Recent tectonic evolution and present stress in the Northern Apennines (Italy)

Mariucci, M. T.; Amato, A.; Montone, P.

doi:10.1029/1998tc900019

Cited by 91 publications

(65 citation statements)

References 28 publications

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“…The current rate of extension is 4 mm/year [D'Agostino et al, 2008] and its orientation is consistent with available focal mechanism solutions [Anderson and Jackson, 1987;Montone et al, 2004], borehole breakout [Mariucci et al, 1999] and geological data [Lavecchia et al, 1994;Roberts and Michetti, 2004].…”

Section: Seismicity and Tectonic Settingsupporting

confidence: 82%

The anatomy of the 2009 L'Aquila normal fault system (central Italy) imaged by high resolution foreshock and aftershock locations

et al. 2011

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[1] On 6 April (01:32 UTC) 2009 a M W 6.1 normal faulting earthquake struck the axial area of the Abruzzo region in central Italy. We study the geometry of fault segments using high resolution foreshock and aftershock locations. Two main SW dipping segments, the L'Aquila and Campotosto faults, forming an en echelon system 40 km long (NW trending). The 16 km long L'Aquila fault shows a planar geometry with constant dip (∼48°) through the entire upper crust down to 10 km depth. The Campotosto fault activated by three events with 5.0 ≤ M W ≤ 5.2 shows a striking listric geometry, composed by planar segments with different dips along depth rather than a smoothly curving single fault surface. The investigation of the spatiotemporal evolution of foreshock activity within the crustal volume where the subsequent L'Aquila main shock nucleated allows us to image the progressive activation of the main fault plane. From the beginning of 2009 the foreshocks activated the deepest portion of the fault until a week before the main shock, when the largest foreshock (M W 4.0) triggered a minor antithetic segment. Seismicity jumped back to the main plane a few hours before the main shock. Secondary synthetic and antithetic fault segments are present both on the hanging and footwall of the system. The stress tensor obtained by inverting focal mechanisms of the largest events reveals a NE trending extension and the majority of the aftershocks are kinematically consistent. Deviations from the dominant extensional strain pattern are observed for those earthquakes activating minor structures.

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Section: Seismicity and Tectonic Settingsupporting

confidence: 82%

The anatomy of the 2009 L'Aquila normal fault system (central Italy) imaged by high resolution foreshock and aftershock locations

et al. 2011

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“…1) features a complex tectonic structure and evolution characterized by highly variable geologic and geomorphologic patterns (e.g., Malinverno and Ryan, 1986;Patacca and Scandone, 1989;Doglioni, 1991Doglioni, , 1995Scrocca, 2006). At present, the central sector of the Apennines chain involves northeast-trending horizontal extension (e.g., Mariucci et al, 1999;Hunstad et al, 2003;Montone et al, 2004;Li et al, 2007) related to the opening of the Tyrrhenian back-arc basin (e.g., Malinverno and Ryan, 1986). This extensive regime causes the formation of several intramountain basins of varying dimensions, such as the L'Aquila, Sulmona, and Fucino basins, which are covered by Plio-Quaternary continental sediments (e.g., Cavinato and De Celles, 1999;Chiarabba et al, 2010;Fig.…”

Section: The 2009 L'aquila Earthquakementioning

confidence: 99%

Spectral-Element Simulations of Seismic Waves Generated by the 2009 L'Aquila Earthquake

