Successive structural events in the Hatay ophiolite of southeast Turkey: Distinguishing oceanic, emplacement and post-emplacement phases of faulting

Inwood, J.; Anderson, Mark; Morris, Antony; Robertson, Alastair H.F.

doi:10.1016/j.tecto.2008.10.037

Cited by 29 publications

(20 citation statements)

References 48 publications

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“…These ophiolites are inferred to have formed by spreading above a northward-dipping intra-oceanic subduction zone (Al-Riyami et al 2002b;Bagcı et al 2005Bagcı et al , 2008Rızaoglu et al 2006;Parlak et al 2009). These ophiolites were emplaced southwards onto the Arabian continental margin during CampanianMaastrichtian time (Inwood et al 2009). These ophiolites were then transgressed by non-marine to shallow-marine sediments, locally from Maastrichtian time onwards (Boulton et al 2006;Boulton & Robertson 2008).…”

Section: Discussionmentioning

confidence: 99%

“…In contrast, (1) the southern belt ophiolites are represented by basic to highly depleted boninite-type plutonics and extrusives (Al-Riyami et al 2002b;Bagcı et al 2008), suggesting a forearc setting; (2) the volcanics are locally interbedded with or overlain by metalliferous oxide sediments (Robertson 1986); (3) these ophiolites were emplaced southwards onto the Arabian continental margin during Campanian -Maastrichtian time (Inwood et al 2009); (4) granite intrusion is absent; (5) Eocene contractional tectonics does not affect the Arabian platform; and (6) the age of the Hatay and the Trodoos ophiolites is c. 92 Ma (Mukasa & Ludden 1987;Dilek & Thy 2009;Karaoglan et al in press). In addition, the the Bitlis and Pütürge metamorphic units of southern Turkey were affected by high pressure/low temperature and low pressure/low temperature metamorphism, both during the latest Cretaceous (Oberhansli et al 2010).…”

Section: Discussionmentioning

confidence: 99%

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Petrology of the İspendere (Malatya) ophiolite from the Southeast Anatolia: implications for the Late Mesozoic evolution of the southern Neotethyan Ocean

Parlak

Karaoğlan

Rızaoğlu

et al. 2012

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The İspendere ophiolite forms part of the Tauride active continental margin assemblage in SE Anatolia. The ophiolite exhibits an intact oceanic lithosphere section and is intruded by Late Cretaceous calc-alkaline granites. The ophiolite comprises mantle tectonites, ultramafic to mafic cumulates, isotropic gabbros, isolated diabase dykes, a sheeted dyke complex, plagiogranite and volcanic rocks. The volcanics and the sheeted dyke complex exhibit (1) similar rare earth element patterns, with flat to light rare earth element depletion (La-Yb) N ¼ 0.71-1.14 and 0.65-1.22, (2) negative Nb anomalies and (3) flat-lying high field strength element trends. These features differ from a typical Normal-Mid Ocean Ridge Basalt fractionation trend and could have resulted from c. 15% partial melting of a previously depleted mantle source. The whole-rock chemistry and the mineral chemistry of the ultramafic to mafic cumulates [high Ca plagioclases (An 89 -81 ), magnesian olivines (Fo 88 -81 ) and clinopyroxenes (Mg# 90 -83 )] show that the primary magma of the plutonic suite is compositionally similar to modern island arc tholeiites. The available evidence suggests that the İspendere ophiolite formed at a northerly supra-subduction zone spreading centre of the Southern Neotethys, between the Taurides and the Bitlis-Pütürge metamorphic units, during the Late Cretaceous. Comparison with the adjacent Göksun, Kömürhan and Guleman ophiolites suggests that the İspendere ophiolite represents part of a single regional-scale sheet of oceanic lithosphere that was accreted to the base of Tauride active continental margin where it was cut by arc-type magmatic rocks.

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Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

Petrology of the İspendere (Malatya) ophiolite from the Southeast Anatolia: implications for the Late Mesozoic evolution of the southern Neotethyan Ocean

Parlak

Karaoğlan

Rızaoğlu

et al. 2012

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“…On the other hand, all levels of the ophiolite pseudostratigraphy are present in the well-documented Hatay ophiolite to the south (e.g. Aslaner, 1973;Bağcı, Parlak, & Höck, 2008;Dilek & Thy, 2009;Inwood, Morris, Anderson, & Robertson, 2009a, 2009bKaraoğlan, Parlak, Klötzli, Thöni, & Koller, 2013;Lytwyn & Casey, 1993).…”

Section: Heterogeneous Melange; Emplaced Accretionary Complexmentioning

confidence: 99%

“…Robertson and Dixon, l984;Lytwyn & Casey, 1993;Robertson, 2002;Parlak & Robertson, 2004;Chan, Malpas, Xenophontos, & LO, 2007;Parlak et al, 2009;Inwood et al, 2009b;Robertson et al, 2012;Karaoğlan et al, 2013). During CampanianMaastrichtian time the subduction zone collided with the Arabian passive continental margin around the periphery of the Arabian continental margin, from the Eastern Mediterranean region to Oman (Glennie et al, 1973; Glennie, Boeuf, Hugues-Clarke, Pilaar, & Reinhardt, Taking account of evidence from the Arabian foreland in SE Turkey, the deformation can be generally related to the initial collision of the Eurasian and Arabian plates (Boulton, 2009;Boulton & Robertson, 2007;Robertson, Boulton et al, 2016).…”

