was fa r more widespread then they had been in the Triassic. The Jurassic sea level rose and flooded large portions of the continents across the world. The Jurassic and Cretaceous succession in India has yielded rich varieties of fauna and flora. The planktic fo raminifera are one of the most abundant and best studied straigraphic records among the fossil group. Planktic fo raminiferal diversity and ranges make them suitable for evolutionary studies. The phylogenetic evolution of planktonic foraminifera is considered closely associated with global and regional changes in climate and oceanography. It is generally agreed that the planktic fo raminifera group probably evolved from a benthic ancestor via a meroplanktic (partially planktic) stage into a holoplanktic (totally planktic) mode of life in the Mid-Jurassic (Bajocian) sea-level highstand (Haq et al.,1987) enforced the evolution and distribution of the early planktic fo raminifera. Fuchs (1967) described a group of 'Trias-Globigerinen' and suggested that this was the first group with a planktic mode of life. According to Fuchs' (1975) scheme, the Triassic genus Oberhau�erel/a was the ancestor of the Jurassic planktic genera Co noglobigerina and Praegubkinella and gave rise to the evolution and diversification ofthe planktic fo raminifera. Hart et al. (2003) confirm that the ancestral stock of planktic fo raminifera is identified as Oberhauserella quadrilobata s.s.. According to Hemleben et al. (1989) the sea surface temperature is one of the controlling fa ctors fo r evolutionary trends. During cold periods, the diversity of species decreases and the morphology of the tests become simple, where as in the species radiate and spread to various ecological niches with newly evolving species. Throughout the Mesozoic the evolution and diversification of planktic foraminifera appears to coincide with the repeated development of anoxic water masses in the world oceans and a subsequent sea-level rise (Leckie, 1985, 1987, 1989, Hart eta/. 2003; Leckie eta/., 2002). The appearance of foraminifera with a planktic mode of life in the Mesozoic was arguably the most important event in the entire evolutionary history of foraminifers, as subsequently their development had a significant impact on the whole marine biosphere (Boudagher-Fadel, 2013). She indicated that the planktic foraminifera made their first appearance in the Late Triassic (Fig. 1). The planktic mode of life evolved again independently in the Jurassic, with the appearance of the Conoglobigerinidae in the Late Bajocian. Simmons eta/. (1997) recorded the oldest known planktic species viz. Conoglobigerina avariformis Kasimova, C.balakhmatovae (Morozova), C. dagestanica Morozova and (?) C.avarica Morozova from the Bajocian of eastern Europe. Initially the benthic fo rms evolved as partially planktic ( meroplanktic) and fi nally evolved as fully planktic mode (holoplanktic) and widespread taxon. The Conoglobigerinids seem to persist across the Jurassic-Cretaceous boundary, but their occurrence in the Upper Jurassic is rare and across the Jurassic-Cretaceous boundary the record is very incomplete. 37

Age Origins of Trlassic-Jurasslc planklonlc foramlnlfera (Ma) Period � � � � Globigerinida � -� Conoglobigerinidae , ? 11 3 ., I \ Robertinida Sphaerogerini:tae � 200 \ Rotaliida t. � () "i 11 "I: t- AJiogromida

250 I Fig. 1. The evolution of early planktonic fo raminifera (Boudagher-Fadel, 2013). After examining Fuchs collections in Vienna, Hart (2010) opined that, "it is unlikely that any of these Triassic taxa exhibited a planktic mode of life". He suggested that the earliest Conoglobigerina are probably derived from Oberhauserella-Praegubkinella lineage in the mid-Toarcian, in association with the post-extinction event recovery. In the Bajocian of Carpathians in Poland and the Bakony Mountains in Hungary there is evidence of the first t fo raminiferal ooze in red limestone facies. In hese successions there is a 99:1 o/o planktic: benthic (P/B) ratio and the rocks can be described as foraminiferal packstones. It was in the region of the Jurassic-Cretaceous boundary that the planktic foraminifera changed their tests from aragonite to calcite: a transition yet to be documented. After remaining a low diversity assemblage, with quite restricted distribution, in the earliest Cretaceous, the planktic fo raminifers evolved and diversified in the middle and late Cretaceous until a final warming pulse in the latest Maastrichtian was followed by evidence of cooling immediately before the K/Pg boundary (Hudson et al. 2009, Hart et al. 2012). Hart et al., (2003) are of the opinion that the Early Toarcian Oceanic Anoxic Event in combination with a sea-level highstand as the triggering mechanism fo r a change from a benthic to a planktic mode oflife (Fig. 2). In spite its importance, their origin in Jurassic rocks of India and their evolution and diversification in Cretaceous of India are less understood. While there are still many questions to resolve, new data from Jurassic and Cretaceous sediments from India may provide some answers or support to the evolution of the planktic foraminifera. The taxonomy and stratigraphic distribution of Cretaceous planktic foraminifera are also revised. Understanding the evolution of fo raminifera will be usefulness in correlation of marine strata and paleobiogeography. References Bolli, H.M., Saunders, J.B., Perch Nielson, K. 1985. Plankton stratigraphy. Cambridge University Press, Cambridge, 1032 pp. Boudagher-Fadel M.K. 2013. Biostratigraphic and Geological Significance of Planktonic Foraminifera. (2nd ed.). Office ofthe Vice Provost (Research), UCL: London, UK. 287 pp. 38

