ALBERT

Description: Author(s): Luca Tanzi, Eleonora Lucioni, Saptarishi Chaudhuri, Lorenzo Gori, Avinash Kumar, Chiara D’Errico, Massimo Inguscio, and Giovanni Modugno We investigate the momentum-dependent transport of 1D quasicondensates in quasiperiodic optical lattices. We observe a sharp crossover from a weakly dissipative regime to a strongly unstable one at a disorder-dependent critical momentum. In the limit of nondisordered lattices the observations sugges... [Phys. Rev. Lett. 111, 115301] Published Mon Sep 09, 2013

Description: Author(s): Chiara D’Errico, Eleonora Lucioni, Luca Tanzi, Lorenzo Gori, Guillaume Roux, Ian P. McCulloch, Thierry Giamarchi, Massimo Inguscio, and Giovanni Modugno We employ ultracold atoms with controllable disorder and interaction to study the paradigmatic problem of disordered bosons in the full disorder-interaction plane. Combining measurements of coherence, transport and excitation spectra, we get evidence of an insulating regime extending from weak to st... [Phys. Rev. Lett. 113, 095301] Published Mon Aug 25, 2014

Description: The influence of the structural setting of mountain slopes on the evolution of large scale gravitational deformations

Description: Published

Description: Rimini

Description: 3.2. Tettonica attiva

Description: open

Description: During the last decades, the study of seismic anisotropy has provided useful information for the interpretation and evaluation of the stress field and active crustal deformation. Seismic anisotropy can yield valuable information on upper crustal structure, fracture field, and presence of fluid-saturated rocks crossed by shear waves. Several studies worldwide demonstrate that seismic anisotropy is related to stress-aligned, filled-fluid micro-cracks (EDA model). An automatic analysis code, “Anisomat+”, was developed, tested and improved to calculate the anisotropic parameters: fast polarization direction (φ) and delay time (∂t). Anisomat+ has been compared to other two automatic analysis codes (SPY and SHEBA) and tested on three zones of the Apennines (Val d’Agri, Tiber Valley and L’Aquila surroundings). The anisotropic parameters, resulting from the automatic computation, have been interpreted to determine the fracture field geometries; for each area, we defined the dominant fast direction and the intensity of the anisotropy, interpreting these results in the light of the geological and structural setting and of two anisotropic interpretative models, proposed in the literature. In the first one, proposed by Zinke and Zoback, the local stress field and cracks are aligned by tectonics phases and are not necessarily related to the presently active stress field. Therefore the anisotropic parameters variations are only space-dependent. In the second, EDA model, and its development in the APE model fluid-filled micro-cracks are aligned or ‘opened’ by the active stress field and the variation of the stress field might be related to the evolution of the pore pressure in time; therefore in this case the variation of the anisotropic parameters are both space- and time- dependent. We recognized that the average of fast directions, in the three selected areas, are oriented NW-SE, in agreement with the orientation of the active stress field, as suggested by the EDA model, but also, by the proposed by Zinke and Zoback model; in fact, NW-SE direction corresponds also to the strike of the main fault structures in the three study regions. The mean values of the magnitude of the normalized delay time range from 0.005 s/km to 0.007 s/km and to 0.009 s/km, respectively for the L'Aquila (AQU) area, the High Tiber Valley (ATF) and the Val d'Agri (VA), suggesting a 3-4% of crustal anisotropy. In each area are also examined the spatial and temporal distribution of anisotropic parameters, which lead to some innovative observations, listed below. 1) The higher values of normalized delay times have been observed in those zones where most of the seismic events occur. This aspect was further investigated, by evaluating the average seismic rate, in a time period, between years 2005 and 2010, longer than the lapse of time, analyzed in the anisotropic studies. This comparison has highlighted that the value of the normalised delay time is larger where the seismicity rate is higher. 2) In the Alto Tiberina Fault area the higher values of normalised delay time are not only related to the presence of a high seismicity rate but also to the presence of a tectonically doubled carbonate succession. Therefore, also the lithology, plays a important role in hosting and preserving the micro-fracture network responsible for the anisotropic field. 3) The observed temporal variations of anisotropic parameters, have been observed and related to the fluctuation of pore fluid pressure at depth possibly induced by different mechanisms in the different regions, for instance, changes in the water table level in Val D’Agri, occurrence of the April 6th Mw=6.1 earthquake in L’Aquila.Since these variations have been recognized, it is possible to affirm that the models that better fit the results, both in term of fast directions and of delay times, seems to be EDA and APE models.

