За последнее десятилетие появляется все больше данных, позволяющих утверждать, что в пределах абиссальной зоны дна Мирового океана важнейшую геоморфологическую деятельность осуществляют плотностные донные течения, производящие огромную работу по переносу осадочного материала и создающие крупнейшие аккумулятивные и эрозионные формы рельефа. Некоторые аккумулятивные образования этого рода начали формироваться еще в конце мела или в самом начале кайнозоя, что указывает на исключительную устойчивость существования и действия этих течений.

Выделяются четыре генетико-возрастные категории поверхностей выравнивания -первичные поверхности, отмечающие период перехода от доплатформенного развития к платформам, догеоморфологические поверхности, вырабатывавшиеся в период формирования платформенного чехла, исходные поверхности, путем деформации которых формировался современный рельеф, молодые придолинные поверхности незавершенного выравнивания.

На основании данных о величине вдольберегового потока и дефицита наносов, вызываемого задерживающим их сооружением, прогнозируется объем размыва берега и подводного склона, а также форма кривой береговой линии. Исходными данными являются направление равнодействующей ветро-волнового режима, длина и характер сооружения.

Предложена методика построения физиографических карт с помощью ЭВМ с привлечением аксонометрических проекций. Приводится пример построения физиографической карты на участок дна Антарктики. Карта может быть использована как точная основа в геоморфологическом картировании для нанесения штрихового рисунка типа расчлененности, структурных линий и форм.

По водоразделам (3-го и более высокого порядков), лежащим в плоскости поверхности, на которой известны коры выветривания и бокситоносные отложения, восстанавливается ее вершинный уровень. Затем производится графическое вычитание современного рельефа из вершинной поверхности. Полученная таким путем система изолиний отражает мощность слоя, снесенного при разрушении исходной поверхности, и глубину пострудного (плиоцен-четвертичного) эрозионного среза.

Peculiarities are considered of material (lithologic-mineralogical) composition of slope sediments depending on slope-forming processes. Insignificant enrichment by heavy minerals was established of basal horizons of defluctional scree and defluctional slope deposits. Useful component concentration can't be expected in the sediments of solifluctional slopes.

Five stages of the Kolyma Lowland formation can be identified on the base of the geomorphic interpretation of large-scale aerial photographs as well as field studies conducted by the author at the lower reaches of the Kolyma River. The stages are as follows: Neogene-Early Pleistocene (N-Q₁), Middle Pleistocene (Q₂¹⁺²), two stage during Late Pleistocene (Q₃¹⁺² and Q₃³⁺⁴) and recent - Holocene (Q₄). Each stage left relicts of ancient valleys and deltas of the Kolyma River at the modern topography. The relicts show evidence that during the Quaternary a series of block subsidences along fault lines resulted in the river migration eastward (until it took its present position), the distance of the migration being 135 kilometers.

Some data are given on erosional resistance of loose, coherent and solid rocks, the resistance have been determined by rock erosion with horizontal jet of water, on the base of calculation of the ratio of the jet power N to erosion rate V: R=N/V. The resistance to erosion varies within wide limits - from 1 (sands) and 30 (light loam) to 1*10²⁰ (basalt, quartzite).

H. Hess's hypothesis of «encased» troughs was critisized at the beginning of this century and wasn't confirmed afterwards by a detailed research. Now it is of interest only from the historical point of view. Paleogeographical ideas based on «encased» troughs are to be discarded or ascertained by other evidence.

Developing further Penck's theory on the formation of different profiles of weathering crust at slopes, the authors distinguish steady and non-steady weathering crust, which character and thickness are determined by the correlation of weathering and denudation rates. Besides, having a steady weathering crust mostly at natural slopes it is suggested to distinguish qualitatively different types of denudation slopes basing on the completeness of the weathering crust profile. lt permits to map with high accuracy slope areas with different denudation rate and different character of the material removed. The indicators of denudation slopes' types are as follows: steepness, density of grass cover and thickness of soils profile.

On the basis of many-year data, obtained in the study of sheet wash processes at key plot, situated in the arid zone, quantitative evaluation is given of the intensity of washing processes on the slopes of different exposition. It is shown that the intensity of sheet wash is controlled by physical-geographical peculiarities of the arid zone and geological-geomorphological features of the slop.es. It is revealed that a sheet wash process in space and time is of a complicated wave-like character - a temporal accumulation takes place during a washing process as well.

Neotectonic development of Western Kamchatka does not show direct inheritance from the Bolsheretskaya depression structure. Neotectonic structure of the region is characterized with differentiated movements within separate zones. Internal and northern parts of Western Kamchatka underwent to a slow uplift controlled by uplift of Central Kamchatka mountain ridges. Maritime zone adjacent to the descending regions of the Sea of Okhotsk was relatively stable or slightly moved downward and upward. Ancient sea terraces have not been established at Western Kamchatka with the exception of low marine surfaces (up to 20 meters) within the coastal zone.

The development of the Kara Sea bottom topography is connected with eustatic Neogene-Quaternary fluctuations of the sea level. With regard to morphological and genetic .aspects the bottom topography is represented by surfaces of dissection and by surf aces of complete and incomplete planation formed both under subaerial, subaqual conditions and under «mixed» conditions of the present-day coastal zone. Besides genetically homogeneous surfaces there exist submarine valleys of different genesis and forms of coastal morphosculpture. Submarine valleys were changed to a different degree by wave abrasion-accumulative processes. Their mouths, reflecting the epochs of maximum regressions, are strictly related to certain bathimetric levels.

On the basis of new lithological geomorphological data composition and distribution is considered of marginal glacial formations, as well as the main features of lithogenesis and morphogenesis and the character of the Barents Sea shelf glaciation. Conclusion is made of the formation of submarine glacial relief by the continental glaciers of Scandinavia, Kola Peninsula, Novaya Zemlya. Spitzbergen, Franz-Josef Land and Bear Island. During the maximum Middle Pleistocene glaciation ice sheets occupied the most part of the Barents Sea shelf. During the Valdai glaciation only near-shore shelf and marginal troughs were under glaciers, while in the shelf depressions there were basins with pack and fast ice, shelf glaciers being destructed.

Morphology of Pre-Quaternary bedrock erosional surface at the Gorki Povolzhye as well as history of development of the Volga and Oka valleys and their junction area allow to determine Pre-Oka and Lower Pre-Volga to be the single, main ancient river, Pre-Unzha being its main tributary.

Развитие берегов водохранилищ

Русско-французский геоморфологический словарь

V Всесоюзное совещание по изучению краевых образований