guidebook

Turkish Association of Petroleum Geologists SPECIAL PUBLICATION: 7

ISBN: 978-975-95677-2-9

Paleozoic of Northern Gondwana and Its Petroleum Potential A Field Workshop 09-14 September 2012 Kayseri, Turkey

GUIDEBOOK Paleozoic of Eastern Taurides

Editors: M. Cemal Göncüo¤lu & Nihat Bozdo¤an

PUBLISHED BY Turkish Association of Petroleum Geologists

Organization

ISBN: 978-975-95677-2-9

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SPECIAL PUBLICATION: 7 Organization Secretariat

F‹GÜR

GUIDEBOOK

CONGRESS & ORGANIZATION

Editors: M. Cemal Göncüo€lu & Nihat Bozdo€an

KÜNYE ISBN: 978-975-95677-2-9 Güncellenmifl yeni bask›, Eylül 2012. 200 adet bas›lm›flt›r.

Tasar›m Uygulama ve Yay›na Haz›rl›k Pasifik Reklam Tel: 0216 348 97 22 e-posta: [email protected]

Bask› Armoni Nuans Görsel Sanatlar ve ‹letiflim Hizmetleri Yukar›dudullu, Bostanc› Yolu Cad. Keyap Çarfl› B- 1 Blk. N.24 Ümraniye / ‹STANBUL Tel: 0216 540 36 11 pbx e-posta: [email protected]

Telif Hakkı Paleozoic of Northern Gondwana and its Petroleum Potential: A Field Workshop guidebook for sariz, tufanbeyli and saimbeyli area Türkiye Petrol Jeologlar› Derne¤i’nin yayınıdır. Tüm hakları saklıdır. Türkiye’deki da¤ıtım hakkı ve yetkisi sadece Türkiye Petrol Jeologlar› Derne¤i’ne aittir. Önceden Türkiye Petrol Jeologlar› Derne¤i’nin yazılı izni olmaksızın kopyalanamaz, ço¤altılamaz ve tanıtım amaçlı bile olsa alıntı yapılamaz.

Türkiye Petrol Jeologlar› Derne¤i ‹zmir ll Cad. No:47 / 14 K›z›lay / Ankara Tel: 0312 419 86 42 • Fax: 0312419 86 43 E-mail: [email protected]

PREFACE

Dear Participants, the Paleozoic of southern Turkey has a key position for understanding the geological evolution of the NW Gondwana margin and correlation with other Gondwana-derived terranes in space and time. Beside this importance, geological investigations, especially detailed biostratigraphical and sedimentological work on the Paleozoic successions in the Taurides are very limited. This is even more remarkable considering that the Paleozoic successions in the Taurides and in particular in the Geyikda¤› Unit of the Eastern Taurides are complete and very well exposed. By this they deserve a higher reputation for the international Earth Sciences community. This guidebook aims not only to present information on the outstanding geology of the Paleozoic of the Eastern Taurides but also provide a brief review of the Paleozoic of other Turkish terranes, including the SE Anatolian Autochthon in northern continuation of Arabia.

The Turkish Association of Petroleum Geologists (TAPG) had organized the first field-meeting on the Paleozoic of southern Turkey in 1995 within the ambit IGCP. By organization of this second meeting on the “Paleozoic of Northern Gondwana and Its Petroleum Potential” TPAG fulfilled its mission.

We hope that the participants will benefit the excursion and this guidebook with a wealth of new contributions will be an important source for the stratigraphy and sedimentology of the Paleozoic of N Gondwana.

M. CEMAL GÖNCÜO⁄LU In the name of the Excursion Committee

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ORGANIZING COMMITTEE

Chairman M. Nam›k YALÇIN

Istanbul University

Vice Chairman Nihat BOZDO⁄AN

Turkish Petroleum Corporation

Secretary Ömer AKSU


Treasurer Hasan SARIKAYA


Members fi. Do¤a ATAY


Hüsnü ÇORBACIO⁄LU


Ayfle GÜZEL


Özge Ça¤layan KAYA


EXCURSION COMMITTEE Demir ALTINER

Middle East Technical University

M. Cemal GÖNCÜO⁄LU

Middle East Technical University

Hüseyin KOZLU


Nazif fiAH‹N


Achim WEHRMANN

Senckenberg Research Institute

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SCIENTIFIC COMMITTEE

Halit ALKAN

Turkish Petroleum Corporation (TPAO)

Demir ALTINER

Middle East Technical University (METU)

Özer BALKAfi

Turkish Association of Petroleum Geologist (TPJD)

Yavuz BED‹

Mineral Research and Exploration (MTA)

Nihat BOZDO⁄AN


M. Cemal GÖNCÜO⁄LU


Erdin BOZKURT


W.T. DEAN

National Museum of Wales (NMW)

A. Sami DERMAN


Jean François GHIENNE

Institut de Physique du Globe de Strasbourg (IPGS)

Erdem ‹D‹Z

Shell International B.V.

Sedat ‹NAN

TUB‹TAK Marmara Research Center

Atilla KARABULUT


Hüseyin KOZLU


Oliver MONOD

Centre National de la Recherche Scientifique (Retired)

Gonca NALCIO⁄LU

Mineral Research and Exploration (MTA)

Atike NAZ‹K

Çukurova University (CU)

Necdet ÖZGÜL


Olaf PODLAHA


Khalid RAMADAN

King Fahd University of Petroleum and Minerals

Alastair ROBERTSON

University of Edinburgh

Valeri SACHANSKI

Bulgarian Academy of Sciences

Salih SANER

Middle East Technical University NCC (METU)

Eberhard SCHINDLER


Cengiz SOYLU


Pieter SPAAK


Nazif fiAH‹N


Muhittin fiENALP

Saudi Arabian Oil Company (Retired)

Mustafa fiENEL

EnerjiSA

Aus TAWIL

Saudi Arabian Oil Company

Timur USTAÖMER

Istanbul University (IU)

Achim WEHRMANN


M. Nam›k YALÇIN


P›nar Oya YILMAZ

ExxonMobil Exploration Company

Yücel YILMAZ


‹sak YILMAZ


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SESSIONS and SESSION CONVENER

Sedimentary Basins Dr. Muhittin fiENALP Retired Saudi Aramco Sr. Geological Consultant At present consulting to Saudi Aramco and KFUPM projects Modern Evler Mah. 102 Cad. Aglarci Apt. No:72/13, Isparta / TURKEY

Stratigraphic Frame & Paleogeography Prof. Dr. Alastair ROBERTSON Professor of Geology F.R.S.E. Grant Institute, The King's Buildings, West Mains Road, Edinburgh EH9 3JW Prof. Dr. Demir ALTINER Middle East Technical University Geology Department, Ankara / TURKEY

Petroleum Systems Dr. Olaf PODLAHA Team Leader Basin Analysis and Inversion Shell Global Solutions International B.V. Kessler Park 1, 2288 GS Rijswijk, The Netherlands

Sea-level Changes and Paleoclimate Prof. Dr. Jean François GHIENNE Ecole et Observatoire des Sciences de la Terre Institut de Physique du Globe de Strasbourg (UMR 7516) 1, rue Blessig, 67084 Strasbourg Cedex

Unconventional Resources & Hot Shales Dr. Erdem ‹D‹Z Principal Technical Expert - Geochemistry; Research/Exploration Adviser E&P Innovation and Research/Development Shell International B.V. The Hague, The Netherlands - Trade Register no. 27155369 Address: c/o Kessler Park 1, 2288 GS Rijswijk, The Netherlands

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EXECUTIVE COMMITTEE OF TURKISH ASSOCIATION OF PETROLEUM GEOLOGIST

President ‹smail BAHT‹YAR

Vice President Hasan SARIKAYA

Secretary Ömer AKSU

Treasurer Cem KARATAfi

Member U¤rafl IfiIK

Member Zeynep ALAY

Member M. Bülent ERCENG‹Z

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TABLE OF CONTENTS

AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE M. C. GÖNCÜO⁄LU ................................................................................................................... 1

STRUCTURAL UNITS OF THE EASTERN TAURIDES M. C. GÖNCÜO⁄LU, N. fiAH‹N ............................................................................................... 16

