Sunrise effect on atmospherics and its relation to the direction of the night noise source

a auauu m ma ¶rt;a a a amua aama m¶rt;, m n¶rt;m anau umu, u m nu¶rt;um ¶rt;a a nu mau am . m¶rt; nu a¶rt;u amu a ¶rt; mau aauu nu (nu, au, 27 , u uma, au, 29 ) mu 1967–1970 . m¶rt; n¶rt;mam ¶rt;a u, u aaua mam, m n¶rt;nmu a¶rt; m¶rt;am anau umua u am, u m umuu a m mnua. ¶rt;u u mam aaua m ma nuau ¶rt;u n u ma ¶rt;a a. anau um a u mau mu¶rt;a ¶rt; u u -ana¶rt;u anauu. au ¶rt;a u n¶rt;¶rt;uam aau m ¶rt;a u a¶rt;a a a amua a¶rt; n [15]. m, m mu¶rt;a um m m aa m anmauu ¶rt;u a¶rt;u, m a auum u ¶rt; anmau a¶rt;u u mau ¶rt;m (uu m m u), u ma m um a¶rt; m auauu anauu amu nu¶rt;u a¶rt;am ¶rt; ¶rt;a a.     

Seismic response analysis of two-dimensional absorbing structures

Summary A computational method (based on finite differences) is proposed for the seismic response analysis of the Earth's structures. The method is applied to the earth fill and the sedimentary basin. It was found that the lateral inhomogeneity of non-absorbing structures caused remarkable effects on synthetic seismograms, viz. strong horizontal reflections at later arrivals. In absorbing structures these effects are much less pronounced and the response is determined primarily by the variable thickness of the structures. The responses of structures with non-causal or causal absorption differ only slightly, but they are strongly influenced by the magnitude of the absorption itself.     

Thermal and electric conductivity of three basaltic rocks of the Bohemian Massif under high temperatures

Summary The thermal, temperature and electric conductivities of three alkaline basalts are compared for temperatures ranging from 20 to 900 °C.     

Appreciation of spherically symmetric models of electrical conductivity

A procedure is suggested of a more effective and faster computation of the impedance, the transfer function and amplitudes of the induced field in a spherically symmetric model of the electrical conductivity. The existing induction data have been supplemented by about 80 new values derived from the analysis of daily means. The fit of the existing 1-D models of the electrical conductivity of the mantle to the set of induction data is investigated. The characteristic equation for the free electromagnetic oscillations of a radially inhomogeneous Earth is derived and its possible importance in solving the inverse problem of electric conductivity is pointed out.     

ЧИСЛЕННЫЕ ЭКСПЕРИМЕНТЫ С ИСКУССТВЕННЫМИ ЯДРАМИ СУБЛИМАЦИИ В СТРУЙНОЙ МОДЕЛИ КУЧЕВОГО ОБЛАКА

nuam aau ¶rt; amu a um ¶rt; ¶rt;a uauu. ¶rt; ¶rt;a, ¶rt;mu auumu m mnam u nu mum ¶rt;a, umam m ¶rt;u z aa n¶rt; uuu, a aau. u¶rt; auum ¶rt;au z naa m mauu ¶rt; amu, naam, m ¶rt;au ¶rt;z naa zauuam u amu ¶rt;.

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Summary A formation of ice particles on artificial deposition INis described. INacting in dependence on the temperature and supersaturation over the ice are considered in the 1 D SSconvection cloud model with detailed microphysics including freezing. The limiting influence of the water vapour pressure upon the concentration of active INis shown resulting from the dependence of water vapour pressure on the ice particle concentration.

     

Geometrical aspects of differential GPS positioning

Differential GPS positioning is considered from the purely geometric point of view. The tetrahedron formed by two ground stations and two satellite locations is the basic geometrical building block for differential satellite positioning. Relationships between the various vectors involved in this tetrahedron are described. These relationships are used to develop linear mathematical models which relate the vector baseline between the two ground stations to various kinds of differential GPS observations. Geometrically, all proposed observation types can be considered as either differential range observations or differential range difference observations. In the absence of instrumental and refraction effects, it is found that differential range observations are geometrically superior to differential range difference observations. Some implications of these geometrical considerations to practical differential GPS positioning are discussed.     

Remarks on seismic energy release related to strike slip and tensile crack mechanisms

¶rt;u u uu uuu ¶rt; n¶rt; ¶rt;au m ¶rt;u uu m n¶rt;uu u numuu m¶rt;. mam n¶rt; aamumuu anamu u ; n¶rt; mu aaa amu ¶rt;u n¶rt;uu nmu aua ¶rt;u u uu a mu m muna.     

On latitudinal variations of temporal characteristics of the VLF chorus in the upper ionosphere

Summary The elements of the VLF chorus, observed simultaneously at a ground station and satellite in polar orbit, can be used to determine the differences in the arrival times of waves and their dependence on latitude. Mostly does not change practically over a wide range of latitudes, however, in some cases it may increase appreciably at low value of L. Model computations of the propagation time, based on the assumption that the source of the chorus is located close to the equatorial plane, have indicated the possibility of explaining the increase in at low latitudes by the presence of a step in the electron density profile close to this plane.

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a¶rt;u m a u a um nmu nun um nm n¶rt;um amu u nu¶rt;a ma a u u um auum (L). um a a m ¶rt;uana um, m a a¶rt;am aum uu a a L-a. am anmau n¶rt;nuu amua umua naam m um uu a uu uma auu mnu an¶rt;uu m mauu amua nmu.

     

On the estimation of the heat flow at the earth's crust lower boundary

Summary The paper deals with a comparison of two models used in determining the heat flow q_M at the lower boundary of two-dimensional geothermal models of the Earth's crust. Method I is based on a linear relationship between the component of the surface heat flow, which is not generated by heat sources inside the model, and the heat flow q_M. This method uses a regularization process, in which the variation of the sought function q_M is limited from above. Method II is the most frequently used iterative method, in which the (i + 1)-th approximation of q_M is determined from the surface heat flow, corresponding to the i-th approximation of q_M used as a boundary condition in solving the direct problem. The comparison of both methods has revealed that the solution obtained by method I satisfies the supposed reality better than the solution obtained by method II. Method II is attractive especially for its simplicity. To eliminate the local variations of the estimated heat flow q_M, which are due to automatic transmission from the surface heat flow, a combination of method II with some smoothing procedure could be applied.

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¶rt;am ¶rt;a m¶rt;a uu mn nma q_M a uau ¶rt; muu ¶rt; . m¶rt; unm u ¶rt; ma nm nma, ma uaa umuau mna mu ¶rt;u, u nm q_M. m m¶rt; nu n uauu, auuau auau u uu q_M . m m¶rt;, mu nm ¶rt; u n a , umau: (i + 1)-a annuau nma q_M um n auma nm nma, ma i- annuauu q_M. au ¶rt;m, m nm q_M, a¶rt; n m¶rt;, mam n¶rt;naa ¶rt;mummu , u, n m m¶rt;. m m¶rt; nuam nmm. ¶rt; mau a auau a¶rt; nma q_M, uu ¶rt;mu amamu na u auau nm nma, ¶rt;a uuam au-u¶rt; m¶rt; auau.