Reassessment of earthquakes, 1900-1999, in the Eastern Mediterranean and the Middle East

Ambraseys, N. N.

doi:10.1046/j.0956-540x.2001.01396.x

Cited by 136 publications

(37 citation statements)

References 30 publications

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“…Table A1 summarizes published references to historical earthquakes that may be associated with surface rupture along the NAF [Ambraseys, 2002[Ambraseys, , 1970Ambraseys and Finkel, 1987, 1995Ambraseys and Jackson, 1998;Ambraseys, 2001;Guidoboni et al, 1994;Guidoboni and Comastri, 2005;Nur and Cline, 2000;Nur and Burgess, 2008;Stein et al, 1997;Tibi et al, 2001]. Many of the reported earthquakes come from near Erzincan in the east and Istanbul in the west, while the records from the central portion of the NAF are sparser.…”

Section: Historical Earthquake Recordmentioning

confidence: 99%

Recent behavior of the North Anatolian Fault: Insights from an integrated paleoseismological data set

2010

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The North Anatolian Fault (NAF) is a right‐lateral plate boundary fault that arcs across northern Turkey for ∼1500 km. Almost the entire fault progressively ruptured in the 20th century, its cascading style indicating that stress from one fault rupture triggers fault rupture of adjacent segments. Using published paleoseismic investigations, this study integrates all of the existing information about the timing of paleoearthquakes on the NAF. Paleoseismic investigation data are compiled into a database, and for each site a Bayesian, ordering‐constrained age model is constructed in a consistent framework. Spatial variability of recurrence intervals suggests a spatial pattern in the behavior of earthquakes on the NAF that may correspond to the tectonic provinces within the Anatolian plate. In the west, the shear stress associated with the escaping Anatolian plate interplays with the tensile stress associated with the Aegean extensional province. Along this western transtensional section we recognize short recurrence intervals and switching between the furcated fault strands. The central section of the NAF is translational with little influence of fault‐normal stresses from other tectonic sources. This section tends to rupture in unison or close succession. The eastern section of the NAF is transpressional due to the compressional fault‐normal stress associated with the indenting Arabian plate. Along this section the recurrence intervals are bimodal, which we attribute to variable normal stress, although there are other possible causes.

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Section: Historical Earthquake Recordmentioning

confidence: 99%

Recent behavior of the North Anatolian Fault: Insights from an integrated paleoseismological data set

2010

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“…This earthquake resulted in over 600 deaths, largely in the city of Erciş (Figure 2, population 97,000) on the northern shore of Lake Van, on the hanging wall of the fault [Erdik et al, 2012;Daniell et al, 2011]. The largest aftershock (M w 5.9, USGS NEIC) occurred just over 10 h later; although a M w 5.7 aftershock on 9 November killed a further 40 people, largely due to additional damage in the city of Van. [3] The largest instrumentally recorded earthquake to have struck the region before was the 1976 M w 7.1 strikeslip earthquake on the right-lateral Chaldiran Fault, 60 km north-east of Van (Figure 2), although a M 7 earthquake also struck north of Erciş in April 1903 [Ambraseys, 2001]. Two significant pre-instrumental earthquakes are known to have affected the immediate region of Van in the last few centuries, estimated to be in the upper magnitude 6 range [Ambraseys, 1989].…”

Section: Introductionmentioning

confidence: 99%

The 2011 Mw 7.1 Van (Eastern Turkey) earthquake

Elliott

Copley

Holley³

et al. 2013

JGR Solid Earth

100

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[1] We use interferometric synthetic aperture radar (InSAR), body wave seismology, satellite imagery, and field observations to constrain the fault parameters of the M w 7.1 2011 Van (Eastern Turkey) reverse-slip earthquake, in the Turkish-Iranian plateau. Distributed slip models from elastic dislocation modeling of the InSAR surface displacements from ENVISAT and COSMO-SkyMed interferograms indicate up to 9 m of reverse and oblique slip on a pair of en echelon NW 40°-54°dipping fault planes which have surface extensions projecting to just 10 km north of the city of Van. The slip remained buried and is relatively deep, with a centroid depth of 14 km, and the rupture reaching only within 8-9 km of the surface, consistent with the lack of significant ground rupture. The up-dip extension of this modeled WSW striking fault plane coincides with field observations of weak ground deformation seen on the western of the two fault segments and has a dip consistent with that seen at the surface in fault gouge exposed in Quaternary sediments. No significant coseismic slip is found in the upper 8 km of the crust above the main slip patches, except for a small region on the eastern segment potentially resulting from the M w 5.9 aftershock on the same day. We perform extensive resolution tests on the data to confirm the robustness of the observed slip deficit in the shallow crust. We resolve a steep gradient in displacement at the point where the planes of the two fault segments ends are inferred to abut at depth, possibly exerting some structural control on rupture extent.

