The paper represents the results of regular measurements of the main exogenous processes at three test sites in the low mountains of subtropics (Central Apennines, Western Caucasus, and Tien-Shan). A set of methods included fids, benchmarks, traps, Yang method, etc. The strongest denudation (up to 2 cm/year in the West Caucasus and up to 6 cm/year in the Apennines) takes place at those parts of badlands, which were formed as a result of human activity. The total denudation is the sum of several processes, the set of which depends on lithology, relief, and climate. On the whole, the denudation rate of the studied catchments is increased by 2–3 orders due to human impact in comparison with natural denudation rates. 

Different approaches to evaluation of riverbed stability are analyzed. It is shown that indexes like Lokhtin number, coefficient of riverbed stability by N.I. Makkaveev, and their modifications allow to reveal general features of riverbed formation and to characterize in generalized form the gradation of bed deformations and hazardous processes. Hydromorphometric relations are indicative of cross-section shape and depend on riverbed stability, but can not be used as its index; they are applied in hydrotechnical engineering calculations.

The possibilities of ecology-geomorphologic analysis of karst caves are considered, taking 76 the most frequent caves of Irkutsk amphitheatre as an example. The new definitions of cave rock relief – gallery, grotto, pit, and split are suggested. The regions with different degree of cave changes are distinguished on the base of the ecological studies of cave environment.

Long-term observations (1958-2010) of the erosion on Volgograd reservoir banks proved the linear trends of process, which evidence the lasting character of washout. In the course of abrasion-accumulation profile development the coefficient of accumulation keep minimal values, that extends the active phase of bank erosion. Characteristics of bank profiles depend mainly on currents.

An assessment of gully erosion hazard on slopes of drainage basins of small rivers and balkas was fulfilled using the method of extreme parameter calculation. Potential length of gullies was calculated that helped to divide slope drainage basins into “gully-generating” and “non- gully-generating”. The degree of number- and length-realization was evaluated for each gully-generating catch basin as well as the possible increment of gully network length. An approach to assessment of “risk” was suggested. The probability of gully rise was calculated using morphometric characteristics of slope catch basins obtained from topographical maps.

General-theoretical and methodical problems of creation and use of the global geoinformation system, which reflects the basic regularity of formation, spatial and temporal variability of suspended sediment yield of the Earth’s rivers, are considered. The role of river basins as geosystem formation in research of sediment yield is shown. Approaches to the automatic detection of river basin boundaries, methods of geoinformation system integration with thematic databases for purpose of geomorphological analysis of river suspended sediment yield are offered and tested.

Based on the analysis of the relief structure and relief-forming deposits, five geologic-geomorphologic regions were distinguished within Surgut region. Each of these regions has certain peculiarities of structure, origin and age which are reflected in the structure of the corresponding landscape. 

Morphometric characteristics and soil conditions in the catenas developed on earthen fortification ramparts of the Scythian time (2300 years BP), have been studied by complex of methods. Statistical relationships have been established between estimated mean annual rate of erosion loss in microhabitats of the pedo-topo-catenas and the slope length and steepness. In addition, specific character of soil formation in microzones of catenas has been evaluated using the coefficients of the surface insolation and relative humidity, the results being taken into account in the calculations of erosion intensity. The net result of the joint action of erosion and soil processes on the slopes can be adequately described with the help of recommended types of relief characteristics. 

Bank escarpments are high and steep slopes of river valley. The “head-on” escarpments are undermined by river, the “shadow” ones are far from riverbed. All northward escarps of the Privolzhskaya highland facing the Oka and the Volga rivers within Nizhniy Novgorod region form a single linear morphostructure with specific landscapes modeled by mass wasting. 

Toward the middle of the XX century the large stage of dynamic geomorphology development was accomplished; it was the stage of qualitative description of morphogenetic processes and generalization of these knowledge in concept of geographical cycle by W. Davis. At that time N.I. Makkaveyev began his geomorphological studies with criticism of speculative character of this concept and reasoned the want of quantitative methods. Later he put through the unique by its relevance investigation of geomorphic processes, worked out resumptive qualitative-quantitative conception of the single erosion-accumulative process in a river basin. Towards the end of his life he blocked out the frames of the theory of geographic cycle and geomorphologic landscape evolution. These works reflect the main paths of dynamic geomorphology and often anticipate other scholars’ investigations. In the result of quantitative analysis of geomorphic processes it has become possible to develop numerical 3-d models of geomorphic landscape evolution at the interaction of endogenic and exogenic processes. 

G.N. Phenin ascertained that the range of the Fergana Basin downwarping during the N-Q stage amounts to 2000–3000 m, and not to 6000–7000 m as had been previously assumed. He also suggested an expansion of the Central Asia mountain systems to be but a particular case of a general regularity; the latter consists in that stages of greater differentiated tectonic activity in particular morphostructural zones (e.g. axial, frontal, medium-high and low mountains) alternate  with stages of general uplift or subsidence of the entire mountain system.