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Deep Structure & Slab Rollback in the Mediterranean

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Deep Structure & Slab Rollback in the Mediterranean Aegeis – deep structure & slab rollback in the Mediterranean A paper for the Naxos field trip with Prof. Dr. Janos Urai, Summer Term 2014 Caspar Sinn, Martin Schlemmer August 31st, 2014 RWTH Aachen University, Teaching and Research Area Geology – GED 1 Introduction Figure 1 several plates – the African, Eurasian, The Mediterranean realm has a relatively short Anatolian and Arabian plate – are involved in but, a fortiori, intensive history of geologic the process of continental convergence and research since the 70’s. Especially the Aegean influence the deformation of the Aegean Sea region features numerous studies relating its plate in rather complex ways. Consequently, development nowadays as well as discussions deformation in the Aegean region is known to and modelling of the deep structure be very active since the ongoing subduction of environment (JOLIVET et al. 2013). In general the African-Arabian plate underneath the the Mediterranean area comprises many Eurasian major and Anatolian respectively geologic large-scale phenomena based on Aegean micro plates (DOGLIONI 2002). The different characteristic processes like initial collision of the African and Eurasion “subduction, accretion, arc magmatism [& continental bodies is assumed to have started metamorphism], exhumation, […] faulting, […] in Oligocene times (JOLIVET & FACCENNA 2000). continental extension” (RING et al. 2010) and so In this meaning the Aegean Sea is on. considered to be one of the Mediterranean The continental collision of Africa and Cenozoic backarc basins – which started to Europe and its resulting subduction events form 30–35 Ma ago as per Jolivet et al. 2009 – define the area and indicate to “a complex controlled by the underlying and retreating evolution that started at the end of the African slab that is still sinking below Crete and Cretaceous with the closure of the Tethyan the Mediterranean Ridge (JOLIVET & BRUN ocean” (JOLIVET & BRUN 2010). As illustrated in 2010). This process is explained by a slow initial Figure 1. A: Plate boundaries and geodynamic pattern of the Aegean Sea plate. B: Tectonic sketch of the Aegean present day situation. Modified after VÖTT (2007) and RING et al. (2010). 2 Figure 2. Simplified sketch showing a retreating subduction zone and slab draping (A-C) along with back-arc extension (close-up). Modified after RING et al. (2010). convergence rate of Africa and Eurasia, while Not all of those consequences related to the the velocity of backarc extension was larger, so Mediterranean subduction zone are entirely that the subduction rate overcame conver- understood yet, but with the seminal gence rate (JOLIVET et al. 2009). The basic discoveries of the Aegean metamorphic core principles and effects of subduction plus slab complexes by LISTER (1984), for example, more rollback are shown in Figure 2. accurate geodynamic models – featuring Besides, there are commonly three subject areas like slab rollback or extensional models associated to a subducting slab as detachment faulting – became the focus of concluded by MAGNI et al. (2013). While slab attention (e.g. BUICK 1991, URAI et al. 1990 detachment refers to a complete decoupling etc.). It has thus been possible to overcome or so called break-off of the lithosphere, a initial models which, for example, “used separation between the upper section of the several subduction zones that jumped continental crust and lithospheric mantle is southward through time, instead of a single occurring during slab delamination (Figure 3). migrating subduction used in most models nowadays” (JOLIVET et al. 2013). Figure 4 represents a present day situated N-S cross-section through the Aegean realm from the northern passive margin of Figure 3. Schematic distinction between continental Africa to the Moesian platform across the main subduction mechanisms: Slab delamination versus Slab structural features Crete, the Cyclades and the break-off (MAGNI et al. 2013). Rhodope massif. 3 Figure 4. Schematic N-S cross-section of the present day situation through the Aegean realm from the northern passive margin of Africa to the Moesian platform across the main structural features Crete, the Cyclades and the Rhodope massif. CD: Cretan detachment, NCDS: North Cycladic Detachment System. Modified after JOLIVET et al. (2013). including several microplates and fragments of This paper focusses mainly on the research of both oceanic and continental lithosphere. The the Aegean deep structure and slab retreat trench is to be found to the south of Crete with including tomographic images, while Volcanic activity north towards the Aegean numerous studies also assess analyses of high- Sea, including the islands of Santorin, Nisiros, pressure metamorphism units or meta- etc. The slab was first assumed to dip morphic core complexes (MCC) to derive northward at an angle of about 35° after information about geodynamic evolution. CAPUTO (1970) but is suggested to have been steeper in the past. The slab is known to be continuous and as evidence of tomographic Deep structure images over 1500 km long. It penetrates the In the Hellenic subduction system the Hellenic 660 km discontinuity and continues in the slab subducts under the Eurasian plate, Figure 5. Topographic images across the Aegean realm. The dashed lines in the tomographic section indicate the 410 and 660 km discontinuities (WORTEL & SPAKMAN 2000). 