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The 1999 Ain Temouchent Earthquake ( 5.7, Algeria) Case Study Samir Belabbès, Mustapha Meghraoui, Ziyadin Çakir, Youcef Bouhadad

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The 1999 Ain Temouchent Earthquake ( 5.7, Algeria) Case Study Samir Belabbès, Mustapha Meghraoui, Ziyadin Çakir, Youcef Bouhadad InSAR analysis of a blind thrust rupture and related active folding: the 1999 Ain Temouchent earthquake ( 5.7, Algeria) case study Samir Belabbès, Mustapha Meghraoui, Ziyadin Çakir, Youcef Bouhadad To cite this version: Samir Belabbès, Mustapha Meghraoui, Ziyadin Çakir, Youcef Bouhadad. InSAR analysis of a blind thrust rupture and related active folding: the 1999 Ain Temouchent earthquake ( 5.7, Algeria) case study. Journal of Seismology, Springer Verlag, 2008, 13 (4), pp.421-432. 10.1007/s10950-008-9135-x. hal-00478440 HAL Id: hal-00478440 https://hal.archives-ouvertes.fr/hal-00478440 Submitted on 30 Apr 2010 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. J Seismol (2009) 13:421–432 DOI 10.1007/s10950-008-9135-x ORIGINAL ARTICLE InSAR analysis of a blind thrust rupture and related active folding: the 1999 Ain Temouchent earthquake (Mw 5.7, Algeria) case study Samir Belabbès · Mustapha Meghraoui · Ziyadin Çakir · Youcef Bouhadad Received: 5 March 2008 / Accepted: 28 August 2008 / Published online: 14 October 2008 © Springer Science + Business Media B.V. 2008 Abstract We study the surface deformation as- the coseismic surface displacement field despite sociated with the 22 December 1999 earthquake, poor coherence. The interferogram measures four a moderate sized but damaging event at Ain fringes and displays an ellipse-shaped lobe with Temouchent (northwestern Algeria) using Inter- ∼11 cm peak line-of-sight displacement. The elas- ferometric Satellite Aperture Radar images tic modeling using a boundary element method (InSAR). The mainshock focal mechanism so- (Poly3Dinv) indicate coseismic slip reaching up to lution indicates reverse faulting with a NE–SW 1mat5kmdepthontheN57◦ E trending, dipping trending rupture comparable to other major seis- 32◦ NW Tafna thrust fault. The geodetic estimate mic events of this section of the Africa–Eurasia of seismic moment is 4.7 × 1017 N m. (Mw 5.7) plate boundary. Previously, the earthquake fault in is good agreement with seismological results. parameters were, however, poorly known because The elliptical shape of the surface displacement no aftershocks were precisely determined and no field coincides with the NE–SW trending Berdani coseismic surface ruptures were observed in the fault-related fold. The consistency between the field. Using a pair of ERS data with small baseline geological observations and InSAR solution shed and short temporal separation in the ascending light on the precise earthquake location and orbit we obtained an interferogram that shows related Tafna fault parameters. Keywords InSAR · Algeria · Earthquake · S. Belabbès · M. Meghraoui Thrust fault · Active folding Institut de Physique du Globe de Strasbourg, UMR 7516, Strasbourg 67084, France Z. Çakir Department of Geology, Istanbul Technical 1 Introduction University, Istanbul, Turkey On 22 December 1999, the city of Ain Y. Bouhadad Centre du Génie Parasismique (CGS), Temouchent and surrounding area located on Algiers, Algeria the northwestern Tell Atlas mountains were af- B fected by a moderate-sized earthquake (Mw 5.7, M. Meghraoui ( ) EMSC). The mainshock epicenter was located EOST-IPG Strasbourg, 5 rue René Descartes 67084, ◦ ◦ Strasbourg Cedex, France at 1.3 W 35.25 N by the Algerian Geophysical ◦ ◦ e-mail: [email protected] Centre (CRAAG) and 1.22 W 35.17 Nbythe 422 J Seismol (2009) 13:421–432 SED-ETH Zurich (Figs. 1 and 2). Focal mecha- no surface ruptures were observed. The precise nism solutions indicate a NE–SW striking reverse fault location and related rupture parameters of fault planes, and the seismic moment reaches the 22 December 1999 Ain Temouchent earth- 4.37 × 1017 Nm (EMSC, Table 1). Using the quake remained unknown. waveform modeling, Yelles et al. (2004) obtain The SAR interferometry is able to assess the Mo = 4.1 × 1017 Nm and estimate a simple coseismic surface deformation which provides ac- rupture process with 5.0 s source duration. The cess to the rupture parameters (Burgmann et al. isoseismal map displays contours elongated in the 2000;Wrightetal.2004; Fielding et al. 2004; NE–SW direction and a maximum intensity of VII Cakir et al. 2006; Motagh et al. 2006; Belabbes with a radius of 30 km within the epicentral area 2008). Although it is relatively easy to determine (Yelles et al. 2004). Large historical earthquakes the surface deformation of large earthquakes affected