Middle-Upper Miocene paleogeography of southern Turkey: insights from stratigraphy and calcareous nannofossil biochronology of the Olukpınar and Başyayla sections (Mut-Ermenek Basin)

Abstract

"The age of the marine succession capping the basement rocks of the central Taurides in the Mut-Ermenek Basin is constrained. using calcareous nannofossil biochronology. The Olukpınar section, which correlates with the biozones between MNN5a and MNN6b. (late Langhian-late Serravallian), represents a deeper marine environment developed lateral to the Ermenek platform. The long-term. transgressive–regressive cycle of the Olukpınar section, which corresponds to the middle-upper part of the TB2 supercycle, can be. subdivided into 2 large-scale (106 years) cycles (TB2.4 and TB2.5) based on the occurrence of 2 major debris flow deposits linked. to sea-level drop. The younger late Tortonian Başyayla section represents a transgressive–regressive sedimentary cycle (TB3.2 cycle). responsible for the major transgressive event that occurred at the southern margin of the Central Anatolian Plateau during the Late. Miocene. This major transgressive event is responsible for the migration of the coastal onlap of the Mediterranean Sea towards the. interior of the Anatolian Peninsula, almost 100 km inland from the present Eastern Mediterranean coast line. The ~8 Ma age of the. younger marine sediments deposited during the TB3.2 cycle, which onlap the basement rocks of the central Taurides at an elevation of. ~2 km, represents a maximum age for the start of surface uplift of the Central Anatolian Plateau’s southern margin.

Dynamic diversification history with rate upshifts in Holarctic bell‐flowers (Campanula and allies)

“…14 Ma led to global decline of evergreen tropical broadleaved forest vegetation and an increase in deciduous and open vegetation types, especially grassland, also in the SE European–SW Asian region (Potts and Behrensmeyer, ; Eronen et al., ; Potter and Szatmari, ). Finally, in the Late Miocene (11.62–5.33 Ma) as a result of plate collision, orogenic activity in the Eastern Mediterranean–SW Asian region and beyond took place (Meulenkamp and Sissingh, ), illustrated by the uplift of the Zagros Mountain belt in Iran (Mouthereau, ), the uplift of the Central Anatolian Plateau (Schildgen et al., ; Cipollari et al., ; Fernández‐Blanco et al., ), the uplift of the Caucasus (Mitchell and Westaway, ), and episodes of uplift also occurred in the European Alpide belt ca. 9–8 Ma (Meulenkamp and Sissingh, ).…”

Neogene Uplift and Magmatism of Anatolia: Insights From Drainage Analysis and Basaltic Geochemistry

“…It is necessary to prescribe a topographic starting condition for this inverse model. Miocene marine sedimentary rocks are distributed across portions of Anatolia, which implies that modest topographic relief existed at this time (Figure b and Table ; Bartol & Govers, ; Cipollari et al, ; Cosentino et al, ; Hüsing et al, ; Poisson et al, ; Schildgen et al, , 2014). This implication is consistent with stable isotopic compositions of sediment samples from continental basins across Central Anatolia, which indicate a lack of significant orographic barriers until middle Miocene times (Lüdecke et al, ; Schemmel et al, ).…”

“…Along the southern edge of the Central Anatolian Plateau, there are important independent constraints for the history of uplift (Figures d and h). For example, a suite of uplifted marine sedimentary rocks became emergent at about 8 Ma and record ∼2 km of regional uplift at rates of up to 0.7 mm yr −1 for the last 1.5 Ma (Table ; Cipollari et al, ; Cosentino et al, ; Schildgen et al, ). In our inverse model, uplift begins slightly earlier at 10 Ma and we do not resolve such rapid uplift rates toward the present day.…”

Sea level and climate forcing of the Sr isotope composition of lateMioceneMediterranean marine basins

“…From the Olukpınar section (Figure ), we analyzed 1 aliquot each (∼50–100 planktonic foraminifera tests) from five sampled horizons. Nannofossil assemblages constrain the age of the full section to between 15.6 and ∼12.5 Ma [MNN5a to MNN6b, Cipollari et al ., ], while three additional nannofossil bioevents allow us to constrain the ages of our Sr isotope samples to between 14.4 and 12.5 Ma (Figure ). We found no evidence for important gaps in sedimentation, so we assumed a constant sediment accumulation rate between bioevents to assign individual ages to the samples.…”