Aristotle University of Thessaloniki School of Geology Department of Geology

ARISTOTLE UNIVERSITY OF THESSALONIKI SCHOOL OF GEOLOGY DEPARTMENT OF GEOLOGY

GEORGIA KOSTAKI Diploma Geology

STRATIGRAPHY AND GEOTECTONIC SETTING OF THE ?KIMMERIDGIAN-TITHONIAN SHALLOW WATER PLATFORM SEDIMENTS ON TOP OF THE AXIOS OPHIOLITES (EASTERN AXIOS SUTURE ZONE, NORTHERN GREECE)

MASTER THESIS

THESSALONIKI 2013

GEORGIA KOSTAKI Diploma Geology

STRATIGRAPHY AND GEOTECTONIC SETTING OF THE ?KIMMERIDGIAN- TITHONIAN SHALLOW WATER PLATFORM SEDIMENTS ON TOP OF THE AXIOS OPHIOLITES (EASTERN AXIOS SUTURE ZONE, NORTHERN GREECE)

Submitted to the School of Geology Department of Geology 16/12/2013

Thesis Advisors Committee Professor Adamantios Kilias, Principal Advisor Professor Hans-Jürgen Gawlick, Advisor Committee Lecturer Nicolaos Kantiranis , Advisor Committee

STRATIGRAPHY AND GEOTECTONIC SETTING OF THE ?KIMMERIDGIAN- TITHONIAN SHALLOW WATER PLATFORM SEDIMENTS ON TOP OF THE AXIOS OPHIOLITES (EASTERN AXIOS SUTURE ZONE, NORTHERN GREECE)

Duplication and distribution of this publication or parts is not permitted for commercial purposes. Whether the whole or part of the material of this thesis is being used for noncommercial, educational or research purposes the source must always be referred and this message should be preserved. Issues concerning the use of this thesis for commercial purposes must be addressed to the writer.

The aspects and conclusions that are referred in this thesis declare only the writer and must not be consider as an official stand of the Aristotle University of Thessaloniki.

Declaration of authorship

„I declare in lieu of oath that this thesis is entirely my own work except where otherwise indicated. The presence of quoted or paraphrased material has been clearly signaled and all sources have been referred. The thesis has not been submitted for a degree at any other institution and has not been published yet.”

Preface

The present thesis was carried out in the frame of the Program of Postgraduate Studies in Geology and Geoenvironment in the specialization of Structural Geology and Stratigraphy and attempts to contribute an understanding of the tectonic development and geodynamic history of the Hellenides. The Hellenides constitute the southeastern part of the Alpine orogenic belt in Europe (Figure 1). They are traditionally divided into the Internal Hellenides and the External Hellenides. The Internal Hellenides are subdivided into several metamorphic zones, from East to West (Figure 1) (Brunn 1956, Godfriaux 1968, Mercier 1968, Jacobshagen et al. 1978, Jacobshagen 1986, Mountrakis 1986, Kilias 1991, Gawlick et al. 2008, Papanikolaou 2009): Rhodope Massif, Serbomacedonian Massif, Circum- Rhodope Belt, Vardar/Axios Zone and Pelagonian Zone. The Pelagonian Zone is situated between the two ophiolitic belts of Greece the Mirdita/Pindos to the west and the Vardar/Axios to the east. The geotectonic evolution of the Internal Hellenides was influenced by the Eohellenic Phase which took place during Middle to Late Jurassic. The evolution of the Eohellenic Phase is related to intra-oceanic subduction during Middle to early Late Jurassic followed by westward obduction of the Vardar/Axios Ophiolites on top of the Pelagonian Units. There is a variety of published scientific aspects concerning the number and location of the Tethyan Ocean basins, the origin and direction of emplacement of the Tethyan Ophiolites and the timing of ocean basin closure (e.g. Mercier et al. 1975, Mountrakis 1986, Robertson and Shallo 2000, Stampfli and Borel 2002, Brown and Robertson 2004, Gawlick et al. 2008, Schmid et al. 2008, Kilias et al. 2010, Missoni and Gawlick 2011). One group of authors (e.g. Smith and Spray 1984, Channell and Kozur 1997, Stampfli and Kozur 2006, Robertson et al. 2012) propose that the Vardar/Axios Ocean should represent an independent ocean between Pelagonian continent to the west and the wider Rhodope Massif to the east, which existed during most of the Mesozoic era. However, another group of authors (Schmid et al. 2008, Gawlick et al. 2008, Bortolotti et al. 2012) considers Vardar/Axios Ocean a as part of the Neotethys Ocean floor, which was obducted on top of Pelagonian continent in westward direction in Middle to early Late Jurassic time. The aspect of this work is based on is the following: In Triassic to Early Cretaceous times the Hellenides formed together with the Albanides, Dinarides, Western Carpathians, Northern Calcareous Alps and other regions a continuous NNE- SSW trending belt facing the north-western margin of the Neotethys Ocean and undergoing the same history. Formation of oceanic crust since Late Anisian, onset of inneroceanic thrusting in late Early Jurassic, ophiolite obduction in Middle-Late Jurassic, followed by the formation of shallow-water platforms, extensional collapse due to tectonic thickening and mountain uplift before the Jurassic/Cretaceous boundary (Kilias et al. 2010), and infilling of the foreland basins with erosional products of this orogeny in the Early Cretaceous (Missoni and Gawlick 2011). In the frame of the present thesis, field observations, biostratigraphic and microfacies analysis were carried out in an area, which is located 15 km north-west of Thessaloniki in Northern Greece and provides an excellent opportunity to investigate the Late Jurassic to Early Cretaceous geodynamic history of Vardar/Axios Zone. Microfacies studies were based on thin section of samples which were taken from carbonate rocks near the villages Neochorouda, Oreokastro and Kampanis. This research focuses mostly on the mass-flow deposits, which were found near the village Neochorouda, that are important for the reconstruction and the timing of the obduction processes of the Vardar/Axios Ophiolites. The analysis of the different components in the mass-flow deposits can be used as a tool to reconstruct an eroded carbonate platform sealing the emplacement of the ophiolites. The first chapter describes the general geology and provides a geological overview of the area. The second chapter is an introduction to the microfacies concept and carbonate classification. In the third chapter, each formation is separately described using also previous studies. Then the results of the biostratigraphic, microfacies and structural analysis are presented. At the end a correlation of the results of this work with others is made and the biostratigraphic, microfacies and structural data are combined towards an evolutionary scenario for the obduction processes of Vardar/Axios Ophiolites.

Acknowledgements

I would like to express the deepest appreciation to my supervisor Prof. Adamantios Kilias for his kind help during field work, his valuable comments and advice during research time and also for the long discussions we held on this work and other interesting subjects of geology. This study comes as a sequence of work that took place at Leoben University through the European Community Action Scheme for the Mobility of University Students program. I am indebted to my supervisor Prof. Hans-Jürgen Gawlick who gave me the great chance to go to Leoben and work on this project. I am most grateful for his valuable help in all aspects of my study. My sincere gratitude to the third member of the Thesis advisor committee Nikolaos Kantiranis for his support. I wish to thank Dr. Felix Schlagintweit for the fossil determination that was a significant part of this work. I would like to offer my special thanks to Dr. Effimia Thomaidou for her invaluable guidance during the course of my studies at the School of Geology of Aristotle University of Thessaloniki. For the allowance to use of the laboratory facilities, the Department of Applied Geosciences and Geophysics, Chair of Petroleum Geology at the University of Leoben is gratefully acknowledged. I own my deepest gratitude to Dr. Sigrid Missoni for her help and assistance during the laboratory work. I also would like to thank Katerina Kostaki and Dr. Georgios Sagriotis for helping me with the text editing and the Phd candidate Anastasios Plougarlis who was a valuable help with all computer problems. Finally, I am sincerely grateful to my friends Bernd Dahlinger, Eleni Sapountzi and Michalis Vlachos for accompanying me during field work.

TABLE OF CONTENTS

CHAPTER 1. Introduction and Geological Overview 1

CHAPTER 2. Methodology 9 2.1 Microfacies, Facies Zones and Standard Microfacies Types 10 2.2 Classification 11

CHAPTER 3. Geological Setting 13 3.1 Gneiss and Micaschist Unit 13 3.2 Melissochori Formation 14 3.3 Aspri Vrisi-Chortiatis Unit 15 3.4 Volcanosedimentary series 16 3.5 Triassic limestones 18 3.6 Ophiolite Complex 18 3.7 Neochorouda Unit 21

CHAPTER 4. Microfacies and Facies Interpretation - Results 22 4.1 Melissochori Formation 23 4.2 Aspri Vrisi-Chortiatis Unit 27 4.3 Triassic limestone 28 4.4 Neochorouda Unit 35 4.4.1 Reconstruction of the Jurassic to Early Cretaceous tectonic evolution 57

CHAPTER 5. Discussion and Conclusions 63

Abstract 65

Περίληψη 66

References 67

CHAPTER 1. Introduction and Geological Overview

Vardar/Axios Zone

The Vardar/Axios Zone is located parallel to the Hellenides-Dinarides chain in Northern Greece, FYROM and Serbia (Figure 1). The Vardar/Axios Zone was named after the Vardar/Axios River which is the longest river in FYROM and also a major river of Greece. Kossmat (1924) was the first who described the Vardar/Axios Zone as a 30 to 70 km wide NNW-SSE trending belt between the Serbomacedonian Massif to the east and Pelagonian Zone to the west, in Northern Greece. Southwards it extends in to the Thermaic Golf and Aegean Sea and then bends to Anatolia with a possible SW-NE trending. The Greek part of the Vardar/Axios Zone has been subdivided by Mercier (1968) into three subzones according to their palaeogeographic, lithological and facial characteristics. The western part of the Vardar/Axios Zone is the Almopia Subzone, characterized by ophiolites and deep sea sediments, as well as gneiss and schists. The Almopia Subzone to the east is in tectonic contact with the Paikon Subzone. The most characteristic rocks of the Paikon Subzone are Triassic marbles intercalated with schists and phyllites, overlain by volcanoclastic and carbonate rocks of Jurassic to Early Cretaceous age, as well as ophiolites. The eastern part of the Paikon Subzone is overthrusted by the Peonias Subzone which has a more complex arrangement than the previous two. The dominant rocks of the Peonias Subzone are Mesozoic sedimentary and igneous rocks, various types of metamorphic rocks and ophiolites with associated mélanges, including the Oreokastro Ophiolites. The latter together with the ophiolites of Guevguely, Thessaloniki and Chalkidiki, form the Innermost Hellenic Ophiolite Belt (Bebien et al. 1986).

Figure 1 Main structural domains of the Dinarides and Hellenides with the study area pointed. After Kilias et al. (2002). Insert: The Alpine orogenic belt and Tertiary extensional basins in Mediterranean region. Modified after Platt et al. (1998).

The presence of ophiolites is of great interest for the geotectonic evolution and crucial for their still controversially discussed palaeogeographic setting and therefore a key for the geodynamic interpretation of the whole Hellenides. The Vardar/Axios Ophiolites should represent according to today most popular reconstructions (Smith and Spray 1984, Channell and Kozur 1997, Stampfli and Kozur 2006, Robertson 2012) an independent ocean between Pelagonian continent to the west and the wider Rhodope Massif to the east which existed during most of the Mesozoic era. However, another concept see these ophiolites as a part of the Neotethys Ocean floor, which was obducted in westward directions on top of Pelagonian continent in Middle to early Late Jurassic times. Some parts of the obducted ophiolites underwent the extensional collapse due to tectonic thickening and mountain uplift around the Jurassic/Cretaceous boundary and slid down to the west (= Mirdita/Pindos Ophiolites) or to the east (= Vardar/Axios Ophiolites), e.g. as described by Kilias et al. (2010) or Missoni and Gawlick (2011).

Pelagonian Zone

The Pelagonian Zone forms an elongate, NNW-SSE trending nappe pile of continental origin extending from Serbia, Albania and FYROM to the south, through the central Greek mainland and Evvoia, into the Cyclades (Attico-Cycladic Massif) (Figure 1, 2). The Pelagonian Zone represents a microcontinent upon which a carbonate platform evolved adjacent to deeper marine zones: the Vardar/Axios Zone and Mirdita/Pindos Zone at its eastern and western margins, respectively (Figure 2). It consists of basement rocks, such us schists, gneisses and granitoids of Paleozoic or older age which are overlain by Mesozoic carbonates and younger sediments, intensively deformed and metamorphosed during the Alpine orogeny (Mountrakis 1986, Kilias and Mountrakis 1987, Kilias et al. 2010, Katrivanos et al. 2013). In Triassic to Jurassic time, the palaeogeographic position of the Pelagonian Zone is discussed controversially. One group of authors (e.g. Mountrakis 1986, Robertson et al. 1996, Stampfli and Borel 2002) proposes Pelagonian as a/- continental block/fragments that was/were bordered by two Tethyan oceanic realms. The Mirdita/Pindos Ocean at its western margin and the Vardar/Axios Ocean at its eastern margin. In contrast, another group of authors (e.g. Mercier et al. 1975, Gawlick et al. 2008, Schmid et al. 2008, Kilias et al. 2010, Bortoloti et al. 2012, Katrivanos et al. 3

2013) favors a single oceanic basin to the east, the Vardar/Axios =Neotethys Ocean. According to this concept the Pelagonian Units formed the eastern passive continental margin of Gondwana/Apulia facing the Neotethys Ocean. There is also an ongoing discussion about the displacement direction of the obducted ophiolites during Middle to Late Jurassic time onto Pelagonian continent: E- to NE-ward direction (e.g. Robertson and Shallo 2000) or W- to SW-ward direction (e.g. Gawlick et al. 2008, Schmid et al. 2008, Kilias et al. 2010) or both (e.g. Bernouli and Laubscher 1972, Mountrakis 1986).

