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    188宝金博页面版: Gravity data inversion for Moho depth modeling in the Hellenic area

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    内容提示： Gravity data inversion for Moho depth modeling in the Hellenic areaV ASSILIOS N. G RIGORIADIS , 1 I LIAS N. T ZIAVOS , 1 G RIGORIOS N. T SOKAS , 2 and A LEXANDROS S TAMPOLIDIS 2Abstract—The main objective of this study is the determinationof the Moho discontinuity in the Hellenic area based on gravitydata inversion. High-resolution (2 arcmin) and accuracy (±2 to ±3mGal) gravity data were used in the computations following theParker–Oldenburg iterative method, and a low-pass filter wasapplied to gravity...

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    Gravity data inversion for Moho depth modeling in the Hellenic areaV ASSILIOS N. G RIGORIADIS , 1 I LIAS N. T ZIAVOS , 1 G RIGORIOS N. T SOKAS , 2 and A LEXANDROS S TAMPOLIDIS 2Abstract—The main objective of this study is the determinationof the Moho discontinuity in the Hellenic area based on gravitydata inversion. High-resolution (2 arcmin) and accuracy (±2 to ±3mGal) gravity data were used in the computations following theParker–Oldenburg iterative method, and a low-pass filter wasapplied to gravity information towards the convergence of the finalsolution. To determine the cut-off wavenumber of the filter, wetested different mean depths and density contrasts of the crust andthe mantle (Mohorovic ˇic ´ discontinuity). The selected densitycontrast and mean depth of the Mohorovic ˇic ´ discontinuity are thosewhich agree with the Moho depth interpreted from deep seismicimaging data. By comparing the Moho depth estimated, coveringboth land and marine areas and including the Ionian and AegeanSea, with those interpreted from previous studies, it is shown thatour solution is consistent with the available seismic data interpre-tation. Moreover, the resolution of the gravity data and theappropriate filtering used in this study contributed to the repre-sentation of local features of the Moho discontinuity. Finally, area-dependent discrepancies detected between the Moho depths of thecurrent solution and those derived from previous studies areextensively discussed.Key words: Gravimetric inverse problem, Bouguer gravityanomalies, Mohorovic ˇic ´ discontinuity, Moho depth, digital terrainand bathymetry model (DTBM).1. IntroductionThe Hellenic area is characterized by complicatedgeomorphologic and geotectonic characteristics (e.g.,P APAZACHOS et al. 1995; J OLIVET and B RUN 2010). Theplate interactions and associated crustal deformationtaking place in the region makes it one of the mostseismically active and rapidly deforming areasworldwide (e.g., T SOKAS and H ANSEN 1997; T AYMAZet al. 2007). Tectonic evolution of the region isdominated by the effects of the northward subductionof the African under the Eurasian plate along theHellenic arc (see Fig. 1). Thinner oceanic lithosphereis currently subducting under Crete and is causingextension of the continental crust and volcanism inthe overlying Aegean extensional province. In addi-tion, differential displacements of several microplates(Aegean, Anatolian, and Apulian plates) are makingthe overall active tectonic setting significantlycomplicated.The aforementioned characteristics are reflectedin the gravity field of the earth, hence allowing thestudy of the earth’s interior with the use of gravitydata by solving the inverse gravity problem. Thisproblem has infinite solutions, because gravity sig-natures may be caused by different densitydistributions. To find a unique solution to the prob-lem, constrains, assumptions, and prior informationfor the Earth’s gravity field and interior must bespecified in advance. This is also the case of esti-mating the thickness of the Earth’s crust, i.e., thedepth of the Mohorovic ˇic ´ discontinuity (Moho depth)by gravity data inversion.Various methodologies have been developed andapplied in determining the Moho discontinuityemploying only gravity data or a combination ofgravity with seismic data using different scales.Regarding the Hellenic area, the studies carried out todetermine the crust’s thickness employed methodsbased on either the interpretation of seismic data (see,e.g., P APAZACHOS et al. 1995; L I et al. 2003; K ARA-GIANNI et al. 2005; S ODOUDI et al. 2006; S ACHPAZI et al.2007; L UCCIO and P ASYANOS 2007), or the inversion ofgravity data (see, e.g., T SOKAS and H ANSEN 1997;T IBERI et al. 2001; T IREL et al. 2004) and the 3Dmodeling of the crust using both seismic and gravitydata (see, e.g., M AKRIS and Y EGOROVA 2006; C ASTEN1Department of Geodesy and Surveying, Aristotle Univer-sity of Thessaloniki, University Box 440, 54124 Thessaloniki,Greece. E-mail: nezos@topo.auth.gr2Department of Geophysics, Aristotle University ofThessaloniki, 54124 Thessaloniki, Greece.Pure Appl. Geophys.? 2015 Springer BaselDOI 10.1007/s00024-015-1174-yPure and Applied Geophysics

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