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. Candan, , 2011.

, Il est associé à (i) un épaississement crustal induit par l'imbrication de la plate-forme Anatolide-Tauride et par un transport vers le sud des Nappes Lyciennes et de la couverture du Menderes (i.e. Kurudere) ; (ii) la présence en quantité importante du socle du Menderes augmentant ainsi la production de chaleur générée par la radioactivité, Selon différentes études géochronologiques (e.g. sur micas, 1986.

;. Hetzel-&amp;-reischman and . Schmidt, ] (i.e. âge moyen de 60 Ma pour la plus jeune unité de la couverture affectée par le métamorphisme barrovien), le métamorphisme barrovien commence à l'Eocène et se termine à l'Oligocène dans sa partie sud (42 -35 Ma, En accord avec de nombreuses études, 1996.

, Ces anomalies régionales, liées à l'épaississement crustal et par conséquent à une augmentation de la production de chaleur radioactive, Le métamorphisme barrovien du Menderes est donc corrélé à des anomalies thermiques importantes, principalement visibles à l'échelle crustale

. Paradoxalement, aucune activité magmatique n'a été recensée dans le massif à cette période et par conséquent aucune minéralisation en lien avec ce magmatisme n'a été enregistrée (e.g. absence de systèmes porphyriques

, Synthèse -Discussion -Perspectives & Abridged english version une extension NNE-SSW, Ces observations sont donc cohérentes depuis l'Oligo

;. Miocène and . Jolivet, au fragile) a été enregistré sur l'ensemble du domaine (Figs. VII.1 et VII.2), Jolivet & Brun, 2010.

G. , ]) associée à cette dynamique n'a été enregistrée depuis la fin du Miocène dans la plaque supérieure. Par ailleurs, un évènement E-W compressif, daté à 9 -8.6 Ma, VII.1), 2013.

, Samos (cf. chapitre IV, 1999.

, Alors que ces auteurs les associent à des structures compressives, les données de terrain acquises lors de différentes missions suggèrent plutôt des géométries similaires à celle des slumps (structures d'effondrement résultant d'un glissement gravitaire). Ainsi, les instabilités gravitaires à l'origine de ces slumps pourraient être associés à une dynamique extensive où l'activité des failles délimiterait les bassins. Cette hypothèse pourrait donc remettre en cause l'âge de l'évènement compressif. Par ailleurs, les structures compressives (i.e. failles inverses) décrites sur cette île ne sont pas fréquentes en Mer Egée. Néanmoins, on retrouve sur l'île de Mykonos une transition dans le temps d'une extension NE-SW à une compression WNW-ESE, en passant par un stade décrochant, Il se traduit par (i) un jeu de failles inverses qui affectent principalement les bordures des bassins Miocène mais également par (ii) des plis orientés NW-SE développés dans certaines unités sédimentaires Néogène

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. Seyitoglu, Bien que l'âge de ces structures soit peu contraint, cette phase enregistrée sur les îles de Samos et de Mykonos et potentiellement dans le Menderes doit être expliquée. L'une des possibilités consisterait à utiliser le mouvement de la faille nord-anatolienne (NAF) et de ses satellites au Miocène supérieur, 1999.

. Armijo, , 2003.

, Si l'âge de la compression est compris entre 9 et 8,6 Ma, la NAF se propagerait plus tôt que prévu (âge Synthèse -Discussion -Perspectives & Abridged english version tectoniques régionales vont également influencer la circulation des fluides et par conséquent la localisation des réservoirs

, VII.2.1. Caractéristiques des systèmes géothermaux amagmatiques actifs de HT

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, Cycladic archipelago The geology of the Cycladic archipelago is divided into three units

. Altherr, This unit is correlated with the Pindos Unit in continental Greece (Bonneau, 1982, 1984) and consists of alternating marbles, metapelites, metabasites and meta-ophiolite. CBU rocks have undergone a dominant HP-LT metamorphism in the Eocene (K-Ar, 40 Ar-39 Ar and Rb-Sr on phen, Cycladic Blueschist Unit (CBU), and the Cycladic Basement Unit, 1979.

?. Trotet, which took place contemporaneously with back-arc extension. The overprint is generally characterized by greenschist-facies parageneses and locally by amphibolitefacies ones, reaching partial melting conditions in Naxos, Ikaria and Mykonos, Previous studies, 1979.

. Jolivet, 2010) have shown that Miocene low-angle normal faults have accommodated the late-stage exhumation of the metamorphic core complexes during extension. As a result, several detachments were formed and are now exposed in the northern and western Cyclades, they are the NCDS (North Cycladic Detachment System) and WCDS (West Cycladic Detachment System, 1994.

. Iglseder, According to Ring et al. (2011), the morphology of Sifnos is partly controlled by NE-and SW-dipping normal faults, and E-or W-dipping younger faults. This island is characterized by an apparently inverse metamorphic gradient within the CBU (Schliestedt and Matthews, Sifnos Island geology Sifnos lies in the back-arc region of the Hellenic subduction and is situated in the south-western part of the Aegean Sea between the Serifos metamorphic core complex, 1987.

. Wijbrans, Unit (CU) lays on top and it is further divided into three lithologic subunits, which are from top to bottom, 1) the Upper Marble Complex, exposed in the north-western part of the island (mainly calcitic and dolomitic marbles with lenses of quartzites and well preserved blueschists and eclogites), 2) the Eclogite and Blueschist Unit (interbedded quartzites, metabasites, metasediments and acidic gneisses), 3) the Main Marble Unit (a succession of thick marble levels alternating with metasediments and metabasites metamorphosed in the blueschist-to greenschistfacies, The contact between the two units is named COF (Cheronissos Over Faros) in the following. Cheronissos, 1987.

W. ;. Schmädicke and . Ring, Faros unit (FU) crops out underneath Cheronissos Unit mainly in the southeastern part of the island (Fig. 2). It is composed of metabasites and metasediments strongly retrograded in the greenschist-facies, 2003.

. Trotet, Two main stages have been inferred in the metamorphic evolution of Sifnos during the Eocene and Miocene. The first was characterized by HP-LT metamorphism under blueschist-to eclogite-facies conditions possibly due to the subduction of Apulia and the Pindos oceanic basin below Eurasia (Avigad, 1993) in the Eocene with peak conditions around 21kbar and 550 ? C (Fig. 3a, Locally, lenses of albite-and epidote-bearing blueschists (AEBSfacies of Evans, 1990) are preserved at the base of Cheronissos Unit and the top of Faros Unit, 2001.

A. , have related this tectono-metamorphic event (their D1 and D2 stages) to a top-to-the-SE shearing event. This episode has been dated around 45 Ma with different methods such as K-Ar and Rb-Sr on white micas (see compilation on Fig. 3a and b, 1979.

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