Figure 6 - uploaded by Tiziana Sgroi
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Differences in terms of latitude a), b), longitude c), d) and depth e), f) between locations performed with and without NEMO-SN1. Histograms show that the main differences in latitude a) and longitude c) are within ±5 km, while the differences in depth e) are roughly doubled. The distribution of these differences within the values of ±5 km is indicated in the three maps (b), latitude; d), longitude; f), depth). Latitude and longitude have similar values in the central part of the study area, showing higher values in the peripheral areas, while differences in hypocentre depth are more consistent in the whole study area. Dots indicate the locations performed with data of NEMO-SN1 and their dimensions are proportional to the recomputed M L . The main tectonic structures (Malta escarpment -ME, Alfeo-Etna Fault -AEF and Ionian Fault -IF, splay faults -S1, S2, S3) are sketched in black.
Source publication
The Western Ionian Sea is characterised by an active and diffuse seismicity, directly related to the convergence of the European and African Plates and by gravitational sinking and rollback of the oceanic lithosphere. In this area, the location of earthquakes is characterised by considerable uncertainties due to large azimuthal gaps, resulting in n...
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Citations
... Earthquake fault plane solutions from the CMT provide important information on the fault mechanism at depth. Each earthquake CMT (Pondrelli, 2002) is color-coded to represent one of five kinematic categories: thrust, strike, normal, oblique (i.e., thrust-strike or normal-strike), and horizontal-vertical, following a classification scheme similar to Frohlich (1992) based on the plunge angles of P-and T-axis (e.g., Lindenfeld et al., 2012;Sgroi, Barberi, & Marchetti, 2021). Distinct mechanisms at different areas of the central Mediterranean and at different depths can be noted in Figures 11 and 12. ...
The evolution of the Sicily Channel Rift Zone (SCRZ) is thought to accommodate the regional tectonic stresses of the Calabrian subduction system. Much of the observations we have today are either limited to the surface or to the upper crust or deeper from regional seismic tomography, missing important details about the lithospheric structure and dynamics. It is unclear whether the rifting is passive from far‐field extensional stresses or active from mantle upwelling beneath. We measure Rayleigh‐and Love‐wave phase velocities from ambient seismic noise and invert for 3‐D shear‐velocity and radial anisotropic models. Variations in crustal S‐velocities coincide with topographic and tectonic features. The Tyrrhenian Sea has a ∼10 km thin crust, followed by the SCRZ (∼20 km). The thickest crust is beneath the Apennine‐Maghrebian Mountains (∼55 km). Areas experiencing extension and intraplate volcanism have positive crustal radial anisotropy (VSH > VSV); areas experiencing compression and subduction‐related volcanism have negative anisotropy. The crustal anisotropy across the Channel shows the extent of the extension. Beneath the Tyrrhenian Sea, we find very low sub‐Moho S‐velocities. In contrast, the SCRZ has a thin mantle lithosphere underlain by a low‐velocity zone. The lithosphere‐asthenosphere boundary rises from 60 km depth beneath Tunisia to ∼33 km beneath the SCRZ. Negative radial anisotropy in the upper mantle beneath the SCRZ is consistent with vertical mantle flow. We hypothesize a more active mantle upwelling beneath the rift than previously thought from an interplay between poloidal and toroidal fluxes related to the Calabrian slab, which in turn produces uplift at the surface and induces volcanism.
