Our results, especially the local crustal models, are in good accordance with the known results of others, and reflect the principle characters of crustal velocity structure beneath each epicenter on the whole.

Meanwhile, the pressure deviations (△P) of different depths and the isostatic crustal thickness of Airy-woollard type in this region have been calculated, and the crustal models of different tectonic units have been analysed as well.

Meanwhile, the pressure deviations(△P)of different depths and theisostatic crustal thickness of Airy-woollard type in this region have been calculated, and the crustal models of different tectonic units have been analysed as well.

Liaohe Basin is a Mz-'Cenozoic rifted basin, developed on the Pre-Mesozoic basement. Observed heat flow in Liaohe Basin is about 65 mW/m2, ranging from 44 to 83 mW/m2. On the basis of the determination of radiogenic heat productivity for different rock strata of the Basin and crustal models, mantle heat flow was calculated by means of "stripping" method.

To test this method gravitational data from three hypothetic crustal models are intruduced here as example. We obtained that the maximum relative error is less than 2.0 percent,mean relative error 1.0 percent.

The model is compiled in an a priori fashion entirely from existing geophysical literature, specifically, combining two regionalized crustal models with a high-resolution global sediment model and a global upper mantle model.

Initial 20-layer crustal models are inverted for using prior tomographic results for the initial models.

The profile was acquired to map the crustal structure in the northernmost part of the V?ring Basin, and to link crustal models of the Lofoten and central V?ring Basin obtained by previous OBS studies.

Using three families of simple crustal models, we compare the effects of an anisotropic surface layer with reverberations caused by both "thick" and "thin" layers of anisotropy at depth.

The numerical simulation leads to successful comparison between observed seismograms in stable continental areas and synthetics computed for simple standard crustal models.

This paper presents a method called the "Compressed Mass Plane" to approximate, a two-dimensional geological body. At first, the data of a gravity data is inversed, using matrix analysis to get the surface density of each element of the compressed mass plane. Then, from the relation between surface density and mass density of each element, the thickness of each two-dimensinal element can be calculated and the approximate thickness of the crust tentatively obtained. Further improvements of the estimation of the...

This paper presents a method called the "Compressed Mass Plane" to approximate, a two-dimensional geological body. At first, the data of a gravity data is inversed, using matrix analysis to get the surface density of each element of the compressed mass plane. Then, from the relation between surface density and mass density of each element, the thickness of each two-dimensinal element can be calculated and the approximate thickness of the crust tentatively obtained. Further improvements of the estimation of the crustal thickness can be made by direct gravity computation of the crustal model thus obtained and repeated adjustments of the results in order to minimize the difference between computed and observed gravity anomalies. In that way, it may be possible to get the better depths of the lower boundary of the crust.Based on the assumed values of contrast between the "Basaltic", the "Granitic" layers and the Upper Mantle and also the above calculated crustal thickness, it is again possible to calculate the gravity anomalies coming from the undulations of the Mohorovicic and (Conrad interfaces respectively. By the same way, the inversion of the gravity anomaly of the Conrad interface, a comparatively correct position of this interface can be obtained.To test this method of gravity inversion, three hypothetic crustal models and an observed gravity profile are introduced here as examples. In comparing with other methods of determining crustal interfaces, the results of the present method of compressed mass plane seem to be better.

In this paper according to the data of Asian continental 1°×1° mean gravity field of Bouguer anomaly and a monolayer, homogenous, calculative crustal model, the total 10456 gravity data belonging to 131 gravity profiles have been calculated for determining the depth of Moho discontinuity. Obtained from this has been an outline map showing the distribution of Asian continental crustal thickness. Based on these results gained, the features of distribution of the crustal thickness and outline...

In this paper according to the data of Asian continental 1°×1° mean gravity field of Bouguer anomaly and a monolayer, homogenous, calculative crustal model, the total 10456 gravity data belonging to 131 gravity profiles have been calculated for determining the depth of Moho discontinuity. Obtained from this has been an outline map showing the distribution of Asian continental crustal thickness. Based on these results gained, the features of distribution of the crustal thickness and outline of crustal structure under the Asian continent have been analyzed and studied. Finally, this paper advances the principal characteristics of the Asian continental crust. There exist four vast areas of relatively minor variations in the crustal thickness, namely, northern, eastern southern and central areas of Asian crust; three great comprehensive steep (progressive) variational zones of crustal thickness, i. e. Pamir-Altai-Trans-Khingan complex steep variational zone, Trans-Khingan and Da Hinggan-Taihang-Wuling-Miaoling-Hengduan mountains progressively variational zone, and Zagros-Pamir-Himalayas steep variational zone; two complex convergent "node" of steep variational zones of crustal thickness, Pamirs "node" and Hengduan mountains "node"; and one Qinghai-Xizang crustal block with great thickness.

The fundamental principles of deducing parameters of a homogeneous, horizontally layered crustal model from the inversion of the travel times of body waves are developed and two effective inversion methods are presented: the '' layered inversion'' under some restraints and the '' composite in version'' of several seismic phases. Some artificial models are tested and a satisfactory solution may be obtained by either of the two methods.