Vertical Anatolian mavoment project

TÜBİTAK ÇAYDAG01.09.201

Post-Paleogene (post-Middle Eocene-pre-Miocene) geodynamic evolution of the Upper Cretaceous-Paleogene Basins in Central Anatolia, Turkey.

Central Anatolia is one of the key areas on the evolution of Cretaceous-Paleogene Tethys where stratigraphy of the region is well studied. However not well linked with tectonics. The so-called "Ankara Mélange" belt (AOM) and the basins on top are important elements in the understanding of the İzmir-Ankara-Erzincan suture belt (İAES) evolution in Anatolia (Turkey) and in the evolution of Tethys in minor Asia (Turkey). Some of the basins are directly situated on top of the tectonic slices of the accretionary prism (IAES). However, some are not tectonically well explained as in the case of Haymana basin. The southern continental fragments (eg. Kütahya-Bolkardaǧ and Kırșehir blocks from Gondwana) are approaching to northern continents (Pontides of Lauriasia) where basins like Haymana, Alçı, Kırıkkale and Orhaniye extensional basins are evolved in between the closing margins of two continents. Haymana basin is an extensional basin developed under contractional regime on top of both northward subducting oceanic fragments and an approaching fragments of southern continents. Paleogene (end of Eocene) is the time where the Seas were retreated to S-SE Anatolia leaving a continental setting in Anatolia during Oligocene-Miocene. The slip data gathered from the faults cross-cutting the Paleogene Units and the fabric from Cretaceous mélanges depicts a NNW-SSE to NNE-SSW compressional stress regime operated during post-Eocene-pre-Miocene period. Lately the slip surfaces were overprinted by post-Pliocene normal faulting. Key words: fault slip data, Paleogene, NNW-SSE compression, Anatolia

Tectonic evolution of the Cretaceous Ankara Ophiolitic Melange during the Late Cretaceous to pre-Miocene interval in Central Anatolia, Turkey

The chaotic tectonic belt, which is distinguished in northern Anatolia, is called the - Ankara Accretionary Complex - in the Ankara region, central Anatolia. The belt is differentiated into three imbricated tectonic subbelts, namely, pre-Triassic metamorphics, Melange with calcareous blocks and Cretaceous melange with ophiolitic blocks (Ankara Ophiolitic Melange)

Tectonostratigraphy and neotectonic characteristics of the southern margin of Merzifon-Suluova Basın (Central Pontides, Amasya).

Ph.D. - Doctoral Progra

Geç Kretase-Eosen Yaşlı Haymana Havzasının Paleojen Sonrası-Neojen Öncesi Deformasyonu, İç Anadolu

Geç Kretase-Eosen Yaşlı Haymana Havzasının Paleojen Sonrası-Neojen Öncesi Deformasyonu, İç Anadol

Tectonic setting of some Paleozoic metamorphics in northern Anatolia

In northern Anatolia along the Izmir-Ankara-Erzurum Suture, the low-grade metamorphics display strong protolithologic similarities. However, the classification of these metamorphics with respect to ' their prototithological stratigraphy, internal organization, age and boundary relations are still not clear due to limited number of metamorphic studies. Amasya region in NW Central Anatolia is selected and studied to shed some light onto the metamor-phic problem in northern Anatolia. TectonostratigraphicaUy, three distinctly different metamorphic rock assemblages are differentiated on the basis of their internal organizations and protolithologies, as bottom to top; 1) grayish-black schists with quartz boudins and veins, 2) green schists, 3) green schists with marble blocks and/or boudins. The lower unit is originally a clastic sequence, made of shales, sandstones, cherts and calcareous clas-tics. It is t.ectonically overlain by green schists protoliths of which are volcanic and carbonate rocks. The upper unit, composed of huge mar-ble blocks and/or lenses embedded within a volcanic sequence. The protoliths of greenschist facies metamorphics are interpreted as a magmatic arc-related basinal being metamorphosed by regional dynamothermal metamorphism during pre-Permian. These meta-morphics can protolithologically be correlated with Agvanis and Yenise-hir low-grade metamorphics which all are believed to be in Carboniferous age

An Active Composite Pull-apart Basin Within the Central Part of the North Anatolian Fault System: the Merzifon-Suluova Basin, Turkey

The North Anatolian Fault System (NAPS) that separates the Eurasian plate in the north from the Anatolian microplate in the south is an intracontinental transform plate boundary. Its course makes a northward convex arch-shaped pattern by flexure in its central part between Ladik in the east and Kargi in the west. A number of strike-slip basins of dissimilar type and age occur within the NAFS. One of the spatially large basins is the E-W-trending Merzifon-Suluoya basin (MS basin), about 53 km long and 22 km wide, located on the southern inner side of the northerly-convex section of the NAFS. The MS basin has two infills separated from each other by an angular unconformity. The older and folded one is exposed along the fault-controlled margins of the basin, and dominantly consists of a Miocene fluvio-lacustrine sedimentary sequence. The younger, nearly horizontal basin infill (neotectonic infill) consists mainly of Plio-Quaternary conglomerates and sandstone-mudstone alternations of fan-apron deposits, alluvial fan deposits and recent basin floor sediments. The two basin infills have an angular unconformity between them and the deformed pattern of the older infill reveals the superimposed nature of the MS basin. The MS basin is controlled by a series of strike-slip fault zones along its margins. These are the E-W-trending Merzifon dextral fault zone along its northern margin, the E-W-trending Saribugday dextral fault zone along its southern margin and the NW-trending Suluova normal fault zone along its eastern margin. The basin is cut by the E-W-trending Uzunyazi dextral fault zone, which runs parallel to the northern and southern bounding fault zones and displays a well-developed overlapping relay pattern by forming a positive flower structure. The faults of the zone cut Quaternary neotectonic infill and tectonically juxtapose the fill with older rock units. The central faults are seismically more active than the bounding faults, and are therefore relatively younger faults. The early-formed rhomboidal basin is subdivided by these E-W-trending younger faults into several coalescing sub-basins, converting it into a composite pull-apart basin. The total cumulative post-Pliocene dextral offset along the southern bounding faults is about 12.6 km