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The Erzincan (Turkey) earthquake (MS = 6.8) of March 13, 1992 and its aftershock sequence

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Grosser,  Helmut
2.1 Physics of Earthquakes and Volcanoes, 2.0 Physics of the Earth, Departments, GFZ Publication Database, Deutsches GeoForschungsZentrum;

Baumbach,  M.
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Berckhemer,  H.
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Baier,  B.
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Karahan,  A.
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Schelle,  Holger
2.6 Seismic Hazard and Stress Field, 2.0 Physics of the Earth, Departments, GFZ Publication Database, Deutsches GeoForschungsZentrum;

Krüger,  F.
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Paulat,  A.
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Michel,  G. W.
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Demirtas,  R.
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Genocoglu,  S.
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Yilmaz,  R.
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Grosser, H., Baumbach, M., Berckhemer, H., Baier, B., Karahan, A., Schelle, H., Krüger, F., Paulat, A., Michel, G. W., Demirtas, R., Genocoglu, S., Yilmaz, R. (1998): The Erzincan (Turkey) earthquake (MS = 6.8) of March 13, 1992 and its aftershock sequence. - Pure and Applied Geophysics, 152, 3, 465-505.
https://doi.org/10.1007/s000240050163


https://gfzpublic.gfz-potsdam.de/pubman/item/item_226188
Zusammenfassung
The Erzincan strike-slip earthquake of March 13, 1992 ruptured a section of the North Anatolian fault (NAF) at the northern margin of the Erzincan basin. The focal depth of about 10 km was less than given by ISC and NEIC. Erzincan and the surrounding villages were considerably damaged. In the Erzincan basin and in the neighbouring mountains a seismic network of ten stations was installed. It was operating continuously from March 21 through June 16, 1992. More than 3,000 aftershocks were recorded of which 505 could be located. The spectral parameters of 394 and the fault-plane solutions of 53 aftershocks were determined. For the given region the frequency dependent coda Q was derived as Qc = 122*f^0.68. The aftershock area increased with time, reflecting the process of stress redistribution. Some events clustered in the immediate vicinity of the town of Erzincan close to the epicentre of the main event and seem to trace the NAF. Their source mechanism is similar to that of the main event (strike slip). About 150 aftershocks clustered in the southeastern part of the Erzincan basin where a concentration of the events in a small volume of 5 x 5 x 3 km^3 was observed. The majority of fault-plane solutions available for these aftershocks showed a normal faulting mechanism with an east-west directed extension. Most of the aftershocks southeast of the basin clustered between two lineaments that were mapped by satellite images. The P-wave velocity below the Erzincan basin, derived from travel-time residual analysis, is lower compared to areas NE and SW of the basin. Three-dimensional stress modelling of the Erzincan region qualitatively explains the occurrence of the aftershocks southeast of the basin. The calculated displacement distribution which exhibits the north-westward motion of the basin and tension at its southeastern margin, caused by the Erzincan earthquake, is in agreement with derived fault-plane solutions.