Arabia–Eurasia collision and the forcing of mid-Cenozoic global cooling

Abstract

Publisher's copyright statement: NOTICE: this is the author's version of a work that was accepted for publication in Palaeogeography, palaeoclimatology, palaeoecology. Changes resulting from the publishing process, such as peer review, editing, corrections, structural formatting, and other quality control mechanisms may not be reected in this document. Changes may have been made to this work since it was submitted for publication. A denitive version was subsequently published in Palaeogeography, palaeoclimatology, palaeoecology, 265/1-2, 2008Palaeogeography, palaeoclimatology, palaeoecology, 265/1-2, , 10.1016Palaeogeography, palaeoclimatology, palaeoecology, 265/1-2, /j.palaeo.2008 Additional information: Use policyThe full-text may be used and/or reproduced, and given to third parties in any format or medium, without prior permission or charge, for personal research or study, educational, or not-for-prot purposes provided that:• a full bibliographic reference is made to the original source • a link is made to the metadata record in DRO • the full-text is not changed in any way The full-text must not be sold in any format or medium without the formal permission of the copyright holders.Please consult the full DRO policy for further details. This is a PDF file of an unedited manuscript that has been accepted for publication. As a service to our customers we are providing this early version of the manuscript. The manuscript will undergo copyediting, typesetting, and review of the resulting proof before it is published in its final form. Please note that during the production process errors may be discovered which could affect the content, and all legal disclaimers that apply to the journal pertain. The end of the Eocene greenhouse world was the most dramatic phase in the 9 long-term cooling trend of the Cenozoic Era. Here we show that the Arabia-Eurasia 10 collision and the closure of the Tethys ocean gateway began in the Late Eocene at ~35 11 Ma, up to 25 million years earlier than in many reconstructions. We suggest that 12 global cooling was forced by processes associated with the initial collision that 13 reduced atmospheric CO 2 . These are: 1) waning volcanism across southwest Asia; 2) 14 increased organic carbon storage in Paratethyan basins (e.g. Black Sea and South 15 Caspian); 3) increased silicate weathering in the collision zone and, 4) a shift towards 16 modern patterns of ocean currents, associated with increased vigour in circulation and 17 organic productivity. 18 A C C E P T E D M A N U S C R I P T ACCEPTED MANUSCRIPT

Post-collisional polycyclic plutonism from the Zagros hinterland: the Shaivar Dagh plutonic complex, Alborz belt, Iran

“…Ph.D. thesis, Tarbiat Modares Univ., 2009, among others). An Early Mesozoic age of collision between the Arabian and Eurasian continental blocks is supported by new data (Ghasemi & Talbot, 2006;Allen & Armstrong, 2008;Horton et al 2008). Ghasemi & Talbot (2006) suggested an Early to Middle Eocene collision age for the Zagros suture.…”

“…However, many authors have related the Early Cenozoic intense magmatism along the UDMA, AMB and Central Iran with the time of collision at this or later periods during Middle Late Cenozoic time (e.g. Hempton, 1987;Hooper et al 1994;Dewey &Şengör, 1979;Sengör & Kidd, 1979;Homke et al 2004;McQuarrie et al 2003;Stoneley, 1981;Philip et al 1989;Allen & Armstrong, 2008;M. Aghazadeh, unpub.…”

Kinematic reconstructions and magmatic evolution illuminating crustal and mantle dynamics of the eastern Mediterranean region since the late Cretaceous

“…Compressional front in the northern Tauride margin then migrated southward up to the Bey Dağları platform and its foreland basin, overthrusted by the non-metamorphosed Lycian nappes in the Miocene [de Graciansky, 1967;Poisson, 1977;Gutnic et al, 1979;Collins and Robertson, 1998;van Hinsbergen et al, 2010a]. Further east, the late Cretaceous-early Cenozoic subduction of the Mesogean oceanic lithosphere below the southern Tauride margin was followed by the Oligocene-early Miocene continental subduction/collision of the Arabian plate allowing for the building of the Bitlis belt (figure 5) Hempton, 1987;Jolivet and Faccenna, 2000;Agard et al, 2005;Allen and Armstrong, 2008;Barrier and Vrielynck, 2008;Okay et al, 2010b;McQuarrie and van Hinsbergen, 2013].…”

“…Although its timing is debated, the continental subduction and subsequent collision of Arabia with the Eurasian margin seem to have occurred in the Oligocene-early Miocene, resulting in the building of the Bitlis-Zagros belt [Hempton, 1987;Jolivet and Faccenna, 2000;Agard et al, 2005;Allen and Armstrong, 2008;Okay et al, 2010b;McQuarrie and van Hinsbergen, 2013]. Such lithospheric-scale processes could also have induced major tectonic changes within the AnatolideTauride block.…”

Seismotectonics and rupture process of theMW 7.1 2011 Van reverse-faulting earthquake, eastern Turkey, and implications for hazard in regions of distributed shortening

“…Copley & Jackson 2006). Early estimates suggest that the initial collision was at ∼10 Ma (Dewey et al 1986), though palaeoclimate studies suggest it may have begun as early as ∼35 Ma (Allen & Armstrong 2008). Much of the current rate of ArabiaEurasia convergence (23 mm yr −1 ) is accommodated by shortening in the Caucasus, but around ∼10 mm yr −1 is distributed across the Turkish-Iranian Plateau (TIP; Reilinger et al 2006).…”