GNGTS 2018 - 37° Convegno Nazionale

GNGTS 2018 S essione 3.1 567 has been taken from Rybakov and Segev (2004), while for the densities a gradient in the vertical direction starting from 2000 kg/m 3 up to 2600 kg/m 3 has been considered. In the stripping procedure the effect of the subduction plate beneath Cyprus has also been modelled (from Ergün et al., 2005) and removed. The shape of the geological provinces has been taken from Longacre et al. (2007) and modified to be coherent with the observed gravity disturbances reduced for the effect of topography, bathymetry and sediments (see Fig. 1). As for the crystalline crust density model both the horizontal as well as the vertical variations are considered. For each geological province, a function defining the density variation with depth is created from data documented in Chirstensen and Mooney (1995) and Carlson and Raskin (1984). Finally, the Mantle density is taken from the CRUST1.0 model (Laske et al. , 2013). Some interpreted seismic profiles, derived from Longacre et al. (2007) and Ben-Avraham et al. (2002) are also considered in the inversion. Results. The results of the inversion in terms of Moho depth is presented in Fig. 2 and Fig. 3. Fig. 2 - Estimated Moho depth and corresponding accuracy (standard deviation). It can be seen the presence of a shallower Moho typical of the oceanic crust in correspondence of the Herodotus Basin, and the presence of an intermediate continental crust for the Levant Basin. As an example of the Monte Carlo accuracy analysis we report in the following Tab. 1 the effect of the uncertainties of the most important input in terms of accuracy of the retrieved Moho depth. Fig. 3 - Estimated density distribution along two sections at constant Longitude equal to 23.7° (up) and constant Latitude equal to 33.75° (down).