– Geological map of Kato Seli. 3.1. Geologic Map Units 3.1.1. Pelagonian Zone Units @BULLET Triassic–Jurassic marbles and schists. This unit comprises gray, light gray and white recrystallized limestones–marbles. They are often dolomitic and are part of the  

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... emplacement of the Vermion Nappe, and the geotectonic evolution of the area where the Pelagonian and Almopias Zones come in contact. Field work was undertaken in order to decipher the uncertainties concerning the rocks that crop-out south of Kato Seli and also the contacts of these rocks. As a result, a new geologic map of the area is presented (Fig. 2) based on our field investigations, accompanied by a geologic cross-section (Fig. 3). The new data contribute to the better understanding of the geology of the area and put new constraints on the geotectonic evolution of the wider ...

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... platform limestones that overlie the metamorphic basement of the Pelagonian Zone (Brunn, 1959;Mountrakis, 1983;Kilias and Mountrakis, 1989;Sharp and Robertson, 2006). Green chloritic-serikitic schist horizons up to a few meters thick that represent metamorphosed clastic sediment intercalations are found mostly at the upper part of the marbles (Figs. 2, ...

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... Jurassic melange. A Jurassic melange consisting of green-brown colored chloritic-sericitic schists and phyllites (Figs. 2, 3, 4c) is tectonically overlying the Triassic-Jurassic marbles. It is considered a melange because of (a) the existence of large blocks of recrystallized limestones which are floating as olistholites (Figs. 2, 3, 5a), (b) its intense deformation i.e., folded with tight-isoclinal folds (Fig. 5e), (c) the existence at the upper part and the top ...

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... Jurassic melange. A Jurassic melange consisting of green-brown colored chloritic-sericitic schists and phyllites (Figs. 2, 3, 4c) is tectonically overlying the Triassic-Jurassic marbles. It is considered a melange because of (a) the existence of large blocks of recrystallized limestones which are floating as olistholites (Figs. 2, 3, 5a), (b) its intense deformation i.e., folded with tight-isoclinal folds (Fig. 5e), (c) the existence at the upper part and the top of the melange of ophiolites of up to a few meters thick of mainly serpentinitic composition that appear as floating lensoidal bodies (Figs. 2, 3). They are clastic sediments that were formed and ...

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... of recrystallized limestones which are floating as olistholites (Figs. 2, 3, 5a), (b) its intense deformation i.e., folded with tight-isoclinal folds (Fig. 5e), (c) the existence at the upper part and the top of the melange of ophiolites of up to a few meters thick of mainly serpentinitic composition that appear as floating lensoidal bodies (Figs. 2, 3). They are clastic sediments that were formed and metamorphosed during the emplacement of the ophiolites during the Upper Jurassic ( Mountrakis and Soulios, 1978;Sharp and Robertson, ...

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... the top, they become thin-bedded, clastic, and pass to flysch. The flysch is brown-light brown and consists of very thin to thin siltstone and sandstone turbiditic intercalations. The age of the flysch is Maastrichtian (Brunn, 1959(Brunn, , 1982aMercier, 1968). The Upper Cretaceous sedimentary rocks dip to the West with intermediate angles (Fig. 2) as the Maastrichtian flysch, while the latter is tectonically overlain by the Vermion Nappe (Fig. 2). ...

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... and consists of very thin to thin siltstone and sandstone turbiditic intercalations. The age of the flysch is Maastrichtian (Brunn, 1959(Brunn, , 1982aMercier, 1968). The Upper Cretaceous sedimentary rocks dip to the West with intermediate angles (Fig. 2) as the Maastrichtian flysch, while the latter is tectonically overlain by the Vermion Nappe (Fig. 2). ...

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... low grade metamorphic facies. The rudites contain quartz, ophiolite, schist and carbonate clasts ranging in size from granules to pebbles. Upwards, these rocks pass to beige-gray colored calcirudites and calcarenites because the carbonate clasts become more abundant. The thickness of this unit does not exceed 30m and wedges out towards the north (Figs. 2, 5a). These rocks are heterogeneously deformed during Tertiary, with a strong developed mylonitic foliation parallel to bedding at parts. These rocks resemble similar lithological features with metaclastic rocks mapped more easterly as "flyschoidal rocks", and which have been included in the "zone broyée" mentioned in the geological map of ...

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... the contacts between the mapped rocks, our observations suggest that the contact between the overlying Cretaceous rocks and the underlying ones is sub-horizontal near Kato Seli, but to the SW, it trends NE-SW dipping to the NW with low angles (Fig. 2). The main foliation of the Triassic-Jurassic marbles is sub-parallel to the main foliation of the Jurassic melange and dips to the NW with intermediate angles (Figs. 2, 6a). On the other hand, the bedding of the overlying rocks generally dips to the NW with low angles (Figs. 2, ...

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... that the contact between the overlying Cretaceous rocks and the underlying ones is sub-horizontal near Kato Seli, but to the SW, it trends NE-SW dipping to the NW with low angles (Fig. 2). The main foliation of the Triassic-Jurassic marbles is sub-parallel to the main foliation of the Jurassic melange and dips to the NW with intermediate angles (Figs. 2, 6a). On the other hand, the bedding of the overlying rocks generally dips to the NW with low angles (Figs. 2, ...

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... Seli, but to the SW, it trends NE-SW dipping to the NW with low angles (Fig. 2). The main foliation of the Triassic-Jurassic marbles is sub-parallel to the main foliation of the Jurassic melange and dips to the NW with intermediate angles (Figs. 2, 6a). On the other hand, the bedding of the overlying rocks generally dips to the NW with low angles (Figs. 2, ...