The Siberian pole of cold is located, as is known, in the north-east of the U.S.S.R., within an extensive geodetic trapezium formed by lat. 62° and 68° N. and long. 94° and 160° E. (Fig. 1). The main factor determining its existence is an intense refrigeration of this part of the Asiatic continent during the cold half of the year and the formation of a stable centre of high atmospheric pressure. Owing to such a meteorological situation, exceptionally low temperatures of the air during a very long Winter, virtually free of snow, are replaced here by a short but warm and arid Summer. The following climatological data illustrate some of the outstanding features of this region.

Fig. 1. Map showing the position of the Siberian pole of cold

The middle part of the Siberian pole of cold area is occupied by the Verkhoyansk mountain range with peaks not exceeding 2,000 m. above sea-level. West of it is the central Yakutsk plain, which is the lowest and most eastern part of the middle Siberian upland. East of the Verkhoyansk range is a series of mountain masses of complex geological structure around the upper reaches of the rivers Yana, Indigirka and Kolyma, which includes the Yana-Oymyakon highland, the Suntar-Khayata range, the Matyushkin chain, the Cherskiy mountain system, etc. This territory includes two of the highest mountain areas which have been subjected to recent glacierization; the Suntar-Khayata and Buordakh Mountains are the highest groups with Mus-Khaya (2,959 m.) and Pobeda (3,147 m.) as the summit peaks of each range, respectively. However, the coldest regions within the area of the Siberian pole of cold are intermontane depressions within the mountain country on the rivers Yana, Indigirka and Kolyma. The coldest of these areas is the Oymyakon depression, where an absolute tempera-ture minimum of −71° C. has been registered.

Obviously, the coldest area in the world inhabited by man has long interested Russian geographers, such as A. A. Krasnov, M. I. Sumgin, A. A. Grigor’yev, etc., as well as geologists I. D. Cherskiy, A. L. Chekanovskiy and V. N. Zverev, who have studied and described this territory. However, only recently have systematic geographical researches been organized in this territory. They have resulted from the demands of the rapidly developing national economy of Yakutiya and Kolyma, the natural resources of which include very rich deposits of gold, diamonds and other valuable minerals, and the surface provides varied agricultural and biological resources. The widespread character and increase in tempo of geographical research work in north-eastern Siberia have made it one of the best-known territories in the Soviet Union.

The author has had the opportunity of visiting this area twice.Reference Gerasimov ¹ The first trip, in 1952, was to the city of Yakutsk with a short excursion into the central Yakutsk plain. The second excursion, in 1959, also started from Yakutsk flying to the northern end of the famous Kolyma route to Magadan, crossing the Yana-Kolyma mountain land en route. This paper is concerned with the general impressions of the physical geography gained on these journeys, supplemented by some data from published sources.

Owing to the great expanse and variety of the relief and geological structure, the present-day natural landscape of the Siberian pole of cold area is far from uniform (Figs. 2 and 3, p. 1093) Yet, it is quite distinctive in the same way that its climatic conditions are so special. The main features of this landscape can be shown to be due to the later phases of the last glaciation. This first of all assumes that the specific climatic features of the Siberian pole of cold are, to a certain extent, an analogue of the climatic situation, characteristic of the end of the glacial period in the mountain–plain regions of middle and eastern Europe. Special importance is attached in these situations to the combination of intense aridity and severe cold during the long winter season (caused by strong azonal factors) with a short, warm Summer, characteristic of the mid-latitudinal geographical position of the compared regions.

Fig. 2. The typical landscape of the Siberian pole of cold

Fig. 3. A typical valley of the Siberian pole of cold

Such a climatic analogy is confirmed by comparing many of the recent Siberian landforms with the old morphology of Europe.

The most important and widespread feature in the physical landscape of the territory of the Siberian pole of cold is the development of permafrost, icingsFootnote * (taryns) and masses of fossil ice, despite the limited extent of recent glacierization. As already mentioned, the latter is developed only in two mountain areas and is of a small size. Thus, the area under ice in Suntar-Khayata amounts to only 160 km.², though individual glaciers may reach several kilometres in length and are up to 100 m. thick. At the same time, below the snouts of the recent glaciers, we find very fine trough valleys, with well-preserved moraines at a distance of 20–30 km. from the fronts of the glaciers.Reference Grave ² During our trip to the Kolyma River area (in 1959) we visited a typical area of old glaciation, around Jack London Lake. We found here beautifully preserved trough valleys with a system of morainic forms, i.e. obvious traces of a recent mountain–valley ice cover.