this region of the Tell Atlas (e.g., in (Mw ≥ 6) with InSAR, even with long tempo- 1790 with Io X MKS in Oran; in 1819 with ral separation between SAR images, it is of- Io X MKS in Mascara; (Rothé 1950)) and ten difficult to reveal the surface deformation of imply a high seismic potential of this section small- and moderate-sized earthquakes (Mw < 6; of the Africa–Eurasia plate boundary (Fig. 1). Lohman and Simons 2005). However, under fa- However, no accurate aftershocks location that vorable conditions (e.g., short temporal and spa- could contribute to a clear identification of the tial baselines), InSAR may provide significant seismogenic fault geometry was determined, and results for small- and moderate-sized shallow -3˚ -2˚ -1˚ 0˚ 1˚ 2˚ 36.5 36.5 ˚ Eurasia ˚ 40˚ Mediterranean Sea 10 35˚ Africa cm 1 cm/yr. Chlef (El Asnam) 36˚ -10˚ -5˚ 0˚ 5˚ 10˚ 15˚ 1790 36˚ Chellif Basin Oran Track144 Kalaa Murdjajo (c) 35.5 ERS2-991125/000413 L‘Habra Basin 35.5˚ ˚ 24046/26050 (m) Mleta Basin Ain Temouchent Mascara 0 500 1000 Ghriss Basin Mw > 7 Folds Tessala mountains Beni Chougrane mountains 6 < Mw < 7 Thrust faults 35 35û ˚ 5 < Mw < 6 Faults Tafna Basin (b) 1887 Fig.5a 4 < Mw < 5 1851 Mw < 4 Tell Atlas 1819 (a) Large historical earthquakes 34.5˚ -3˚ -2˚ -1˚ 0˚ Fig. 1 Seismotectonics of the Ain Temouchent earthquake respectively (from Global CMT). Active folds and faults area with shaded relief image from SRTM data. The 1999 are from Meghraoui (1988). Dashed box shows the ERS Ain Temouchent mainshock location (red star)isfrom SAR data frame (track 144) and black arrows indicate CRAAG and the seismicity from Benouar (1994) 1900– the satellite flight direction (ascending) and the line of 1993 catalogue and ISC 1993–2006 catalogue. Circles are sight direction (towards east). Inset box shows the con- for instrumental events and squares for main historical vergence between African and Eurasian plates in western events. Beach balls a, b,andc are the focal mechanism solu- Mediterranean with white arrows indicating the motion of tions of the 1999 Ain Temouchent (Mw 5.7), 1994 Mascara, Africa relative to Eurasia (Serpelloni et al. 2007) (Mw 5.7) and the 1980 El Asnam (Mw 7.3) earthquakes, J Seismol (2009) 13:421–432 423 Fig. 2 Morphotectonic -1.5˚ -1.4˚ -1.3˚ -1.2˚ -1.1˚ map of the earthquake area. Stars show the 35.4˚ km 35.4˚ earthquake epicenter Mediterranean 0 5 10 sea given by different seismological centers. HarvardGlobal CMT The arrowed line shows -1.5û -1.4û USGS the fold orientation. EMSC Ain Temouchent Black line with thrust 35.3˚ 35.3˚ symbols shows the modeled fault (see also CRAAG Ain Tolba Figs. 8 and 9). Dashed line indicates the active fault Ain Alem extension. T is the Ain Kihal cross-section of Fig. 9b 35.2˚ 35.2˚ SED Tafna River 35.1˚ 35.1˚ T Remchi 35˚ 35˚ Tafna Basin -1.5˚ -1.4˚ -1.3˚ -1.2˚ -1.1˚ earthquakes even in regions with variable topog- For the Mw 6.8, 2003 Zemmouri (Northern raphy and dense vegetation (Salvi et al. 2000; Algeria) earthquake, the InSAR results suggest a Mellors et al. 2004; Akoglu et al. 2006). NE–SW trending and 50-km-long thrust rupture SAR interferometry applied to the 1994–2004 with two offshore fault segments and ∼0.15 m in- (Mw 6.0; 6.4) Al Hoceima earthquake sequence duced right-lateral slip on an E–W fault (Belabbes in North Africa (Cakir et al. 2006; Akoglu et al. 2008). 2006) revealed blind NE–SW and NW–SE conju- In this paper, we use ERS Synthetic Aperature gate strike–slip faults affecting the Rif Mountains. Radar (SAR) data to compute coseismic inter- Table 1 Rupture parameters of the 22/12/1999 Ain Temouchent earthquake Source Long (◦)Lat(◦) Depth (km) Plane1 Plane2 Mo (Nm) Strike Dip Rake Strike Dip Rake HRV −1.45 35.34 15 29◦ 45◦ 67◦ 240◦ 49◦ 111◦ 2.95 × 1017 SED −1.22 35.17 12 221◦ 57◦ 80◦ 59◦ 34◦ 106◦ 4.26 × 1017 USGS −1.28 35.32 – – – – – – – EMSC −1.28 35.32 8 59◦ 21◦ 118◦ 209◦ 71◦ 80◦ 4.7 × 1017 Yelles et al. −1.3a 35.25a 460◦ 36◦ 63◦ 272◦ 54◦ 108◦ 4.1 × 1017 This study −1.3a 35.25a 557◦ 32◦ 90◦ 237◦ 58◦ 90◦ 4.7 × 1017 HRV Harvard, SED Swiss Seismological Network, USGS US Geological Survey, EMSC Euro-Mediterranean Seismological Center aEpicentral location from CRAAG 424 J Seismol (2009) 13:421–432 ferograms of the Ain Temouchent earthquake, between Africa and Eurasia (Nocquet and Calais locate the area of surface deformation and infer 2004; Serpelloni et al. 2007). The transpressive the fault rupture characteristics. In parallel, In- active deformation is essentially due to the NNW– SAR results and field observations, which show SSE to NW–SE shortening as inferred from P evidence of Quaternary deformation and active axes of thrust focal mechanisms (Meghraoui et al.
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