The Menderes Massif forms the western of the two large metamorphic culminations within the Turkish Alpide orogen. It has three major lithologic units, with a gneissic “core” at the base and a “schist” and a “marble” envelope overlying it successively, although relations between them have been largely obscured by the polymetamorphic and structurally complex history of the Massif. We present a review of the available stratigraphic evidence and combine it with new isotopic ages from the central and southern parts of the Massif to constrain the timing of major tectonic events that shaped the Massif since the late Proterozoic (Pt3). In the southern part of the Massif (sensu stricto) three episodes of deformation and metamorphism are distinguished, whereas in its northern part there are four. The first episode occurred at −500 ± 10 Ma with intense deformation and metamorphism at high grade amphibolite facies with local anatexis. In the central part of the Massif, the 470 ± 9 Ma‐old now highly deformed tonalitic and granitic intrusions mark the end of this episode. On a Cambrian reconstruction of continents around the eastern Mediterranean, the Menderes Massif forms the southern end of the Pan‐African orogenic collage of northeastern Africa and Arabia. The area of earliest Palaeozoic deformation in the Menderes may connect with the northwest African orogenic collage along the strike via the Bozburun and Saricicek diabases, arkoses, and schists in the center of the Karacahisar dome interpreted herein as fragments of a Pan‐African suture. The earliest Palaeozoic deformations to affect the rocks were probably related to the last Pan‐African collisions and associated postcollisional convergence. The southern part of the Massif was undeformed from early Ordovician to the early (? later) Eocene, whereas the northern part was deformed, metamorphosed and intruded possibly during the late Triassic, related to the closure of the Karakaya marginal basin of Palaeo‐Tethys. The next major event affecting the whole of the Massif was the intense deformation and widespread metamorphism that reached high amphibolite grade in the structurally lower parts, and only greenschist grade in the outermost envelope. This metamorphism, here called the “main Menderes metamorphism” (MMM), is biostratigraphically constrained between early Eocene and early Oligocene time. Rb/Sr isotopic data show a spread of ages between 60 Ma and 25 Ma, with the greatest number of determinations around 35 ± 5 Ma. This number is in excellent agreement with the stratigraphic evidence and shows that MMM took place during latest Eocene time or at the transition from Eocene to Oligocene time. Along the northern border of the Massif, deformation and metamorphism had already taken place during the late Cretaceous in a high pressure/low temperature (HP/LT) metamorphic belt (northernmost part of Menderes Massif sensu lato), which was then covered by Palaeocene molasse. The evolution of the HP/LT belt was probably related to the obduction of the Bozkir ophiolites from the Izmi...

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The time of the onset and the nature of the extension in the Aegean area have been problematic owing to the confusion of neotectonic replacement structures with neotectonic revolutionary structures. This paper concerns two rift systems of different ages and orientations in the Gokova region of southwestern Anatolia. The first system has a northwest-southeast trend with a Middle to Upper Miocene infill, whereas the second system is orientated in an east-west direction and filled with Plio-Quaternary rocks. Structural and palaeomagnetic data indicate that the first system originally had a north-south trend, and then bodily rotated anticlockwise to its present orientation before the end of the Miocene. Both the orientations and the structural patterns of these cross-cutting rift systems suggest that they resulted from two different and successive tectonic regimes. Regional geology suggests that the generative regime of the older system was characterized by north-south compression and related to the palaeotectonic evolution of southwestern Anatolia, whereas that of the younger system is characterized by north-south extension and relates to the neotectonic evolution of this region. This inference contradicts, at least in southwestern Anatolia, some recent claims that the extensional tectonics and the related rift formation in the Aegean region began in the early Miocene, with the alleged demise of the compressional palaeotectonics during the late Oligocene, but is consistent with older views that placed the onset of north-south extension into the later middle Miocene. The formation of the Aegean Sea seems to be the result of these two complicated and contrasting, succesive tectonic regimes that have affected this region since middle Miocene times.

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