Section: Late Cretaceous Ophiolite Emplacementmentioning

confidence: 99%

Palaeozoic-Recent geological development and uplift of the Amanos Mountains (S Turkey) in the critically located northwesternmost corner of the Arabian continent

Duman¹,

Robertson

Elmacı

et al. 2017

Geodinamica Acta

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We have carried out a several-year-long study of the Amanos Mountains, on the basis of which we present new sedimentary and structural evidence, which we combine with existing data, to produce the first comprehensive synthesis in the regional geological setting. The ca. N-Strending Amanos Mountains are located at the northwesternmost edge of the Arabian plate, near the intersection of the African and Eurasian plates. Mixed siliciclastic-carbonate sediments accumulated on the north-Gondwana margin during the Palaeozoic. Triassic rift-related sedimentation was followed by platform carbonate deposition during Jurassic-Cretaceous. Late Cretaceous was characterised by platform collapse and southward emplacement of melanges and a supra-subduction zone ophiolite. Latest Cretaceous transgressive shallow-water carbonates gave way to deeper-water deposits during Palaeocene-Eocene. Eocene southward compression, reflecting initial collision, resulted in open folding, reverse faulting and duplexing. Fluvial, lagoonal and shallow-marine carbonates accumulated during Late Oligocene(?)-Early Miocene, associated with basaltic magmatism. Intensifying collision during Mid-Miocene initiated a foreland basin that then infilled with deep-water siliciclastic gravity flows. Late Miocene-Early Pliocene compression created mountain-sized folds and thrusts, verging E in the north but SE in the south. The resulting surface uplift triggered deposition of huge alluvial outwash fans in the west. Smaller alluvial fans formed along both mountain flanks during the Pleistocene after major surface uplift ended. Pliocene-Pleistocene alluvium was tilted towards the mountain front in the west. Strike-slip/transtension along the East Anatolian Transform Fault and localised sub-horizontal Quaternary basaltic volcanism in the region reflect regional transtension during Late Pliocene-Pleistocene (<4 Ma).

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“…At the visible base of the region, a well-studied ophiolitic complex (Figure 4), the Kızıldağ Ophiolite (Aslaner, 1973;Bağcı, Parlak, & Höck, 2005Dubertret, 1953;Inwood, Anderson, Morris, & Robertson, 2009 and references herein), consists of, from bottom to top, ultramafic tectonites, mafic and ultramafic cumulates, gabbros, sheeted dyke complexes, plagiogranites, pillow lava, and epi-ophiolitic sediment, such as cherts and pelagic limestones. U-Pb zircon ages for the plagiogranites in the Kızıldağ Ophiolite indicate its magmatic age as 90.3 ± 2.4 Ma (Parlak et al, 2009).…”

Section: The Basement Rocksmentioning

confidence: 99%

The geology and morphology of the Antakya Graben between the Amik Triple Junction and the Cyprus Arc

et al. 2013

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In southeastern Turkey, the NE-trending Antakya Graben forms an asymmetric depression filled by Pliocene marine siliciclastic sediment, Pleistocene to Recent fluvial terrace sediment, and alluvium. Along the Mediterranean coast of the graben, marine terrace deposits sit at different elevations ranging from 2 to 180 m above present sea level, with ages ranging from MIS 2 to 11. A multisegmented, dominantly sinistral fault lying along the graben may connect the Cyprus Arc in the west to the Amik Triple Junction on the Dead Sea Fault (DSF) in the east. Normal faults, which are younger than the sinistral ones, bound the graben's southeastern margin. The westward escape of the continental İskenderun Block, delimited by sinistral fault segments belonging to the DSF in the east and the Eastern Anatolian Fault in the north caused the development of a sinistral transtensional tectonic regime, which has opened the Antakya Graben since the Pliocene. In the later stages of this opening, normal faults developed along the southeastern margin that caused the graben to tilt to the southwest, leading to differential uplift of Mediterranean coastal terraces. Most of these normal faults remain active. In addition to these tectonic movements, Pleistocene sea level changes in the Mediterranean affected the geomorphological evolution of the area.

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Successive structural events in the Hatay ophiolite of southeast Turkey: Distinguishing oceanic, emplacement and post-emplacement phases of faulting

Cited by 29 publications

References 48 publications

Petrology of the İspendere (Malatya) ophiolite from the Southeast Anatolia: implications for the Late Mesozoic evolution of the southern Neotethyan Ocean

Petrology of the İspendere (Malatya) ophiolite from the Southeast Anatolia: implications for the Late Mesozoic evolution of the southern Neotethyan Ocean

Palaeozoic-Recent geological development and uplift of the Amanos Mountains (S Turkey) in the critically located northwesternmost corner of the Arabian continent

The geology and morphology of the Antakya Graben between the Amik Triple Junction and the Cyprus Arc

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