CAMBRIAN M. C. GÖNCÜO⁄LU, O. EL‹CK‹, H. KOZLU, S. GÜRSU ....................................................... 22

ORDOVICIAN H. KOZLU, J. F. GHIENNE ........................................................................................................ 42

SILURIAN H. KOZLU, V. SACHANSK‹, M. C. GÖNCÜO⁄LU ................................................................... 61

DEVONIAN M.N. YALÇIN, A. WEHRMANN, E. SCHINDLER, I. YILMAZ, V. WILDE, A. NAZIR, N. BOZO⁄AN, R. ÖZKAN, H. KOZLU, R. BROCKE ................................................ 79

CARBONIFEROUS D. ALTINER, N. fiAH‹N, H. SANCAY....................................................................................... 100

PERMIAN D. ALTINER, N. fiAH‹N ............................................................................................................ 115

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE M. Cemal GÖNCÜO⁄LU Middle East Technical University, Dept. Geological Eng., 8500 Ankara-TURKEY

HISTORICAL BACKGROUND The earliest attempts to recognize the Paleozoic rocks in Turkey in a more or less systematic approach and correlate them with those in Europe dates back to the second half of the 19. Century, where a number of natural scientists reported in their classical work also the stratigraphy and fossil findings in different Paleozoic successions in Turkey (e.g. Tchihatcheff, 1864; de Verneuil, 1869). The interest of the international geological community grew with the building of the Anatolian and later the Bagdat railways and the “discovery” of the Kirkuk (Musul) oil fields in northern Iraq during the end of the 19. and early 20. Century, where a number of studies on the Paleozoic of Turkey were published (e.g. Frech, 1916; Penck, 1919). The establishment of the Mineral Research and Exploration Institute of Turkey (MTA) followed by the Turkish Petroleum Corporation (TPAO) resulted in systematic mapping of Paleozoic in Turkey, pioneered by a small number of geologists (e.g. Tolun and Ternek, 1952; Dean 1961 to 2006, Ketin, 1966, Kaya, 1973). The litho- and biostratigraphic information obtained between 1950 and 1990 was discussed during a field-meeting of IGCP 256 (Paleozoic of NW Gondwana) in 1995, organized again by the Turkish Association of Petroleum Geologists (TPJD) and published in a special issue of the Association (Göncüo¤lu & Derman, 1996). Following the Iraq War in 2003, the interest of the petroleum companies on the geology of the Northern Mesopotamia made another peak. A number of new research and exploration projects were started also in southern Turkey and a number of detailed studies with new data and models were put forward. To discuss them and record the state-of –art knowledge, TPJD organized this second field-meeting to one of the best preserved Paleozoic sections in the Eastern Mediterranean. THE TECTONIC FRAMEWORK Turkey with Thrace in the European continent and Anatolia on the Asiatic one is located in the central part of the Alpine Orogenic Belt between the Balkans and the western Asia. It was formed by the closure of at least three oceanic stands of the Neotethys between the continents Laurasia in the N and Gondwana in the south. These oceanic strands were separating smaller continental microplates rifted off from Gondwana. During the closure of the Neotethys during the Late Mesozoic-Early Tertiary by the counter-clockwise rotation of Africa, the oceanic as well as continental units (terranes) accreted to form a complex mosaic, what makes up Turkey now. For the alpine period (for a brief review see Göncüo¤lu, 2010) the geological evolution as well as the boundaries of these terranes, as shown in Figure 1, are more or less well-established. From N to S these alpine units are: the Istranca Terrane with a complex pre-alpine history including a Variscan arc, not yet fully understood; the Istanbul-Zonguldak Composite Terrane including a Cadomian basement and a Variscan passive margin; the Intra-Pontide Suture Belt with remnants of Triassic-Cretaceous northernmost Neotethys; the Sakarya Composite Terrane with Variscan and Cimmerian compounds; the Izmir-Ankara-Erzincan Suture Belt with the remnants of the middle branch of Neotethys; the Tauride-Anatolide Terrane with a Cadomian/Pan-African basement and a well-developed Paleozoic platform sequence underlying its Mesozoic platform cover; the Amanos-Elaz›¤-Van-Zagros Suture Belt with

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE remnants of the southern branch of Neotethys and the SE Anatolian Autochthon with well-developed PaleozoicMesozoic platform sequences on the N continuation of the Arabian Continent. Considering the presence of at least three pre-alpine orogenic events in the alpine terranes of Turkey, it is obvious that the configuration of the continental and oceanic micro-plates in relation to the Cimmerian, Variscan and Cadomian/Pan-African Wilson cycles is a multi-disciplinary puzzle-work as well as a challenge for the earth scientists. In this introduction we will briefly concentrate on the geological record of the Paleozoic in different alpine terranes in Turkey and evaluate its evolution within the NW Gondwanan perspective.

Figure 1: Distribution of the Paleozoic rocks in the alpine tectonostratigraphic units (terranes) of Turkey.

DISTRIBUTION OF PALEOZOIC ROCKS IN THE ALPINE TERRANES IN TURKEY The Istranca Terrane, which is considered as a “suspect terrane”, comprises a number of nappes with arc-type granitoids that yielded Early Permian ages (Okay et al, 2001) that intrude a metasedimentary succession of probably Late Paleozoic age. The Paleozoic of Istanbul and Zonguldak terranes is one of the relatively well-studied successions in Turkey and had been revised recently by Özgül (2012 and the references there in). The generalized columnar section of the Istanbul Terrane (Figure 2) shows an almost complete cycle that starts with Ordovician rift-related continental clastics above a Cadomian basement. The Late Ordovician transgression is followed by the deposition of open shelf carbonates and clastics during Silurian – Middle Devonian interval. By progressive deepening of the Paleozoic basin during the Late Devonian and Early Carboniferous, slope to basin conditions with deposition of nodular limestones and radiolarian cherts were realized. From the Early Carboniferous onwards deposition of flysch-type clastics with sporadic limestone bands indicates the onset of Variscan tectonics that culminated with the intrusion of Permian granites and folding of the Paleozoic rocks. -2-

AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE

Figure 2: Paleozoic stratigraphy of the Istanbul Terrane (Özgül, 2012).

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE To the E, a regional scale thrust seperates the Paleozoic of the Zonguldak Terrane from Istanbul. In this unit, Lower Ordovician clastics transgress onto a Cadomian basement with arc-type granitoids. The Middle OrdovicianMiddle Silurian interval is mainly represented by black shales with rare limestone intervals. In contrast to the continuous Silurian-Devonian deposits in the Istanbul Terrane, the Wenlock graptolitic shales in Zonguldak are affected by a low-grade metamorphic event and unconformably overlain by Middle Devonian shelf-type carbonates (Bozkaya et al, 2012). The carbonate deposition lasted until the Late Mississippian. Unlike the Istanbul Terrane, the Early Pennsylvanian in Zonguldak is represented by coal bearing fluvial sediments. Recently, late Middle Permian fluvial and lagoonal deposits were discovered in the Zonguldak Terrane. By this, Zonguldak unit correlates with the Moesian Terrane (Yanev et al, 2006) rather then to the Avalonian-Central European terranes.

Figure 3: Generalized columnar section of the Paleozoic rocks in the Zonguldak Terrane (Göncüo¤lu et al., 2004a, Bozkaya et al., 2012).

