Diachronous uplift and cooling history of the Menderes core complex, western Anatolia (Turkey), based on new Zircon (U-Th)/He ages

Baran, Zeynep; Dilek, Yıldırım; Stöckli, Daniel F.

doi:10.1016/j.tecto.2016.12.005

Cited by 11 publications

(5 citation statements)

References 109 publications

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“…f) Early Miocene continental magmatism has continued without significant interruption to the present. g) Miocene metamorphic core complexes, such as the Menderes and Kazdağ massifs, form mountains and are associated with active extensional to transtensional faults (e.g., Baran et al, 2017;Cavazza et al, 2009;Okay et al, 2008).…”

Section: Discussionmentioning

confidence: 99%

Uplift of Anatolia

Okay¹,

Zattin²,

Özcan³

et al. 2020

Turkish J Earth Sci

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IntroductionPlateaus are major physiographic structures on the Earth that influence tectonics, sedimentation, hydrography, and climate. Their mode of formation and duration are significant geological problems. The Central Anatolian Plateau, with a surface area of 800 km by 400 km, an average height of ~1 km, and low relief (<300 m), is one of the world's major plateaus (Figure 1). In the north and south, it is bounded by the higher elevation Pontide and Tauride mountains, respectively (e.g., Cosentino et al., 2012). It lies between the higher elevation (~2 km) East Anatolian Highlands, which has been undergoing active shortening between the colliding Arabian and Eurasian plates, and the lower elevation extensional Aegean province (e.g., Reilinger et al., 2006). The recent fast uplift of the Taurides is now well constrained, and is linked to delamination and/or slab breakoff during the Late Miocene (e.g., Schildgen et al., 2014). Various post-Late Miocene (<8 Ma) subcrustal processes are invoked for the formation of the Central Anatolia Plateau (e.g., Bartol and Govers, 2014;Göğüş et al., 2017); however, there are few data on its timing. Here, the formation of the Anatolian Plateau was investigated using four data sets: a) the ages of the last marine strata, b) the ages of the continental Neogene sequences, c) the age of Cenozoic magmatism, and d) thermochronology. New thermochronological data from central Anatolia are also provided.There have been several recent studies on the Quaternary surface uplift in Anatolia, generally based on surface dating of marine or fluvial terraces (e.g., Yıldırım et al., 2013;Çiner et al., 2015;Berndt et al. 2018). The data from these studies covered the last few hundred thousand years and are local. They are difficult to extrapolate back to several tens of millions of years and to all of Anatolia; therefore, they are not used in this study. MethodsThis study involved the compilation and critical evaluation of a large number of published papers, as well as collection of new thermochronological data from central Anatolia.

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Section: Discussionmentioning

confidence: 99%

Uplift of Anatolia

Okay¹,

Zattin²,

Özcan³

et al. 2020

Turkish J Earth Sci

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“…In the Hellenides, these are of Mid-Late Jurassic age, while, in the Menderes province, they are of Late Cretaceous age [80,116,117]. Another difference is the larger amount of basement rocks in the Menderes massif than in the Cycladic massif (Figure 2; [45,90,103,105,106,109]).…”

Section: Gavrovo Zonementioning

confidence: 98%

“…The pre-Alpine basement of the Gavrovo carbonate platform (the Apulian Plate) is exhumed as metamorphic core complexes in the Cyclades province beneath the Gavrovo carbonate series, the Cyclades blue schists unit, and the overlain remnants of the Pelagonian nappe with obducted Neotethyan ophiolites (Figures 2 and 4; [9,89,93,[100][101][102][103][104]). It is possibly continued further to the east in western Turkey in the Menderes metamorphic core complex as its deeper structural level (Figure 2; [9,102]).…”

Section: Gavrovo Zonementioning

confidence: 99%

“…Oligocene-Miocene granitoid intrusions also occur in both the Menderes and Cyclades domains, but in different amounts. They are more common in the Cyclades massif (Figure 2; [9,10,15,45,89,95,103,[105][106][107][108][109][110][111][112][113]). Furthermore, kinematic indicators show real similarities in both areas of the Cyclades and the Menderes.…”

Section: Gavrovo Zonementioning

confidence: 99%

“…The Gavrovo zone is thrust over the Ionian zone towards the west during the Oligocene-Miocene time (Figures 1, 2 and 4). Nevertheless, some lithological and structural differences should also be referred to here between the two regions, leaving some question marks about the correlation of the two areas and raising the need for further detailed research for the correct answer (for example, the absence of the Pelagonian nappe in Menderes province, where the Lycian nappes may be equivalent structural sequence to the Pelagonian nappe, taking the same tectonic position [9,10,103]).…”

Section: Gavrovo Zonementioning

confidence: 99%

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The Alpine Geological History of the Hellenides from the Triassic to the Present—Compression vs. Extension, a Dynamic Pair for Orogen Structural Configuration: A Synthesis

