Mediterranean extension and the Africa‐Eurasia collision

Jolivet, Laurent; Faccenna, Claudio

doi:10.1029/2000tc900018

Cited by 936 publications

(730 citation statements)

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“…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.…”

Section: Eurasia-arabia Collisionmentioning

confidence: 99%

“…Behind this compressional front, back-arc extension propagated southward during the OligoceneMiocene [Le Pichon and Angelier, 1979;Jolivet and Faccenna, 2000] leading to intense crustal thinning observed now in the Aegean-west Anatolian region [Tirel et al, 2004;Karabulut et al, 2013]. Thus, while the exhumation of the central Rhodope core complex ceased in the Oligocene [Marchev et al, 2004a;Wüthrich, 2009], the southern Rhodope massif continued to be exhumed as MCC below the top-to-the SW Kerdylion detachment (figures 9 and 11) [Brun and Sokoutis, 2007].…”

Section: Back-arc Extension In the Cyclades And Western Anatoliamentioning

confidence: 99%

“…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].…”

Section: The Anatolide-tauride Blockmentioning

confidence: 99%

“…Tethyan active margin and do not specifically focus on the smaller-scale eastern Mediterranean region, where subduction, collision, obduction, slab roll-back and tearing processes have occurred since the Mesozoic [Le Pichon and Angelier, 1979;Şengör and Yilmaz, 1981;Jolivet and Faccenna, 2000;Jolivet et al, 2003;Faccenna et al, 2006Faccenna et al, , 2013Brun and Faccenna, 2008;Ring et al, 2010;Brun and Sokoutis, 2010;Jolivet and Brun, 2010]. Detailed kinematic reconstructions…”

Section: Introductionmentioning

confidence: 99%

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

2016

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Section: Eurasia-arabia Collisionmentioning

confidence: 99%

Section: Back-arc Extension In the Cyclades And Western Anatoliamentioning

confidence: 99%

Section: The Anatolide-tauride Blockmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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

2016

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“…Separation from Africa resulted in the formation of ocean spreading in the Red Sea and Gulf of Aden [Chu and Gordon, 1998;Cochran, 1981] and in 200-500 km of compression along a continental collision zone in eastern Turkey, the Zagros, and the Caucasus Mountains [e.g., Jolivet and Faccenna, 2000;McQuarrie et al, 2003]. This continental collision is a major driver of the active tectonics of the eastern Mediterranean region [e.g., Sengor et al, 1985Sengor et al, , 2003Allen et al, 2004] and the devastating earthquakes that have affected this area throughout recorded history [e.g., Ambraseys and Jackson, 1998].…”

Section: Introductionmentioning

confidence: 99%

Geodetic constraints on present‐day motion of the Arabian Plate: Implications for Red Sea and Gulf of Aden rifting

ArRajehi

McClusky²,

Reilinger³

et al. 2010

Tectonics

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Five years of continuously recording GPS observations in the Kingdom of Saudi Arabia together with new continuous and survey‐mode GPS observations broadly distributed across the Arabian Peninsula provide the basis for substantially improved estimates of present‐day motion and internal deformation of the Arabian plate. We derive the following relative, geodetic Euler vectors (latitude (°N), longitude (°E), rate (°/Myr, counterclockwise)) for Arabia‐Nubia (31.7 ± 0.2, 24.6 ± 0.3, 0.37 ± 0.01), Arabia‐Somalia (22.0 ± 0.5, 26.2 ± 0.5, 0.40 ± 0.01), Arabia‐India (18.0 ± 3.8, 87.6 ± 3.3, 0.07 ± 0.01), Arabia‐Sinai (35.7 ± 0.8, 17.1 ± 5.0, 0.15 ± 0.04), and Arabia‐Eurasia (27.5 ± 0.1, 17.6 ± 0.3, 0.404 ± 0.004). We use these Euler vectors to estimate present‐day stability of the Arabian plate, the rate and direction of extension across the Red Sea and Gulf of Aden, and slip rates along the southern Dead Sea fault south of the Lebanon restraining bend (4.5–4.7 ± 0.2 mm/yr, left lateral; 0.8–1.1 ± 0.3 mm/yr extension) and the Owens fracture zone (3.2–2.5 ± 0.5 mm/yr, right lateral, increasing from north to south; 1–2 mm/yr extension). On a broad scale, the Arabian plate has no resolvable internal deformation (weighted root mean square of residual motions for Arabia equals 0.6 mm/yr), although there is marginally significant evidence for N‐S shortening in the Palmyride Mountains, Syria at ≤ 1.5 mm/yr. We show that present‐day Arabia plate motion with respect to Eurasia is consistent within uncertainties (i.e., ±10%) with plate tectonic estimates since the early Miocene when Arabia separated from Nubia. We estimate the time of Red Sea and Gulf of Aden rifting from present‐day Arabia motion, plate tectonic evidence for a 70% increase in Arabia‐Nubia relative motion at 13 Ma, and the width of the Red Sea and Gulf of Aden and find that rifting initiated roughly simultaneously (±2.2 Myr) along the strike of the Red Sea from the Gulf of Suez to the Afar Triple Junction, as well as along the West Gulf of Aden at 24 ± 2.2 Ma. Based on the present kinematics, we hypothesize that the negative buoyancy of the subducted ocean lithosphere beneath the Makran and the Zagros fold‐thrust belt is the principle driver of Arabia‐Eurasia convergence and that resisting forces associated with Arabia‐Eurasia continental collision have had little impact on plate motion.

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Mantle dynamics in the Mediterranean

et al. 2014

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The Mediterranean offers a unique opportunity to study the driving forces of tectonic deformation within a complex mobile belt. Lithospheric dynamics are affected by slab rollback and collision of two large, slowly moving plates, forcing fragments of continental and oceanic lithosphere to interact. This paper reviews the rich and growing set of constraints from geological reconstructions, geodetic data, and crustal and upper mantle heterogeneity imaged by structural seismology. We proceed to discuss a conceptual and quantitative framework for the causes of surface deformation. Exploring existing and newly developed tectonic and numerical geodynamic models, we illustrate the role of mantle convection on surface geology. A coherent picture emerges which can be outlined by two, almost symmetric, upper mantle convection cells. The downwellings are found in the center of the Mediterranean and are associated with the descent of the Tyrrhenian and the Hellenic slabs. During plate convergence, these slabs migrated backward with respect to the Eurasian upper plate, inducing a return flow of the asthenosphere from the back-arc regions toward the subduction zones. This flow can be found at large distance from the subduction zones and is at present expressed in two upwellings beneath Anatolia and eastern Iberia. This convection system provides an explanation for the general pattern of seismic anisotropy in the Mediterranean, first-order Anatolia, and Adria microplate kinematics and may contribute to the high elevation of scarcely deformed areas such as Anatolia and eastern Iberia. More generally, the Mediterranean is an illustration of how upper mantle, small-scale convection leads to intraplate deformation and complex plate boundary reconfiguration at the westernmost terminus of the Tethyan collision.

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Mediterranean extension and the Africa‐Eurasia collision

Cited by 936 publications

References 88 publications

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

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

Geodetic constraints on present‐day motion of the Arabian Plate: Implications for Red Sea and Gulf of Aden rifting

Mantle dynamics in the Mediterranean

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