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE In the Sakarya Composite Terrane, Paleozoic rocks are represented by Devonian (Aysal et al., 2012) and Carboniferous (Okay et al., 2006; Ustaömer et al, 2012) granitoids intruding a Variscan metamorphic basement. This basement is unconformably overlain by Middle Permian carbonates (Okuyucu and Göncüo¤lu, 2010). Moreover, Devonian, Carboniferous and Permian sedimentary rocks of unknown origin were found as allochthonous blocks within the Cimmerian mélange complexes. The main body of the Paleozoic rocks occurs within the Tauride-Anatolide Terrane located on the northern continuation of Arabia-NW Africa before its Late Permian rifting and drifting towards north by the opening of the southern branch of Neotethys or the Avanos-Elaz›¤-Van-Zagros Ocean (Göncüo¤lu et al., 1997a). By this, the Paleozoic successions in the Tauride-Anatolide and the N-Arabian-SE Anatolian units display similarities and facial continuities as they were formed on the same N-facing platform. The Paleozoic rocks in the Anatolites, representing the N edge of the Tauride-Anatolide Platform were metamorphosed and intensively imbricated during the closure of the middle branch of alpine Neotethys (Izmir-Ankara-Erzincan Ocean) during the end of Mesozoic and Early Tertiary. By this, the Paleozoic outcrops in the Anatolides (Figure 1) are variably metamorphosed and rarely represent continuous successions. Lower Paleozoic sedimentary rocks are not proven by reliable data. Sporadic data from the Konya and Karaburun (Izmir) area (Göncüo¤lu et al, 2011), however, suggests a deep marine deposition towards N of the Paleozoic carbonate platform that lasted until the Carboniferous (Figures 4 and 5). In the Anatolides, Middle Permian is disconformable on different Paleozoic successions indicating the re-establishment of the carbonate platform after a Variscan-time event at the N Tauride-Anatolide margin (Figures 4 and 5).

Figure 4: Carboniferous-Permian evolutionary model of the N edge (Anatolides) of the Tauride-Anatolide Platform (Göncüo¤lu et al., 2007b).

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Figure 5: Low-grade metamorphic Paleozoic succession of the Anatolides in the Konya area (Göncüo¤lu, 2011)

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE The Taurides, where the main bulk of the non-metamorphic Paleozoic rocks are found, comprises a pile of nappes, or tectono-stratigraphic units (Özgül, 1976, 1984). A comprehensive tectonic classification of these nappes was proposed by Özgül (1976, 1984) regarding their palaeogeographic origins. Özgül (1984) suggested the presence of a central “autochthonous” belt (Geyikda¤› Unit), overthrust by northerly (Bozk›r, Bolkar, and Alada¤ units) and southerly (Alanya and Antalya units) derived tectono-stratigraphic units (Figure 6). From these, the Bozk›r and Alada¤ units do not comprise Lower Paleozoic successions (Figure 7). All along the belt, the Geyikda¤ Unit provides more or less continuous Paleozoic successions.

Figure 6: Palinspastic restoration of the Tauride tectonostratigraphic units (Özgül, 1984)

The most prominent and uninterrupted Paleozoic successions, however, are observed in the Geyikda¤› Unit in the Eastern Taurides, to where the field-excursion of this meeting will be realized. The details of these units will be the topic of the following chapters. The SE Anatolian Autochthon (Figure 1) on the northern edge of the Arabian Plate is another area, where metamorphic as well as non-metamorphic Paleozoic units crop out. The metamorphic Paleozoic rocks (BitlisPötürge Massifs, Figure 1) are of allochthonous character and were affected by the alpine closure of the Southern branch of Neotethys that was opened between Tauride-Anatolide Platform and the Arabian Plate during the Permian. They were imbricated together with Neotethyan oceanic units and were thrust initially during the Early Tertiary on top of each other, and then onto the Arabian Platform in successive pulses at the end of Eocene and during the Miocene. The Main Thrust Zone (Figure 1) between the Metamorphic Allochthons and the Arabian Autochthon is still an area of compression. Also supported by subsurface data from about 70 wells, the Paleozoic of the SE Anatolian Autochthon is subdivided (Y›lmaz and Duran, 1997) in the following lithostratigraphic units (Figure 8): Cambrian; Derik Group (Sadan, Koruk and Sosink formations), Ordovician; Habur Group (Seydiflehir and Bedinan formations), Silurian-Middle Devonian; Diyarbakir Group (Dadafl, Hazro and Kayayolu formations), Late Devonian-Early Carboniferous; Zap Group (Y›¤›nl›, Köprülü and Belek formations), Upper Permian; Tanin Group (Kafl and Gomaniibrik formations).

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Figure 7: Stratigraphy of the Tauride Units (after Özgül, 1984).

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Figure 8: Stratigraphic chart of the Paleozoic of the SE Anatolian Autochthon (after Bozdo¤an and Ertu¤, 1997)

Correlations between the Tauride and SE Anatolian Paleozoic units are reported in Göncüo¤lu and Kozlu (2002) evaluated in detail in the following related chapters. THE NW GONDWANAN FRAMEWORK Geological records from SE Anatolia and further E in the Zagros Belt and Oman suggests that pieces of the Arabian-Gondwanan margin, including the Tauride-Anatolide platform were rifted off the main body, by the opening of the southern branch of Neotethys (e.g. fiengör and Y›lmaz, 1981; Göncüo¤lu et al, 1997; Stampfli, 2000, Kozlu and Göncüo¤lu, 2001). Based on this and the lithological correlations, oversimplified evolutionary models (Figure 9) were proposed for the Turkish terranes within the N Gondwanan framework (Göncüo¤lu, 1995). In the last years, supported by more detailed work on paleobiogeography, paleomagnetism, zircon provinciality etc has resulted in better constrained but still speculative models (Ruban et al., 2007; van Raumer et al., 2002; Bozkurt et al, 2008; Torsvik and Cocks, 2011; Nance et al, 2012).

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Figure 9: An earlier attempt to model the evolution of the Turkish terranes in NW Gondwana (Göncüoglu, 1995, 1997).

Briefly, these models suggest the following: During the Late Neoproterozoic, the northern margin of central Gondwana (in the sense of Torsvik and Cocks, 2012; see Figure 10 below) was the site of the Cadomian Orogeny. The products of this event are found as arctype magmatic rocks and back-arc-type volcanism in the southern Turkey (e.g. Gürsu and Göncüo¤lu, 2005) and attributed variably to the Pan-African (e.g. Oberhaensli et al, 2010) or Cadomian (e.g. Göncüo¤lu et al, 2011) magmatism. The Taurides and the SE Anatolian areas (Figure 10) in NE central Gondwana, remained from Cambrian to Late Permian in the platform margin position. They may have been affected by extensional or transtensional events related to the opening of the Rheic Ocean that separated the Avalonian terranes from NW Central Gondwana during the Early Ordovician. The rifting of the Armorican (or Cadomian by Nance et al, 2012) terranes from the central part of central Gondwana during the Early Devonian has also been affecting the NE Central Gondwana. Both in the Taurides and SE Anatolian autochthon local unconformities in respective periods may be related to these events as discussed in

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Figure 10: The position of the “central Gondwana” terranes at about 480 Ma (Torsvik and Cooks, 2011).

Göncüo¤lu et al. (2004a). These events are very probably also responsible for the separation of the Istanbul and Zonguldak terranes of NW Anatolia, which drifted during Devonian (Figure 11) towards N and collided with the Laurussian continent by the closure of the Rheic Ocean (Yanev et al, 2006). The Late Carboniferous closure of the Rheic Ocean and the amalgamation of several terranes to form Pangea has obviously not directly affected the NE central Gondwana and hence the southern Turkish area. However, in the northern edge of the Taurides, in the Anatolides, a narrow back-arc basin developed during the Carboniferous was closed by creating mélanges (Figure 4; Konya Mélange, Göncüo¤lu et al, 2007; Robertson and Ustaömer, 2009). In the Tauride-Anatolide platform and in SE Anatolia, the affects of this Variscan-time event is recorded by regional

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Figure 11: Paleogeographic position of the NW Anatolian and Balkan terranes with respect to the Taurides (Yanev et al., 2007).

unconformities (Figures 5, 7 and 8). In most cases, Middle Permian is transgressive upon variably eroded Paleozoic successions (e.g. Alt›ner et al, 2000; Alt›ner and Özgül, 2001). This event is evidently not related to the Variscan orogeny on the northern margin of Paleotethys generated by the closure of the Rheic Ocean but to the collision of an oceanic plateau and the closure of a marginal back-arc basin with the Anatolide margin. Late Permian in Turkey is characterized by the deposition of oceanic sediments in the prevailing (Paleotethys) and new oceans (Neotethys). Paleontological record from the Paleotethys in NW Turkey (radiolarian data, e.g. Göncüo¤lu et al., 2004b) evidences oceanic basin conditions during the Changxingian. In Oman, on the E continuation of the Bitlis-Zagros Belt, similar findings were reported (e.g. fiengör, 1990). On the continental microplates, such as the Tauride-Anatolide Unit or Sakarya Composite Terrane, on the other hand, platform-type carbonates were deposited. To conclude, the Paleozoic Turkish terranes in the N (Istanbul-Zonguldak) and in the S (Tauride-Anatolide and SE Anatolia) although derived from N Gondwana, went through completely different evolutionary paths. Our available data is still very fragmentary to be able to reconstruct this complex geological history. -12-

AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE REFERENCES Alt›ner D. & Özgül N. 2001. Carboniferous and Permian of the allochthonous terranes of the Central Tauride Belt, Southern Turkey. Guide Book of Paleo-Forams 2001, 35p. Alt›ner, D., Özkan-Alt›ner, S. & Koçyi¤it, A. 2000. Late Permian foraminiferal biofacies belts in Turkey: palaeogeographic and tectonic implications. In: Bozkurt, E., Winchester, J. A. & Piper, J. A. D. (eds) Tectonics and Magmatism in Turkey and the surrounding Area. Geological Society, London, Special Publications, 173, 83–96. Aysal, N., Ustaömer, T., Öngen, S., Keskin, M., Köksal, S., Peytcheva, I. & Fanning. M. 2012. Origin of the LowerMiddle Devonian magmatism in the Sakarya zone, NW Turkey: Geochronology, geochemistry and isotope systematics. Journal of Asian Earth Sciences, 45, 201-222. Bozdo¤an, N. & Ertu¤, K. 1997. Geological evolution and paleogeography of SE Anatolia in the Paleozoic. In: Göncüo¤lu, M.C. & Derman, A.S. (Eds) Early Paleozoic Evolution in NW Gondwana Proceedings. Turkish Association of Petroleum Geologists, Special Publication, 3, 39-50. Bozkaya, O., Yalcin, H. & Göncüo¤lu, M.C. 2012. Mineralogic evidences of a mid-Paleozoic tectonothermal event in the Zonguldak terrane, northwest Turkey: implications for the dynamics of some Gondwana-derived terranes during the closure of the Rheic Ocean.Can. J. Earth Sci. 49: 559–575. Bozkurt, E., Pereira, M.F., Strachan, R. & Queseda, C. 2008. Evolution of the Rheic Ocean. Tectonophysics, 461, 1-8. Dean, W.T. & Krummenacher, R. 1961. Cambrian trilobites from the Amanos Mountains, Turkey. Palaeontology, 4, 71-81. de Verneuil, E., 1869. Appendice à la faune Dévonienne du Bosphore. Append. Asie Mineure de Tchihatcheff, Paleontologie 425-495. Paris . Frech, F. 1916. Geologie Kleinasiens im Bereich der Bagdatbahn. F. Enke Verlag, Stuttgart-Deutschland. Göncüo¤lu, M.C. 2011. Kütahya-Bolkarda¤ Kufla¤›n›n Jeolojisi. MTA Dergisi, 142, 227-282. Göncüo¤lu, M.C. 1995, Lower Paleozoic Units in the Alpine Terranes of Turkey. 3. Int. Meeting of IGCP 351, “Early Paleozoic Evolution in NW Gondwana”, Turkish Assoc. Petrol. Geologists, Spec. Publ. No 1,1. Göncüo¤lu, M.C. 1997. Distribution of Lower Paleozoic Units in the Alpine Terranes of Turkey: paleogeographic constraints. In: Göncüo¤lu, M.C. and Derman, A.S.(Eds), Lower Paleozoic Evolution in northwest Gondwana, Turkish Assoc. Petrol. Geol., Spec. Publ.No:3, 13-24, Ankara. Göncüo¤lu, M.C. and Kozlu, H., 2000, Early Paleozoic evolution of the NW Gondwanaland: data from southern Turkey and surrounding regions. Gondwana Research, 3, 315-323. Göncüo¤lu, M.C. Dirik, K. & Kozlu, H. 1997a. General Characteristics of pre-Alpine and Alpine Terranes in Turkey: Explanatory notes to the terrane map of Turkey. Annales Geologique de Pays Hellenique, 37, 515-536. Göncüo¤lu, M.C., Çapkinoglu, S., Gürsu, S, Noble, P, Turhan, N, Tekin, UK, Cengiz Okuyucu, C. & Göncüoglu, Y. 2007. The Mississippian in the Central and Eastern Taurides (Turkey): constraints on the tectonic setting of the Tauride-Anatolide Platform. Geol. Carp, 58, 427-442. Göncüo¤lu, M.C. Göncüoglu, Y., Kozlu, H. & Kozur, H. 2004a, Geological evolution of the Taurides during the Infra-Cambrian to Carboniferous period: a Gondwanan perspective based on new biostratigraphic findings. Geol Carphatica 55/6, 433-447. Göncüo¤lu, M.C., Kuwahara, K., Tekin, K.U. & Turhan, N. 2004b. Upper Permian (Changxingian) radiolarian cherts within the clastic successions of the “Karakaya Complex” in NW Anatolia. Turkish Journal of Earth Sciences 13, 201-213. Göncüo¤lu, M.C., Saydam, DG, Gedik, ‹., Okuyucu, C, Özgül, N, Timur, E, Yanev, S, Boncheva, ‹, Lakova, ‹, Sachanski, V & Maliakov, Y. 2004c. Correlation of the Paleozoic successions in the Bulgarian and NW Turkish terranes. MTA-BAS-TUBITAK Project Nr: 2004-16B4, 44p.

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE Göncüo¤lu, M.C., Koksal, S. & Gürsu, S., 2011. How to classifie the Late Neoproterozoic magmatism in diverse alpine terranes in Anatolia: Cadomian or Pan-African. 23. Colloq. African Geology., 8-14 Jan., 2011 Johannesburg, Abstract Vol., 160. Gürsu, S. & Göncüo¤lu, M. C. 2005. Early Cambrian back-arc volcanism in the western Taurides, Turkey: implications for rifting along the northern Gondwanan margin. Geol Mag. 142, 617-631. Kaya, O. 1973. Paleozoic of Istanbul. Ege Univ. Sci. Faculty, Ser. 40. Izmir. Ketin, I. 1966. Güneydo¤u Anadolu’nun Kambriyen teflekkülleri ve bunlar›n do¤u Iran Kambriyeni ile Mukayesesi. MTA Dergisi 1966. Kozlu, H. and Göncüo¤lu, M.C., 2001 Geological evolution of the Taurides during the Infracambrian to Carboniferous period: a Gondwanan perspective. 4th Int. Symposium on the Eastern Meditteranean Geology. 21-25 May 2001, Isparta, Abstracts, 14-15. Murphy, J.B., Keppie, J.D., Nance, R.D. & Dostal, J. 2009. Comperative evolution of the Iapetus and Rheic Oceans: a North American perspective. Gondwana Research, 17, 482-499. Nance, R.D., Gutierrez-Alonso, G., Keppie, J.D., Linnemann, U., et al., 2012. A brief history of the Rheic Ocean. Geoscience Frontiers, 3, 125-135. Oberhaensli, R., Candan, O. & Wilke, F. 2010. Geochronological Evidence of Pan-African Eclogites from the Central Menderes Massif, Turkey. TJES, 19, 431-447 Okay, A.I., Sat›r, M., Tüysüz, O., Akyüz, S. & Chen, F. 2001. The tectonics of the Strandja Massif: late Variscan and mid Mesozoic deformation and metamorphism in the northern Aegean. Int. J. Earth Sci., 90, 217-233. Okay, A.I., Sat›r, M. & Siebel, W. 2006. Pre-Alpide Palaeozoic and Mesozoic orogenic events in the Eastern Mediterranean region. Geol. Soc. Memoir, 32, 389-405. Okuyucu, C. & Göncüo¤lu, M.C. 2010. Middle–late Asselian (Early Permian) fusulinid fauna from the post-Variscan cover in NW Anatolia (Turkey): Biostratigraphy and geological implications. Geobios, 43, 225–240. Özgül, N. 1976. Toroslar’›n baz› temel jeoloji özellikleri. Bulletin of the Geological Society of Turkey, 19, 65-78. (In Turkish with an English abstract) Özgül, N. 1984. Stratigraphy and tectonic evolution of the Central Taurides. In: Tekeli, O. & Göncüo¤lu, M. C. (eds), Geology of the Taurus Belt. Mineral Research and Exploration Institute of Turkey Publication, 77-90. Özgül, N. 2012. Stratigraphy and some structural features of the ‹stanbul Palaeozoic. Turkish Journal of Earth Sciences, 21, 817-866. Penck, W. 1919. Grundzüge der Geologie des Bosphorus. Veröff. Inst. für Meereskunde, N. F., . 4, pp.1-57. Raumer, J.V. von, Stampfli, G.M., Borel, G. & Bussy, F. 2002. Organization of pre-Variscan basement areas at the north-Gondwanan margin. International Journal of Earth Sciences, 91, 35-52. Robertson, AHF & Ustaömer, T., 2009. Formation of the Upper Palaeozoic Konya Complex and comparable units in southern Turkey by subduction-accretion processes: Implications for the tectonic development of Tethys in the Eastern Mediterranean region. Tectonophys., 473, 113-148. Ruban, D.A., Al-Husseini, M.I., & Iwasaki, Y. 2007. Rexiew of the Middle East Palaeozoic plate tectonics, GeoArabia, 12, 35-56. fiengör, A.M.C. 1990. A new model for the late Paleozoic-Mesozoic tectonic evolution of ›ran and implications for Oman. Geological Society, London. Spec. Publ., 49, 797-831. fiengör, A.M.C. & Y›lmaz, Y. 1981. Tethyan evolution of Turkey: a plate tectonic approach. Tectonophysics, 75, 181-241. Stampfli, G.M. 2000. Tethyan oceans. In: Bozkurt, E., Winchester, J.A., Piper, J.D. (Eds.): Tectonics and Magmatism in Turkey and Surrounding Area. Geological Society, London, Special Publications, 173, 1-23. Strickland, H. E. 1848. On the present state of knowledge of the geology of Asia Minor. Philosophical Magazine Series 3, Volume 32, Issue 213, 137-139. Tchihatcheff de, P. 1866 -1869. Asie Mineure, description physique de cette contrée. Paris