Serbomacedonian Massif

The Serbomacedonian Massif of Northern Greece is the southern continuation of the metamorphic rocks outcropping in the southwestern Bulgaria and eastern FYROM (Figure 1, 3). It was first defined by Dimitrijevic (1974, 1997) as an elongated structurally complicated basement complex that is situated between the Vardar/Axios Zone and the Pelagonian Zone in the west and the Rhodope Massif in the east. Serbomacedonian Massif is about 300 km long but only 30 to 60 km wide and has a complicated tectonic structure with a heterogeneous mix of metamorphic lithological units of Palaeozoic or older age, intruded by Mesozoic and Cenozoic granitoids. Two NW-SE trending basins are aligned along the classical boundaries of the Serbomacedonian Massif, namely the Axios basin in the west and the Strymon basin in the east. The Serbomacedonian Massif is divided into two crystalline series on the basis of lithological characteristics by Kockel et al. (1971) and Kockel and Mollat (1977): an eastern one, the Kerdilia Series, largely composed of migmatitic gneisses, amphibolites and marble, and a western one, the Vertiskos Series, composed of intercalations of schists, leucocratic and augen gneisses and amphibolites (Kilias et al. 1999). From their tectonostratigraphic position the Kerdilia Series represents the lower unit and the Vertiskos Series the upper unit.

Figure 2 Outline tectonic sketch showing the main ophiolites sutures and the location of the field study area (Robertson et al. 2012).

Circum-Rhodope Belt

To the west, the Serbomacedonian Massif tectonically borders with Mesozoic metasediments and magmatic rocks of the Circum-Rhodope Belt (Figure 3) (Kauffmann et al. 1976, Kilias et al. 1999, Tranos et al. 1999, Meinhold et al. 2009, Meinhold and Kostopoulos 2012). The Circum-Rhodope Belt constitutes the interface between the Axios/Vardar Zone and the Serbomacedonian Massif and is a well- defined steep arcuate, NNW-SSE trending complicated thrust system (Figure 1). This thrust system is called the Circum-Rhodope Thrust System (Tranos et al. 1999) and consists of carbonate, metasedimentary and volcanosedimentary rocks, as well as granitic and metamafic rocks. Transpressive deformation and NE-directed back- thrusts locally modify the boundary by emplacing rocks of the Circum-Rhodope Belt Thrust System onto the Serbomacedonian Massif (Tranos et al. 1999). The Circum-Rhodope Belt is subdivided into three lithostratigraphic units that are placed from east to west: Deve Koran-Doubia Unit, Melissochori-Cholomontas Unit and Aspri Vrisi-Chortiatis Unit (Kauffman et al. 1976, Kockel and Mollat 1977). The Deve Koran-Doubia Unit consists of Late Paleozoic volcanoclastic sediments and shallow-water Triassic carbonate rocks. The Melissochori-Cholomontas Unit is composed of Triassic pelagic carbonate rocks and a turbiditic succession known as Svoula or Melissochori Formation of Early-Middle Jurassic age (Kockel and Mollat 1977) or Late Triassic - early Late Jurassic in age (Dimitriadis and Asvesta 1993). The Aspri Vrisi-Chortiatis Unit is composed of carbonate rocks in the lower parts, deep-sea metasediments (schists, phyllites, radiolarian cherts) and dolerites. Some of those rocks included by Kauffmann et al. (1976) in the Circum-Rhodope Belt are equivalent with several rocks included by Mercier (1968) at the Peonias Subzone.

Study area

The study area is located 10 km NW of Thessaloniki and consists of rocks from the Vardar/Axios Zone and the Circum-Rhodope Belt (Figure 3). Those rocks are volcanosedimentary, Triassic limestones, clastic sediments, various types of metamorphic rocks, ophiolites with associated mélanges and deep-sea metasediments. In detail, the western part of the study area consists of the Oreokastro Ophiolites

(Peonias Subzone) that are overlain unconformably by a fossiliferous Early Cretaceous sedimentary succession (referred here as the Neochorouda Unit) (Kockel and Mollat 1977, Mussallam and Jung 1986, Meinhold et al. 2009). This succession contain mass-flow deposits which contain components of different reefal limestones of Late Jurassic age. To the east the ophiolites are overlain by the Melissochori Formation from the Melissochori-Cholomontas Unit. The Melissochori Formation bounds tectonically to the east with Triassic limestones. Easternmost volcanosedimentary rocks, phyllites, sandstones and cherts from the Aspri Vrisi- Chortiatis Unit occur. The Aspri Vrisi-Chortiatis Unit bounds to the east with gneiss and micaschist. Those units are going to be described further in the following chapter. Samples for microfacies and biostratigraphic analysis were collected from the Melissochori Formation, the Neochorouda Unit, and the Triassic limestones as well as from a chert horizon from the Aspri Vrisi-Chortiatis Unit. The present thesis emphasizes on the mass-flows components in the Neochorouda Unit in the interest of the results of the biostratigraphic and microfacies analysis that allow us to reconstruct the formation of a Late Jurassic carbonate platform on top of the nappe stack of the Vardar/Axios ophiolites sealing their emplacement. Their emplacement can be dated as older then the formation of the shallow-water carbonates on top and therefore at least as late Middle to early Late Jurassic. The sequence of the Neochorouda Unit in the Vardar/Axios Zone with the incorporated eroded components resembles identical successions known in the west of the Pelagonian units, e.g. in Albania or Serbia (e.g. Gielisch et al. 1993, Carras et al. 1998, Scherreiks 2000, Radoicic 2005, Schlagintweit and Gawlick 2007, Gawlick et al. 2008, Schlagintweit et al. 2008).

Figure 3 Geological map of the Serbomacedonian Massif and the bordering Vardar/Axios Zone (After Kilias et al. 1999). The red dots are showing the sampling locations used for microfacies analysis. (I) Kampanis area, (II) Oreokastro area, (III) Neochorouda area.

CHAPTER 2. Methodology

Geological mapping and structural investigations combined with stratigraphic as well as microfacies analysis were carried out on the eastern part of the Axios/Vardar Suture Zone. Maps of 1:50.000 scale from the Institute of Geology and Mineral Exploration (IGME), Greece named Kilkis and Thessaloniki were the guide during field work. In the outcrops of the study area the lithology and texture as well as the sedimentary structures were studied. Measurements of the bedding and the tectonic structures were made in order to reconstruct the geometry and kinematics. Also macroscopically observations led to determine the suitable sampling locations for microfacies analysis. Seventy one (71) samples were collected from different sedimentary formations of the Axios/Vardar Zone and the Circum-Rhodope Belt NW of Thessaloniki. The samples were transferred to the laboratory facilities of the Department of Applied Geosciences and Geophysics, Chair of Petroleum Geology at the University of Leoben, where ninety three (93) thin sections were prepared (Figure 4 a, b). The size of the thin sections is 5 cm x 5 cm. Finally, Microscopic study of the thin sections was conducted in order to obtain the microfacies data (Figure 4 c).

Figure 4 Thin section preparation and analysis.

2.1 Microfacies, Facies Zones and Standard Microfacies Types

Microfacies is regarded as the total of all sedimentological and paleontological data which can be described and classified from thin sections, peels, polished slabs or rock samples (Flügel 2004). According to Flügel (2004) microfacies studies aim at recognizing the overall patterns which reflect the history of carbonate rocks, by means of a thorough examination of their sedimentological and paleontological characteristics. Also microfacies studies provide an invaluable source of information on the depositional constraints, environmental controls of carbonate, on the properties of carbonate rocks as well as the age of the deposition. Microfacies are essential for defining depositional models and recognizing facies zones (Flügel 2004). Wilson (1975) noticed that changes in sedimentological and biological criteria across shelf-slope-basin transects form the basis of generalized models for carbonate platforms, ramps and shelves. The Standard Facies Zones (FZ) (Figure 5) describes idealized facies belts along an abstract transect from open-marine deep basin across a slope, a pronounced platform marginal rim, and an inner platform to the coast (Wilson 1975). The Facies Zones differ in setting, dominant sediments and prevailing biota, and common lithofacies. Carbonates formed within these Facies Zones often exhibit specific Standard Microfacies Types (SMF) assemblages that are used as additional criteria in recognizing the major facies belts (Flügel 2004). “Standard Microfacies Types are virtual categories that summarize microfacies with identical criteria. These criteria are simple and easy to recognize. Revised and refined SMF types are meaningful tools in tracing facies belts, but must be used with care. Most SMF Types are based on only a few dominant characteristics comprising grains types, biota or depositional textures.” (Flügel 2004). Wilson distinguished 24 SMF Types and used these types as additional criteria in differentiating the major facies belts of an idealized rimmed carbonate shelf (Figure 5).

Figure 5 Rimmed carbonate platform: The Standard Facies Zones of the modified Wilson model (Flügel 2004). 10

2.2 Classification

The fossiliferous carbonate classifications proposed by Dunham (1962) and Folk (1959, 1962) have proven to be the most practical and are used in this thesis. Both classifications distinguish allochthonous limestones (mudstone, wackestone, packstone, grainstone) and autochthonous limestones (boundstones). The Dunham classification stresses the depositional fabric, whereas the Folk classification tries to evaluate hydrodynamic conditions (Flügel 2004). Two major groups are distinguished by Dunham (Figure 7), carbonates whose original components were bound together during deposition (boundstones), and carbonates whose original components were not organically bound. The second group is subdivided to mud-support (mudstone and wackestone) or grain-support (packstone and grainstone). Folk (1959) (Figure 6) distinguished three end members, discrete carbonates grains, microcrystalline calcite matrix and sparry calcite, regarded as pore-filling cement. Using the relative proportions of these three end members, Folk distinguished sparry allochemical rocks, microcrystalline allochemical rocks and microcrystalline rocks (Flügel 2004). Classification is simply a tool for organizing information. Considering a name based on texture and composition cannot replace well-defined microfacies types.

Figure 6 Fossiliferous limestone classification Folk (1959, 1962). http://sedimentology.blogsohu.com (01/07/2013)

Figure 7 Fossiliferous limestone classification after Dunham (1962) with modifications by Embry and Klovan. http://www.beg.utexas.edu/lmod/_IOL-CM01/cm01-step03.htm (01/07/2013)

CHAPTER 3. Geological Setting

The following paragraphs give a brief geological overview about the major units cropping out in the area of study as mention above (Figure 8). According to previous studies (Kauffmann et al. 1976, Kockel and Mollat 1977) the Melissochori Formation and the Aspri Vrisi-Chortiatis Unit as well as the Triassic limestones are included to the Circum-Rhodope Belt and the Oreokastro Ophiolites and the Neochorouda Unit are included to the Peonias Subzone of the Axios/Vardar Zone. Also at the easternmost part of the study area outcrop gneiss and micaschist. All units have been tectonically juxtaposed to their present locations during the Alpine and younger orogenic processes.

Figure 8 Geological map of study area modified after Kockel & Mollat (1977).

3.1 Gneiss and Micaschist Unit

Gneiss and micaschists Unit is considered as of crystalline basement provenance and occurs as small, discontinuous outcrops along the eastern part of the Aspri Vrisi- Chortiatis Unit (Figure 3, 8). This Unit is Paleozoic or older and have been subjected to intense Alpine metamorphism and deformation (Kockel et al. 1971). According to previous geological mapping by the Institute of Geology and Mineral Exploration (IGME) and other studies is included to the Vertiskos Series of the Serbomacedonian Massif. However, recent studies (Katrivanos et al. 2013) concerning the basement rocks at the core of Paikon subzone (Vardar/Axios Zone) propose that these rocks may be of Pelagonian origin, exhumed as a multiple tectonic window under the overthrusted nappe pile. The tectonic window formed due to successive compressional and extensional events from Jurassic to Tertiary time. Firstly, W-SW directed tectonic emplacement of the Vardar/Axios ophiolites on the Pelagonian continent during the Late Jurassic led to crustal thickening. Later, gravitational sliding of the nappe pile towards west and east of the Pelagonian continent led to the exhumation of deeper crustal rocks. An equivalent situation could have taken place at the Gneiss and micaschist Unit in the study area, although the primary tectonic contacts are not visible due to the later deformation processes. Nowadays this Unit appears only as tectonic sheets interfering the Circum-Rhodope Belt.

