The Beyşehir-Hoyran-Hadim Nappes crop out over 700km, from east to west in the Pisidian and Central Taurus Mountains of southern Turkey. During this study, field obsevations of lithological, structural and sedimentological features are combined with igneous geochemical data derived from samples collected to help redefine a series of tectono-stratigraphic units and also determine the origin of the Beyşehir-Hoyran-Hadim Nappes. Above a regionally autochthonous Tauride carbonate platform, the Beyşehir-Hoyran Nappes begin with Ophiolitic Melange, consisting of blocks of neritic and pelagic limestone, basalt, serpentinite, radiolarian chert and, in places, amphibolite-grade metamorphic sole-type rocks, together set in a highly sheared siltstone and mudstone matrix. Locally, large slices of serpentinized harzburgite are incorporated in the melange. The peridotite sheets include lenses of chromitite and dunite and are cut by a series of dolerite dykes. The higher thrust sheets in the Hadim area begin with the Korualan Unit; a thrust sheet (ca. 400m thick) of mainly redeposited carbonates, quartzose sandstones and mudstones of Mid-Late Triassic age, interpreted as a proximal slope/base-of-slope succession. Regionally above is the Huğlu-type Unit; a thrust sheet (ca. 1 km thick) of Mid-Late Triassic intermediate-acidic extrusives, volcaniclastics and minor pelagic carbonates, interpreted as a continental rift. Post-rift subsidence in this thrust sheet is recorded by thin (<100m thick) Upper Triassic-Upper Cretaceous pelagic carbonate and radiolarian chert, depositionally above. The uppermost thrust sheet, the Boyali Tepe-type Unit, comprises broken formation and melange, including Jurassic shallow-water carbonate, Ammonitico Rosso condensed pelagic limestone, radiolarian chert and Upper Cretaceous pelagic limestone, representing a Bahaman-type carbonate platform which subsided in Early Jurassic time. Anastomosing zones of tectonic-sedimentary melange separate these higher units. The Beyşehir-Hoyran Nappes document Triassic rifting and Jurassic-Cretaceous passive margin subsidence bordering the Northern Neotethyan Ocean. The Late Cretaceous harzburgitic ophiolite probably formed above a northerly dipping subduction zone within the Neotethyan ocean basin. Ophiolitic melange formed along the leading edge of the overiding plate. The ophiolite was emplaced southwards onto the northern margin of the Tauride platform in latest Cretaceous time, probably during collision of the passive margin with a trench. The nappe pile and underlying platform (Hadim Nappe) were thrust ca. 150km further south in Late Eocene time during regional continental collision and suture zone tightening. Several alternative palaeo-tectonic models are considered and tested in the light of data presented from this study. Assuming ‘in-sequence’ thrusting, the Beyşehir-Hoyran Nappes restore to a location north of a northerly Neotethyan spreading axis. More probably, they originated near the south margin of the northern Neotethys, but reached their position by ‘out-of-sequence thrusting’. Formation within a localised southerly strand of the northern Neotethys (Inner Tauride ocean) is more probable than within the main Neotethys further north. Wider implications for the Tethyan ocean as a whole and several other orogenic belts are also considered.

Dans de nombreuses chaînes de montagnes, on observe des témoins du processus d’obduction, correspondant au transport de la lithosphère océanique sur la croûte continentale. Le paradoxe intrinsèque de ce phénomène est celui-ci : des roches denses (ρ>3) se retrouvent au-dessus de roches moins denses (ρ≈2,7). Les processus à l’origine de cette bizarrerie tectonique sont encore mal compris. Les ophiolites du Petit Caucase et du NE de l’Anatolie correspondent à un exemple extrême de ce phénomène puisqu’on constate un transport de fragments de lithosphère océanique sur plusieurs centaines de kilomètres, à l’échelle de l’ensemble d’une bordure continentale (>1000 km) vers 90 Ma. En adoptant une stratégie pluridisciplinaire lors de l’étude de ces ophiolites, nous avons pu préciser l’évolution des premiers stades de la fermeture néotéthysienne et en conséquence l’obduction de ces dernières. Ces données suggèrent fortement une mise en place commune de l’ensemble de ces corps ophiolitiques de la région d’étude sous la forme d’une nappe, dont l’épaisseur actuelle est très réduite (quelques kilomètres tout au plus). Ceci en fait l’une des plus grandes nappes ophiolitiques obduites du globe. La modélisation numérique a validé l’hypothèse que la mise en place de cette nappe s’est faite grâce à des conditions thermiques particulières. Elle suggère que l’obduction d’ophiolites vieilles nécessite un état thermique de la lithosphère océanique proche de celui d’une lithosphère jeune (0-40 Ma). / Within many mountain ranges slivers of preserved oceanic lithosphere evidence tectonic processes responsible for their emplacement on top of the continental crust. The first order anomaly inherent to this phenomenon is that dense rocks (ρ>3) end up on top of less dense rocks (ρ≈2.7). The processes responsible for such a tectonic oddity remain uncertain. The ophiolites of the Lesser Caucasus and NE Anatolia are prime examples of this phenomenon, tectonic transport of fragments of oceanic lithosphere is evidenced on the entire continental marge (>1000 km) around 90 Ma. The multidisciplinary approach used throughout the study of the ophiolites of the Lesser Caucasus and NE Anatolian regions yielded clues specify the evolution of the Tethys and consequently the obduction of the ophiolites. This dataset strongly suggests common emplacement of the ophiolites of the study area, resembling a thrust sheet. This would be one of the biggest ophiolite nappe complexes in the world. Numerical modeling validates the hypothesis that emplacement of the ophiolitic nappe is due to particular thermal conditions. It suggests that in order to obduct old oceanic lithosphere obduction it needs to have a thermal state close to that of young oceanic lithosphere (0-40 km). Such a thermal rejuvenation is supposed for the ophiolites of the Caucasus s.l. evidenced by alkaline lavas emplaced on the ophiolite prior to the obduction event during the Late Cretaceous. Resulting seamounts and/or oceanic plateaus upon entery of the subduction zone under Eurasia would block it.