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AN INTRODUCTION TO THE PALEOZOIC OF ANATOLIA WITH A NW GONDWANAN PERSPECTIVE Tolun, N. & Ternek, Z., 1951. Notes Géologiques sur la Région de Mardin. Bull. Geol. Soc. Turkey, 3, 15-19 Torsvik, T.H.& Cocks LRM. 2011. The Palaeozoic of central Gondwana. Geological Society, Spec. Publ., 357, 137-166. Ustaömer, PA, Ustaömer, T & Robertson AHF. 2012. Ion Probe U-Pb Dating of the Central Sakarya Basement: A peri-Gondwana Terrane Intruded by Late Lower Carboniferous Subduction/Collision-related Granitic Rocks. Turkish Journal of Earth Sciences, 21, 905-932. Yanev, S., Göncüoglu, M.C., Gedik I., Lakova, I., Boncheva, I., Sachanski, V., Okuyucu, C., Özgül, N., Timur, E., Maliakov, Y & Saydam, G. 2006. Stratigraphy, correlations and palaeogeography of Palaeozoic terranes in Bulgaria and NW Turkey: A review of recent data. (Robertson, AHF & Mountrakis, D. (Eds) In: Tectonic development of the Eastern Meditteranean Region. Geological Society London Spec. Publ. 260, 51-67. Y›lmaz, E. & Duran, O. 1997. Güneydo¤u Anadolu Bölgesi Otokton ve Allokton Birimler Stratigrafi Adlama Sözlü¤ü “Lexicon”, TPAO Araflt›rma Merkezi Grubu Baflkanl›¤›, E¤itim Yay›nlar›, 31, 460 s.

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STRUCTURAL UNITS OF THE EASTERN TAURIDES STRUCTURAL UNITS OF THE EASTERN TAURIDES M. Cemal GÖNCÜO⁄LU1 and Nazif fiAH‹N2 1

Middle East Technical University, Department of Geological Engineering, Ankara-Turkey 2 Turkish Petroleum Corporation, Ankara Turkey

The Taurus Belt is geographically subdivided into three portions by two N-S oriented major faults (Figure 1) The Eastern Taurus region is bordered in the east by the Munzur Mountains and in the west by the Ecemifl fault.

Figure1: The geographical subdivision of the Taurus Belt (Özgül,1973)

STRATIGRAPHY AND STRUCTURAL RELATIONS OF THE EASTERN TAURUS REGION: Detailed geological mapping in the Eastern Taurides area revealed the pres ence of several structual units (Blumenthal, 1952; Demirtafll›, 1967; Özgül et al., 1973; Aziz and Erakman, 1980; Ayhan, 1988; Metin et al., 1986, 1990; Kozlu, 1990). These units are arranged from northwest to southeast as the Alada¤, Geyikda¤›, Nurhak-Munzur, Engizek-Binbo¤a, Berit-Yüksekova, Missis-And›r›n, Maden-Pötürge units and the SE Anatolian Autochthon or the N Arabian Platform (Figure 2). The nappe structure was gained during the Tertiary compressional event. Subsequent strike-slip faulting during the Neotectonic period has additionally resulted in a very complex tectonic framework. From these the Alada¤ Unit comprises shelf type clastics and carbonates of Upper Devonian-Upper Cretaceous age (see Figure 7 in Introduction). In the Eastern Taurides Alada¤ Unit is completely allochthonous and forms a flat lying nappe over the Lutetian (Middle Eocene) flysch of the Geyikda¤› Unit.

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STRUCTURAL UNITS OF THE EASTERN TAURIDES

Figure 2: Tectonic units of the Eastern Taurides ( after Özgül,1976; 1985)

The Geyikda¤ Unit is also known as the “Eastern Tauride Para-autochthone’’ as new findings (Özgül and Kozlu, 2002) suggests the presence of Cretaceous rocks in a tectonic window beneath the Infracambrian basement of the Unit. It is characterized by an almost complete Paleozoic succession, which will be studid in detail during this excursion. The simplified geological map of the Geyikda¤ Unit is given in Figure 3.

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STRUCTURAL UNITS OF THE EASTERN TAURIDES

Figure 3: Geological map of the Geyikda¤ Unit with the locations of the sections to be visited during the excursion.

The excursion will focus on Paleozoic sections in three areas: A- De¤irmentafl- Halevik Dere Section (Section A in Figure 3) to the W of Sar›z, where from bottom to the top; the Middle Cambrian Çaltepe Formation, the Upper Cambrian-Middle Ordovician Seydiflehir Formation, Upper Ordovician fiort Tepe and Halevikdere formations, Lower Silurian Puflçutepe Formation, Upper Silurian Lower Devonian Yukar›yayla Formation, and the Lower-Upper Devonian Ay›tepesi, fiafaktepe and Gümüflali formations will be visited. B- Naltafl Section to the SE of Naltafl Village (Figure 3) with Lower Carboniferous Ziyarettepe and Permian Y›¤›l›tepe formations will be studied. C- Kösrelik Section to the E of Tufanbeyli (Fig. 3) with the complete Middle-Upper Permian succession (Y›¤›l›tepe Formation) and its transition to the Triassic Kataras› Formation will be evaluated. The 3D Google Earth images as well as the 1/500.000 scaled geological maps (MTA, 1989) of the areas to be visited are enclosed in the front of the respective chapters of the sections .