Kilias

2023

Geosciences

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In this paper, the Hellenic orogenic belt’s main geological structure and architecture of deformation are presented in an attempt to achive a better interpretation of its geotectonic evolution during Alpine orogeny. This study was based not only on recent research that I and my collaborators conducted on the deformational history of the Hellenides but also on more modern views published by other colleagues concerning the Alpine geotectonic reconstruction of the Hellenides. The structural evolution started during the Permo–Triassic time with the continental breaking of the supercontinent Pangea and the birth of the Neotethyan ocean realm. Bimodal magmatism and A-type granitoid intrusions accompanied the initial stages of continental rifting, followed by Triassic–Jurassic multiphase shallow- and deep-water sediment deposition on both formed continental margins. These margins were the Apulian margin, containing Pelagonia in the western part of the Neotethyan Ocean, and the European margin, containing continental parts of the Serbo-Macedonian and Rhodope massifs in the eastern part of the Neotethyan ocean. Deformation and metamorphism are recorded in six main deformational stages from the Early–Middle Jurassic to the present day, beginning with Early–Middle Jurassic Neotethyan intra-oceanic subduction and ensimatic island arc magmatism, as well as the formation of a suprasubduction oceanic lithosphere. Compression, nappe stacking, calc-alkaline magmatism, and high-pressure metamorphic events related to subduction processes alternated successively over time with extension, orogenic collapse, medium- to high-temperature metamorphism, adakitic and calc-alkaline magmatism, and partial migmatization related to the uplift and exhumation of deep crustal levels as tectonic windows or metamorphic core complexes. A S- to SW-ward migration of dynamic peer compression vs. extension is recognized during the Tertiary Alpine orogenic stages in the Hellenides. It is suggested that all ophiolite belts in the Hellenides originated from a single source, and this was the Neotethyan Meliata/Maliac-Axios/Vardar ocean basin, parts of which obducted during the Mid–Late Jurassic on both continental margins, Apulian (containing Pelagonia) and European (containing units of the Serbo-Macedonian/Rhodope nappe stack), W-SW-ward and E-NE-ward, respectively. In this case, the ophiolite nappes should be considered far-traveled nappes on the continental parts of the Hellenides associated with the deposition of Middle–Late Jurassic ophiolitic mélanges in basins at the front of the adjacent ophiolite thrust sheets. The upper limit of the ophiolite emplacement are the Mid–Upper Jurassic time(Callovian–Oxfordian), as shown by the deposition of the Kimmeridgian–Tithonian Upper Jurassic sedimentary carbonate series on the top of the obducted ophiolite nappes. The lowermost Rhodope Pangaion unit is regarded as a continuation of the marginal part of the Apulian Plate (External Hellenides) which was underthrust during the Paleocene–Eocene time below the unified Sidironero–Kerdylia unit and the Pelagonian nappe, following the Paleocene–Eocene subduction and closure of a small ocean basin in the west of Pelagonia (the Pindos–Cyclades ocean basin). It preceded the Late Cretaceous subduction of the Axios/Vardar ocean remnants below the European continental margin and the final closure of the Axios/Vardar ocean during the Paleocene–Eocene time, which was associated with the overthrusting of the European origins Vertiskos–Kimi nappe on the Sidironero–Kerdylia nappe and, subsequently, the final collision of the European margin and the Pelagonian fragment. Subsequently, during a synorogenic Oligocene–Miocene extension associated with compression and new subduction processes at the more external orogenic parts, the Olympos–Ossa widow and the Cyclades, together with the lower-most Rhodope Pangaion unit, were exhumed as metamorphic core complexes.

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Age, origin and tectonic controls on rapid recent exhumation of the Sibela Mountains, Bacan, Indonesia

Hennig-Breitfeld,

Hall,

White

et al. 2024

Int J Earth Sci (Geol Rundsch)

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The Sibela Mountains of the island of Bacan in eastern Indonesia contain one of the Earth’s youngest metamorphic complexes that is now exposed at elevations up to 2000 m. New mica 40Ar/39Ar and apatite (U–Th–Sm)/He data from metamorphic and igneous rocks indicate that these rocks were rapidly exhumed in the Pleistocene (c. 0.7 Ma). Exhumation of the metamorphosed Permo-Triassic basement (c. 249–257 Ma) was accompanied by metamorphism (recorded by schists) as well as partial melting (recorded by c. 1.4 Ma granitic dykes). These processes must have occurred at extremely high cooling and exhumation rates. The rapid exhumation on land was associated with significant subsidence in adjacent basins offshore that reach depths up to 2.4 km. Neogene metamorphic core complexes and other metamorphic complexes are well-known from eastern Indonesia, but they usually record much higher exhumation rates than those reported from older classic metamorphic core complexes found in other parts of the world and require a different formation mechanism. Unlike classic metamorphic core complexes that are characterized by low-angle detachment faults, the Bacan metamorphic rocks were exhumed on steep bounding normal faults forming a rectilinear block pattern. We suggest such complexes are termed metamorphic block complexes (MBC). The Bacan MBC is exceptionally young and like the other east Indonesian complexes was rapidly exhumed during subduction rollback. A flexure formed during arc-arc collision as the Sangihe forearc loaded the Halmahera forearc which reactivated steeply-dipping faults in a rectilinear chocolate block pattern. Graphical abstract

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Diachronous uplift and cooling history of the Menderes core complex, western Anatolia (Turkey), based on new Zircon (U-Th)/He ages

Cited by 11 publications

References 109 publications

Uplift of Anatolia

Uplift of Anatolia

The Alpine Geological History of the Hellenides from the Triassic to the Present—Compression vs. Extension, a Dynamic Pair for Orogen Structural Configuration: A Synthesis

Age, origin and tectonic controls on rapid recent exhumation of the Sibela Mountains, Bacan, Indonesia

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