The residual map was divided into 14 overlapping spectral blocks, and the log of spectral energies were plotted against frequency. Regional/Residual separation was performed on the total magnetic intensity using polynomial fitting. The study area lies within the Longitude 9вЋ вЂ“ 10вЋ and Latitude 8В°N вЂ“ 9.50В°N with an estimated total area of 18,150 km2.

This research deals with assessment of geothermal potential in parts of middle Benue Trough, north-east of Nigeria. Finally, it is imposed on two real underground examples an urban gas pipe and a roughly spherical orebody and the results confirm the methodology of this syudy. The method is tested on solitary and binary simulated data for bodies with varying physical characteristics, inclinations and declinations.

To reduce the turbulent effects of noise, вЂњMoving Twenty five Point AveragingвЂќ method and upward continuation filter are used. These obtained depth values are 0.56 and 0.74 of COM vertical components for a line of dipoles and point-dipole, respectively. In this study, by reduction to the pole (RTP) transformation and calculation of CMGT, a point is estimated that its horizontal components are exactly the horizontal components of the COM and its vertical component is a fraction of the COM vertical component. Rather, in the best condition, when there is no remanent magnetization and the body is in the magnetic poles, their directions are a function of data point locations. However, due to the nature of the magnetic field, it is shown that these eigenvectors for the similar shaped magnetic bodies (line of dipoles and point-dipole), in CMGT, are not convergent to COM anymore. At the eigenvector analysis of Gravity Gradient Tensors (GGT) for a line of poles and point pole, the eigenvectors of the largest eigenvalues (first eigenvectors) point precisely toward the Center of Mass (COM) of a body. According to the distribution and number of stations used, this study is more comprehensive than previous studies.Д¬omputed Magnetic Gradient Tensor (CMGT) includes the first derivatives of three components of magnetic field of a body. Furthermore, the clear image of the Moho at depths as modeling of PRF, ranging from 37 km beneath KCHF station to maximum 55 km beneath HAGD station was presented. The Moho depths are estimated from the delay time of the Moho converted phase relative to the direct P wave beneath each network. The results indicate clear Ps conversions at the Moho boundary. The teleseismic data (Mb в‰Ґ5.5, epicentral distance between 30Лљ-95Лљ) recorded from 2004 to 2016 at 17 permanent broadband and short-period stations of the Iranian Seismological Center (ISC, ) of Kermanshah, Khoramabad, Hamedan and Boroujerd and one broadband station of the International Institute of Earthquake Engineering and Seismology (IIEES, ) were used. In this study, the P receiver function technique beneath the west Iran is used to map out the lateral variation of the Moho boundary. Receiver functions are usually used to detect Ps converted waves and are especially useful to picture seismic discontinuities in the crust and upper mantle.

Ш±Ш§Щ‡Щ†Щ…Ш§ЫЊ res2dinv