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STRUCTURAL UNITS OF THE EASTERN TAURIDES REFERENCES Ayhan, A. 1988. Explanations to 1/100.000 scaled reconnecance geological map series: Kozan J21 Sheet. 23p. Gen. Direct. Min. Res. Explor. Publication (in Turkish). Aziz, A. & Erakman, B. 1980. Geology and hydrocarbon potential of the area between Tufanbeyli (Adana) Sar›z (Kayseri), Gürün (Sivas). Turkish Petrol. Corp., Report Nr: 1526, Ankara (in Turkish, unpublished). Blumenthal, M.M. 1952. Das taurische Hochgebirge des Aladag: Neuere Forschungen zu seiner Geographie, Stratigraphie und Tektonik. MTA Monographies, D6, 136pp. Demirtafll›, E. 1967. P›narbafl›-Sar›z-Ma¤ara civar›n›n jeoloji raporu. M.T.A. Report, Nr.: 1935 (in Turkish, unpublished). Kozlu, H. 1990. Geology and hydrocarbon potential of the area between Tufanbeyli-Sar›z-Gürün. Turkish Petrol. Corp., Report Nr: 2851, Ankara (in Turkish, unpublished). Metin, S., Ayhan, A. & Papak, ‹. 1990. Elbistan – ‹22 Paftas›. Maden Tetkik ve Arama Genel Müdürlü¤ü, 1:100 000 ölçekli aç›nsama nitelikli Türkiye Jeoloji Haritalar› Serisi, 1-15. (In Turkish) Metin, S., Ayhan, A. & Papak, ‹. 1986. Do¤u Toroslar’›n bat› kesiminin jeolojisi (GGD Türkiye). M.T.A. Dergisi, 107, 1-12. (In Turkish) Özgül, N. 1976. Toroslar’›n baz› temel jeoloji özellikleri. Bulletin of the Geological Society of Turkey, 19, 65-78. (In Turkish with an English abstract) Özgül, N. & Kozlu, H. 2002. Kozan-Feke (Do¤u Toroslar) yöresinin stratigrafisi ve yap›sal konumu ile bulgular. The Bulletin of Turkish Association of Petroleum Geologists, 14, 1-36. (In Turkish with English abstract)

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3D image of the excursion route to De¤irmentafl-Halevik Dere section.

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Geological route map of the De¤irmentafl-Halevik Dere Excursion (MTA 1/500.000 scaled geological map, Sheet Kayseri)

Legend of the geological map

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CAMBRIAN CAMBRIAN M. Cemal GÖNCÜO⁄LU1, Olaf ELICKI2, Hüseyin KOZLU3, Semih GÜRSU4 1Middle

East Technical University, Department of Geological Eng., Ankara-Turkey 2Freiberg University, Geological Institute, Freiberg, Germany 3Çi¤dem Mah.1575 Sok. 41/22-Cankaya/Ankara-Turkey 4Mu¤la University, Department of Geological Eng., Kötekli-Mu¤la-Turkey

INTRODUCTION A number of the crystalline rocks with Cambrian radiometric ages are reported in the northern Istanbul-Zonguldak Terrane. Other than in the southern terranes, these arc-type granodiorites intrude or are associated with Late Neoproterozoic metagabbros, orthoamphibolites and pyroxenites (Ustaömer and Rogers, 1999). Overall, the Cambrian rocks are interpreted as representatives of a Cadomian intra-oceanic arc, formed within the IapetusTornquist oceanic lithosphere (Göncüo¤lu, 1997; Göncüo¤lu and Kozlu, 1997). In some successions in the Menderes Massif and the Central Anatolian Crystalline Complex of the Anatolides, rock units very similar to those in the Tauride-Anatolide platform are reported by Kozlu and Göncüo¤lu (1997). The Cambrian in the Taurides shows in general very similar features across the belt (Figure 1) and will be evaluated in detail in the following chapters.

Figure 1: Correlation of the Cambrian successions in the Taurides (modified after Göncüo¤lu, 1997)

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CAMBRIAN In the SE Anatolian Autochthon the Cambrian rocks are represented by the Sadan (=Zabuk), Koruk and Sosink formations, respectively. The Sadan Formation is transgressive on the pre-Cambrian fluvial sediments and volcanic rocks. The geological evolution of the Cambrian has been recently reviewed by Ghienne et al. (2010 and the references therein) and briefly summarized by Kozlu and Ghienne (this volume) in the following chapter. This recent evaluation of these authors suggests that in ascending order the following depositional sequences can be distinguished on the basis of recognition of major transgressive events and subsequent shelf progradations. The first one is earliest Cambrian (early Terreneuvian) in age and corresponds to the initiation of a cratonic platform regime upon a Late Neoproterozoic basement with bimodal volcanism (Gürsu et al., 2010). The deposits are alluvial fan, lagoonal and lake and playa type in ascending order. Very recently Demircan et al. (2011) reported ichnofossils of Terreneuvian Series in this unit. The second depositional sequence is late Terreneuvian? to early Furongian (early Cambrian to early Late Cambrian in the former terminology) in age, whereas the third one includes the late Furongian to early Middle Ordovician (Late Cambrian to middle Arenig in the British regional terminology) interval. These two sequences are related to the development of a stable platform, represented by the deposition of fluvial to tidal siltstones and sandstones (Sadan Formation) shallow marine carbonates (Koruk Formation in SE Anatolian Autochthon), and the Çal Tepe formation in the Taurides (Figure 2). The succession comprises dolomite-limestone-nodular limestone in ascending order and is relatively well-dated by trilobites and chitinozoans (Dean and Monod, 1997; Ghienne et al., 2010). The third depositional sequence is characterized by the storm-dominated, essentially carbonate-free, detrital deposits constituting the Sosink Formation in the SE Anatolian Autochthon and the Seydiflehir Formation in the Taurides (Dean and Monod 1990). The biostratigraphic control is based on trilobites and acritarchs (Dean and Martin 1992, Paris et al., 2007). The classification may also help for a reliable correlation between the Turkish and Arabian Lower Paleozoic formations as given in Figure 3.

Figure 2: Depositional features and distribution of the Middle and Late Cambrian in the Taurides and the SE Anatolian Autochthon (Ghienne et al., 2010).

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CAMBRIAN CAMBRIAN STRATA IN THE TAURIDES Western and Central Taurides In the western Central Anatolia, Cambrian rocks disconformably overlie the Neoproterozoic “Sand›kl› Basement Complex” (Gürsu and Göncüo¤lu 2001). The Basement Complex is composed of siliciclastic rocks with rare black chert and dolomite lenses and includes conglomerates, dark colored brecciated limestones, cherty and laminated limestones interbedded with sandstones. This low-grade metamorphic unit is intruded by porphyroids and microgranites with latest Neoproterozoic zircon ages (Gürsu et al., 2004), which in turn are unconformably overlain by variegated conglomeratic sandstones and shales with basic to intermediate lava flows. Upwards, they grade into green, violet and yellow quartz siltstones (Gö¤ebakan Formation, Figure 4) and variegated mudstones. They are transgressively overlain by tidal-dominated deltaic sandstones, siltstones and rare shales (Celilo¤lu Member)

Figure 3: Tentative correlation of Cambro-Ordovician successions in the Near and the Middle East and N Africa with special emphasise on the Middle Cambrian Çal Tepe Formation (Elicki et al., 2012).

that have yielded Early Cambrian trace fossils (Erdo¤an et al., 2004). The overlying tidal sandstones (Hüdai and Feke formations) are very widespread throughout the Taurides. They are conformably overlain by the Çal Tepe Formation. The Çal Tepe Formation forms a trilogy of dolomite-dolomitic limestone, black limestone and nodular limestone. It starts with inter-to shallow subtidal, partly restricted-marine carbonates, followed by subtidal to deepsubtidal, open marine limestones with microbial formations. The nodular limestones are condensed and open marine. It includes microbial-archeocyathan biostromes. The ages and fossil contents are shown on Figure 5.

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CAMBRIAN

Figure 4: Generalized Columnar Section of the Cambro-Ordovician rocks in Sand›kl› area (After Gürsu et al., 2004 and Elicki et al., 2012).