Magnoni¹,

Casarotti²,

Michelini³

et al. 2013

Bulletin of the Seismological Society of America

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We adopt a spectral-element method (SEM) to perform numerical simulations of the complex wavefield generated by the 6 April 2009 M w 6.3 L'Aquila earthquake in central Italy. The mainshock is represented by a finite-fault solution obtained by inverting strong-motion and Global Positioning System data, testing both 1D and 3D wavespeed models for central Italy. Surface topography, attenuation, and the Moho discontinuity are also accommodated. Including these complexities is essential to accurately simulate seismic-wave propagation. Three-component synthetic waveforms are compared to corresponding velocimeter and strong-motion recordings. The results show a favorable match between data and synthetics up to ∼0:5 Hz in a 200 km × 200 km × 60 km model volume, capturing features mainly related to topography or low-wavespeed basins. We construct synthetic peak ground velocity maps that, for the 3D model, are in good agreement with observations, thus providing valuable information for seismic-hazard assessment. Exploiting the SEM in combination with an adjoint method, we calculate finite-frequency kernels for specific seismic arrivals. These kernels capture the volumetric sensitivity associated with the selected waveform and highlight prominent effects of topography on seismic-wave propagation in central Italy.

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“…The southwest-dipping normal faults of the UFS are Quaternary age at the base of the basin's infill and are considered active from geomorphological (e.g., Ficcarelli and Mazza, 1990;Coltorti et al, 1998;Messina et al, 1999), geologic (e.g., Lavecchia et al, 1994;Calamita et al, 1999;Barchi et al, 2000;Mirabella and Pucci, 2002), and seismological evidence (e.g., Deschamps et al, 1984;Haessler et al, 1988;Amato et al, 1998;Ekström et al, 1998;Mariucci et al, 1999;Stramondo et al, 1999;Barba and Basili, 2000). Historical seismicity data (Imax = XMCS, CPTI, 1999) and recent earthquakes [Norcia, 1979, Ms (surface-wave magnitude) = 5.9; Gubbio, 1984, Ms = 5.2;Colfiorito, 1997Colfiorito, -1998, maximum Mw = 6.0] (Deschamps et al, 1984;Haessler et al, 1988;Deschamps et al, 2000) indicate an active stress field consistent with a geologic long-term stress field that has been active since the Quaternary (Mariucci et al, 1999).…”

Section: Tectonic Settingmentioning

confidence: 99%

“…Historical seismicity data (Imax = XMCS, CPTI, 1999) and recent earthquakes [Norcia, 1979, Ms (surface-wave magnitude) = 5.9; Gubbio, 1984, Ms = 5.2;Colfiorito, 1997Colfiorito, -1998, maximum Mw = 6.0] (Deschamps et al, 1984;Haessler et al, 1988;Deschamps et al, 2000) indicate an active stress field consistent with a geologic long-term stress field that has been active since the Quaternary (Mariucci et al, 1999).…”

Section: Tectonic Settingmentioning

confidence: 99%

Comparison between reprocessed seismic profiles: Seismologic and geologic data — A case study of the Colfiorito earthquake area

2006

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Seismic reflection data are used to reconstruct the subsurface geologic structures below the Umbria-Marche region in Italy, a highly seismogenic area with a recent history of seismic activity (the 1997-1998 Colfiorito sequence). We reprocess three vibroseis seismic profiles (acquired in the early 1980s for hydrocarbon exploration) whose stacked sections were optimized for relatively deep oil targets. On the reprocessed seismic profile closest to the epicentral area, we construct the main reflectors to a depth of about 4 s (two-way time) and compare this interpretation with the available hypocenters of the 1997 earthquakes.The improvements in visualizing the shallow and deep reflections provide a better correlation between the reflectors and the observed surface structures as well as a better delineation of the basement-rock geometry. We find that part of the Colfiorito sequence is localized around some of the reflectors in the reflection profile, which we interpret as related to the active normal faults that outcrop at the surface.

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Recent tectonic evolution and present stress in the Northern Apennines (Italy)

Cited by 91 publications

References 28 publications

The anatomy of the 2009 L'Aquila normal fault system (central Italy) imaged by high resolution foreshock and aftershock locations

The anatomy of the 2009 L'Aquila normal fault system (central Italy) imaged by high resolution foreshock and aftershock locations

Spectral-Element Simulations of Seismic Waves Generated by the 2009 L'Aquila Earthquake

Comparison between reprocessed seismic profiles: Seismologic and geologic data — A case study of the Colfiorito earthquake area

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