INGV. Giuseppe Pezzo. Istituto Nazionale di Geofisica e Vulcanologia, CNT, Roma. Sessione 1.1: Terremoti e le loro faglie

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1 Giuseppe Pezzo Istituto Nazionale di Geofisica e Vulcanologia, CNT, Roma giuseppe.pezzo@ingv.it

2 The study of surface deformation is one of the most important topics to improve the knowledge of the deep mechanisms governing the seismic cycle To measure the crustal ground deformation associated to fault activity and to the earthquake-cycle we use DInSAR (Differential Interferometric Synthetic Aperture Radar), MAI (Multi Aperture Interferometry) (centimetric accuracy), and multitemporal InSAR methods (millimetric accuracy) Interseismic phase: we need to identify tectonic patterns and to integrate geological and geodetic data. Geological Data Slip rate averaged over many seismic cycles (several thousands of years) Geodetic Data Ground velocity maps (averaged over few years) To reconcile the different data we need to identify the deformation sources and to evaluate the slip rate along the fault plane. Coseismic phase: we need to identify seismic deformation patterns, to understand/parameterize the seismic sources, and to study their interaction Postseismic phase: we need to discern the afterslip pattern from other geodetic signals to correctly interpret possible transient deformation patterns from one tectonic structure to another, as well as the evolution of the seismic sequence.

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4 The Gargano area is characterized by active (instrumental and historical) seismicity that can originate strong earthquakes reaching intensities of XI MCS. The E-W Mattinata Fault (MF) has been frequently proposed as a natural candidate to represent the major seismogenic structure in the Gargano area; however the spatial distribution of the recorded seismicity does not concentrate along this structure.

5 A C B D Using the SBAS multitemporal DInSAR technique (Berardino et al., 2002) we analyzed a SAR dataset of 88 descending (from 1992 to 2010) and 46 ascending (from 1995 to 2008) ERS and ENVISAT images to retrieve high resolution, mean velocity maps). Combining ascending and descending line of sight velocity maps, we obtained the East and Up component velocity maps. The former shows a NW-SE oriented maximum gradient of about 0.03 mm yr -1 km -1 across the MF, in good agreement with GPS data and the main stress axis orientation.

6 We modeled the MF using the elastic dislocation model proposed by Okada (1985).Our measurements are compatible with a right-lateral kinematics of MF with a slip rate of about 1.5 mm yr -1 to a depth of 15 km, as shown by comparing observed and modeled velocity profile We inverted the SAR maps using the MF source parameters, subsequently evaluating the inversion goodness by comparing with bibliographic data. Without fundamental a priori information about the geometry of the fault and geological knowledge, it would have been impossible to carry out a correct data interpretation and source modeling. C

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8 The Emilia sequence occurred in the Apennines' thrust front below the Po plain, well documented by many previous works and geophysical data from the petroleum industry. The easternmost CSK1 interferogram covers the first mainshock (May 20th ) The CSK2 westernmost interferogram covers the second one (May 29th ) Radarsat-1 records the ground displacement of the entire seismic sequence

9 - To obtain a ground displacement map of the entire deformation occurred during the May 20 th seismic event, for which only a partial map is available (CSK1), we subtract to the Radarsat deformation map the CSK2 map (a reasonable procedure due to the similarity of the two geometries). = C

10 For the May 20 th event we invert 3 datasets: CSK1, Radarsat-1 minus CSK2 and GPS data. For the May 29 th event we invert 2 datasets: CSK2 and GPS.

11 The 2008 Baluchistan (western Pakistan) sequence took place in the Quetta Syntaxis, the most seismically active region of Baluchistan, tectonically located between the colliding Indian Plate and the Afghan block of the Eurasian Plate.

12 We studied the sources of the three largest events of the 2008 Baluchistan (western Pakistan) seismic sequence, namely two Mw 6.4 events only 11 hours apart and an Mw 5.7event 40 days later. We use Synthetic Aperture Radar Differential Interferometry (DInSAR) and Multi-Aperture Interferometry (MAI) A C B D E F G

13 Elastic dislocation modelling of the surface displacements derived from ascending and descending ENVISAT ASAR acquisitions, yields slip distributions with peak values of 80 cm and 70 cm for the two main events on a pair of almost parallel and near-vertical faults striking NW- SE, and values up to 50 cm for the largest aftershock on a NE-SW fault located in between the sources of the mainshocks. The MAI displacements, with their high sensitivity to the north-south motion component, are crucial in this area to resolve the fault plane ambiguity determined by moment tensors.

14 Our results provide insight into the deformation style of the Quetta Syntaxis, suggesting the latter behaves as a right-lateral shear zone at a regional scale, in which NW-SE structures accommodate the northward motion of the Kirthar range and Chaman Fault System to the west and the southward motion of the Sulaiman Lobe to the east, whereas at a more local scale NE-SW structures are created through a bookshelf mechanism.

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16 We used 25 COSMO- SkyMed SAR images (beam 09 asc.) to obtain a postseismic deformation time series and mean velocity map (spanning 12/04/2009 to 13/10/2009). In addition to the afterslip correlated pattern, the postseismic velocity map shows many other features related to gravity, like deep seated gravitational slope deformations (DSGSD).

17 Post seismic multitemporal SAR analysis of the 2008 Emilia seismic sequence (15 COSMO-SkyMed stripmap SAR images). We observe a quasiexponential afterslip deformation pattern in the epicentral area. In addition we detect a velocity pattern not directly attributable to the postseismic phenomena.

18 Profile 2 Profile 1 We observe a general agreement between the preseismic and postseismic, albeit for the afterslip pattern located in the epicentral area

19 Integration of geodetic and geological data provide an optimum union to study and identify the seismic cycle deformations and related faults. Fault modeling is a useful tool to reconcile the long term geological data and present day velocity measured by SAR/GPS Interseismic cases: except for unmistakable cases (e.g. San Andreas Fault), interseismic signals are very low and SAR velocity maps provide an important constraint to the source modeling. SAR maps alone cannot constrain all fault parameters without independent geological constraints. Coseismic cases: If a good SAR dataset is available (at least three points of view), it is possible to identify the coseismic pattern and related seismic sources (e.g. Pakistan earthquakes). Where few geodetic constrains are available (for example only one line of sight), we need geological constraints to identify the seismic sources (e.g. Emilia earthquakes). Postseismic cases: the major problem for the post seismic velocity maps are related to pattern interpretation. In fact, many deformation features could be related to non tectonic cause: for example gravity (e.g. L Aquilia posteseismic map) or subsidence phenomena (Emilia postseismic map). Sessione 2-1: Emilia: il terremoto inatteso? Potenza, 22 Nov. 2012

20 The author is funded by the -ASI MUSA project. The COSMO-SkyMed SAR data are copyright of the Italian Space Agency (ASI), and were provided by the Department of Civil Protection (DPC) in the framework of the ASI--Spacebased Monitoring System for Seismic Risk Management (ASI- SIGRIS) project. The ENVISAT ASAR data are copyrighted by the European Space Agency and were provided through CAT1 proposal Some figures were prepared using the public-domain GMT software (Wessel and Smith, 1998). The ASTER GDEM is a product of METI and NASA. The author thanks J.P. Merryman Boncori and C. Tolomei for their fundamental support in the SAR data processing; S. Atzori and A. Antonioli for their precious help for the data inversions and CFF analysis and S. Salvi for the fruitful geological discussions and comments. Sessione 2-1: Emilia: il terremoto inatteso? Potenza, 22 Nov. 2012

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