Figure 5: Ages and fossil content of the Çal Tepe Formation (Elicki et al., 2012)

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CAMBRIAN In the type-section of the Çal Tepe Formation in the Seydiflehir area (Figure 6), only the Çal Tepe formation and its transition to the overlying Seydiflehir Formation are observed. Here again the dolomite- black limestone/light gray limestone-nodular limestone subdivision is very well established and had been relatively well-studied considering its biostratigraphy (Sarmiento et al., 2001; Dean, 2005; Elicki et al., 2007; Elicki and Gürsu, 2009)

Figure 6: Cross section of the Çal Tepe Formation in its type-locality (after Dean, 2005 and Elicki and Gürsu, 2009)

Further Cambrian outcrops in the W and Central Taurides are reported in the Tahtal›da¤ (fienel et al., 2000), Antalya-Kemer (Göncüo¤lu and Kozur, 1999), Silifke-Ovac›k and Alanya-Anamur (Demirtafll›, 1984), Sultan Mountains (Shergold & Sduzy, 1984) and Sar›çiçek (Dumont, 1972) regions and correlated in Figure 1. CAMBRIAN IN THE EASTERN TAURIDES The Cambrian rocks in the Eastern Taurides are mainly represented by two formations in the Geyikda¤› Unit of Özgül (1976). The lower one is represented by quartzites and quartz-arenites, variably called as the Koçyaz› (Özgül and Kozlu, 1993) or Feke Quartzite (Kozlu and Göncüo¤lu, 1997). It is the equivalent of the Hüdai Formation in the W and Central Taurides. It conformably overlies a very thick basement succession made of siliciclastic rocks cut by felsic dykes, black and gray shales, lydites (Oruçlu Member) and stromatolitic, ankeritic and cherty limestones and dolomites (‹çmetepe Member). The unit was named as the Emirgazi Formation by Özgül et al. (1972) and well-exposed along numerous sections in the Kozan, Feke, Tufanbeyli and Saimbeyli areas (Figure1) in the Geyikda¤› Unit of the E Taurides. The illite crystallinity (IC) value of the white micas of the Emirgazi Formation is 1000 m) that is usually strongly folded and imbricated by Alpine tectonics. But, the exceptional Sar›z-Saimbeyli region in the eastern Taurus offers several continuous, clearly exposed sections of Depositional Sequence 3 (Figure 5), which correspond essentially to the Lower Ordovician Seydiflehir Fm. (Monod, 1967; Dean and Monod 1970; Özgül 1973).

Figure 5: General view of the upper part (ca. 500 m thick) of the coarsening-upward Floian succession in the De¤irmentafl area (Seydiflehir Fm.). Wave-dominated, 10 to 40 m thick parasequences including transgressive tidal sandstones are welldefined (cf. Figure 13).

Most of Depositional Sequence 3 commonly comprises a fine-grained lower part, and a sandier upper part, which together constitute the regressive system tract. The lower part corresponds to thick (300-1000 m) shale- to siltstone-dominated successions with subordinate sandstone beds and rare red limestone horizons, the age of which is mainly Tremadocian (Özgül et al., 1972; Göncüo¤lu et al., 2004; cf. STOP 2). Lithofacies and graptolites indicate inner to outer shelf, offshore depositional environments. The upper part (> 500 m), of Floian and early Middle Ordovician age (i.e. Arenig in the British regional terminology; Dean, 1971), is made up of alternating siltstones and sandstones, and has provided most of the recorded macrofossils (trilobites, cephalopods, brachiopods, gastropods, Dean and Monod, 1970; Monod, 1967). In the southern and western Taurides (Antalya Nappes, Sultan Da¤, Akyaka), the latter strata typically form a succession of storm-dominated, shallowing-upward facies suites (i.e. parasequences, 5-10 m thick, comprising siltstones and sandstones (HCS, wave ripples, climbing ripples, cogenetic ripples, gutter casts). Bioturbation occurs frequently and is most often of Phycodes type, the Cruziana ichnofacies being very rare. Sandy, calcareous bioclastic lenses occur as reworked shell-beds in the upper half of the formation. In the eastern Taurus (Sar›z-Saimbeyli area) the regressive system tract of Depositional sequence 3 is initially dominated by offshore facies. It comprises three distinct coarsening, thickening-upwards units, which represent three vertically superimposed individual prograding wedges (Figure 5). In particular, the Tremadocian/ earliest Floian cycle was initiated late in the Upper Cambrian is documented. It is however relatively poorly evidenced in the distal setting of southern Turkey, in comparison with more proximal settings such as Oman or Algeria.

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ORDOVICIAN Bedinan-Qasim sag-basin development (Kilgen Lake and fiort Tepe formations) A widespread but laterally differentiated, predominantly fine-grained succession characterizes Depositional Sequence 4. It is a thin to very thick (20 m to over 1000 m) clastic wedge, resting unconformably on Depositional Sequences 3 and 2. It is topped regionally by Upper Ordovician glacial deposits. Related deposits were identified long ago in the Border Folds (Perinçek et al., 1981; Dean and Monod, 1990). Recently, deposits ascribed to Depositional Sequence 4 were formally identified throughout the Taurides thanks to the recovery of palynomorphs spanning the whole Middle to Late Ordovician (Paris et al., 2007). Depositional Sequence 4 corresponds essentially to the Qasim Fm. in central Saudi Arabia and to the Khabour Fm. in Iraq. In Turkey, the lower boundary of Depositional Sequence 4 corresponds to a sharp lithologic break usually associated with a stratigraphic hiatus. In the Border Folds, a significant but localized (Mardin High, Figure 3) hiatus may occur with an up to 50 Ma hiatus underlying the base of the Bedinan Fm. In adjacent areas, the continuous record of Depositional 4 highlights a clear tectonic differentiation of uplifting/ subsiding areas during the Middle Ordovician (Paris et al., 2007; Ghienne et al., 2010). In the Taurides, a more or less expanded stratigraphic hiatus is identified all along the chain (except in the Antalya Nappes owing to tectonic imbrications). The unconformity is usually underlined by a ferruginous oolitic bed and/or a several metres thick limestone unit (Sobova Fm., Beyflehir area, Dean, 1973; Kozan area, Figure 6), which yielded Early Darriwilian conodonts (Sarmiento et al., 2003). Where present, upper Darriwilian strata are typified by the occurrence of gravity-driven deposits or a turbidite-prone delta setting (Ghienne et al., 2010). Contrasting with the extraordinarily widespread and long lasting stability of the northern part of the Gondwana platform from Cambrian to Early Ordovician, tectonic instability led in the Middle Ordovician to a new platformscale palaeogeographic organisation with the development of the Bedinan-Qasim depocentre to the south and the end of subsidence to the north in the Taurus domain (Figures 3 & 4; Ghienne et al., 2010). This evolution is superimposed on(?) -or at least coeval with- the signature of the major, late Middle Ordovician transgression (MFS O30 of Sharland et al., 2001; Haq and Al-Qahtani, 2005; Molyneux et al., 2006 ; Ghienne et al., 2007a; “Late Llanvirn peak transgression” of Galeazzi et al., 2010). Lower Darriwilian to Upper Ordovician deposits of Depositional Sequence 4 then subsequently progressively onlapped the basal unconformity. Surprisingly, although the thickness of Depositional Sequence 4 rarely exceeds 100 m in the Taurides, it can be consistently identified (Figure 3), in spite of various facies differentiations. Latest Darriwilian, Sandbian and Katian strata are best exposed in the eastern Taurides where they comprises an onlapping, regionally diachronous, 30 to 80 m thick, siltstone to fine-grained sandstone succession. In the eastern Taurus (Kilgen Lake section, north of Kozan), it consists of graptolite-bearing siltstones and fine-grained sandstones (Kilgen Lake Fm., Figure 6). The highest beds include poorly preserved trilobites (uppermost Sandbian to lower Katian?). These condensed, poorly differentiated successions that include fine-grained sandstone deposited below storm-wave base and deep-water faunas (graptolites, cyclopygid trilobites) suggesting a non-subsiding, condensed, outer shelf/ upper slope depositional environment, dominated by shallow-water bottom-current sand deposits. This unusual facies is in good agreement with in-situ reworking as noted for palynomorph mixing (Paris et al. 2007). In the De¤irmentafl area (Sar›z region, cf. STOP 4), a much younger siltstone-dominated succession, essentially late Katian in age (Early Ashgill, Dean and Monod, 1990) rests disconformably on Lower Ordovician strata. Here, the underlying unconformity at the top of the Lower Ordovician sandstones represents a time interval including the Middle Ordovician, the Sandbian and probably most of the lower (to middle?) Katian (Figure 6).

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ORDOVICIAN

Figure 6: Sedimentary section of the Middle to Upper Ordovician record near Kozan (ca. 100 km south of De¤irmentafl), compared to that of De¤irmentafl. Despite similar fine-grained successions in both areas, they are for their most part fully diachronous. While a minor hiatus (within the Middle Ordovician) is documented in Kozan, a major hiatus up to the Lower Katian is evidenced in De¤irmentafl. It is interpreted as a depositional wedge overlying and onlapping an uplifted (or uplifting?) structural high located in an outer shelf setting (cf. Figure 4).

