By G. I. Marchuk, B. A. Kagan (auth.)

ISBN-10: 9027725527

ISBN-13: 9789027725523

ISBN-10: 9400925719

ISBN-13: 9789400925717

ISBN-10: 9401076618

ISBN-13: 9789401076616

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Variations of the Earth's gravitational potential U 0 and of the tidal potential U 2 produced by them will be equal to ~. {JU oIOr and U', respectively, so that the total gravitational potential U will now be equal to U =Uo+~. 3) Let g be the gravity acceleration answering to the total gravitational potential. g, between g and go will then describe the tidal variations of the gravity force on the elastic Earth without the ocean. If ~. , by Garland [9], U' - r- 3 • At the same time, the tidal potential U 2 is related to r by the quadratic dependence U 2 - r2.

Satellite altimetry can prove to be an effective means of attaining the desired objective. A radiolocating altimeter mounted on a satellite measures the instantaneous height of the ocean surface relative to the Earth's center. e. the sum of the geocentriC heights of the geoid and stationary perturbations of different origin, and subject the found values of height differences to spectral or standard harmonic analysis, it will be in principle possible to obtain the parameters of the ocean tide at any given point.

It should be noted that the position of none of them can be regarded as established with sufficient reliability. The reason is again the absence, or in some cases the uncertainty, of observation data in the deep ocean. Let us illustrate the aforesaid taking as an example the pattern of cotidallines Methods and Results of Experimental Studies of Ocean Tides 23 in the north-western and north-eastern parts of the Indian Ocean. In the first, according to Dietrich, there is an amphidrome with clockwise rotation with its center at 10" N, 63° E, and in the second a nodal zone extends from the eastern coast of Sri Lanka to the northern extremity of Sumatra.

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Dynamics of Ocean Tides by G. I. Marchuk, B. A. Kagan (auth.)

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