Description: Published

Description: Torino

Description: 3.1. Fisica dei terremoti

Description: 3.2. Tettonica attiva

Description: open

Description: We present a collection of pictures of the coseismic secondary geological effects produced on the environment by the 2012 Emilia seismic sequence in northern Italy. The May-June 2012 sequence struck a broad area located in the Po Plain region, causing 26 deaths and hundreds of injured, 15.000 homeless, severe damage of historical centres and industrial areas, and an estimated economic toll of ~2 billion of euros. The sequence included two mainshocks (Figure 1): the first one, with ML 5.9, occurred on May 20 between Finale Emilia, S. Felice sul Panaro and S. Martino Spino; the second one, with ML 5.8, occurred 12 km southwest of the previous mainshock on May 29. Both the mainshocks occurred on about E-W trending, S dipping blind thrust faults; the whole aftershocks area extends in an E-W direction for more than 50 km and includes five ML≥5.0 events and more than 1800 ML〉1.5 events. Ground cracks and liquefactions were certainly the most relevant coseismic geological effects observed during the Emilia sequence. In particular, extensive liquefaction was observed over an area of ~1200 km2 following the May 20 and May 29 events. We collected all the coseismic geological evidence through field survey, helicopter and powered hang-glider trike survey, and reports from local people directly checked in the field. On the basis of their morphologic and structural characteristics the 1362 effects surveyed were grouped into three main categories: a) liquefactions related to overpressure of aquifers, occurring through several aligned vents forming coalescent flat cones (485 effects); b) liquefactions with huge amounts of liquefied sand and fine sand ejected from fractures tens of meters long (768); c) extensional fractures with small vertical throws, apparently organized in an en-echelon pattern, with no effects of liquefaction (109). The photographic dataset consists of 99 pictures of coseismic geological effects observed in 17 localities concentrated in the epicentral area. The pictures are sorted and presented by locality of observation; each photo reports several information such as the name of the site, the geographical coordinates and the type of effect observed. Figure 1 shows a map of the pictures sites along with the location of the two mainshocks; Figure 2 shows a detail of the distribution of the liquefactions in the area of S. Carlo. The complete description of the coseismic geological effects induced by the Emilia sequence, their relation with the aftershock area, the InSAR deformation area and the I〉6 EMS felt area, along with the description of the technologies used for data sourcing and processing are shown in Emergeo Working Group [2012a and 2012b].