j & Stage Zonation 85 --====- � c.--· - 70 o..-tNI �u.u-- ,.,...,

75 · � � � 80· � -- -ft � Oielri!We ...... as. �·�·.. la � COIIiMIIft --... J----.tsCI.L --11 go L TIII'Oftllwl _ .! �----- �.o -� ._? _,.., , D5 ...}_. c-.n ...n ,..._ MiriMI...... --� 100 .. ... - " � ·- :» .I _ .. 0 I ,_. .., w J'JcNII � •" .,...... 105 u � ,--J "'*'-"' h I e � I ' I 110 � �-�- - u -We t.- '"' ------115 7MIIill� �--�D ll a.-.-. . ... �11 - -- 120 I---U1.11t.- a 11 I ...... 12$ ��:-� �tl1.0 t 1A------� ... 130· ...... �--- • 1---UI.O ,..,._ 1� � �------�t)r.O au- ,__. � I : 1<40 __ ..._ �------�--1-- t I . 144.1 a� I 145 ? � 150 �lw.tru- � � 155 f---*' *'"- IIM � 0111 $ l; r1llldl f--.UtU.... 180· CllcMift

185 - �---...,.. ,..__ ...... ,. � 170 = i---*-2•4.6- � .... 115· ::» .., t---•N.J· ·-- " � I l t80· f--1&t t4- f' t t

1 �• 186 Toecim ' -- --

,� f---11Ut.4.a.- ...... , '"· i---ttU,, .__ i I ..__ 200 �·,·- � _,, 208 ..._

Fig. 2: Jurassic origin and Cretaceous evolution of planktic fo raminifera (Hart et al., 2003), with biostratigraphical zonation of Sliter (1989) and Premoli Silva and Sliter (1999). 39

Caron, M. & Homewood, P. 1983. Evolution of early planktic foraminifera. Marine Micropaleontology, 7: 453-462. Fuchs, W. 1967. Ober Ursprung und Phylogenie der Trias-'Globigerinen' und die Beurteilung dieses Formenkreises fiirdas echte Plankton. Verh. Geol. Bundesanst. Wien 1-2: 135-161. Fuch, W. 1975. Detailuntersuchungen an Trias-"Globigeren" mit Hilfe eines Rasterelektronenmikroskopes. Verh. Geol. B.-A., 4: 235-246, Wien.

Hart, M.B., Hudson, W., Smart, C.W. & Tyszka, J. 2012. A reassessment of 'Globigerina bathoniana' Pazdrowa, 1969 and the palaeoceanographic significanceof Jurassic planktonic fo raminifera from southern Poland. Journal ofMicropaleontology, 31: 97-109.

Hart, M.B., Hylton, M.D., Oxford, M.J., Price, G.D., Hudson, W., & Smart, C.W. 2003. The search of the origin of the planktic Forminifera. Journal of the Geological Society, London, 160: 341- 343.

Haq, B.U., Hardenbol, J., & Vail, P. R. 1987. Chronology of fluctuating sea levels since the Triassic. Science, 235: 1156-1167.

Hemleben, Ch., M. Spindler, & 0. R. Anderson. 1989. Modern Planktonic Foraminifera, SpringerVerlag, Berlin, 363 pp.

Hudson,W., Hart,M.B., & Smart,C.H. 2009. Palaeobiogeography of early planktonic foraminifera. Bulletion Society Geology. France, 180: 2738. . Leckie, R.M. 1985. Foraminifera of the Cenomanian-Turonian boundary interval, Greenhorn Formation, Rock Canyon Anticline, Pueblo, Colorado. In: Pratt, L.M. Kauffman, E.G., Zelt, F.B. (Eds.), Fine-Grained Deposits and Biofacies of the Cretaceous Western Interior Seaway: Evidence of Cyclic Sedimentary Processes. SEPM Field Trip Guidbook 4, Tulsa, pp. 139-149. Leckie, R.M. 1987. Paleocecology of mid-Cretaceous planktonic foraminifera: A comparison of open ocean and epicontinental sea assemblages. Micropaleontology, 3 3: 164-176. Leckie, R.M. 1989. A paleoceanographic model for the early evolutionary history of planktonic Foraminifera. Palaeogeography, Palaeoclimatology, Palaeoecology, 73: 107-138.

Leckie, R.M., Bralower,T. J. & Cashman, R. 2002. Oceanic anoxic events and plankton evolution: Biotic response to tectonic forcing during the mid-Cretaceous. Palaeoceanography 17(3): 10.2029/2 001PA000623. Lipps, J.H., 1970. Plankton evolution. Evolution, 24: 1-22.

Premoli Silva, I. & Sliter W.V. 1999. Cretaceous paleoceanography: Evidence from planktonic foraminiferal evolution. Geological Society ofAmer ica. Special Paper, 332: 301-328.