No description available.

The Eastern Mediterranean marks the site of the Southern Neotethys Ocean that was created, then largely destroyed near the northern margin of Gondwana. Sedimentary and structural evidence is well preserved in the Girne (Kyrenia) Range, a several hundred kilometrelong, narrow, E – W-trending, broadly arcuate lineament that encompasses northern Cyprus and a submarine ridge that links southeastern Turkey (Misis–Andırın Complex). This study focuses on the Oligocene-Miocene sequence exposed on both flanks of the Girne (Kyrenia) Range, based on sedimentology, microfacies, Sr-isotope dating and structural analysis. Two related sedimentary basins are today separated by an E – W-trending high-angle, fault zone, the Değirmenlik (Kythrea) Fault. The northern basin encompasses the Range, whereas the southern basin is located between the Değirmenlik (Kythrea) Fault and an E – W trending fault lineament (Dar dere (Ovgos) Fault Zone), to the south of which is the Troodos Ophiolitic Massif. The Değirmenlik (Kythrea) Fault is interpreted as a convergence-related thrust fault that was active during the Mid-Late Miocene creating an E – W submarine ridge that separated subbasins to the north and south. The sedimentary sequence in the northern basin unconformably overlies Mesozoic platform carbonates and latest Cretaceous-Palaeogene pelagic carbonates with interbedded volcanics. Above basal conglomerates (probably derived from underlying Eocene debris flows based on chemical evidence), there is a fining-upward siliciclastic turbidite sequence (Late Oligocene), then biogenic calciturbidites and marls (Aquitanian-Langhian). The northerly basin is characterised by thin-, to medium-bedded, pale hemipelagic calciturbidites and marls (Serravallian; ~400 m thick), overlain by thick-bedded, medium- to coarse-grained lithic sandstones with carbonate concretions (Tortonian; ~250 m thick). The succession in the southern basin, which is more deformed by thrusting, begins with poorly dated pelagic marls (Early Miocene?), followed by regularly bedded siliciclastic turbidites (~1000 m thick), with abundant sole structures (Serravallian-Tortonian). Palaeocurrent evidence shows mainly E to W flow for the southern basin, and locally a generally E to W flow for the northerly basin, at least for the Late Miocene. Gypsum accumulated in local depocentres during the Messinian salinity crisis and was locally deformed by contemporaneous southward thrusting. Petrographic studies of the Serravallian – Tortonian sandstones indicate that the northern basin is richer in recrystallised limestone grains compared to the southern basin, which contains more abundant siliciclastic and ophiolite-derived material; this trend is also present in results from XRD analysis of clays. The likely source area was the Eurasian-African suture zone in the Tauride Mountains to the northeast. The greater detrital limestone abundance in the south may record relatively deep-level erosion of the source area, through ophiolites to an underlying Mesozoic carbonate platform. Two phases of clastic input are recognised from SE Turkey, the first related to Early Miocene continental collision, and the second reflecting Late Miocene suture tightening, both to the east of Cyprus within the Tauride Suture Zone. Based on the measurement and kinematic analysis of a large number (>1290) of faults, combined with a knowledge of the tectono-stratigraphy, the timing and nature of faulting is inferred. The majority of the faults are south-verging, high-angle reverse faults, while sinistral strike-slip faults dominate several areas of the Girne (Kyrenia) Range and the Dar dere (Ovgos) Fault Zone of the south. Most of the faults in the Girne (Kyrenia) Range are attributed to Mid – Late Eocene and Late Miocene – Early Pliocene phase of thrusting, followed by relative quiescence until Pleistocene uplift of the Girne (Kyrenia) Range. The Dar dere (Ovgos) Fault Zone is interpreted as a long-lived terrane boundary that accommodated sinistral movement during Late Miocene to Recent. In summary, the Girne (Kyrenia) Range reflects the diachronous closure of the Mesozoic Southern Neotethys Ocean, culminating in westward tectonic escape from continent-continent collision zone to the east, coupled with thick-skinned uplift that was triggered by collision with a crustal block to the south, the Eratosthenes Seamount.