Description: Published

Description: 1-70

Description: 3.2. Tettonica attiva

Description: N/A or not JCR

Description: open

Description: The main goal of this study is to increase the understanding of the physical mechanisms behind the ongoing seismic activity in the Pollino area and its influence on the seismic hazard of the Apennines-Calabrian arc boundary region. The study area, near the Pollino massif, is located at the northernmost edge of the Calabrian Arc, which is the last oceanic subduction segment along the Africa-Eurasian plate. The subduction results from the sinking of the Ionian oceanic plate beneath the Calabrian Arc-Southern Tyrrhenian Sea and is part of the fragmented tectonic boundary between two macro-plates: Africa and Eurasia. The subduction geometry is well-documented by several seismological studies (i.e. Chiarabba et al., 2005), and the lithospheric structure of the area is quietly well known (i.e. Totaro et al., 2014 and Piana Agostinetti and Amato, 2009) Despite the slow N-S convergence between these major plates, the Southern Tyrrhenian Sea is a large basin characterized by E-W extensional tectonic. Since Late Miocene, the Calabrian Arc slab experienced rapid rollback, moving E to SE at a rate of 5-6 cm/yr, which is by far higher than the ~1-2 cm/yr rate of convergence between Africa and Europa (Faccenna et al., 2004). However, during late Pleistocene, rollback and subduction have slowed and is likely proceeding at less than 1 cm/yr (D’Agostino and Selvaggi., 2004). Geodetic measurements show that the Pollino Range is subject to NE-SW anti-apenninic extension. In the region the strain rate field shows a continuous belt of extensional deformation that follows the ridge of the Southern Apennines and extends in the Pollino region. The extension rate appears to decrease from the Southern Apennines to the Calabria- Lucania border region (D’Agostino et al., 2013). This finding indeed reveals that the Pollino region is deforming and accumulating tectonic strain which results in a complex system of normal active faults striking sub-parallel to the Apennines. Two principal normal faults are present in the Italian Database of the Individual Seismogenic Sources DISS version 3.1.1 (DISS Working Group, 2010) in the Pollino area: the Pollino (P) fault and the “Rimendiello-Mormanno” (RM) fault system. The RM fault is an active seismogenic structure it strikes about NNW-SSE and dips toward NE; it has hosted in its northernmost part a M 5.0 earthquake on 9th September 1998. The P fault has similar strike but dips toward SW: it shows no recent seismicity and is hence one of the most prominent seismic gaps in the Italian historical seismic catalogue (Rovida et al., 2011). Paleoseismic studies have shown that the P fault was active in the last ten thousand years and is capable to produce events with magnitude above 6.0. The DISS database reports as debated source also the Piana Perretti fault (Brozzetti et al., 2009). A detailed structural map of the area interested by the seismic sequence shows three fault systems (Brozzetti et al., 2013) consisting of several aligned fault segments that have been active during the Late Pleistocene and are reasonably presently active. The first fault system strikes NW-SE and dips toward SW (including the Piana Perretti fault at the NE edge of the Mercure Basin), the second one has similar strike and NE dip, while the third one strikes about E-W. Earthquakes reported in the historical catalogues for this area are not very strong. Few earthquakes with magnitude probably less than 6 affected the area, including the Mw=5.6 “Mercure” event in 1998 (Brozzetti et al., 2009). The Parametric Catalogue of Italian earthquakes (CPTI11, Rovida et al., 2011), shows very well the lack of strong earthquakes in the region: there is a clear evidence of large earthquakes in the Campania-Basilicata area (M~7.0) and several strong earthquakes in the Sila region and in the whole Calabrian territory. According to the seismic classification of the national territory, the area affected by the 2010-2014 seismic activity have a relatively higher probability to be shaken by a strong acceleration (Gruppo di Lavoro MPS, 2004). Most of the seismic events occurred in areas where the peak ground acceleration having 10% chance of being exceeded in next 50 years is between the values of 0.225 g and 0.275 g.

Description: Published

Description: Bologna

Description: 2T. Tettonica attiva

Description: 3T. Pericolosità sismica e contributo alla definizione del rischio

Description: 5T. Sorveglianza sismica e operatività post-terremoto

Description: 1IT. Reti di monitoraggio e Osservazioni

Description: open

Description: On 6 April 2009, at 01:32 GMT, an Mw 6.3 seismic event hit the central Apennines, severely damaging the town of L’Aquila and dozens of neighboring villages and resulting in approximately 300 casualties (Istituto Nazionale di Geofisica e Vulcanologia, http://www.ingv.it; MedNet, http://mednet.rm.ingv.it/proce- dure/events/QRCMT/090406_013322/qrcmt.html). This earth- quake was the strongest in central Italy since the devastating 1915 Fucino event (Mw 7.0). The INGV national seismic net- work located the hypocenter 5 km southwest of L’Aquila, 8–9 km deep. Based on this information and on the seismotectonic framework of the region, earthquake geologists traveled to the field to identify possible surface faulting (Emergeo Working Group 2009a, 2009b). The most convincing evidence of pri- mary surface rupture is along the Paganica fault, the geometry of which is consistent with seismological, synthetic aperture radar (SAR) and GPS data. Investigation of other known nor- mal faults of the area, i.e., the Mt. Pettino, Mt. San Franco, and Mt. Stabiata normal faults suggested that these structures were not activated during the April 6 shock (Emergeo Working Group 2009a, 2009b). In this report, we first describe the seismotectonic frame- work of the area, and then we present the field information that supports the occurrence of surficial displacement on the Paganica fault.

Description: Published

Description: 940-950

Description: 3.2. Tettonica attiva

Description: JCR Journal

Description: open