Thus, this minor glacierized area of the Siberian pole of cold is a remnant of a somewhat larger mountain–valley glaciation, which existed here during the recent geological past. Unlike more western (as well as more eastern) territories with a much greater humidity than north-east Siberia, this area never had a thick continental ice cover. Since the ice bodies of this area were smaller in area and thickness than in adjacent regions, they were in existence for a long period owing to the constancy of climatic conditions.

Permafrost is developed almost everywhere; isings (taryns) are also very widely developed. In the mountainous areas of Suntar-Khayata and Jack London Lake they are especially thick and persistent. Masses of fossil ice are much more localized. They are especially characteristic of old alluvial plains. Within the central Yakutsk plain, for instance, masses of fossil ice are especially numerous, associated with typical thermokarstic reliefFootnote * forms in unforested areas (“allasses”).

The origin and age of these cryogenic forms raises many interesting scientific problems. The age of permafrost is the subject of much discussion amongst Soviet geographers. Some of them have advanced a number of arguments in favour of a considerable age for the perma-frost (for instance, a great thickness, intense supercooling, preservation of animal bodies, etc.). Others, on the contrary, have presented different proof of its later origin (like the freezing of flood plain deposits, etc.). It is quite possible, that both viewpoints should be combined; in other words, maybe one should assume that, having been formed a considerable time ago, permafrost within the area of the Siberian pole of cold continued to be formed under conditions similar to the present. Recent perennial river icings serve as an indirect proof of such an assertion.

Also, a matter of dispute is the question of the origin of fossil ice. Former views, that the majority of such forms represent buried old firn, or ice of atmospheric origin are losing more and more adherents. On the contrary, with greater insistence the viewpoint is advanced that these ice bodies are due to secondary infiltration (congelation ice according to P. A. ShumskiyReference Shumskiy ³ ), i.e. that they are accumulations of frozen underground waters which have penetrated through frost clefts into the internal voids of the rocks.

Anyway, the wide development of these cryogenic forms throughout the entire area of the Siberian pole of cold is an important indication of the recent late glacial regime of this terri-tory. It is more than probable that all such physical and geographical phenomena were extensively developed in the periglacial area of the Scandinavian ice sheet. However, it is obvious that their presence was not the only factor.

Recent natural landscapes in the area of the Siberian pole of cold can, generally speaking, be divided into four main types. The first type is represented by the so-called goletzy–treeless landscapes of a mountain–tundra type with a characteristic micro-relief on all more or less horizontal stretches (Fig. 4, p. 1094). At the Khotynnakh Pass (720 m. a.s.l.), for instance, in the basin of the River Kolyma, the surface of a typical goletz,Footnote † consists of the following elements:

1. Flat, bare knolls up to 2 m. in diameter and 0.5 m. in height, built of rubble, obviously squeezed out from below (occupying 30–40 per cent of the area).

2. Depressions between the knolls (up to 50 per cent of the surface) with a continuous moss-lichen cover and crippled bushes of dwarfed birches.

3. Patelliform depressions, which are actually separate expansions of large clefts with larger bushes of birch and young larch.

Fig. 4. Typical goletzy landscape; a treeless landscape of a mountain–tundra type with a characteristic micro-relief

Soil sections cut in the goletz revealed peculiar cryogenic soils, which are acidic and well-leached, with distinct signs of an intense intermixing of the soil mass by the frost action and thixotropic phenomena.Footnote * Such goletzy landscapes, exhibiting the features described above, occupy all the upper zones of the large and small uplands in this region.

The second type of natural landscape in the territory of the Siberian pole of cold is the humid frozen larch taiga (Fig. 5, p. 1094). This type of landscape is developed here on all more or less flat (poorly drained) relief elements below the goletzy belt. As an example of such a landscape a stretch can be described in the basin of the River Indigirka (Ust’-Nera), located on a high terrace-like surface built of old pebbly alluvium. We find here a sparse larch taiga with birches and willows in the undergrowth. The soil is covered by a thick moss-lichen cushion; the ground is frozen to a depth of 60 cm. and the surface is slightly hummocky. The soil is rather peculiar—cryogenic-solifluction, very acid, with obvious signs of internal movements reflected in intense intermixing of the soil mass due to freezing and thawing.

