Both theoretical studies [3; 4; 5] and in situ measurements [6; 7; 8] can be used for studies related to the regularities of signal propagation and the formation of acoustic fields in liquid and solid half-space. At the same time, other complex problems such as ocean thermometry and the location of and communication with underwater objects located in the water space and on the seabed can be solved in parallel [9; 10; 11]. In the water environment, the depth of the sea and the size of the near-surface channel play the main role [12]. It is clear that with a decrease in the frequency of the radiated signals, the axis of the sound channel plays a smaller role, and at certain frequencies, the boundary of the density jump can be transparent for the radiated signals. It is clear that in this case the main radiated hydroacoustic energy will propagate both in the water and move into the seabed in the form of volumetric seismoacoustic waves; it also propagates in the form of attenuating and unattenuating surface waves of Rayleigh type along the \"water-bottom\" boundary. When solving tomographic problems, it is important to know the relationships of all the components propagating in the water media, at the bottom and at the \"water-bottom\" boundary. These relationships are especially interesting when performing works on a shelf of monotonously decreasing depth and when operating radiators that generate signals of varying complexity in the low-frequency audio range. In recent years, we have conducted experiments using low-frequency hydroacoustic signals of various frequencies, which allowed us to better understand the patterns and mechanisms of formation of the acoustic field on the shelf, as well as the transfer of energy from the liquid to the solid half-space and vice versa. These studies were carried out using a complex [13] consisting of coastal laser-interference measuring systems recording seismic signals and low-frequency acoustic radiation systems of 22, 33, and 245 Hz. In addition, for measuring the characteristics of the acoustic fields created by the radiators, the complex includes several autonomous receiving systems with hydrophones. Thus, one work [14] describes an experiment on the emission of harmonic signals with a frequency of 33 Hz, generated by a low-frequency hydroacoustic radiator in Vityaz Bay, which, having passed along the shelf of decreasing depth and having transformed into seismoacousticsignals of the upper layer of the earth's crust and bedrock of Shultz Cape, excited hydroacoustic signals at the corresponding frequency in the waters of the shelf of the open part of the Sea of Japan. The experimental data were compared with a model, constructed taking into account the geological structure of the water areas, as a result of which the mechanisms of the transformation of hydroacoustic energy into seismoacoustic and back were described. In [15], we considered some patterns of hydroacoustic signal generation in the bay, the depth of which is comparable to half the wavelength of the radiated harmonic hydroacoustic signal (22 Hz wavelength of about 68 m). When studying the patterns of radiated hydroacoustic signals transformation into seismoacoustic signals at the corresponding frequencies recorded by the laser strainmeter (V.I. II'ichev Pacific Oceanological Institute, Far Eastern Branch, Russian Academy of Sciences, 690041 Vladivostok, Russia) located at Shultz Cape in the Sea of Japan, we believed that the laser strainmeter registered mainly surface Rayleigh waves, which propagate in water, along the \"water-bottom\" boundary, and on land--along the \"Earth's crust-air\" boundary. In the described case, the sea depth is approximately two times smaller than the length of the hydroacoustic wave. This is a special case of hydroacoustic signal generation, in which the elastic bottom plays a certain role in the value of the radiated hydroacoustic signal's amplitude. The considered case is not entirely typical when performing such hydroacoustic work.