Mesozoic–Tertiary Sedimentary and Tectonic Evolution of Neotethyan Carbonate Platforms, Margins and Small Ocean Basins in the Antalya Complex of Southwest Turkey

  1. L. E. Frostick2 and
  2. R. J. Steel3
  1. A. H. F. Robertson

Published Online: 16 APR 2009

DOI: 10.1002/9781444304053.ch22

Tectonic Controls and Signatures in Sedimentary Successions

Tectonic Controls and Signatures in Sedimentary Successions

How to Cite

Robertson, A. H. F. (1994) Mesozoic–Tertiary Sedimentary and Tectonic Evolution of Neotethyan Carbonate Platforms, Margins and Small Ocean Basins in the Antalya Complex of Southwest Turkey, in Tectonic Controls and Signatures in Sedimentary Successions (eds L. E. Frostick and R. J. Steel), Blackwell Publishing Ltd., Oxford, UK. doi: 10.1002/9781444304053.ch22

Editor Information

  1. 2

    Reading, UK

  2. 3

    Bergen, Norway

Author Information

  1. Department of Geology and Geophysics, University of Edinburgh, Edinburgh EH9 3JW, Scotland, UK

Publication History

  1. Published Online: 16 APR 2009
  2. Published Print: 28 FEB 1994

ISBN Information

Print ISBN: 9780632037452

Online ISBN: 9781444304053

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Keywords:

  • Mesozoic-tertiary sedimentary and tectonic evolution;
  • Neotethyan carbonate platforms in Antalaya Complex. Southwest Turkey;
  • methodology and tectonostratigraphy;
  • autochthonous carbonate platform;
  • volcanic-sedimentary melange

Summary

The allochthonous Antalya Complex (‘Antalya nappes’) in the Isparta angle of southwest Turkey exemplifies important sedimentary and tectonic processes, related to the interaction of carbonate platforms, margins and small ocean basins in the Eastern Mediterranean Neotethyan area. The complex is mainly composed of Mesozoic sedimentary, igneous and minor metamorphic rocks of mostly microcontinental and oceanic origin. Individual areas are discussed in turn. The western area illustrates an original eastward transition from a large carbonate platform (Bey Daǧlari), across a passive margin, to an oceanic basin, with one or more off-margin carbonate platforms. The northwestern area is restored as a small oceanic basin (Isparta Çay unit), between a continuation of the large Bey Daǧlari carbonate platform and a smaller carbonate platform to the east (Davras Daǧ). The northern area preserves remnants of several other carbonate platforms, with contrasting Mesozoic depositional histories, either shallow-water (Kaymaz Daǧ), or more deeply submerged (Barla Daǧ). The northeastern area, uniquely, preserves a lithological transition from a carbonate platform to the northeast (Anamas Daǧ), across its former passive margin to an oceanic basin located to the southwest. The eastern and southeastern areas preserve a westward transition from another large carbonate platform (Karacahisar), across an ocean strand, to a large off-margin carbonate platform (Sütçüler–Dulup unit). Finally, the previously much discussed southwestern area (Antalya–Kumluca) preserves a palaeogeographically complex passive margin, influenced by Neotethys strike-slip movement prior to tectonic emplacement.

Following stable shelf deposition along the northern margin of Gondwana in Late Permian time, rifting in the Early Triassic was followed by final continental break-up and sea-floor spreading in the Late Triassic (Carnian-Norian) to form a mosaic of continental slivers, volcanic seamounts and small carbonate platforms within the Neotethyan ocean. Oceanic crust was also generated in the Late Cretaceous, possibly in a supra-subduction zone setting. Regional compression began in the latest Cretaceous (Maastrichtian), and led to subduction-accretion, as evidenced by volcanic–sedimentary mélange. The deep-water passive margins of the carbonate platforms were also deformed and thrust-imbricated. Emplacement directions were generally outwards, away from the Isparta angle in all areas. Suturing was completed during Late Palaeocene–Early Eocene, with collision and imbrication of the carbonate platforms. In the Late Eocene, the northeast area was rethrust towards the southwest, related to suturing of a separate Neotethyan strand further northeast. The suture zone in the Isparta angle area then subsided to form an Oligo-Miocene clastic basin (Aksu basin). During the Early Miocene (Burdigalian) the apex of the Isparta angle subsided as a foredeep ahead of thrust sheets advancing from a separate Neotethyan ocean basin system to the northwest (Lycian nappes). During Late Miocene (pre-Messinian), the eastern limb of the Isparta angle experienced westward and southward thrusting and reverse faulting. Crustal extension and strike-slip faulting exploited the Isparta angle suture zone in the Plio-Quaternary, with development of the north-south Kovada graben and its offshore continuation into Antalya Bay.