3.2 Melissochori Formation

The Melissochori Formation (Figure 3, 8) referred by Kockel and Mollat (1977) as Svoula flysch and by Kauffmann et al. (1976) as Svoula Formation, is a turbiditic succession. The Melissochori Formation is interpreted as Early-Middle Jurassic, since the discovery of Triassic fauna in limestone olistoliths and breccias, by Kauffmann et al. (1976) and by Kockel and Mollat (1977) or Late Triassic-early Late Jurassic by Dimitriadis and Asvesta (1993). This succession consists of a slightly metamorphosed sequence of sandstones, conglomerates, argillites, cherts, detrital limestones and calcareous sandstones and

incorporation of olistholiths and olistostromes of Triassic shelf carbonates (Dimitriadis and Asvesta 1993). Mussalam (1991) proposed a Middle-Late Jurassic westward subduction bellow a “Chortiatis volcanic arc”. He interprets the Melissochori Formation as sediments deposited at a fore-arc setting, between the arc and a trench which was lying further to the east. Dimitriadis and Asvesta (1993) interpret the Melissochori Formation as a continental slope and rise sedimentary sequence deposited from Late Triassic or Early Jurassic until early Late Jurassic at a passive margin which was developed after a Late Triassic continental rifting and opening of an oceanic basin. Elimination of this basin happened during Late Jurassic by east-dipping subduction bellow and obliquely to the previous passive margin. After conducting geochemical and zircon geochronological analysis Meinhold et al. (2009) conclude that the Melissochori Formation was deposited close to a hinterland with prominent Carboniferous rocks of volcanic-arc origin as well as some older basement rocks exposed at the slope of carbonate platform probably in the Early Jurassic. Limestone breccias and olistoliths such as those described by Kockel and Mollat (1977) are suggestive of an unstable slope setting that was probably tectonically controlled (Meinhold et al. 2009).

3.3 Aspri Vrisi-Chortiatis Unit

The Aspri Vrisi-Chortiatis Unit of Kockel and Mollat (1977) is situated between Oreokastro in NW and Sithonia peninsula in SE along the western Serbomacedonian margin (Figure 3, 8). The lower part consists of rocks of Permian-Triassic age, metasediments, shallow water carbonates and volcanosedimentary rocks (the letter is going to be described further in 3.4). The upper part comprises deep sea sediments e.g., green sandstones and dark red shales, with intercalations of chert horizons, and lenses and layers of sericitized and chloritized dolerite. The sequence is metamorphosed into chlorite quartzite, epidote quartzite, quartz-sericite schists, meta- arkoses, chlorite schists, brownish-green phyllites, cloritized basic intrusive rocks. Kockel and Mollat (1977) suggested a Jurassic age, based on the underlying Upper Triassic limestones and the observed intercalations of sedimentary rocks of the

Melissochori Formation. However, Ferriere and Stais (1995) suggested a Carboniferous-Permian age for the Aspri Vrisi Series, based on lithostratigraphic correlations with other chert-bearing successions of the Hellenides. The metamorphosed gabbros, diorites, basalts, quartz diorites, trondjemites and granitoids comprising the Chortiatis magmatic series have been inferred as arc-related magmatics (Kockel and Mollat 1977). The Chortiatis magmatic series and the volcanoclastic series were interpreted by Michard et al. (1998) as having developed in an intra-oceanic island arc setting related to an intra-oceanic subduction predating the obduction of the Axios/Vardar ophiolites rocks. Mussalam (1991) proposed that this magmatics were created by a Middle-Late Jurassic westward subduction below the “Chortiatis volcanic arc”. However, according to Kockel and Mollat (1977) and De Wet (1989) the vergence of the early folding and the thrusting in the Aspri Vrisi-Chortiatis unit towards the west favors an eastwards subduction.

3.4 Volcanosedimentary series

The Volcanosedimentary series (Figure 3, 8) is a discontinuous belt of low grade metavolcanics and metasediments of supposed Early Triassic age (Mercier 1968, Kockel and Mollat 1977). Massive rhyolitic ignimbrites and lavas are the main volcanic products (Figure 9). Metasediments are fewer and are phyllitic, cherty or calcareous sandstones and pelitic or calcareous phyllites and shales, usually incorporating limestones or rhyolitic megaclasts and in some cases interbedded with thin recrystallized dark colored limestones (Dimitriadis and Asvesta 1993). The sediments are intricately alternating with the volcanics and it is difficult to decide whether this is due to original interbedding or to tectonic juxtaposition (Figure 10). The presence of accretionary lapilli interbedded with ignimbrites suggests simultaneous subaerial phreatomagmatic eruptions (Dimitriadis and Asvesta 1993). According to Dimitriadis and Asvesta (1993) at the western margin of Vertiskos Terrain an epicontinental extensional basin started forming during the Permian- Skythian. Marine transgression in this basin probably occurred sometime during the Skythian to early Anisian and made the growth of ramps there possible. Rhyolitic

volcanism probably started by that time and is interpreted by Dimitriadis and Asvesta (1993) as a Triassic rift-related volcanism.

Figure 9 The Volcanosedimentary series north of the Oreokastro village (40o75΄22΄΄N, 22o90΄26΄΄E). Schmidt diagram of the bedding (Lower hemisphere).

Figure 10 Photograph illustrating the outcrop situation. Tectonic contact between the Volcanosedimentary series and the Triassic Carbonates north of the Oreokastro village (40o75΄16΄΄N, 22o89΄49΄΄E). Schmidt diagram of the tectonic contact (Lower hemisphere).

3.5 Triassic limestones

Those carbonates represent the Triassic shallow-water and hemipelagic sedimentation of the Tethys realm which is characterized by a complex carbonate platform-basin pattern. The sedimentary cycle was initiated after the Late Permian transgression. From late Early Triassic until almost the early Late Triassic, carbonates of considerable thickness were deposited. According to Mercier (1968) those carbonates consist of limestones and dolomites of Skythian to Carnian age: The upper Skythian limestones are dark-grey, thin bedded, detrital, locally at the base alternating with whitish sandstones layers and fine-grained conglomerates as well as yellow marls. The Anisian limestones are black, thin-bedded and detrital. The Ladinian limestones are white, massive or thick-bedded, recrystallized alternating with yellow to whitish, thick-bedded dolomite. The Carnian limestones are dark-grey, thick-bedded, with intercalated layers and lenses of reddish to pink limestone.

3.6 Ophiolite Complex

The Oreokastro Ophiolites of the Vardar/Axios Zone, is situated in northern Greece about 5 km north-northwest of the city of Thessaloniki. It occupies 12 km long and 2.5 km wide area, trending NW-WE (Figure 3, 8). In the study area to the east are in tectonic contact with Melissochori Formation. To the west the ophiolites are overlain unconformably by a fossiliferous Early Cretaceous (Mussalam and Jung 1986) sedimentary succession (referred here as Neochorouda Unit) (Figure 11). The Oreokastro Ophiolites is built up of gabbros and extrusive rocks such as basalts and basaltic andesites (Zachariadis 2007). A pillow lava section is well exposed at the area of study (Figure 12). However, they are described by Zachariadis (2007) as an incomplete ophiolitic sequence because of the absent of a well-exposed sheered dyke complex as well as a detailed cumulate section. The Oreokastro Ophiolites together with the ophiolites o Guevguely, Thessaloniki and Chalkidiki form the Innermost Hellenic Ophiolite Belt (Bebien et al. 1986). The Innermost Hellenic Ophiolite Belt is a discontinuous northwest-southeast trending

belt of ophiolites that lies near the contact between the Hellenides and the Serbomacedonian Massif (Figure 2). As deduced from geochemical and petrological investigations by Zachariadis (2007) the formation of these ophiolites took place between 170-155 in the back-arc region of an intra-oceanic subduction. There are many controversial model concerning the formation and origin of Vardar/Axios Ophiolites. According to some authors (e.g. Smith and Spray 1984, Channell and Kozur 1997, Stampfli and Kozur 2006, Robertson et al. 2012) Vardar/Axios Ophiolites should rooted in an independent ocean between Pelagonian continent to the west and the wider Rhodope to the east and were thrusted on top of the Pelagonian Units (e.g. Roddick et al. 1979, Brown and Robertson 2004). Another group of authors considers the Vardar/Axios Ophiolites as the easternmost part of a huge ophiolite nappe which derived from the Neotethys Ocean (e.g. Schmid et al. 2008, Gawlick et al. 2008, Kilias et al. 2010). A possible evolution of these ophiolites would include an intra-oceanic subduction during Middle to early Late Jurassic which resulted westward ophiolite obduction on top of the Pelagonian Units. Uplift of the thickenend crust, around the Jurassic/Cretaceous, led to gravitational sliding of some parts of the obducted ophiolites towards the west (= Pindos/Mirdita Ophiolites) or to the east (= Vardar/Axios Ophiolites) (Kilias et al. 2010, Missoni and Gawlick 2011). After Late Jurassic ophiolite emplacement a much reduced ocean is inferred to have remained open, with remnants of the oceanic crust surviving until latest Cretaceous time (Gawlick et al. 2008). The onset of westward intra-oceanic thrusting and ophiolite obduction in Middle- Late Jurassic is also known in Eastern Alps, Dinarides and Albanides (Gawlick et al. 2008, Schlagintweit et al. 2008, Missoni and Gawlick 2011).

Figure 11 Neochorouda Unit overlying the Oreokastro Ophiolite Complex northeast of the Neochorouda village (40044΄53.33΄΄N, 22052΄39.0΄΄E).

Figure 12 Pillow lavas of the Oreokastro Ophiolite Complex northeast of the Neochorouda village (40044΄53.33΄΄N, 22052΄39.0΄΄E).

3.7 Neochorouda Unit

The Neochorouda Unit referred by Kockel and Mollat (1977) as “Konglomerat von Dubkon” and by Ricou et al. (1998) as Limestone Breccia is a NW-SE elongated sedimentary succession, which unconformable overlies the Oreokastro Ophiolites complex east of Neochorouda village (Figure 3, 8, 11). This succession consists of turbidites and mass flows with considerable macroscopic appearance of fossils (Figure 13). The mass flows contain components of different reefal limestones. Based on the recovered fauna, the age of the Neochorouda Unit is interpreted to be Late Jurassic to earliest Early Cretaceous (e.g., Mercier 1968, Kockel and Mollat 1977). Later, Mussalam and Jung (1986) described sandstones, which are located in the same area, comprising the ammonoids Berriasella ex gr. subcallisto (Toucas) and Berriasella ex gr. oppeli (Killian) which characterize the Berriasian age. Meinhold et al. (2009) described Neochorouda Unit as a conglomerate calcareous succession consisting of limestone pebbles, partly fossiliferous, calcareous sandstones, wackes and quartzites as well as metamafic and felsic igneous clasts. Platy limestones and sandy beds are intercalated. The limestone blocks are interpreted by Meinhold et al. (2009) as olistoliths that derived from an Upper Jurassic carbonate platform and were deposited in the slightly younger Neochorouda Unit.

Figure 13 Macroscopic appearance of fossils in the mass flows deposits from the Neochorouda Unit.

CHAPTER 4. Microfacies and Facies Interpretation - Results

In total 71 samples were collected and 93 thin sections were made. In the present thesis only the most characteristic thin sections are presented. Samples K1, K2, K3, K4 and GR16 and samples 1a, 1b, 3a, 3d, 5a and X, were collected from Triassic limestones from the Kampanis area (Figure 3, I) and northwest of the Oreokastro village, respectively (Figure 3, II). Also at the Oreokastro area, samples 2a, 2b, 4a, 4b, 4g, F1, F2, F3 and F4 were collected from Melissochori Formation and sample 10 was collected from a chert horizon within the Aspri Vrisi- Chortiatis Unit. The remaining thin sections were made from samples that were collected from the Neochorouda Unit a succession with considerable macroscopic appearance of fossils east of Neochorouda village (Figure 3, III).

According to the biostratigraphic and microfacies analysis Neochorouda Unit is distinguished from bottom to top (Kostaki et al. 2013): a- To a breccia with gabbroic and few shallow-water carbonate clasts from which, samples GR1, GR2, GR3 and GR4 were collected. b- A coarse-grained breccia with mixed ophiolite material and shallow-water carbonate clasts from which, samples GR6, GR7, GR11, GR13, 6a, 6b, 6z, 6e, 6g, 6h and 6th were collected. c- Samples GR12, GR14, 7a, 7b, 7d, 7e and 7g were collected from a turbiditic sequence of sandstones, with some intercalated coarse-grained mass flows. d- Samples 8a and 8a2 were collected from a polymictic conglomerate e- Samples 9a, 9b, 9b2, 9d, 9g, 9e and NP1 from shallow-water carbonates.

4.1 Melissochori Formation

For the purpose of this work samples 2a, 2b, 4a, 4b, 4g, F1, F2, F3, and F4 were collected from carbonate clasts inside the Melissochori Formation north of Oreokastro area (Figure 14, 15). These clasts are grainstones to rudstones consisting of grains of various origins. Grains are rounded and consist of bioclasts, imported shallow-water material, quartzs and siliciclastics. The fossils and fossils fragments are mostly from reef-derived organisms. Some fragments are coated and encrusted. One common microencruster is Crescentiella morronensis (Crescenti) that ranges from Jurassic to Cretaceous and is extremely abundant in upper Jurassic. Some other bioclasts are algae, gastropods, foraminifera and crinoids (Plate 1). The carbonate clasts must have derived from a carbonate platform and the siliciclastic material from a hinterland. Melissochori Formation therefore was deposited close to a hinterland at the slope of a carbonate platform probably in Late Triassic-early Late Jurassic (see also Meinhold et al. 2009, Dimitriadis and Asvesta 1993).