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ORDOVICIAN The Hirnantian glaciation (Halevikdere Fm.) Glaciation-related deposits have only recently been formally identified throughout Turkey (Halevikdere Fm.), except in areas where the Paleozoic succession is deeply truncated by Mesozoic or younger deposits, such as Western Taurus (Figures 1 & 2). They have been dated as Hirnantian by palynomorph assemblages (Monod et al., 2003; Paris et al., 2007). Glaciogenics usually exhibit a sharp basal contact but with conformable relationships (e.g. Antalya Nappes, Figure 7).

Figure 7: The Hirnantian glacial record of the Antalya Nappes (Kemer Gorge). A two-fold glaciomarine succession separated by an interglacial shaly interval is documented. Macrophotographs illustrate typical ice-distal glaciomarine facies in the Kemer Gorge, which are similar to those that characterized the outer North Gondwana shelf during the latest Ordovician.

An erosional contact may reaches in places the Lower Ordovician rocks as in the S and SE Taurus (Kozan). On the Mardin High (Border Folds), correlation with the subsurface shows the removal of Ordovician rocks about 200 m thick before deposition of a 75 m thick fining-upward conglomeratic unit onlapping subglacial streamlined bedforms indicating the Hirnantian ice sheet reach this relatively far distal location north of the Arabian plate (Monod et al., 2003; Ghienne et al., 2007a, 2010). By definition of a transgressive-regressive sequence, the upper bounding surface of Depositional Sequence 4 is situated on top of the maximum regressive facies, beneath the overlying deglacial transgressive strata, and thus matches the maximum glacio-eustatic sea-level fall of the Late Ordovician glaciation. Where a glacial surface can be characterized, as in the NE Taurus (Monod et al., 2003) or in the Mardin High, the related unconformity

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ORDOVICIAN is taken as the upper boundary of Depositional Sequence 4. The overlying glaciomarine facies suite forms the lowermost, transgressive part of a fifth sequence extending into the Silurian. The glacial deposits exhibit a fairly constant thickness (60-120 m) throughout the Taurides (Figure 8). Monod et al. (2003) detailed the succession in the southern and eastern Taurus where the strata comprise a basal, conglomeratic, proximal glaciomarine sandy wedge, overlain by thin, discontinuous tidal sandstones. Its top is in places bounded by a striated glacial pavement in the NE Taurus, above which a fining-up, 40-80 m succession contains the full spectrum of recessional glaciomarine depositional environments.

Figure 8: The Hirnantian glaciogenics (Halevikdere Fm.) from north to south of the Eastern Taurus. Two glacial cycles are consistently documented, with few thickness variations. The datum line corresponds to an abrupt transition from glaciomarine facies to finer-grained sediments with only sparse ice-rafted debris (modified from Monod et al., 2003).

In only one section (Ovac›k), the highest parts of the glacially related strata contain rare macrofauna, mainly brachiopod fragments1 . In the Antalya Nappes, glacial strata show a conspicuous two-fold lithostratigraphy, with two sandy diamictite packages separated by non-glacial offshore shales (Figure 7). Basically, the two Hirnantian glacial cycle identified in North Africa (Ghienne et al., 2007b; Loi et al., 2010; Figure 9) and more distal domains (Bohemia, Kosov Fm., Storch, 2006) would be therefore also present in Turkey. 1

Among them, Mirorthis sp. known only from the Hirnantian in Morocco, China, Burma and Thailand; other fragments include Dalmanella? and undetermined orthids.

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ORDOVICIAN

Figure 9: High-resolution sequence analysis in the Late Ordovician of the central Anti-Atlas, Morocco (Loi et al., 2010). Very high frequency to “3rd order” cycles have been documented, permitting the temporal calibration of chitinozoan-based biozones. In addition, a backstripping approach allowed estimated depositional depths (right column) to be interpreted as a glacioeustatic signal because high amplitude events are synchronous with sea-level falls in the paleo-tropics. As far as the Hirnantian record is concerned, two major glacial cycles separated by an interglacial period are documented, which have their counterparts in the Turkish record (cf. Figure 8 and 14).

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ORDOVICIAN The intermediate transgressive episode is represented by offshore shales in the Kemer region (Figure 7) and tidal sandbars in the Kozan area (Figure 6). The maximum glacial advance (Figure 10) is represented by the younger of the two glacial events: this is best illustrated in the Eastern Taurus by a striated glacial surface that underlies the upper glaciomarine succession, as in northern Morocco (Le Heron et al., 2007).

Figure 10: The extent of the Late Ordovician glaciation (from Ghienne et al., 2007a; Guttiérez-Marco et al., 2010). (A) Locations of identified subglacial deformation zones in the more distant areas from the ice centres, including Turkey (other locations: Mauritania, Moroccan Meseta, Spain, and SE Arabia). The five locations were glaciated at the Hirnantian glacial maximum, implying that grounded ice occurred at sea level close to the 60°S parallel. To include glacial successions from South America and South Africa (potentially of Hirnantian age) implies grounded ice occurring at sea level within the 45°S parallel. (B) The minimum-sized Hirnantian ice sheets, with a large North Gondwana Ice Sheet, and possibly penecontemporaneous subordinate ice centres in South America (linked with a pre-cordilleran setting) and South Africa, which may have coalesced together. (C) The maximum-sized Hirnantian West-Gondwana Ice Sheet, assuming fully coalescent synchronous glaciers (favoured scenario). (D) The maximum configuration ice sheet in the North Gondwana tectonic context (from Ghienne et al., 2010).

The glacial maximum event is most probably coeval with the major glacial incision phase documented in central Saudi Arabia (Sarah Fm.). The origin of these glaciers is questionable but we suggest they derive from an ice

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ORDOVICIAN lobe originating from the Gondwana continental ice-sheet (Figures 4 and 10) because of: (i) the rather uniform facies distribution at the 100 km scale, (ii) the NW ward ice-flow direction recognized in the Mardin area, in good agreement with (iii) the widespread ice-generated structures (striated pavements, palaovalleys) indicating a northward flowing ice-sheet in Jordan (Abed et al., 1993; Douillet et al., 2012) and northern Saudi Arabia (Vaslet, 1990; McGillivray and Husseini, 1992; fienalp and Al-Laboun, 2000). These uppermost glaciomarine deposits of the Halevikdere Fm. record the post-glacial transgression related to the late Hirnantian retreating ice front, and hence constitute the base of the fifth sequence that continues with siliceous beds (lydites) and black shales of early Silurian age (Kozlu et al., 2002; Varol et al., 2006 ; cf. STOP 5) potentially reflecting maximum flooding conditions. Hence, during the latest Ordovician, southern Turkey was attached to the Gondwana landmass as reflected by a locally grounded ice sheet, but in a distal position. Paleoglacial reconstructions suggest that southern Turkey was situated at high to intermediate paleolatitudes (higher than 45°) at the end of the Ordovician (Ghienne et al., 2007a; Figure 10). DE⁄‹RMENTAfi-HALEV‹KDERE SECTION STOP DESCRIPTIONS A thick Lower Ordovician succession (in excess of 1000 m) and a relatively thin, unconformity-based Upper Ordovician succession are continuously exposed in the De¤irmentafl area with only minor tectonic complications (Figure 11). After STOP 1 and 2 related to the Cambrian to lowermost Ordovician strata, a panoramic view at STOP 3 will permit to show the stratal stacking pattern in the Lower Ordovician (Tremadocian to Floian) Seydiflehir Fm. Walking along the Halevik Dere section, the Late Katian to Hirnantian deposits will be documented at STOP 4.

Figure 11: Geological sketch map of the De¤irmentafl area with location of the two Ordovician stop. Tectonic complications are minimal and, although the Upper Ordovician succession is relatively thin, it is consistently exposed across the study area.

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ORDOVICIAN STOP 3: LOWER ORDOVICIAN, SEYDIfiEHIR FM. The main features of the Lower Ordovician succession are synthesized in Figure 12. The overall context is that of a siliciclastic shelf enduring relatively high rates of subsidence (1500 m of compacted sandstones and shales/