Fig. 5. Humid frozen larch taiga

A rather widely developed variety of this type of landscape is the swampy frozen larch taiga, associated with lower relief elements, as a rule undrained. A good example was seen on the Elgen state farm, also in the basin of the Kolyma River, on a low terrace above the flood plain. The taiga consists of sparse larch with an undergrowth of willow and dwarfed birch. The soil is covered by thick moss and lichen, the surface being hummocky. The ground is frozen to 40–80 cm. The hummocks consist of a mineral soil and stand above the intervening depressions to a height of 0.4–0.5 m. They consist of masses of soil pressed out from below along deep fissures. In the intervening depressions there is a peaty cryogenic-solifluction soil with a very acid reaction.

The third type of natural landscape in this region is represented by dry frozen larch taiga. These landscapes are also developed below the goletzy zone, but on well-drained stretches on gentle slopes. They are characterized by very sparse larch woods with a poorly developed grassy or moss and lichen cover. A characteristic feature of the soil is an abundance of frost cracks having the shape of large polygons. The cracks are deep and wide, being filled with loose soil material, and are wedge-shape in profile. Soil sections under such landscapes in Yakutiya and Kolyma are represented by soils of two different genetic types: on non-calcareous rocks-cryogenic, ferruginous, acid (podsolized) soils; on calcareous rocks-cryogenic alkaline (solod) soils. The genetic names of these soils indicate their characteristic features.

The fourth type of landscape in the territory of the Siberian pole of cold is the frozen cold forest–steppe. Its main occurrence is in the western part of the territory, within the central Yakutsk plain. It occupies here wide elongated declivities between ridges and slightly undulating old alluvial terraces. Separate fragments of such landscapes are also found east of the Verkhoyansk mountain range. They are associated here with flat but elevated parts of intermontane basins or with steep southern slopes. By the character of its vegetation the frozen cold forest–steppe is a meadow steppe with islets of birch clumps (“kolki”). Under its grassy patches cryogenic black meadow soils are developed, usually containing salts and solods; under the birch kolki there are patches of frozen solonetzs.Footnote † and solods.Footnote ‡ All these soils have a weakly alkaline reaction; at a shallow depth they contain carbonate salts and frozen ground. Their profiles often reveal wedge-like frost fissures and a very characteristic stratified scaly structure with signs of slight gleying, formed under the influence of fluctuations in the level of permafrost.

If the large areas of meadow flood plains and swamps are added to the forms listed above, the general picture of the main natural landscape of the territory of the Siberian pole of cold will be sufficiently complete. As has already been pointed out, it strikes the observer both by its general variety and by the contrast of its sub-types. This picture is completely unlike the monotonous landscape of “periglacial tundras,” which was previously identified with the European “late glacial” period on the one hand and the territory of the Siberian pole of cold on the other. In this connection, it is important to stress that the characteristics of the present Siberian “late glacial” period described above offer a much better basis for palaeogeogra-phical reconstructions of the old European late glacial landscapes than the speculative concepts which have been used to date, based mainly on palaeobiological data.

From this point of view, of special interest are two recent natural phenomena, charac-teristic of the territory of the Siberian pole of cold:

1. Different types and forms of cryogenic formations.

2. Surface sediments of a loess-like character.

The first have already been described in detail above and only the latter require brief-description here.

It has already been pointed out that the majority of soils associated with the frozen forest–steppe of Yakutiya exhibit a weakly alkaline reaction and have accumulations of carbonate salts in their profiles. These soil features are closely associated with the character of the parent material, represented as a rule by powdery calcareous loams. Apparently the latter are of a different origin (alluvial, glacial, etc.), since they are superficial formations in a cold Siberian forest–steppe and they always have a loess-like appearance. In my joint monograph with K. K. MarkovReference Gerasimov and Markov ⁴ I suggested calling this type of superficial deposit the recent cold facies of loess-like deposits. It is more than probable that, by virtue of their origin, such formations are recent analogues of the sheets of loessic loams which usually overlie the moraines of the old glaciated regions of Europe. For this reason, the observations given above are of certain interest in connection with the problem concerning the origin of the loesses, which still remains in dispute.