L’Anatolie fait partie d’un vaste domaine orogénique qui s’étend des Alpes à l’Himalaya. Les sutures ophiolitiques rencontrées marquent les cicatrices de plusieurs domaines océaniques (branches de la Néotéthys Nord), interdigités entre plusieurs blocs crustaux au cours du Mésozoïque. La fermeture de ces domaines au Crétacé supérieur est accompagnée de la mise en place de bassins tertiaires syn-orogéniques dont fait partie le Bassin de Sivas, limité au nord par le bloc du Kırşehir et au Sud par les Taurides. Une étude structurale de terrain, complétée d’analyses géochimiques, biostratigraphiques et thermochronologiques ainsi que l’étude de 700 km de lignes sismiques 2D inédites, a été menée pour tenter de comprendre (i) le contexte géodynamique régional et (ii) l’architecture tectono-sédimentaire de ce bassin.L’étude des ophiolites présentes le long de la bordure sud du Bassin de Sivas met en évidence des péridotites intensément serpentinisées. La partie supérieure de l’ophiolite présente des brèches et ophicalcites caractéristiques de l’exhumation mantellique, alors que l’analyse géochimique des corps magmatiques révèle un environnement de supra-subduction, daté à circa 90 Ma (U-Pb sur zircon). Ces analyses démontrent la présence d’un domaine océanique embryonnaire entre le Kırşehir et les Taurides, dont la fermeture s’initie le long d’ancienne failles de détachement. L’obduction de la nappe de péridotite et de son mélange frontal sur la marge Nord des Taurides entre le Turonien et le Maastrichtien, permet de former le « socle ophiolitique » commun aux bassins est-anatoliens. L’analyse détaillée de la partie centrale du bassin, en carte et à l’aide de lignes sismiques 2D inédites et de thermochronologie basse température [AFTA et (U-Th)/sur apatite], a permis de proposer un modèle d’évolution cinématique sur la base de coupes équilibrées. La propagation de la déformation vers le Nord, initiée dès l’Eocène inférieur, permet l’isolation progressive du bassin et une forte accumulation d’évaporites à l’Eocène supérieur. Les dépôts de l’Oligo-miocène sont ensuite contrôlés par l’halocinèse, permettant la mise en place de deux générations de mini-bassins salifère, séparés d’une canopée. Les géométries dans le domaine halocinétique, et les variations latérales dans le bassin, montrent le contrôle exercé par (i) le bassin pré-évaporite affleurant le long de la moitié sud du bassin et (ii) l’épaisseur du niveau de sel initial.L’intégration de ces observations à l’échelle régionale met en évidence un contrôle du raccourcissement crustal, dans les Taurides et les bassins tertiaires, lié à la fermeture de la Néotéthys Sud, en générant l’émergence de structures de socles. La collision enregistrée à l’Oligocène supérieur - Miocène lors de l’indentation de la plaque Arabe le long des Taurides est contemporaine de la déformation du Bassin de Sivas et des bassins adjacents. / Anatolia is part of a vast orogenic domain that extends from the Alps to the Himalayas. Numerous ophiolitic sutures defined the remnants of several oceanic domains (Northern and southern Neotethys), between continental fragments formed during Mesozoic time. Oceanic closure during Late Cretaceous is recorded by the establishment of syn-orogenic tertiary basins, including the Sivas Basin bounded to the north by the Kırşehir block and to the south by the Taurides. An extended study based on field and completed by geochemistry, biostratigraphy and thermochronology analyzes and more than 700 km unpublished seismic data, was conducted to resolve (i) the regional geodynamic context and (ii) the tectono-sedimentary architecture of this basin.The ophiolites located along the southern edge of the Sivas Basin are made of serpentinized peridotites. The upper part of the ophiolite present breccias and ophicalcites commonly described as associated to mantle exhumation environment, while the geochemical analysis of the magmatic bodies reveals a supra-subduction environment dated at circa 90 Ma (U-Pb on zircon). These observations are in agreement with an embryonic ocean domain located between the Kırşehir and the Taurides, the closure which was initiated along fossil detachment faults. The obduction of the peridotite nappe and its frontal mélange on the northern margin of the Taurides between the Turonian and the Maastrichtian allows forming the “ophiolitic basement” of the east-anatolian basins.A detailed map and cross-section analysis, supported by 2D seismic lines and low-temperature thermochronology [AFTA and (U-Th) / on apatite], resulted in a kinematic evolution model and the realization of balanced cross-sections. The propagation of the deformation towards the north, initiated in the Lower Eocene, results in the progressive isolation of the basin and a strong accumulation of evaporites during the Upper Eocene. The Oligo-Miocene depocenters were controlled by halokinesis, forming two generations of mini-basins, separated by a salt canopy. The geometries in the halokinetic domain and the lateral variations in the basin show the control exerted by (i) the pre-evaporite basin outcropping along the southern half of the basin and (ii) the thickness of the initial salt level.Integration at the regional scale within the Taurides highlights the propagation of crustal shortening related to the Southern Neotethys closure, which formed linear tectonic basement exhumation. The collision recorded in the Upper Oligocene - Miocene during the indentation of the Arabic plate along the Taurides is contemporaneous to the deformation the Sivas Basin.