Many river valleys have steep and smooth bends. The analysis of their pattern and comparison with gйomorphologie situation, especially with the morphostructure, shows five possible causes of river valley turnings: 1) the incised meanders; 2) the impact of rising morphostructure; 3) crossing of the river valley by faults; 4) tectonic bend of land surface; 5) the river captures.

The paper concerns the classification of morphological types of the shallows: shallow-ridges, accessory shallows, shallow-placers, and shallow-spits. The formation conditions for each type of the shallows were determined. Shallows transformation from the flood to the mean water is described. Adjacent shallows are conjugate in their formation: the upper one is washing out while the lover one is accumulating. Position of the shallows in the hierarchy of channel forms is shown.

Paleogeographical reconstructions of the late Pleistocene glaciation of the Chagan-Uzun massif, which separate Chuya and Kurai intermountain depressions, are represented. The ice basin in the Jeldyskel depression on the top of the Chagan-Uzun massif had the maximum square about 80 km² and ice thickness about 100 m. The generation of this glacier happened without preliminary stage of mountain glaciers accumulation and its development proceeded with the weak morpholithogenesis in the depression, partly dew to low-grade of its slopes. The conformity of the Kyzylchin outlet and the Chagan-Uzun glaciers moraines allows considering the Chagan-Uzun massif and the foot of the South-Chuya ridge as an area of the same glaciation - the first of the Late Pleistocene glaciations. The generation and evolution of the Jeldyskel ice basin is the result of both the depression of snow-line in the cold epoch in the beginning of the Late Pleistocene and considerable tectonic uplift of the Chagan-Uzun massif by this time.

Mechanisms of slope formation are analysed on the example of the rock massif Shishinskaya Pissanitsa. Thin clayed layers alternating with sandstones form series of micro-bases of denudation; hence different parts of the slope develop independently. After uncovering the lowest of such micro-bases the slope retreats parallel by the side-cutting (according to L. King).

The paper deals with the dynamics and intensity of the eolian processes during the cold periods from 1989 till 2008 in agricultural landscapes of the southeastern part of the West-Siberian Plain. It was shown that the deflation of the arable soil developed annually, had intermittent nature, different intensity and focal spread. The accumulation of eolian deposits occurred everywhere and was associated with local, regional and global atmospheric processes.

The complex cover of eolian deposits is wide-spread in the southern West Siberia. It overlies all landforms except the first river terraces and the floodplains. The upper part of the cover consists of loess. The ridges on the Kulunda and Baraba plains were formed by the irregular accumulation of sands transported by predominant western winds. The last arid epoch of the Northern hemisphere ("Mangyshlak" aridization) was the time of the last glaciation decay.

The study of the morphogenetic structure of the areal morphological complexes (AMC) in the Ryazan' region demonstrates: 1) each basic AMCs is characterized by a specific organization of interconnected morphogenetic elements; 2) the most part of the small AMCs, which comprise the basic ones has a rather simple structure; 3) the neighbouring basic AMCs and the most part of small AMCs are strongly distinguished by their structure; 4) the absence of the differences between neighbouring small AMCs, raise question about the validity of their boundaries.

The Shulgan-Tash karst system includes two main groups of elements: surface ones (karren, potholes, ponors, karst depressions, dry streams, karst lakes) and underground ones (grottos and caves). One of the largest caves of the Ural - Kapova cave, with the unique palaeolithic painting, is located here. The Shulgan-Tash karst system has vertical amplitude of 442 m; its coefficient of the areal karstification reaches 0.15%.

The morphology of channel and flood-plain has the large influence on the dynamic of their streams. We brought in a new integral morphometric characteristic - the angle a between geometric axes of flood-plain and channel. We suggested a new method of channel stream average velocity calculation for different relative depths of the channel, based on the empirical graphical dependences and the use of this characteristic. The flood-plain constituent of the stream may also be evaluated by empirical graphical dependences and by the data of relative flood-plain areas and their coefficient of roughness.

The Paleo-Volga River valley existed within the present Lower Volga basin during the last 600-700 ka. Periodically its lower parts were transformed into a long and deep ingressive estuary. Over the last 16 ka there have been 6 marine (estuarine) phases within the Volga-Akhtuba valley corresponding to transgressive phases of the Late Khvalyn and New Caspian ages. There are pronounced traces of the 4 transgressive-regressive stages of the Late Khvalyn and New Caspian ages in the present Volga-Akhtuba floodplain topography, correlated with the three generations of ancient floodplains, whose age are decreasing downstream from 16 to 1.5 ka.

There are many paleo-incisions in the Manych depression, which vary in morphology, origin, and age. They were formed by the erosion and abrasion processes under the conditions of unstable sea level of the Caspian and the Black seas. Paleo-incisions may be subdivided into two groups: (1) two-sided forms mainly connected with bottom erosion of rivers and ancient water fluxes, (2) one-sided forms, caused by lateral abrasion and erosion of ancient bayous. Paleo-incisions occur through the whole Pleistocene stratigraphic range of the Manych and often constitute multi-aged systems. The largest of them occur in the Lower and Middle Pleistocene.

The landscape evolution of the San-Pablo river valley near the Serro-Gordo volcano during the end of the late glaciation is described. Stages in the development of landforms, soils, and catenae were distinguished. In the landscape evolution different rhythms and trends can be seen. Climatic changes - trend from warm OIS 3 to maximum of glaciation (LGM) and late glaciation (LGT) - OIS 2, and to new interglacial (Holocene) OIS 1 - played a leading role in the landscape formation. During this time aridization took place. At the limit of glaciation and interglacial time the tracers of disastrous water flow were found. It guttered down from the slopes of the Serro- Gordo to the San-Pablo river valley.

Paper states how the voluminous edition "History of relief development in Siberia and Far East" was created.

To the 80th anniversary of Pavel A. Kaplin