Figure 14 Photographs illustrating outcrop situation. Melissochori Formation north of Oreokastro village (40o75΄16΄΄N, 22o89΄49΄΄E), locality of sample 2a used for microfacies analysis. Schmidt diagram of the bedding (Lower hemisphere).

Figure 15 Tectonic contact between the Melissochori Formation and the Triassic Carbonates north of the Oreokastro village (40o75΄16΄΄N, 22o89΄49΄΄E). Schmidt diagram of the tectonic contact (Lower hemisphere).

Plate 1 Microfacies from carbonate clasts inside the turbiditic sequence from the Melissochori Formation. a: Grainstone with gastropods, reef builders and encrusting organisms as well as clasts of micrite. Sample 2a. b: Crescentiella morronensis (Crescenti). Sample 2a. c: Reef builders. Sample 2a. d, e: Grainstone with foraminifera and the microencruster Crescentiella morronensis (Crescenti) as well as different coated grains. Sample 2b. f: Crescentiella morronensis (Crescenti). Sample 2b. g: Rudstone containing reef builders and micritic clasts. Sample 4a. h, i: Rudstone composed of foraminifera, reef builders and algae, as well as quartz and micritic clasts. Sample 4b. j, k, l, m: Grainstone containing fragments of dasycladales, foraminifera and micritic clasts. Sample 4b. n: Grainstone composed of siliciclastic. Sample 4g. o: Rudstone composed of clasts of micrite and some clasts with foraminifera. Sample F1. p: Rudstone compose of reef builders. Sample F2. q: Dolomitized grainstone. Sample F3. r: Grainstone. Sample F4.

4.2 Aspri Vrisi-Chortiatis Unit

Sample 10 was collected from a chert horizon within the Aspri Vrisi-Chortiatis Unit north of Oreokastro village (Figure 16). The thin section of the sample contains radiolarian. The radiolarians are recrystallized, deformed and occur as quartz. The poor condition of the sample is due to greenschist-facies metamorphism that the whole Aspri Vrisi-Chortiatis Unit has experienced. Thus further information cannot be obtained, nevertheless it seems to be Triassic radiolarians.

Figure 16 Recrystallized radiolarian chert (Sample 10) (a, b, c). Black chert of the Aspri Vrisi-Chortiatis Unit north of the Oreokastro village (40o75΄22΄΄N, 22o90΄26΄΄E), locality of sample 10 (d).

4.3 Triassic limestone

Samples 1a, 1b, 3a, 3d, 5a and X were collected from the Triassic carbonates northwest of Oreokastro village (Figure 7II) and samples K1, K2, K3, K4 and GR16 were collected from carbonates near Kampanis area (Figure 7I). The Triassic limestones northwest of Oreokastro village are grey or white, massive or thick-bedded. These limestones are recrystallized. However, macroscopically some fossils are preserved, such as ammonites that occur at the reddish limestone. Microscopically different foraminifera can be recognized (Plate 3). The samples are mainly peloidal packstones to grainstones consisting of peloids and different coated grains, e.g. cortoids and oncoids (Plate 3). Also isopachous rim cements occurs (sample 1b, Plate 3). This kind of microfacies are common to lagoonal environment and in inner ramp settings. From the Kampanis area samples K4 and GR 16 were collected from the dark- grey, bedded limestones and K1, K2 and K3 were collected from reddish to pink limestone layers. Samples K4 and GR 16 are packstone to grainstone characterized by accumulations of echinoderm fragments (Plate 5). Crinoids concentration represent a specific facies type formed in various settings including slopes, protected platforms, reefs and mounds (Flügel 2004). Samples K1, K2 and K3 which were collected from the reddish layers are mainly packstones with common pelagic microfossils e.g. filaments, echinoderms, foraminifera but also gastropods (Plate 4, 5). Filaments are pelagic thin-shelled bivalves and many authors use them as an indicator of bathyal deep-water settings. The microfacies of the samples which were collected for the purpose of this thesis show shallow-water environment and a deep basinal transition. The lagoonal carbonate underwent drowning, becoming initially buried by crinoidal limestone and subsequently by deeper water filament limestones. Probably this transition can be correlated with the Tethys-wide recorded event that is called Reifling Event. This is a significant and widely developed flooding event that took place during Middle Anisian and has been recognized by Schlager and Schöllnberger (1974). It should be also mentioned that these carbonates seem to have been derived from the eastern Apulia continental margin.

Plate 2 a, b: Reddish layers with Ammonites near Neochorouda area. c, d, e, f, g, h: Macroscopic appearance of fossils at Oreokastro carbonates.

Plate 3 Triassic limestone from the Oreokastro area a, b, c, d, e, f: Grainstone with different foraminifera and peloids. Sample 1b. g, h, i: Grainstone composed of peloids and different coated grains, e.g. cortoids and oncoids. Sample 3d. j, k, l: Peloidal grainstone. Sample 5a. m: Packstone to grainstone containing foraminifera, peloids and isopachous rim cements . Sample 1b. n: Infilling with open marine material. Sample 1a. o: Peloidal grainstone. Sample 3a.

Plate 4 Layers of pink or reddish limestone of Triassic age from the Kampanis area a: Wackestone containing crinoids, filaments and foraminifera. Sample K3. b, d, f, g: Wackestone containing filaments, echinoderms and crinoids. Sample K3. c: Wackestone with foraminifera. Sample K3. e: Wackestone containing a gastropod. Sample K3. h: Filaments. Sample K3. i: Hardground. Sample K3. j, k: Packstone containing filaments, echinoderms, foraminifera, and gastropods as well as hardground clasts. Sample K2. l, m: Packstone containing filaments, fragments of crinoids and hardground clasts. Sample K2. n, o: Packstone containing filaments, foraminifera, gastropods and hardground clasts. Sample K2. p: Fragments of crinoids. Sample K2. q: Hardground clasts and fragment of foraminifera. Sample K2. r: Packstone containing filaments, crinoids, echinoderms, and gastropods. Sample K1.

Plate 5 Layers of pink or reddish limestone of Triassic age from the Kampanis area a: Packstone containing filaments, echinoderms, crinoids, and gastropods. Sample K1.

Dark-grey limestone of Triassic age from the Kampanis area b, c: Crinoidal grainstone. Sample K4. d, e, f, g, h: Crinoidal packstone containing gastropods. Sample GR16.

Triassic limestones from the Oreokastro area i: Isopachous rim cements. Sample X.

4.4 Neochorouda Unit

The Neochorouda Unit is a sedimentary succession of mass-flow deposits and has a thickness of about 320 m. The mass flows contain a large number of reefal limestones, ultramafic of the ophiolite suite such as gabbroic clasts. The components size ranges from a few centimeters up to half a meter (Figure 19). On top of the Oreokastro Ophiolites a matrix of ophiolitic sands of approximately 10 m thickness occurs (Figure 17a). It consists of grains of various origin such as reworked ophiolite material and shallow-water clasts. The clasts are mainly rudstones containing subangular to subrounded grains of bioclasts, imported shallow-water material and other lithoclasts such as gabbroic and quartz clasts. The bioclasts are remains of reef builders, shells, brachiopods, crinoids and foraminifera as well as a fragment of the Dasycladales Griphoporella jurassica (Endo) (Plate 6). Some fragments are coated and encrusted. One common microencruster is Crescentiella morronensis (Crescenti). Also a possible specimen of the benthic foraminifer Labyrinthina mirabilis Weynschenk occurs. These taxa are referred mainly to the Kimmeridgian age (e.g. Schlagintweit et al. 2005, Schlagintweit 2011). Upsection it passes to a coarse-grained carbonate breccia of about 6 m thickness with mixed ophiolite material (Figure 17b). The different carbonate clasts are reworked reef material such as boundstones and bafflestones. They derive from different facies zones, e.g. open and closed lagoon, back-reefal, reefal and fore-reefal. Those boundstones contain corals, sponges, calcareous algae (mainly Dasycladales), benthic foraminifera and a considerable number of predominantly encrusting microorganisms (Plate 7, 8). Among the microencrusters are Crescentiella morronensis (Crescenti), Perturbatacrusta leini Schlagintweit & Gawlick, Radiomura cautica Senowbari-Daryan & Schäfer and Labes atramentosa Eliasova. The microencrusters Crescentiella morronensis (Crescenti) and Labes atramentosa Eliasova exhibit a maximum occurrence as crusts around irregular tube-shaped microfossils incertae sedis. These are a characteristic constituent of Late Jurassic fore- reefal carbonate facies that are also recorded in Northern Calcareous Alps and along the northern European margin of the Alpine Tethys (Schlagintweit and Gawlick 2009).

Common calcareous algae are Thaumatoporella sp as well as the dasycladales Griphoporella jurassica (Endo) and Neoteutloporella socialis (Praturlon). The latter is common in Upper Jurassic (Late Tithonian) shallow-marine carbonates of the Tethyan realm. Pseudocyclammina lituus (Yokoyama) is the most common benthic foraminifer. Upwards the sequence continuous to a turbiditic sequence of sandstones with intercalated coarse-grained mass flows deposits (Figure 17c, 18). The thickness of this sequence is about 20 meters. In the mass flow occur mainly grainstones and rudstones composed of different bioclasts, coated grains and clasts of sandstone. The bioclasts are debris of different reef builders such as corals and sponges as well as foraminifera and algae (Plate 9, 10). Common microencrusters are Labes atramentosa Eliasova, Crescentiella morronensis (Crescenti) and Radiomura cautica Senowbari-Daryan & Schäfer. Some of the benthic foraminifera and the calcareous algae characterize the whole Kimmeridgian-Tithonian time and some are also passing in the Lower Cretaceous e.g. the Dasycladales Salpingoporella pygmaea (Gümbel), Dissocladella? Bakalovae Dragastan and the foraminifera Nautiloculina cf. oolithica Mohler, Anchispirocyclina lusitanica (Egger), Mohlerina basiliensis (Mohler) and Pseudocyclammina lituus (Yokoyama). Furthermore, Mussalam and Jung (1986) described sandstones comprising the ammonoids Berriasella ex gr. subcallisto (Toucas) and Berriasella ex gr. oppeli (Killian) which characterize the Berriasian age. Higher in the succession a polymictic conglomerate that reaches around 250 m in thickness prevails. The components in the conglomerate are a mixture of older carbonate as well as siliciclastic-crystalline rocks (Figure 20). The components vary in size, with blocks larger than 10 cm often occurring. Different metamorphosed shallow-water clasts of most probably Middle Triassic age containing foraminifera dominate (Plate 11). Also in some clasts recrystallized radiolarian occur.

Figure 17 Neochorouda Unit overlying the Oreokastro Ophiolite Complex northeast of the Neochorouda village (40044΄53.33΄΄N, 22052΄39.0΄΄E). Sampling location of samples a: GR1, GR2, GR3 and GR4, b: GR6, GR7, GR11, GR13, 6a, 6b, 6z, 6e, 6g, 6h and 6th, c: GR12, GR14, 7a, 7b, 7d, 7e and 7g.

Figure 18 The turbiditic sequence of Berriasian sandstones (Mussalam and Jung 1986), with the intercalated coarse-grained mass flows deposits (40044΄53.3΄΄N, 22052΄39΄΄E), sampling location of samples GR12, GR14, 7a, 7b, 7d, 7e and 7g.

Figure 19 Stratigraphic column of the Neochorouda Unit (Kostaki et al. 2013).

Finally the conglomerate was sealed by shallow-water carbonates (Figure 21). In the study area the thickness of the carbonates exceeds 30 m. Reefal boundstones with different microencrusters associations, stromatoporoids, sponges, corals are dominating (Plate 12, 13, 14). Common microencrusters include Radiomura cautica Senowbari-Daryan & Schäfer and Crescentiella morronensis (Crescenti). Beside common dasycladales such as Suppiluliumaella aff. methana Dragastan & Richter, Furcoporella? vasilijesimici Radoicic, Linoporella aff. capriotica (Oppenheim), Griphoporella cretacea (Dragastan) and debris of Selliporella neocomiensis (Radoicic), the foraminifera Coscinophragma sp. and Andersenolina sp are identified. This part of the series is Berriasian to Valanginian in age based on the above micropaleontological assemblage e.g. Selliporella neocomiensis (Radoicic), Andersenolina sp. Of special interest are the coarse-grained breccias with mixed ophiolite material and shallow-water carbonate clasts below the early Berriasian turbidites. The shallow- water clasts of different facies are of Kimmeridgian?-Tithonian age. The clasts derive from fore-reef, reef, back-reef and open lagoonal areas containing different microencruster associations, stromatoporoids, sponges, corals, benthic foraminifera and also calcareous algae (mainly Dasycladales). These clasts are interpreted as erosional products of a Kimmeridgian?-Tithonian shallow-water carbonate platform which was formed originally on top of the ophiolites. This platform was eroded and redeposited until Early Cretaceous and is only documented by the clasts described here.