4 lower mantle (JOLIVET et al. 2013) as seen in extension forming the Aegean Sea at 23- Figure 2. 19 Ma. It is therefore suggested that the Tomographic images (Figure 5) show a draping of 300 km of slab on the 660 km 300 km part of the slab draped just above the discontinuity triggered a period of enhanced 660 km discontinuity, this portion of the slab rollback resulting in ca. 300 km of rapid corresponds to the ~320 km long estimate for extension throughout the Aegean (Ring et al. Cenozoic extension. Due to the phase change 2010). of spinel to perovskite and the buoyancy As a result of fast slab rollback, tearing associated with the discontinuity the and slab detachment may occur. While slab penetrating slab is slowed down (RING 2010). rollback is the most important process in the This leads to the rate of convergence of the Aegean, slab detachment would explain overriding plate being lower than the rate of observations of stress field variations, arc subduction which is a major parameter for the migration, and back-arc deformation (WORTEL occurrence of slab rollback and retreating & SPAKMAN 2000). A slab tear below turkey was subduction zones. suggested by DE BROODEr et al. (1998) and The rollback of the Hellenic slab is newer tomographic images by JOLIVET et al. further recorded by the southward migration (2013) show at least two tears below Turkey of the volcanic arc and a steady slowdown of and one under the Corinth Rift as indicated in convergence. The 300 km of draped slab can Figure 6. be correlated to the estimated 320 km of subducted slab during the Cenozoic. From a subduction angle of 30-40° and a subduction Geodynamic evolution rate of 30 km/Ma, the arrival of the Pindos The subduction of the Hellenic slab under the Ocean unit – which started subducting at 60- Eurasian plate forms a continuous subduction 55 Ma – at the 660 km discontinuity can be zone since around 200 Ma starting of as a estimated to have occurred at 25-20 Ma. This simple subduction during the Jurassic and coincides with the start of large-scale Cretaceous though advancing northward as a retreating Subduction zone due to slab rollback from 55 Ma onwards. This is recorded by the southward migration of the magmatic arc and the slowdown of the plate convergence related extension in the back-arc basin (RING et al. 2010). The Hellenides which form an arcurate orogen above the subducting Hellenic slab can be divided into several tectonic domains. These tectonic domains are visible in Figure 7, as there are, from north to south, the Rhodope-Sakarya Block, the Vardar-Izmir Oceanic Unit, the Pelagonian-Lycian Block, the Pindos Oceanic Unit (including the Cycladic Figure 6. Topographic images in a horizontal view of the Blueschist Unit), the Tripolitza as well as the Aegean realm (JOLIVET et al. 2013). Ionian Block, and the East Mediterranean 5 Figure 7. Geodynamic reconstruction of the retreating Hellenic subduction zone and its tectonic domains (RING et al 2010). Ocean (RING et al. 2010). Due to this the where the relative motion between Africa and subduction zone has consumed both, oceanic Europe comes to a complete stop around and continental lithosphere successively the (around 67-65 Ma ago according to JOLIVET Vardar Ocean, the Pelagonian continent, the (2010)), before the subduction of the Pidos Pindos Ocean, the Apulian platform and finally oceanic unit began at ca. 50 Ma (RING et al. the eastern Mediterranean ocean with the 2010). During this period the sinking slab is crustal parts being accreted and forming the only driven by its on weight, leading to Hellenic chain as well as the Mediterranean continued subduction without convergence. Ridge accretion complex (JOLIVET et al. 2013). (JOLIVET & BRUN 2010). From 200 Ma until 125-85 Mya ago The convergence then accelerates again the Rhodope-Sakarya block, the Vardar-Izmir forming a compressional regime and is quickly ∼ ∼ Oceanic Unit and the Pelagonian-Lycian Block subducting the Pindos Oceanic Unit. The were subducted in a simple fashion as subduction and accretion of the Pindos interpretation of tomographic data suggests. Oceanic Unit caused a distinct switch in the After this a distinct time gap of at least 20 Ma, dynamics of the subduction changing it from 6 Figure 8. Geodynamic evolution and tectonic reconstruction of the Aegean realm from 80 Ma to the present day situation (RING et al. 2010) advancing and stationary, to retreating at 20-30 Ma ago in the back-arc forming the some time near 55–50 Ma starting the first Aegean sea.
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