Anisimov and Pospelov: The Landscape and Geobotanical Characteristics
311
majority of cryomorphogenetic processes form dynamic series, in which non-cryogenic
phenomena play determining or secondary roles. Many of the issues surrounding the nature of
cryogenesis remain unclear; however, it is possible to define the general tendency of their
development for a given region.
Almost all cryogenic processes develop only in fine grained soils. It is therefore of primary
importance to consider cryogenic weathering for mountain regions. Together with other
exogenic processes, cryogenic weathering results in the formation of cryoclastites and
cryoclastopelites (Popov et aI., 1985); that is, the monolithic bedrock is destroyed. Certainly,
the most important factor is the seasonal freezing and thawing of the ground, though
meteorological processes (precipitation, wind) playa role as well. As a result of the former
process, boulder debris is formed. Further degradation occurs with spatial irregularity,
depending on the durability of the bedrock, snow cover depth, intensity of aeolian processes
and vegetation. Initial cryogenic forms are sorted soils (or patterned ground). At first, sorted
areas form among coarse material (debris islands); stone pavements may also form among
coarse materials. In the researched region, these forms were observed at the highest elevation
study plots or on stable screes. As secondary weathering processes, cryogenic ground sorting
results in stone polygons and in sorted stone stripes on the slopes. When the sorting locations
are expanded and leveled, the influence of snow intensifies and gravel circles, circumscribed by
coarse material, and gravelly hummocks with cracks between them, faintly pronounced in
nanorelief, are formed. These processes improve the conditions for vegetative growth. The role
of vegetation in nanorelief formation gradually increases. Plants act as thermal insulation and
contribute to the accumulation of water. The vegetative cover has been repeatedly shown to be
determining, or at least essential, in the formation of permafrost (Tyrtikov, 1979; Common
permafrost science, 1974). Vegetation, and especially moss, promotes the accumulation of
moisture in cracks and the formation of ice wedges in autumn and winter. In parallel with these
processes, cryogenetic weathering continues, leading to the formation of silt-gravel and silt
(fine-earth) soils (cryopelits; Popov et aI., 1985). After the soil transformetion to loam, the role
of snow and wind erosion is reduced (as these patterned soils are observed only in locations
where snow cover depth is significant) and the role of ice-segregation in the thawing layer is
increased. Cryoturbation in the centre of sorted circles gradually decreases, but is amplified on
their periphery. The following evolutionary stages are (consistently): hummock-spotty, spottyhummocky and hummocky tundra. Within the limits of the studied region, these features are
most widely distributed at low elevations within the lake basin and on degraded fragments of
lake terraces. Any subsequent ice-segregation activity results in thermo karst and gelifluction
processes.
Examples of these processes are most distinct at low hypsometric levels. First, striped tundra
is evident, which we name dellic. The term "dell", however, also has a general geological
treatment including non-permafrost territories, and we try, therefore, to avoid it. The shallow
(less than 1.2m), wet and flat stripes form drainage channels between their ridges and are one
of the most widespread forms of microrelief in the lake basin. They represent one form of
thermokarst activity, which is well developed on slopes with an ice-rich horizon. Nevertheless,
it is possible to show that the dellic complexes are currently rather stable. Thaw slumping
gelifluction was observed at only one location, but its genesis remains subject to examination.
Thermokarst processes are distributed rather sporadically throughout the lake basin and occur
only at a low hypsometric levels.
In the river valleys, cryogenic forms are rarely found, except in the intermountain depression
of the Krasnaja river mouth. Here, on the lacustrine-alluvial terrace, various forms of polygonal
bog complexes are found, from homogeneous and typical low-centered polygons to paisa bogs.
The latter are relicts of a warmer epoch, as the formation of typical paisa bog complexes is now
possible only in the southern part of Taimyr. The formation of such complexes requires
311
majority of cryomorphogenetic processes form dynamic series, in which non-cryogenic
phenomena play determining or secondary roles. Many of the issues surrounding the nature of
cryogenesis remain unclear; however, it is possible to define the general tendency of their
development for a given region.
Almost all cryogenic processes develop only in fine grained soils. It is therefore of primary
importance to consider cryogenic weathering for mountain regions. Together with other
exogenic processes, cryogenic weathering results in the formation of cryoclastites and
cryoclastopelites (Popov et aI., 1985); that is, the monolithic bedrock is destroyed. Certainly,
the most important factor is the seasonal freezing and thawing of the ground, though
meteorological processes (precipitation, wind) playa role as well. As a result of the former
process, boulder debris is formed. Further degradation occurs with spatial irregularity,
depending on the durability of the bedrock, snow cover depth, intensity of aeolian processes
and vegetation. Initial cryogenic forms are sorted soils (or patterned ground). At first, sorted
areas form among coarse material (debris islands); stone pavements may also form among
coarse materials. In the researched region, these forms were observed at the highest elevation
study plots or on stable screes. As secondary weathering processes, cryogenic ground sorting
results in stone polygons and in sorted stone stripes on the slopes. When the sorting locations
are expanded and leveled, the influence of snow intensifies and gravel circles, circumscribed by
coarse material, and gravelly hummocks with cracks between them, faintly pronounced in
nanorelief, are formed. These processes improve the conditions for vegetative growth. The role
of vegetation in nanorelief formation gradually increases. Plants act as thermal insulation and
contribute to the accumulation of water. The vegetative cover has been repeatedly shown to be
determining, or at least essential, in the formation of permafrost (Tyrtikov, 1979; Common
permafrost science, 1974). Vegetation, and especially moss, promotes the accumulation of
moisture in cracks and the formation of ice wedges in autumn and winter. In parallel with these
processes, cryogenetic weathering continues, leading to the formation of silt-gravel and silt
(fine-earth) soils (cryopelits; Popov et aI., 1985). After the soil transformetion to loam, the role
of snow and wind erosion is reduced (as these patterned soils are observed only in locations
where snow cover depth is significant) and the role of ice-segregation in the thawing layer is
increased. Cryoturbation in the centre of sorted circles gradually decreases, but is amplified on
their periphery. The following evolutionary stages are (consistently): hummock-spotty, spottyhummocky and hummocky tundra. Within the limits of the studied region, these features are
most widely distributed at low elevations within the lake basin and on degraded fragments of
lake terraces. Any subsequent ice-segregation activity results in thermo karst and gelifluction
processes.
Examples of these processes are most distinct at low hypsometric levels. First, striped tundra
is evident, which we name dellic. The term "dell", however, also has a general geological
treatment including non-permafrost territories, and we try, therefore, to avoid it. The shallow
(less than 1.2m), wet and flat stripes form drainage channels between their ridges and are one
of the most widespread forms of microrelief in the lake basin. They represent one form of
thermokarst activity, which is well developed on slopes with an ice-rich horizon. Nevertheless,
it is possible to show that the dellic complexes are currently rather stable. Thaw slumping
gelifluction was observed at only one location, but its genesis remains subject to examination.
Thermokarst processes are distributed rather sporadically throughout the lake basin and occur
only at a low hypsometric levels.
In the river valleys, cryogenic forms are rarely found, except in the intermountain depression
of the Krasnaja river mouth. Here, on the lacustrine-alluvial terrace, various forms of polygonal
bog complexes are found, from homogeneous and typical low-centered polygons to paisa bogs.
The latter are relicts of a warmer epoch, as the formation of typical paisa bog complexes is now
possible only in the southern part of Taimyr. The formation of such complexes requires