Figure 20 Polymictic conglomerate (40044΄53.3΄΄N, 22052΄39΄΄E), sampling location of samples 8a and 8a2.

Figure 21 Shallow-water carbonates (40044΄53.3΄΄N, 22052΄39΄΄E), sampling location of samples 9a, 9b, 9b2, 9d, 9g, 9e and NP1.

Plate 6 Characteristic microfacies of different components in the breccia from the Neochorouda Unit. a: Rudstone with remains of reef builders, fragment of shells, foraminifera, crinoids and the microencruster Crescentiella morronensis (Crescenti) as well as gabbroic and quartz clasts. Sample GR1. b: Fragment of unknown organism surrounded by an encruster. Sample GR1. c: Microencruster Crescentiella morronensis (Crescenti). Sample GR1. d: Rudstone with different clasts and a possible specimen of the benthic foraminifera Labyrinthina mirabilis Weynschenk . Sample GR1. e: Fragment of brachiopod (B) and a foraminifer (F). Sample GR1. f: Foraminifera. Sample GR2. g: Laminated grainstone with foraminifera, reef builders, fragments of shells and remains of crinoids as well as gabbroic and quartz clasts. Sample GR2. h: Rudstone with different lithoclasts and bioclasts. Sample GR4. i, j: Rudstone with foraminifera. Sample GR4. k: Rudstone composed of different lithoclasts and bioclasts with micritic envelope. Sample GR4. l: Floatstone with a fragment of the Dasycladales Griphoporella jurassica (Endo). Sample GR3.

Plate 7 Microfacies and facies interpretation of the different carbonate clasts in the coarse-grained breccia from the Neochorouda Unit. The clasts derive from fore-reef, reef, back-reef and open lagoonal areas. a: Boundstone with the microencruster Labes atramentosa Eliasova. Fore-reef facies. Sample 6a. b, c: Boundstone with the microencruster Radiomura cautica Senowbari-Daryan & Schäfer. Fore-reef facies. Sample 6a. d: Boundstone with the microencruster Crescentiella morronensis (Crescenti). Fore-reef facies. Sample 6b. e: Boundstone with Thaumatoporella sp. Fore-reef facies. Sample 6b. f: Boundstone with Thaumatoporella sp. and oblique cross section of Neoteutloporella socialis (Praturlon). Fore-reef facies. Sample 6b. g: Boundstone with Reophax? rhaxelloides Schlagintweit, Auer & Gawlick. Fore-reef facies. Sample 6b. i, j, k, l: Boundstone with the dasycladale Neoteutloporella socialis (Praturlon) oblique cross section. Fore-reef facies. Sample 6b. h : Boundstone with the dasycladale Neoteutloporella socialis (Praturlon) longitudinal section. Fore-reef facies. Sample 6b. m: Sclerosponge. Fore-reef facies. Sample 6b. n: Boundstone with debris of the dasycladale Griphoporella jurassica (Endo). Fore-reef facies. Sample 6b. o: Crescentiella morronensis (Crescenti). Fore-reef facies. Sample 6b. p, q, r: Bafflestone with reef builders and Crescentiella morronensis (Crescenti). Reef facies. Sample 6z.

Plate 8 Microfacies and facies interpretation of the different carbonate clasts in the coarse-grained breccia from the Neochorouda Unit. The clasts derive from fore-reef, reef, back-reef and open lagoonal areas. a: Boundstone with the microencruster Radiomura cautica Senowbari-Daryan & Schäfer. Fore-reef facies. Sample 6e. b, d, e: Boundstone with the microencrusters Perturbatacrusta leini Schlagintweit & Gawlick (above) and Labes atramentosa Eliasova (below). Fore-reef facies. Sample 6e. c: Bafflestone with different reef builders. Reef facies. Sample 6h. f: Bafflestone with the microencruster Crescentiella morronensis (Crescenti) as well as peloids and ooids. Lagoonal facies. Sample 6g. g: Boundstone with a coral encrusted by Perturbatacrusta leini Schlagintweit & Gawlick and Labes atramentosa Eliasova (above) (general view of b, d, e). Fore-reef facies. Sample 6e. h: Bafflestone with different reef builders. Reef facies. Sample 6h. i: Astraeofungia. Sample 6th. j: Boundstone with corals. Fore-reef facies. Sample GR6. k: Boundstone with the microencruster Labes atramentosa Eliasova. Fore-reef facies. Sample GR6. l: Boundstone with corals and fragment of shells. Fore-reef facies. Sample GR6. m, o, p: Algal-bafflestone with Neoteutloporella socialis (Praturlon). Reef-debris facies. Sample Gr13. n: Bafflestone composed of different reef builders. Reef facies. Sample GR7. q: Benthic foraminifer Pseudocyclammina lituus (Yokoyama). Sample GR13. r: Bafflestone with the microencruster Perturbatacrusta leini Schlagintweit & Gawlick. Sample GR11.

Plate 9 Microfacies of the carbonate clasts of the turbidites from the Neochorouda Unit a, b,c: Grainstone with different bioclasts such as foraminifera and clasts of sandstone and quartz. Sample 7a. d: Grainstone composed of different bioclasts such as the benthic foraminifer Pseudocyclammina lituus (Yokoyama), coated grains as well as clasts of sandstone and quartz. Sample 7b. e: Benthic foraminifer Pseudocyclammina lituus (Yokoyama) (left). Sample 7b. f, h: Benthic foraminifer Pseudocyclammina lituus (Yokoyama) and clasts of sandstone. Sample 7b. g: Benthic foraminifera Anchispirocyclina lusitanica (Egger) and clasts of quartz. Sample 7b. i, k: Grainstone with Mohlerina basiliensis (Mohler) and different clasts. Sample 7b. j: Grainstone composed of different clasts and the microencruster Crescentiella morronensis (Crescenti). Sample 7b. l: Grainstone composed of different clasts and Nautiloculina cf. oolithica Mohler. Sample 7b. m: Rudstone composed of different bioclasts as well as clasts of sandstone and quartz. Sample 7d. n: Rudstone with Crescentiella morronensis (Crescenti) and different clasts (below) and reef framework (above). Sample 7e. o: Debris of crystallized corals. Sample 7e. p: Labes atramentosa Eliasova. Sample 7g. q: Rudstone with reef builders, Crescentiella morronensis (Crescenti) as well as clasts of sandstone and quartz. Sample 7g. r: Radiomura cautica Senowbari-Daryan & Schäfer. Sample 7g.

Plate 10 Microfacies of the carbonate clasts of the turbidites from the Neochorouda Unit a: Grainstone composed of different bioclasts as well as clasts of sandstone, gabbros and quartz. Sample GR12. b: Grainstone with different clasts and Salpingoporella pygmaea (Gümbel). Sample GR12. c, d: Grainstone composed of different clasts and foraminifera. Sample GR12. e: Grainstone composed of different bioclasts as well as clasts of sandstone, gabbros and quartz. f: Grainstone composed of bioclasts such as Crescentiella morronensis (Crescenti) and Nautiloculina cf. oolithica Mohler as well as clasts of sandstone. Sample GR14. g: Grainstone composed of different clasts, bioclasts and coated grains. Sample GR14. h, o: Mohlerina basiliensis (Mohler). Sample GR14. i: Gastropod. Sample GR14. j: Grainstone composed of different clasts and foraminifera. Sample GR14. k, n: Nautiloculina cf. oolithica Mohler. Sample GR14. l: Crescentiella morronensis (Crescenti). Sample GR14. m: Grainstone composed of different clasts and Trinocladus? sp. Sample Gr14

Plate 11 Microfacies of the different clasts of the polymictic conglomerate from the Neochorouda Unit a, b, c, d, e, f: Rudstone composed of clasts of different metamorphosed shallow-water clast and carbonate clasts containing foraminifera. Sample 8a. g, h, i: Rudstone composed of quartzite’s resp. metamorphic radiolarites, different metamorphosed shallow-water clasts. Sample 8a2.

Plate 12 Microfacies from shallow-water carbonates from the Neochorouda Unit. a: Furcoporella? vasilijesimici Radoicic. Sample NP1. b, e: Linoporella aff. capriotica (Oppenheim). Sample NP1. c: Suppiluliumaella aff. methana Dragastan & Richter. Sample NP1. d: Coscinophragma sp. Sample NP1. f: Radiomura cautica Senowbari-Daryan & Schäfer. Sample NP1.

Plate 13 Microfacies from shallow-water carbonates from the Neochorouda Unit. a: Boundstone with stromatoporoids. Sample 9a. b: Boundstone with Griphoporella cretacea (Dragastan). Sample 9b. c: Suppiluliumaella aff. methana Dragastan & Richter. Sample 9b. d: coral. Sample 9b. e, f, g: Debris of tufts of secondary laterals of Selliporella neocomiensis (Radoicic). Sample 9b. h: Boundstone with Suppiluliumaella aff. methana Dragastan & Richter, other dasycladales and corals . Sample 9b. i: Stromatoporoid. Sample 9b. j: Fragment of Furcoporella? vasilijesimici Radoicic (left) and other dasycladale (right). Sample 9b. k: Boundstone with dasycladale algae and debris of Selliporella neocomiensis (Radoicic). Sample 9b. l: Boundstone with Suppiluliumaella aff. methana Dragastan & Richter and debris of Selliporella neocomiensis (Radoicic). Sample 9b. m: Boundstone with fragments of dasycladale algae and debris of Selliporella neocomiensis (Radoicic). Sample 9b. n: Linoporella aff. capriotica (Oppenheim). Sample 9b2. o: Boundstone with foraminifera. Sample 9b. p: Crescentiella morronensis (Crescenti). Sample 9b. q: Boundstone with fragments of dasycladale algae, debris of Selliporella neocomiensis (Radoicic) and Crescentiella morronensis (Crescenti). Sample 9b. r: Suppiluliumaella aff. methana Dragastan & Richter. Sample 9b.

Plate 14 Microfacies from shallow-water carbonates from the Neochorouda Unit. a: Boundstone with sponge. Sample 9b. b: Boundstone with rivulariacean-type algae. Sample 9b. c, d : Suppiluliumaella aff. methana Dragastan & Richter. Sample 9b. e: Boundstone with debris of tufts of secondary laterals of Selliporella neocomiensis (Radoicic) (above) and fragment of Griphoporella jurassica (Endo) (below). Sample 9b. f, g, h, i: Boundstone with debris of tufts of secondary laterals of Selliporella neocomiensis (Radoicic). Sample 9b. j: Boundstone with stromatoporoid sponge. Sample 9d. k: Fragment of pharetronid sponge. Sample 9d. l: Rivulariacean-type algae. Sample 9d. m: Radiomura cautica Senowbari-Daryan & Schäfer. Sample 9g. n: Corals. Sample 9g. o,p: Suppiluliumaella aff. methana Dragastan & Richter. Sample 9g. q,r: Boundstone with stromatoporoid Milleporidium? sp. Sample 9e.

4.4.1 Reconstruction of the Jurassic to Early Cretaceous tectonic evolution

Age dating of the whole sequence including component analysis and detection of an eroded Late Jurassic platform led to following reconstruction of the geodynamic evolution: The closure of the western part of the Neotethys Ocean (Kilias et al. 2010, Missoni & Gawlick 2011, compare Robertson 2012, Papanikolau 2009, 2013) in late Early to Middle Jurassic was triggered by intra-oceanic subduction. This convergence east of the Pelagonian continent resulted in west-directed late Middle to early Late Jurassic ophiolite obduction and WNW to NW directed nappe stacking of the Pelagonian units in the western Vardar/Axios (= Neotethys) Ocean (Kilias et al. 2010). Ophiolite obduction onto the Pelagonian Units and imbrication of the Pelagonian sedimentary sequence are related to the same thrusting process. This process was followed by the onset of a shallow-water platform on top of the obducted ophiolites. This Late Jurassic carbonate platform evolution on top of the Middle to Late Jurassic nappe stack can be traced from the Eastern Alps to the Hellenides (Gawlick and Schlagintweit 2006, Gawlick et al. 2008, Schlagintweit et al. 2008, Missoni and Gawlick 2011). The new biostratigraphic and microfacies analysis of the clasts in the mass flows at the Neochorouda Unit provides new information about this platform pattern. In Greece, there are several localities described with Late Jurassic shallow-water limestones which occur both as carbonates platform sequences and as components (e.g. Gielisch et al. 1993, Carras and Georgala 1998, Scherreiks 2000, Kilias et al. 2010, Katrivanos et al. 2013) but this is the first detailed study about this eroded platform. Early Cretaceous extension and updoming of the nappe stack including the obducted ophiolites due to mountain uplift resulted in a reconfiguration of the nappe stack and sediment supply into newly formed basins. Erosion of the Late Jurassic carbonate platform together with ophiolite material and later the occurrence of metamorphic Triassic clasts clearly prove updoming of the nappe pile, crustal extension and gravitational sliding of the nappe pile to the west and to the east, as it can be demonstrated by identical successions on both sides of the Pelagonian Units in Greece, Albania and Serbia (Schlagintweit and Gawlick 2007, Gawlick et al. 2008, Schlagintweit et al. 2008, Kilias et al. 2010, Katrivanos et al. 2013).

