On the basis of long-term studies carried on both at the World Ocean and inner seas shelves the authors conclude that the term «morpholithogenesis» can be applied to shelves as well as to land areas, it reflects a natural intrinsic interaction and interrelation of geological, geomorphic and sedimentary processes of relief-formation and sedimentation.

The paper is aimed to systematize active and passive factors features depending on the climatic zonality, some azonal factors (volcanism, tides action, delta formation) being also taken into consideration, A special attention is directed to paleogeographic control of the shelves' morpholithogenesis. Some general characteristics are given of the tope» graphy and sea floor sediments with regard to various types of morpholithogenesis.

Main landforms which are modeled by rivers and reflect their channel-forming activity are the following: river valleys; channels (meandering, braided, straight); ridge-like channel bedford (shallows, p-oint bars, ripples). Each landform develops due to a certain complex of channel process factors, which control also combinations of the main varieties of channel deformations, as the forms order increases, they become less frequent and less clearly manifested. On the other hand, special features of channel-forming discharges and the channel stability makes for 2nd and 3rd order bedforms hierarchy, the channel morphology may be extremely complicate in this case. Calculations of channel-forming discharges as an integral characteristic of channel processes permit to reveal regular correlation of channel forms as well as to elucidate a significance of each phase of hydrological regime for the channel deformations.

Morphostructural analysis of the Turan Plain shows its surface reflects general structures of both mantle and basement; it accounts for widespread inherited morphostructures which often are heterogeneous.

Hypsometric levels of the plain form Inner - relatively low - and Outer-relatively high - morphostructural provinces.

Within the Voronezh Region the soil wash rate at arable 'slopes varies from 0.14 to 1.7 mm per year, The map in the paper gives soil erosion value (tons/ha) for,geomorphological regions as well as for administrative units, a sequence of erosion-preventive measures is suggested for each region.

The author subdivides the Norfolk sand ridges of the North Sea into three morphological assemblages. Dynamics of these macro- and mesoforms is considered using the comparison of maps of the same scale dated from 1956 to 1980. The dynamics within the scope of the time interval is of pulsation type, the processes being mostly reversible: shortening gives place to lengthening, dissection into separate links follows coalescence into horseshoe landforms, erosion follows the mesoforms growth and migration. The tidal current regime is proved -to be steady through years, only systems of non-periodical (remanent) components of total currents being changed. Zones of hydrodynamical activity correspond to morphological complexes, the former being under control of maximum speed of currents and pattern of the tidal current vectors roses.

Paleo-topography of the east slope of the Tungusian syneclise having been reconstructed permits to trace placers-forming processes. Most favourable conditions for diamond placers formation existed at uplands' slopes dated from Middle Carboniferous, as well as at islands, Placers remote from the source areas could be formed in the zones of contact between uplands and lowlands and also in the coastal zones of seas and large lakes. These pale-landforms are recommended for search of diamond placers.

Previously known from North Okhotsk region so-called «wrinkled» slopes are reported for the first time within North-West Okhotsk. Some results are given of the slopes analysis in Urak, Okhota, Kukhtui, Ulbea drainage basins. Large scale aerial photoes and field observations data were analysed. Aerial photographs were studied using a special device («interpretoscope») Wrinkled slopes were presumably formed under conditions of more humid climate as a result of macrosolifluctiion process.

The deepest karst chasm of the Earth is Jean-Bernard in the Savoy Alps (France), 1490 meters deep. 20 caves and chasms are deeper than 950 m, including three at the USSR territory- Snezhnaya (1335 in) and Napra (970 m) at the Bzyb Ridge, Caucasus; and Kievskaya (950 in) at the Zeravshan Ridge, Central Asia; they rank 3rd, 18th and 20th according to their depth. The longest (considering total length) karst cave is the Flint - Mammoth Cave, Kentucky, USA-34l,l km. 14 caves are longer than 40 km, including 3 at the USSR territory- Optimisticheskaya (147 km) and Ozernaya (l04,5 km) at Podolia and Zolushka in Bukovina (76 km) which rank 2nd, 4th and 6th according to the length. The paper gives revised and completed data on karst caves dimensions as compared with those published in the «Karst» by the same author («Nature of the Earth» series, Moscow, 1981).

A special type of river valleys is described at the Ukrainian shield-inherited ones; their locations coincide with ancient valleys eroded in the Pre-Cambrian basement surface, the latter being tens times wider. They are especially widespread at the Azov massif and Ovruch Highland which are continuously uprising. At the rest of the shield the inherited valleys are characteristic of few rivers or rather their segments.

Geologic-geomorphic and climatic control of the karst erosion rate is considered. The maximum mean index of general karst erosion (205.9 mm per 1000 v.) is defined at Ara bica-Bzyb massif at the southern slope, the mean value for the whole West Caucasus being about 125.5 mm per 1000 y. The rate of karst erosion at the southern slope is proved to exceed this of the northern slope by factor of 2.5, mostly due to hydrothermal regime differences. At both slopes the erosion rate is noted to increase from low mountains towards middle mountains and the lower part of alpine belt, which is accounted for by the increase in humidity and 'relief's energy. Surficial to deep karstic erosion ratio is mostly about 0.7. The ratio is about 1 at massif Fisht-Oshten, Lagonaki Plateau and Ahtsu-Alek which depends directly on the naked karst widespread over the areas.

Geomorphological indications of plastic ruptures in lithosphere are discussed. The ruptures formation is supposed to proceed similar to the theoretical scheme «neck in two-dimensional band»; they determine the developm.ent of some oceanic and continental zones of riftogenesis. The identification of the plastic ruptures in lithosphere is suggested using geometric criterion: general strike of the morphostructures within the rupture zone forms the angle about 550 with the tension direction, and the angle between conjugate plastic ruptures is about 1 100. Some cases are discussed and geomorphological consequences are considered of certain deviation from the theoretical scheme of two-dimensional plastic deformation.

A distinct zonality of topography and glacial deposits has been established at NW of the area covered with Dnieper tongue of the ice sheet, the zonal pattern being formed by four bands of marginal glacial formations (MGP). As f ar as the geomorphology of MGF is concerned, they consist of glaciomorphic sectors, which in turn include marginal zones, the latter consisting of elementary forms.

Some features of the Dnieper tongue dynamics and geological activity during deglaciation are inferred from data on the MGF geology and geomorphology, as well as from the glacial deposits occurence and lithology. The ice sheet recession at the right bank of the middle Dnieper and within the Pripyat drainage basin took place by means of areal deglaciation, with pronounced sectoral-zonal pattern.

A relation between equilibrium shoreline parameters and hydrodynamics on small storage basins has been inferred from field observations. Bearing and built-up promontories length is a function of wave acceleration distance (D) and of angle (α) of wave approach: y=kDsinα, where k is proportionality factor depending on order and deflection of the equilibrium shoreline festons. For outside shore festons (arcs) y=CR where y is length of bearing promontories, R - the arcs' radius, C - deflection value. Theoretical assumptions of B.A. Popov on the wave refraction and their impact on the shore have been confirmed by data on coasts formation at small water storage basins.

Three-dimensional mapping and its possible application to geomorphology

A new book on ancient peneplains

A new magasin

Time factor and evolution of landforms - Timescales in geomorphology / Eds. Culling ford R. A., Davidson D. A., Lewin J. Chichester - N. Y.: Wiley, 1980.IX+360 p.