Major neotectonic features of eastern Marmara region, Turkey: development of the Adapazarı–Karasu corridor and its tectonic significance

Abstract

Eastern Marmara region consists of three different morphotectonic units: Thrace–Kocaeli Peneplain (TKP) and Çamdağ–Akçakoca Highland (ÇAH) in the north, and Armutlu–Almacık Highland in the south of the North Anatolian Fault Zone (NAFZ). The geologic‐morphologic data and seismic profiles from the Sakarya River offshore indicate that the boundary between the TKP in the west and ÇAH in the east is a previously unrecognized major NNE–SSW‐trending strike‐slip fault zone with reverse component. The fault zone is a distinct morphotectonic corridor herein named the Adapazarı–Karasu corridor (AKC) that runs along the Sakarya River Valley and extends to its submarine canyon along the southern margin of the Black Sea in the north. It formed as a transfer fault zone between the TKP and ÇAH during the Late Miocene; the former has been experiencing extensional forces and the latter compressional forces since then. East–West‐trending segments of the NAFZ cuts the NE–SW‐trending AKC and their activity has resulted in the formation of a distinct fault‐bounded morphology, which is characterized by alternating E–W highlands and lowlands in the AKC. Furthermore, this activity has resulted in the downward motion of an ancient delta and submarine canyon of the Sakarya River in the northern block of the NAFZ below sea level so that the waters of the Black Sea invaded them. The NE–SW‐trending faults in the AKC were reactivated with the development of the NAFZ in the Late Pliocene, which then caused block motions and microseismic activities throughout the AKC. Copyright © 2004 John Wiley & Sons, Ltd.

WITHDRAWN: Geoelectric Structure of Yalova-termal Town Bymagnetotelluric Data, Northwestern Turkey

“…1b). East-west trending oblique faults, which express strike-slip with accompanying normal-slip, cuts the cover units around Termal (Yiğitbaş et al, 2005).…”

On the effectiveness of directional derivative based filters on gravity anomalies for source edge approximation: synthetic simulations and a case study from the Aegean graben system (western Anatolia, Turkey)

“…The less evident ones are NE-SW trending basins (Gördes basin (GB) and Selendi basin (SB) in figure 7) and their interposing horsts (Bozkurt 2001). The cause of the extension has been curiously debated for a long time and four views have been proposed so far: (i) a tectonic escape model: westward extrusion of the Anatolian Block since 12 Ma (late Serravalian) (Dewey and Ş engör Kissel and Laj 1988, Meulenkamp et al 1988, Thomson et al 1998, (iii) an orogenic collapse model: local extension by spreading and thinning of over thickened crust following the latest Paleocene collision across Neotethys during the latest Oligocene-Early Miocene (Dewey 1988, Seyitoglu andScott 1991, McClusky et al 2000), (iv) a two-stage graben model: Miocene-Early Pliocene (orogenic collapse) and Plio-Quaternary (westward migration of the Anatolian Block) of the N-S extension (Koçyigit et al 1999, Bozkurt 2003, 2004).…”

“…Simplified tectonic map and relief of the region and the study area (compiled withYigitbas et al (2004) and CGIAR-CSI GeoPortal (2012)). Abbreviations: SBT, Southern Black Sea Thrust; NAFZ, North Anatolian Fault Zone; NEAFZ, Northeast Anatolian Fault Zone; WAEP, West Anatolia Extensional Province; EAFZ, East Anatolain Fault Zone; DSFZ, Dead Sea Fault Zone; BH, Bozdag Horst; AH, Aydın Horst; GDG, Gediz Graben; KMG, Küçük Menderes Graben; BMG, Büyük Menderes Graben; GB, Gördes Basin; SB, Selendi Basin.Through the GDG, the footwall of the detachment faults consists of different lithologies belonging to metamorphic rocks of the Menderes Massif, described as Pre-Neogene basement in the text (figure 7).…”

Evaluation and comparison of landslide susceptibility mapping methods: a case study for the Ulus district, Bartın, northern Turkey

“…The study area lies between the North Anatolian Fault System and the southern portion of the Black Sea Thrust tectonic features, and within northern Turkey which is accepted as tectonically 'stable' for a period of several decades (Kuşçu et al 2004, Yiğitbaş et al 2004. The instrumental earthquake records of the Kandilli Observatory and Earthquake Research Institute (KOERI 2011) indicate that there have been only two destructive earthquake occurrences (M ≥ 6) reported so far near the study area, namely the 1944 Bolu-Gerede earthquake (M = 7.2) and the 1968 Bartın earthquake (M = 6.8).…”