The Berriasian evolution in the study area is documented by an increasing supply of clastic and ophiolitic debris (the turbiditic sequence of immature sandstones with coarse-grained mass flows below and intercalated). Ongoing uplift of the accreted Pelagonian units led to the exhumation of the metamorphic dome. Deep erosion of the metamorphosed Triassic-Jurassic Pelagonian rocks led to the formation of the polymictic conglomerate of the Neochorouda succession with e.g. quartzite, metamorphic radiolarites, and different metamorphosed shallow-water clasts of most probably late Middle Triassic age. The conglomerate was deposited in a low-stand system during the early stage of sea level rise. This earliest Cretaceous succession was again sealed by a newly formed Late Berriasian?-Valanginian shallow-water ramp most probably in the course of the sea- level rise resp. highstand. This shallow-water carbonates containing e.g. Suppiluliumaella aff. methana Dragastan & Richter, Coscinophragma sp. and Furcoporella? vasilijesimici Radoicic are also known west of the Pelagonian Units (Schlagintweit and Gawlick 2007, Schlagintweit et al. 2008). Plate convergence and westwards thrusting continued during Aptian to Albian times (e.g. Kilias et al. 2010, Katrivanos et al. 2012). Divergences from the main direction which occurred in the study area, are considered to be of regional importance. NW-SE to NNE-SSW trending overturned isoclinal folds with vergence mainly towards SE and an impressive north-westwards dipping S2 crenulation cleavage were observed. Due to transposition the older S1 schistosity is developed mainly parallel to S2. Furthermore, a penetrative stretching lineation and clasts elongation in a NNE/SSW orientation was developed during that time (Figure 23). Upper Cretaceous limestones and Paleocene flysch sediments overlay unconformable these tectonics structures and the Late Jurassic to Early Cretaceous sedimentary succession (Kilias et al. 2010, Katrivanos et al. 2013). After that the Neochorouda Unit has been affected by the younger Tertiary tectonics including compression and nappe stacking, followed by extension and again an orogenic collapse.

Figure 22 Reconstruction of the Middle Jurassic to Early Cretaceous geodynamic evolution. West-directed Middle to Late Jurassic ophiolite obduction onto the Pelagonian Units related to intra-oceanic thrusting followed by the formation of Kimmeridgian-Tithonian shallow- water carbonates after the emplacement of the ophiolites. Extension and updoming of the nappe stack led to erosion of the carbonate platform soon after sedimentation together with ophiolite material. Extensional collapse in Early Cretaceous due to mountain uplift resulted in exhumation of the metamorphic basement, basin subsidence and infilling of the basins with erosional products. After that Berriasian-Valanginian carbonates sealed this event.

Figure 23 NW-SE to NNE-SSW trending overturned isoclinal folds with vergence mainly towards SE and an impressive north-westwards dipping S2 crenulation cleavage (a, c). Schmidt diagram of the geo-metrical data of the fold (b) (Lower hemisphere). Schmidt diagram of the stretching lineation and elongation of the Neochorouda Unit clasts in a NNE/SSW orientation parallel to the folds axis plane (d) (Lower hemisphere).

Regional comparisons and correlations

Albania and Serbia In the Albanides, the radiolaritic-ophiolitic wild flysch or mélange (Perlat Formation) of the Mirdita Zone is covered by Kimmeridgian?-Tithonian mass flow deposits with frequent components of shallow-water lithoclasts and bioclasts (Kurbnesh Formation) (Schlagintweit and Gawlick 2007, Gawlick et al. 2008, Schlagintweit et al. 2008). Reefal components of different facies such as peri-reefal and lagoonal with stromatoporoids, sponges and corals are dominants. Reefal debris is typically encrusted by microencrusters such as Radiomura cautica Senowbari-Daryan

and Schafer. The components are interpreted to derive from an eroded shallow-water carbonate platform which was deposited on top of the Mirdita Ophiolite zone nappe stack (Schlagintweit and Gawlick 2007, Schlagintweit et al. 2008). Mirdita Ophiolites derive from Neotethys Ocean (= Vardar/Meliata) east of the Pelagonian continental fragment and consequently were brought into their present position by far-distance transport during W-vergent thrusting in Middle to Late Jurassic times (Schlagintweit et al. 2008, and references). After obduction and syntectonic formation of the sedimentary mélange (Perlat Formation), the Kimmeridgian?-Tithonian Kurbnesh carbonate platform was deposited. However, due to the mobile tectonic environment, it was completely eroded soon after sedimentation and it is only detectable in form of clasts in the mass-flow deposits of the Kurbnesh Formation. The only autochthonous shallow-water carbonates in the area of the Mirdita zone in central Albania is the Munella platform which represents the Late Berriasian- Valanginian interval (Schlagintweit and Gawlick 2007). In biostratigraphy and facies the Munella platform is similar to shallow-water components in mass-flows in the Mirdita Zone of Serbia (Schlagintweit et al. 2008). A rich diversified microbiota is described by Radoicic (2005) from the lowermost Valanginian of the Metohija Cretaceous Unit. The components contain similar algal and foraminifera associations as the Munella platform carbonates and the Berriasian-Valanginian shallow-water carbonates in Neochorouda area such as Suppiluliumaella aff. methana Dragastan & Richter, Coscinophragma sp. and Furcoporella? vasilijesimici Radoicic.

Greece Late Jurassic shallow-water limestones occur in Greece, both as carbonates platform sequences and as components (see also Schlagintweit et al. 2008). Scherreiks (2000) studying an area of NE Evvoia reported a carbonate succession consisting of reef-debris limestone and neritic debris limestone formed on top of the ophiolites nappes. The emplacement of the ophiolites nappes over the Pelagonian formations took place at latest Jurassic followed by regional uplift and by Lower Cretaceous erosion. This succession ranges in age from Oxfordian to Tithonian and is composed of reefal components and lithoclasts derived from framestones, containing Cladocoropsis mirabilis Felix. 61

Additionally, west of the Pelagonian Units, in the Corinthian area sequences composed of neritic limestone comprise the stratigraphic range of Tithonian to Valanginian. These sequences consist of coated grains, algae, foraminifera, shell- debris of brachiopods, gastropods, echinoderms and small debris of hydrozoans and corals. And are interpreted to lagoonal facies areas of a carbonate platform, which existed from Upper Jurassic to Lower Cretaceous time (Gielisch et al. 1993). Equal microfacies overlying granodioritic rocks are found in the west coast of the Chalkidiki peninsula (Epanomi-New Iraklia). These microfacies indicate Upper Jurassic to Lower Cretaceous reef-type platform margin, inner platform and lagoon environment (Carras and Georgala 1998). Additionally, Robertson et al. (2012) describes Upper Jurassic (Late Tithonian)- Upper Cretaceous mixed carbonate-clastic gravity deposits rich in bioclastic debris overlaying ophiolitic rocks after their emplacement in several section in the Vardar/Axios Zone in Northern Greece and FYROM. Finally, Late Jurassic to Early Cretaceous clastic sediments and shallow-water limestones on top of the obducted ophiolites probably related to extension and basin formation, simultaneously with nappe stacking and metamorphism in the Pelagonian nappes are also underlined by Kilias et al. (2010) in the western Axios Zone (Almopia Subzone) and Katrivanos et al. (2013) in the Paikon subzone.

CHAPTER 5. Discussion and conclusions

The new biostratigraphic and microfacies data combined with structural investigation and geological mapping led to the following conclusions: • The Triassic and Early Jurassic sediments were deposited in a rifted, transtensive passive continental margin setting facing the Neotethys Ocean. This Ocean opened after a Permian-Triassic continental break-up. Crustal extension and rift-related volcanism was dominant during that time (Dimitriadis and Asvesta 1993). • In late Early to Middle Jurassic time the geodynamic regime changed to convergent tectonics starting with intra-oceanic subduction in the Neotethys Ocean (Roddick et al. 1979, Spray and Roddick 1980, Brown and Robertson 2004, Sharp and Robertson 2006, Gawlick et al. 2008, Kilias et al. 2010). The occurrence of the Chortiatis magmatic series and supra-ophiolitic formations in the study area support the intra-oceanic subduction stage (Kockel et al. 1977, Michard et al. 1998, Zachariadis 2007). • Middle to Late Jurassic nappe stacking towards WNW to NW was related to intra-oceanic thrusting in the western Vardar/Axios (=Neotethys) Ocean and subsequent ophiolite obduction onto the Pelagonian Units. In this mobile tectonic environment a Kimmeridgian?-Tithonian carbonate platform was formed, which could be reconstructed by components analysis in the mass-flow deposits of Neochorouda Formation. The detection of the Kimmeridgian?-Tithonian carbonate platform means that the first thrusting process in the underlying ophiolite nappes had already terminated at that time. • Late Tithonian to earliest Cretaceous extension due to mountain uplift resulted in partial erosion of this carbonate platform soon after sedimentation and lithification of its rocks. The erosional products including ophiolitic debris were transported into newly formed adjacent basins. Components in the mass-flow deposits of the Neochorouda Unit in the Vardar/Axios zone resemble the erosional products known west of the

Pelagonian units, e.g. in Albania or Serbia and should derive therefore from the same palaeogeographic provenance area. • Ongoing uplift of the nappe stack in the Early Cretaceous was accompanied by continuous erosion that led to sediment supply into the newly formed basins. In the next stage due to the exhumation of the metamorphic dome, deep erosion led to the formation of the polymictic conglomerate of the Neochorouda Formation. • This earliest Cretaceous succession was again sealed by a newly formed Late Berriasian?-Valanginian shallow-water platform most probably in the course of the next sea-level rise resp. highstand. • The very same history as described above is documented in the Albanides Dinarides, Western Carpathians and Northern Calcareous Alps (e.g., Gawlick et al. 2008, Schlagintweit et al. 2008, Missoni and Gawlick 2011).

Abstract

The Late Jurassic to Early Cretaceous sedimentary succession of the Neochorouda Unit lies unconformable on top of the Oreokastro ophiolites of the Vardar/Axios zone in northern Greece. This succession consists of Early Cretaceous turbidites and mass flows with components of Kimmeridgian-Tithonian age mixed with ophiolite material and provides an upper limit for ophiolite emplacement. New biostratigraphic and microfacies analysis from the clasts in the mass flows were carried out for a better understanding of the Late Jurassic to Early Cretaceous geodynamic history. Microfacies and organism content prove the onset of Late Jurassic carbonate platforms on top of a Middle to Late Jurassic nappe stack striking from the Eastern Alps to the Hellenides. Middle to Late Jurassic nappe stacking towards WNW to NW followed late Early to Middle Jurassic intra-oceanic thrusting in the Western Vardar/Axios (= Neotethys) Ocean and subsequent ophiolite obduction onto the Pelagonian Units forming a thin- skinned orogen on the lower plate. After ophiolite emplacement Kimmeridgian-Tithonian carbonate platforms sealed widespread this tectonic event. Tithonian extension due to mountain uplift resulted in partial erosion of these platforms and new extensional basins were formed. The erosional products of the Neochorouda Unit in the Vardar/Axios zone resemble the erosional products known west of the Pelagonian units, e.g. in Albania or Serbia and should belong therefore to the same palaeogeographic provenance area. Late Tithonian to earliest Cretaceous erosion of the uplifted nappe stack including the obducted ophiolites resulted in sediment supply into the newly formed basins also east of the Pelagonian Units. This succession was sealed by a newly formed Late Berriasian?-Valanginian shallow-water platforms.