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“…They are the margin-boundary faults of grabens of dissimilar size and trends such as the Akdağ fault, Gönen fault, Burdur fault, Dinar fault, Dombayova fault, Sultandağları, and Çay segments of the Akşehir fault zone, and the Esinyurt fault (Figure 1(b) and 4). The most largest and destructive one of the instrumental periods earthquakes is the 3 January 1914 Kılıç (Burdur) earthquake of Ms = 7.1 (Ambraseys, 2001). It struck the city of Burdur resulting in severe to widespread damages and much loss of life over 4000 in a circular area of 60 km in diameter around its field epicenter (Kılıç Town) (Figure 1(b)).…”

Section: Seismicity Of Northern Section Of Iamentioning

confidence: 99%

“…This region has been undergoing continental extension above the Aegean-Cyprian Subduction Zone since at least Late Pliocene (Aldanmaz, 2006;Bozkurt, 2000Bozkurt, , 2001Bozkurt, , 2002Koçyiğit & Özacar, 2003;Koçyiğit et al, 1999Koçyiğit et al, , 2005Yılmaz et al, 2000). This is indicated by highly widespread shallow-focus earthquakes occurring in the continental crust and their focal mechanism solutions (Ambraseys, 2001;Ambraseys & Tchalenko, 1972;Eyidoğan & Jackson, 1985;Kalafat, 1998;Koçyiğit & Özacar, 2003;McKenzie, 1972;Westaway, 1990;Yılmaztürk & Burton, 1999;Zanchi & Angelier, 1993). However, in most of previous papers (Alçiçek, ten Veen, & Özkul, 2006;Barka et al, 1995;Boray, Saroğlu, & Emre, 1985;Kelling, Robertson, & Buchem, 2005;Seyitoğlu & Scott, 1994;Yılmaz et al, 2000), it has been reported that the southwest Anatolian extensional province is bounded by the western flank of the Isparta Angle (IA) to the east, i.e.…”

Section: Introductionmentioning

confidence: 99%

Nature and onset age of neotectonic regime in the northern core of Isparta Angle, SW Turkey

2012

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The Isparta Angle (IA) is a reverse Λ-shaped morphotectonic structure located to the north of Antalya Gulf in the Eastern Mediterranean Sea. It resulted from the northward curvature of the originally E-W-trending Tauride orogenic belt owing to the nappe emplacements and related clockwise and anti-clockwise rotations in a time period of Early Paleocene to Early Pliocene. The IA is included in the southwest Anatolian tensional neotectonic domain and characterized by a series of grabens and horsts bounded by active normal faults of dissimilar length and trend. The evolutionary history of the graben-horst system is episodic. It is evidenced by two graben fills. These are older and modern (younger) graben fills separated by an intervening angular unconformity. The modern graben fill is nearly flat-lying (non-deformed) whereas older graben fill was deformed into a series of anticlines and synclines with ENE-trending curvi-linear axes by a short-term compressive tectonic regime operated in NNW-SSE direction during Late Pliocene. The diagnostic structures taking a part in the development of grabens and shaping the northern section of the IA are the margin-boundary normal faults. They occur in numerous single and several fault zones displaying a basin ward facing step-like land shape. Most of fault segments, particularly the master faults, are active and have a capacity of creating destructive earthquakes with a magnitude (up to Mw = 7.0). This is evidenced by both the historical and instrumental period earthquakes. Both the focal mechanism solution of earthquakes and the stereographic plots of slip-plane data, measured on the active margin-boundary faults of various grabens comprising the IA, on the Schmidt lower hemisphere net obviously reveal that the IA is under the influence of the tensional neotectonic regime, not a compressive tectonic regime, i.e. the sinistral strike-slip shearing along the Pliny arc has not propagated yet onshore, and its commencement age is Early Quaternary.

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Reassessment of earthquakes, 1900-1999, in the Eastern Mediterranean and the Middle East

Cited by 136 publications

References 30 publications

Recent behavior of the North Anatolian Fault: Insights from an integrated paleoseismological data set

Recent behavior of the North Anatolian Fault: Insights from an integrated paleoseismological data set

The 2011 Mw 7.1 Van (Eastern Turkey) earthquake

Nature and onset age of neotectonic regime in the northern core of Isparta Angle, SW Turkey

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