Simmons, M.D., BouDagher-Fadel, M.K., Banner, F.T. & Whittaker, J.E. 1997. The Jurassic Favusellacea, the earliest Globigerinina. In: BouDagher-Fadel, M.K., Banner, F.T., Whittaker,

J.E. (Eds.). The Early Evolutionary History of Planktonic Foraminifera. Chapman & Hall, London: 17-51. Sliter, W.V. 1989. Biostratigraphic zonation for Cretaceous planktonic foraminifers examined in thin sections. Journal ofForaminiferal Research, 19: 1-19.

Tap pan, H., & Loeblich, A.R., 1973. Evolution of the oceanic plankton. Earth Science Reviews, 9: 207-240. 51

List of the participants attending the 9th Ineternational Congress on the Jurassic System

Mr. El Hadj Youcef Brahim Algeria wahidyb @yahoo.fr Prof. Alberta C. Riccardi Argentina riccardi@fc nym.unlp.edu.ar Prof. Miguel Oscar Mancenido Argentina [email protected] Dr. Susana Ester Damborenea Argentina sdambore@fc nym.unlp.edu.ar Dr. Sarah Duarte Brazil [email protected] Dr.Andrew Harry Caruthers Canada [email protected] Dr. Jnelle Yo ung Canada [email protected] Mr. Pengfei Hou Canada [email protected] Dr. Sarah J Porter Canada [email protected] Prof. Dong Ren China [email protected] [email protected] Prof. Huang Diying China Prof.Jingeng Sha China jg [email protected] Dr. Liao Huanyu China [email protected] Prof. Shenghui Deng China dsh [email protected] Dr. Ya nhong Pan China [email protected] Dr. Yaqiong Wang China [email protected] Prof.Yo ngdong Wang China [email protected] Dr. Peter Alsen Denmark pa/@geus.dk Prof. Bernard Lathuiliere France bernard. [email protected] Dr. Guillaume Dera France [email protected] Dr. Pierre Pellenard France Pierre.Pel/enard@u- bourgogne.fr Prof. Axel von Hillebrandt Germany axe/. vonhillebrandt@ campus.tu-berlin.de Dr. Eckhard Monnig Germany e. moennig@naturkunde- museum-coburg Prof. Franz Theodor Fi.irsich Germany fr a nz.fuersich @gzn. u n i- erlangen.de Mrs. Va lsamma Fi.irsich Germany Dr. Joachim Blau Germany [email protected] Ms. Manja Hethke Germany [email protected] Mr. Tobias Felsch Germany Dr. Matthias Alberti Germany a/[email protected] Miss Simone Zippel Germany Prof. Rudolph Scherreiks Germany [email protected] 52

Ms. Luise Scherreiks Germany Dr. Abha Singh India [email protected] Mr. Alok Chaudhari India a/[email protected] Dr. Amita Gill India [email protected] Prof. Anand K. Jaitly India [email protected] Mr. Anant Misra India Prof. Anil Maheshwari India [email protected] Mr. Ankur Bairwa India Dr. Annamraju Rajanikanth India rajanikanth.annamraj [email protected] Ms. Anshika Agarwal India [email protected] Dr. Arpan Misra India [email protected] Prof. Asha Pan de India Dr. Ashu Khosla India khoslal [email protected] Mr. B. K. Meena India Mr. Bhupendra Kumar Dadheech India Dr. Bindhyachal Pandey India [email protected] Dr. Chinnappa Chopparapu India [email protected] Dr. Debahuti Mukherjee India debahuti.mukherjeegsi@gmail. com Dr. Dev Swarup India vc@uniraj. ernet.in Dr. Deo Brat Pathak India [email protected] Mr. Dharamveer Pooniya India [email protected] Mr. Dheeraj Kumar India Prof. Dhirendra K. Pandey India dhirendrap@hotmail. com Mr. Dinesh Saini India Mr. Gaurav Chauhan India [email protected] Mr. Hanuman Sahay India Mr. Harinam Joshi India [email protected] Prof. Harsh Bhu India Dr. Hemant Pareek India Mrs. IlaJaitly India Dr. Jagdish M. Patel India [email protected] Ms. Jaquilin K. Joseph India sjpatel@gmail. com Mr. Jitendra Sharma India Dr. Jyotsana Rai India jy [email protected] Mr. Kailsh Chand Sharma India Dr. Kantimati Girish Kulkarni India [email protected] Mr. Karan Singh Rajawat India Dr. M.G. Thakkar India mgthakkar@rediffmail. com Prof. M.K. Pandit India pa ndi tma noj@hotma il.com Dr. Mamilla Venkateshwarl u India mamila_ [email protected] 53

Mr. Maneesh Lal India [email protected] Dr. Manish Gupta India manish81 [email protected] Dr. Manisha Kumari India drmkumari@ gmail.com Mr. Mukesh Kumar Bairwa India Prof. N.K. Chauhan India Dr. N.S. Mahla India [email protected] Mr. Narendra Swami India narendraswami92@ rediffmail.com Mr. Naveen Kumar Bokoliya India Dr. Neeraj Srivastava India [email protected] Dr. Neerja Jha India [email protected]. uk Dr. Neeru Prakash India [email protected]

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