Περίληψη

Η Άνω Ιουρασική-Κάτω Κρητιδική ιζηματογενής ακολουθία της ενότητας Νεοχωρούδας βρίσκεται ασύμφωνα πάνω στους οφιολίθους του Ωραιοκάστρου, που ανήκουν στη ζώνη συρραφή του Αξιού στη Βόρεια Ελλάδα. Αυτή η ακολουθία αποτελείται από ροές μαζών και τουρβιδίτες και δίνει το ανώτατο όριο για την τοποθέτηση των οφιολίθων. Νέα βιοστρωματογραφική ανάλυση και ανάλυση μικροφάσεων των κροκάλων έγινε για την καλύτερη κατανόηση της γεωδυναμικής ιστορίας του Άνω Ιουρασικού - Κάτω Κρητιδικού. Οι μικροφάσεις και οι μικροοργανισμοί που εμπεριέχονται αποδεικνύουν την ύπαρξη ανθρακικών πλατφόρμων του Άνω Ιουρασικού, που δημιουργήθηκαν πάνω από τη συσσώρευση καλυμμάτων του Μέσου-Άνω Ιουρασικού από τις ανατολικές Άλπεις έως τις Ελληνίδες. Η συσσώρευση καλυμμάτων ηλικίας Μέσο-Άνω Ιουρασικού με φορά προς τα ΔΒΔ και η τοποθέτηση των οφιολίθων πάνω στις ενότητες της Πελαγονικής ακολουθήσαν την ενδοωκεάνια λεπίωση στο δυτικό τμήμα της Νεοτηθύος που έλαβε χώρα κατά τη διάρκεια του Ανωτέρου Κατωτέρου - Μέσου Ιουρασικού. Μετά την τοποθέτηση των οφιολίθων ανθρακικές πλατφόρμες Κιμμεριδίου-Τιθωνίου σφράγισαν αυτό το τεκτονικό γεγονός. Στο Τιθώνιο εκτατική τεκτονική συνδεδεμένη με φλοϊκή ανύψωση προκάλεσε μερική διάβρωση των ιζημάτων πλατφόρμας και νέες λεκάνες δημιουργήθηκαν. Τα προϊόντα της διάβρωσης που βρίσκονται στην ενότητα της Νεοχωρούδας στην ζώνη Άξιού συγκρίνονται με αυτά που αναπτύσσονται δυτικά από της Πελαγονικές ενότητες (στην Αλβανία και Σερβία επίσης) και συνεπώς θα πρέπει να θεωρηθούν ότι προέρχονται από την ιδία παλαιογεωγραφική πηγή. Η διάβρωση των ανυψωμένων καλυμμάτων και των επωθημένων οφιολίθων που έλαβε χώρα κατά το τέλος του Τιθώνιου έως της αρχές του Κρητιδικού συνεισέφερε υλικό που αποτέθηκε στις πρόσφατα δημιουργημένες λεκάνες και ανατολικά των ενοτήτων της Πελαγονικής. Αυτή η ακολουθία σφραγίστηκε από καινούργιες ρηχής θάλασσας πλατφόρμες ηλικίας ?Άνω Βαρριασίου–Βαλανζινίου.

References

Bebien, J., Dubois, R. and Gauthier, A., 1986. Example of ensialic ophiolites

emplaced in wrench zone: innermost Hellenic ophiolite belt (Greek

Macedonia). Geology 14: 1016-1019.

Bernouli, D. and Laubscher, H. 1972. The palinspastic problem of the Hellenides.

Eclogae Geologicae Helvetiae 65: 107-118.

Bortolotti, V., Chiari, M., Marroni, M., Pandolfi., Principi, G. and Saccani, E. 2012.

Geodynamic evolution of ophiolites from Albania and Greece (Dinaric-

Hellenic –belt): one, two or more oceanic basins? Inter. Journal of Earth

Sciences 102: 783-811.

Brown, S.A.M. and Robertson, A.H.F., 2004. Evidence for the Neotethys Ocean

rooted in the Vardar zone: evidence from the Voras Mountains, NW Greece.

Tectonophysics 381: 143-173.

Brunn, J.H., 1956. Contribution à l’ étude géologique du Pinde septentrional et d’ une

partie de la Macédoine occidnetale. Annale Géologique de Pays Hellénique 7:

1-358.

Carras, N., and Georgala, D., 1998. Upper Jurassic to Lower Cretaceous Carbonate

facies of African affinities in a peri-European area: Chalkidiki peninsula,

Greece. Facies 38: 153-164.

Channell, J.E.T. and Kozur, H.W., 1997. How many oceans? Meliata, Vardar and

Pindos oceans in the Mesozoic Alpine paleogeography. Geology 25: 183-186.

De Wet, A. P., 1989. Geology of part of Chalkidiki peninsula, Northern Greece. Ph.D.

thesis, Cambridge University: 177pp.

Dimitriadis, S. and Asvesta, A., 1993. Sedimentation and magmatism related to the

Triassic rifting and later events in the Vardar-Axios Zone. Bull. Geol. Soc.

Greece 28: 149-168.

Dimitrijevic, M.D., 1974. Sur l'âge du métamorphisme et des plissements dans la

masse Sérbo-Macédonienne. Bull. Assoc. Geol. Carpatho-Balkanique 1963

21: 45-48.

Dimitrijevic, M.D., 1997. Geology of Yugoslavia. Special publications, Geological

Institute, Gemini, Belgrade: 1-187.

Dunham, R.J., 1962. Classification of carbonate rocks according to depositional

texture. In: Ham, W.E. (ed.): Classification of carbonate rocks. A symposium.

Amer. Ass. Petrol. Geol. Mem. 1: 108-171.

Ferrière, J. and Stais, A., 1995. Nouvelle interprétation de la suture téthysienne

vardarienne d’ après l’analyse des séries de Péonias (Vardar oriental,

Hellénides internes). Bull. Soc. Géol. France 166(4): 327-339

Flügel, E., 2004. Microfacies of carbonate rocks: Analysis, Interpretation and

Application. Springer.

Folk, R. L., 1959. Practical classification of limestone. Amer. Ass. Petrol. Bull. 43: 1-

38.

Folk, R.L., 1962. Spectral subdivision of limestones types. In: Ham, W.E. (ed.):

Classification of carbonate rocks. A symposium. Amer. Ass. Petrol. Geol.

Mem. 1: 62-84

Gawlick H.-J. and Schlagintweit, F., 2006. Berriasian drowning of the Plassen

carbonate platform at the type-locality and its bearing on the early Eoalpine

orogenic dynamics in the Northern Calcareous Alps (Austria). International

Journal of Earth Sciences 95: 451-462.

Gawlick, H.-J., Frisch, W., Hoxha, L., Dumitrica, P., Krystyn, L., Lein, R., Missoni,

S., and Schlagintweit, F., 2008. Mirdita zone ophiolites and associated

sediments in Albania reveal Neotethys Ocean origin. International Journal of

Earth Sciences 94: 865-881.

Gielisch, H., Dragastan, O. and Richter, D., 1993. Lagoonal to tidal carbonate

sequences of upper Jurassic/Lower Cretaceous age in the Corinthian area:

Mélange blocks of the Parnassus Zone. Bull. Geol. Soc. Greece XXVIII/3:

663-676.

Godfriaux, J., 1968. Etude géologique de la région de l’ Olympe (Grèce). Annale

Géologique de Pays Hellénique 19: 1-271.

Jacobshagen, V., 1986. Geologie von Griechenland. Beitraege zur regionalen

Geologie der Erde. Gebrueder Borntraeger Verlag, Berlin, 363 pp.

Jacobshagen, V., Duerr, F., Kockel, K., Kopp, K.O., Kowalczyk, G., Berckhemer, H.

and Buttner, D., 1978. Structure and geodynamic evolution of the Aegean

region. In: H. Cloos, D. Roeder. and K. Schmidt (eds), Alps, Apennines,

Hellenides. E. Schweizerbart` sche Verlagsbuchhandlung, Stuttgart, pp. 537-

564.

Katrivanos, E., Kilias, A. and Mountrakis, D. 2013. Kinematics of deformation and

structural evolution of the Paikon Massif (Cental Macedonia, Greece): A

Pelagonian tectonic window? N. Jb. Geol. Palaont. Abh. 269/2: 149-171.

Kauffmann, G., Kockel, F. and Mollat, H. 1976. Notes on the stratigraphic and

paleogeographic position of the Svoula Formation in the Innermost Zone of

the Hellenides (Northern Greece). Bull. Soc. geol. France (7) XVIII: 255-230.

Kilias, A., and Mountrakis, D., 1987. Zum tektonischen Bau der Zentral-

Pelagonischen Zone (Kamvounia Gebirge, N. Griechenland). Zeitschift der

Deutschen Geologischen Gesellschaft 138: 211-237.

Kilias, A., 1991. Transpressive Tecktonik in den zentralen Helleniden. Aenderung der

Translationpfade durch die Transgression Nord-Zentral Griechenland). Neues

Jahrbuch fuer Geologie und Palaeontologie Monatshefte 5: 291-306.

Kilias, A., Falalakis, G. and Mountrakis, D., 1999. Cretaceous-Tertiary structures and

kinematics of the Serbomacedonian metamorphic rocks and their relation to

the exhumation of the Hellenic hinterland (Macedonia, Greece). International

Journal of Earth Sciences 88: 513-531.

Kilias, A., Tranos, M., Orozco, M., AlonsoChaves, F. M. and Soto, J. I., 2002.

Extensional collapse of the Hellenides: A review. Revista de la Sociedad

Geologice de Espana 15: 129-139.

Kilias, A., Frisch, W., Avgerinas, A., Dunkl, I., Falalakis, G. and Gawlick, H.-J.,

2010. Alpine architecture and kinematics of deformation of the northern

Pelagonian nappe pile in the Hellenides. Austrian Journal of Earth Sciences

103/1: 4-28.

Kockel, F., Mollat, H. and Walther, H.W., 1971. Geologie des SerboMazedonischen

Massivs und seines mesozoischen Rahmens (Nordgriechenland). Geol. Jb. 89:

529-551.

Kockel, F. and Mollat, H., 1977. Geological map of the Chalkidiki peninsula and

adjacent areas (Greece), Scale 1:100000. Bundesanstalt fur Geowissenschaften

und Rohstoffe, Hannover.

Kossmat, F., 1924. Die Kriegsschauplatze 1914-1918 geologisch dargestellt. Heft 12:

Geologie der zentralen Balkanhalbinsel. Mit einer Übersicht des dinarischen

Gebirgsbaus. (Borntraeger): 1-198.

Kostaki, G., Kilias, A., Gawlick, H.-J. and Schlagintweit, F., 2013. ?Kimmeridgian-

Tithonian shallow-water platform clasts from mass flow on top of the

Vaedar/Axios Ophiolites. Bull. Geol. Soc. Greece XLVII.

Meinhold, G., Kostopoulos, D., Reischmann, T., Frei, D. and Bou Dagher-Fadel,

M.K., 2009. Geochemistry, provenance and stratigraphic age of

metasedimentary rocks from the eastern Vardar suture zone, northern Greece.

Palaeogeography, Palaeoclimatology, Palaeoecology 277: 199-225.

Meinhold, G. and Kostopoulos, D., 2012. The Circum-Rhodope, northern Greece:

Age, provenance, and tectonic setting. Tectonophysics 595-596: 55-68

Mercier, J., 1968. Etude geologique des zones internes hellenides en Macedoine

centrale (Grece). Contribution a l etude du metamorphisme et de l evolution

magmatique des zones internes des Hellenides. Annales geologiques des pays

helleniques 20: 1-792.

Mercier, J., Vergely, P. and Bebien, J., 1975. Les ophiolites helleniques “obductees”

au Jurassique superieur sont-elles les vestiges d une mer marginale peri-

europeenne? C. R. somm. S.G.F.

Michard, A., Feinberg, H. and Montigny, R., 1998. Supra-ophiolite formation from

the Thessaloniki nappes (Greece) and associated magmatism: an intra-oceanic

subduction predating the Vardar obduction. Comptes Rendus de l’Académie

de France Paris 327: 493-499

Missoni, S. and Gawlick, H.-J., 2011. Evidence for Jurassic subduction from the

Northern Calcareous Alps (Berchtesgaden; Austroalpine, Germany).

International Journal of Earth Sciences 100: 1605-1631.

Mountrakis, D., 1986. The Pelagonian Zone in Greece: A polyphase deformed

fragment of the Cimmerian continent and its role in the geotectonic evolution

of the Eastern Mediterranean. Journal of Geology 94: 355-347.

Mussalam, K. and Jung, D., 1986. Geology und Bau des Sithonia-Ophioliths

(Chalkidiki, NE Griechenland: Anmerkungen zur Bildung ozeanischer

Krusten). Geologische Rundschau 75: 383-409.

Mussalam, K., 1991. Geology, geochemistry and the evolution of an oceanic crustal

rift at Sithonia, NE Greece. In: Ophiolite Genesis and Evolution of the

Oceanic Lithosphere, Tj. Peters et al. (eds): 685-704.

Papanikolaou, D., 2009. Timing of tectonic emplacement of the ophiolites and terrane

paleogeography in the Hellenides. Lithos 108: 262-280.

Papanikolaou, D., 2013. Tectonostratigraphic models of the Alpine terranes and

subduction history of the Hellenides. Tectonophysics 595–596: 1–24

Platt, J.P., Soto, J.I., Whitehouse, M.J., Hurford, A.J. and Kelley, S.P., 1998. Thermal

evolution rate of exhumation, and tectonic significance of metamorphic rocks

from the floor of the Alboran extensional basins, western Mediterranean.

Tectonics 17: 671-689.

Radoicic, R. 2005. New Dasycladales and microbiota from the lowermost

Valanginian of the Mirdita Zone. Annales Geologiques de la Peninsule

Balkanique, 57/1: 21-35.

Ricou, L.-E., 1965. Contribution a l'étude géologique de la bordure sud-ouest du

Massif Serbo-Macédonien aux environs de Salonique. Thèse 3éme cycle.

Université de Paris, France.

Robertson, A.H.F., Dixon, J. E., Brown, S., Collins, A., Morris, A., Pickett, E., Sharp,

I. and Ustaömer, T., 1996. Alternative tectonic models for the Late

Palaeozoic-Early Tertiary development of the Tethys in the Eastern

Mediterranean. In: J.E. Dixon and A.H.F. Robertson (eds), The Geological

Evolution of the Eastern Mediterranean. Geological Society of London Special

Publications 17: 1-74.

