The factors that limit the ability to retracing the distribution of sea surface elevation from altimeter return form are considered. It is shown that the current method of calculating the parameters of the distribution can not fully account for the effect of waves on the high ridges of the reflected radio pulses, which in particular leads to an underestimation of the values of skewness obtained by altimetry.

We analyze limitations in the description of radio wave scattering, which employs models of the probability distribution function of sea surface slopes on the basis of the Gram–Charlier series. It is shown that such models allow one to describe the scattering of radio waves for the incidence angles which do not exceed 5°–6° in the case of weak winds, and for the incidence angles 21°– 25° if the wind velocity is equal to 10 m/s. The combined model of the probability distribution function of sea surface slopes is constructed, which corresponds to the Gram–Charlier model in the region of small slopes, and to the Gaussian distribution in the region of large slopes.

We show that the parameters of primary radar images obtained from the Sich-1 satellite depend on the mode of survey and that the time dependence of the coefficient of correction of amplification in the channel of formation of radar signals is nonlinear. We propose to process radar images of the sea surface by using the so-called Bragg normalization of signals, which enables one to get a physically correct dependence of specific effective scattering surface on the elevation angle. We also consider a procedure of determination of the dependence of specific effective scattering surface of the sea on the wind velocity on the basis of the data accumulated by the side-looking radar of the Sich-1 satellite.

The paper examines how radar imagery of the sea surface observed by a satellite-mounted lateral-view radar is generated. The lateral-view radar on the SICH-1 satellite, in comparison with that of the KOSMOS-1500 satellite, is shown to provide better linearity of radar imagery, with identical information capabilities; the RMS strobe deviation within the survey band has been dimiished from about 30–35 to 17–20 m.

In situ data compiled during Cruise 52 of the R/VMikhail Lomonosov in May 1990 have been used to study the space-time variability of the near-surface temperature, with weak wind blowing. Temperature fluctuations within the layer of diurnal warming are shown to be primarily controlled by the heterogeneity of the wind-induced mixing and to be capable of indicating internal waves. The data on the manifestation of internal waves over a bottom rise are submitted, along with the statistical characteristics of temperature fluctuations in a cycle of solar warming.

In application to the Crimean regional centre for satellite data reception, treatment, and dissemination, we have identified the earth’s satellite-surveyed areas, with orbital heights (H) ranging from 650 to 750 km. This paper shows that for the Ukrainian territory and the Sea of Azov-Black Sea environment to be monitored, the regional centre’s receiving station must be capable of receiving radar signals from a range of about 1500 km. For typical high-speed radio lines, this may be achieved through the use of a satellite data-receiving station, with the antenna’s diameter being about 3 m.

This paper reports on the application of coastal radar systems operating in the short-wave frequency band (wavelengths from 10 to 100 m), designed to determine the parameters of wind fields over the sea surface, as well as those of waves and currents. The regularities of radar signal generation by the sea surface and the propagation of short-frequency radiowaves are discussed. The possibility of employing radars in oceanography (including CODAR systems), using ionospheric and ground beams, is considered.

The paper discusses the results of the recovery of the sea surface temperature (SST) in a large-scale hydrological test area. Data from the NOAA AVHRR radiometer (APT mode) and measurements of the surface temperature by a sensor towed by an RV, by an 'STD' sensor and by drifting 'LOBAN TM' buoys were used. The paper describes the data measurement and processing methods. Maps of the spatial distributions of the SST are compared. A numerical estimate of the accuracy of the recovery of the SST field from satellite data is given.