Robertson, A.H.F., and Shallo, M., 2000. Mesozoic- Tertiary tectonic evolution of

Albania in its regional Eastern Mediterranean context. Tectonophysics 316:

197-214.

Robertson, A.H.F., 2012. Late Paleozoic-Cenozoic tectonic development of Greece

and Albania in context of alternative reconstructions of Tethys in the Eastern

Mediterranean region. International Geology Review 54: 373-454.

Robertson, A.H.F., Trivic, B., Djeric, N. and Bucur, I.I., 2012. Tectonic development

of the Vardar Ocean and its margins: Evidence from the Republic of

Macedonia and Greek Macedonia. Tectonophysics. Available online at:

http://dx.doi.org/10.1016/j.tecto.2012.07.022

Roddick, J., Cameron, W. and Smith, A.G., 1979. Permotriassic and Jurassic Ar/Ar

ages from Greek ophiolites and associated rocks. Nature 279: 788-790.

Scherreiks, R., 2000. Platform margin and oceanic sedimentation in a divergent and

convergent plate setting (Jurassic, Pelagonian Zone, NE Evvoia, Greece).

International Journal of Earth Sciences 89: 90-107.

Schlager, W. and Schöllnberger, W., 1974. Das Prinzip stratigraphischer Wenden in

der Schichtenfolge der Nördlichen Kalkalpen. Mitteilungen der Geologischen

Gesellschaft Wien 66/67: 165-193.

Schlagintweit, F., Gawlick, H.-J. and Lein, R. 2005. Mikropalaeontologie und

Biostratigraphie der Plassen-Kaebonatplatform der Typlokalitaet (Ober-Jura

bis Unter-Kreide, Salzkammergut, Oesterreich. Journal of Alpine Geology

(Mitt. Ges. Geol. Bergbaustud. Oesterr.) 47: 11-102.

Schlagintweit, F. and Gawlick, H.-J., 2007. Analysis of the Late to Early Cretaceous

algal debris-facies of the Plassen carbonate platform in the Northern

Calcareous Alps (Germany, Austria) and in the Kurbnesh area of the Mirdita

zone (Albania) – a tool to reconstruct tectonics and paleogeography of eroded

platforms. Facies 53: 209-227.

Schlagintweit, F., Gawlick, H.-J., Missoni, S., Hoxha, L., Lein, R. and Frisch, W.

2008. The eroded Late Jurassic Kurbnesh carbonate platform in the Mirdita

ophiolite Zone of Albania and its bearing on the Jurassic orogeny of the

Neotethys realm. Swiss Journal of Geosciences 101: 125-138.

Schlagintweit, F. and Gawlick, H.-J., 2009. Enigmatic tubes associated with microbial

crusts from the Late Jurassic of the Northern Calcareous Alps (Austria): a

mutualistic sponge–epibiont consortium? Lethaia 42: 452–461.

Schlagintweit, F. 2011. The dasycladalean algae of the Plassen carbonate platform

(Kimmeridgian-Early Berriasian): taxonomic inventory and

palaeogeographical implications within the platform-basin-system of the

Northern Calcareous Alps (Austria, p.p. Germany). Geologia Croatica 64/3:

185-206.

Schmid, S.M., Bernoulli, D., Fugenschuh, B., Matenco, L., Scheffer, S., Schuster, R.,

Tischler, M. and Ustaszewski, k., 2008. The Alpine-Carpathian-Dinaric

orogenic system: correlation and evolution of tectonic units. Swiss Journal of

Geosciences 101: 139-183.

Sharp, I.R. and Roberson, A.H.F., 2006. Tectonicsedimentary evolution of the

western margin of the Mesozoic Vardar Ocean: evidence from the Pelagonian

and Almopias zones, northern Greece. In: A.H.F. Robertson and D.

Mountrakis (eds), Tectonic Development of the Eastern Mediterranean

Region. Geological Society of London, Special Publications, 260: 373-412.

Smith, A.G. and Spray, J.G., 1984. A half-ridge transform model for the Hellenic-

Dinaric ophiolites. In: Dixon, J.E. & Robertson, A.H.F. (eds). The geological

evolution of the eastern Mediterranean. Geological Society of London, Special

Publications 17: 629-644.

Spray, J.G. and Roddick, J.C., 1980. Petrology and 40Ar/39Ar geochronology of some

Hellenic subophiolitic metamorphic rocks. Contribution to Mineralogy and

Petrology 72: 43-55.

Stampfli, G.M. and Borel, G.D., 2002. A plate tectonic model for the Paleozoic and

Mesozoic constrained by dynamic plate boundaries and restored synthetic

oceanic isochrones. Earth and Planetary Science Letters 169: 17-33.

Stampfli, G.M. and Kozur, H., 2006. Europe from the Variscan to the Alpine cycles.

In: Gee, D.G. and Stephenson R.A. (eds) European lithosphere dynamics 32,

Geological Society Memoir, London, pp 57-82.

Tranos, M., Kilias, A. and Mountrakis, D., 1999. Geometry and kinematics of the

Tertiary post-metamorphic Circum Rhodope Belt Thrust System (CRBTS),

Northern Greece. Bull. Geol. Soc. Greece XXXIII: 5-16.

Wilson, J.L., 1975. Carbonate facies in geologic history. Springer.

Zachariadis, P., 2007. Ophiolites of the eastern Vardar Zone, N. Greece. PhD Thesis,

University of Mainz, Germany.

ONLINE SOURSES

http://www.beg.utexas.edu/lmod/_IOL-CM01/cm01-step03.htm 01/07/2013 http://sedimentology.blogsohu.com (01/07/2013)

ΑΝΝΕΧ

NAME CLASSIFICATION SMF BIOGENIC COMPONENTS BIOFABRICS OF TYPE COMPONENTS & SAMPLE STRUCTURES GR1 RUDSTONE SMF 4 Labyrinthina Gabbroic and Encrustation mirabilis quartz clasts Weynschenk Crescentiella morronensis (Crescenti) Foraminifera Crinoids Fragment of Brachiopod GR2 RUDSTONE SMF 4 Reef builders Gabbroic and Laminated Fragments of quartz clasts Shells Crinoids Foraminifera GR3 FLOATSONE SMF 4 Griphoporella Micritic jurassica (Endo) envelopes Reef builders Crinoids GR4 RUDSTONE SMF 4 Reef builders Gabbroic and Bioclasts with Fragments of quartz clasts micritic shells envelopes Crinoids Foraminifera 6a BAFFLESTONE SMF 7 Crescentiella Reef morronensis framework (Crescenti ) Encrustation Radiomura cautica Senowbari-Daryan & Schafer Labes atramentosa Eliasova Reef builders 6b BOUNDSTONE SMF 7 Neoteutloporella Reef socialis (Praturlon) framework Thaumatoporella Encrustation sp Micritic Crescentiella envelopes morronensis Boring (Crescenti) Griphoporella jurassica (Endo) Reophax? rhaxelloides Schlagintweit, Auer & Gawlick Sclerosponge Reef builders Crinoids Foraminifera Fragments of shells 6z BAFFLESTONE SMF 7 Crescentiella Reef morronensis framework (Crescenti) Encrusting Reef builders organisms 6e BOUNDSTONE SMF 7 Perturbatacrusta Reef leini Schlagintweit framework & Gawlick Encrustation Labes atramentosa Eliasova Radiomura cautica Senowbari-Daryan & Schafer Corals Reef builders 6h BAFFLESTONE SMF 7 Radiomura cautica Reef Senowbari-Daryan framework & Schafer Encrustation Sponges Reef builders 6g BAFFLESTONE SMF 7 Crescentiella Reef morronensis framework (Crescenti) Encrusting organisms 6th BAFFLESTONE SMF 7 Crescentiella Reef morronensis framework (Crescenti) Encrusting Radiomura cautica organisms Senowbari-Daryan & Schafer Astraeofungia Crinoids GR6 BAFFLESTONE SMF 7 Labes atramentosa Reef Eliasova framework Corals Encrusting Feef builders organisms Fragment of shells GR7 BAFFLESTONE SMF 7 Reef builders Reef framework Encrusting organisms GR11 BAFFLESTONE SMF 7 Perturbatacrusta Reef leini Schlagintweit framework & Gawlick Micritic envelopes GR13 Algal- SMF 7 Neoteutloporella Reef BAFFLESTONE socialis (Praturlon) framework Pseudocyclammina Encrustation lituus (Yokoyama) Foraminifera 7a GRAINSTONE SMF 4 Foraminifera Clasts of sandstone, gabbros and quartz 7b GRAINSTONE SMF 4 Anchispirocyclina Clasts of Coated grains lusitanica (Egger) sandstone, Mohlerina gabbros and basiliensis quartz (Mohler) Pseudocyclammina lituus (Yokoyama) Crescentiella morronensis (Crescenti) Nautiloculina cf. oolithica Mohler Foraminifera 7d RUDSTONE SMF 4 Crescentiella Clasts of morronensis sandstone, (Crescenti) gabbros and Sponge quartz 7e BAFFLESTONE SMF 7 Crescentiella Clasts of (above) (above) morronensis sandstone and RUDSTONE SMF 4 (Crescenti) quartz (below) (below) Corals

7g RUDSTONE SMF 4 Labes atramentosa Clasts of Micritic Eliasova sandstone, envelopes Crescentiella gabbros and morronensis quartz (Crescenti) Radiomura cautica Senowbari-Daryan & Schafer GR12 GRAINSTONE SMF 4 Salpingoporella Clasts of pygmaea sandstone, (Gümbel) gabbros and Foraminifera quartz GR14 GRAINSTONE SMF 4 Crescentiella Clasts of Coated grains morronensis sandstone (Crescenti) Nautiloculina cf. oolithica Mohler Mohlerina basiliensis (Mohler) Trinocladus? sp. Gastropod Foraminifera

8a RUDSTONE SMF 24 Foraminifera Clasts of different metamorphosed shallow-water clast 8a2 RUDSTONE SMF 24 Quartzite’s resp. metamorphic radiolarites, different metamorphosed shallow-water clasts 9a BAFFLESTONE SMF 7 Stromatoporoid 9b BAFFLESTONE SMF 7 Griphoporella jurassica (Endo) Griphoporella cretacea (Dragastan) Fragment of Furcoporella vasilijesimici Radoicic Suppiluliumaella aff. methana Dragastan & Richter Debris of Selliporella neocomiensis (Radoicic) Crescentiella morronensis (Crescenti) Corals Stromatoporoid Dasycladales Foraminifera Sponge Solenoporaceae 9b2 BAFFLESTONE SMF 7 Linoporella aff. capriotica (Oppenheim) 9d BAFFLESTONE SMF 7 Stromatoporoid sponge Fragment of pharetronid sponge Rivularicean-type algae 9g BAFFLESTONE SMF 7 Radiomura cautica Senowbari-Daryan & Schafer Suppiluliumaella aff. methana Dragastan & Richter Corals 9e BAFFLESTONE SMF 7 Stromatoporoid, Milleporidium? sp. NP1 BOUNDSTONE SMF 7 Furcoporella? vasilijesimici Radoicic Linoporella aff. capriotica (Oppenheim) Suppiluliumaella aff. methana Dragastan & Richter Coscinophragma sp. Radiomura cautica Senowbari-Daryan & Schafer 1b PELOIDAL SMF 16 Foraminifera Peloids PACKSTONE TO GRAINSTONE 3d PACKSTONE TO SMF 16 Coated GRAINSTONE grains, e.g. cortoids and oncoids Micritic envelopes 5a PELOIDAL SMF 16 Micritic PACKSTONE TO peloids GRAINSTONE Micritic envelopes 3a PELOIDAL SMF 16 Peloids PACKSTONE TO GRAINSTONE 1a PELOIDAL Infillings of PACKSTONE TO open marine GRAINSTONE material K1 PACKSTONE SMF 3- Filaments Fil Echinoderms Gastropods K2 PACKSTONE SMF 3- Filaments Clasts of Fil Echinoderms micrite Foraminifera Bivalves Gastropods Fragments of crinoids K3 PACKSTONE SMF 3- Crinoids Hardground Fil Filaments Foraminifera Echinoderms Gastropod K4 CRINOIDAL SMF Crinoids Shallow GRAINSTONE 12-Crin water components GR16 CRINOIDAL SMF Crinoids PACKSTONE 12-Crin Filaments Gastropod X Deformed Isopachous cement 2a GRAINSTONE SMF 5 Crescentiella Micrite clasts morronensis Encrusting (Crescenti) organisms Gastropods Reef builders 2b GRAINSTONE SMF 5 Crescentiella Encrusting morronensis organisms (Crescenti) Foraminifera Crinoids Reef builders 4a RUDSTONE SMF 5 Sponge Reef Algae framework 4b RUDSTONE SMF 5 Crinoids Quartz clasts Micrite clasts Foraminifera Reef builders Algae Dasycladales 4g GRAINSTONE SMF 5 Siliciclastic clasts F1 RUDSTONE SMF 5 Foraminifera Clasts of micrite Bryozoan F2 RUDSTONE SMF 5 Reef builders F3 LAMINATED SMF 5 Laminated GRAINSTONE Dolomitized F4 GRAINSTONE SMF 5