Where is the warmest climate in Siberia? The climate of eastern Siberia

Climate of Siberia

Siberia is known to be one of the coldest countries in the world. The most characteristic features of its climate are explained primarily by its geographical position. Siberia occupies the northern part of the Asian continent and lies in the northern and partly middle latitudes of the Soviet Union, within the belts of a temperate and cold climate. Many thousands of kilometers separate the territory of Siberia from the shores of the Atlantic Ocean, high mountain ranges rise on its southern and eastern borders and prevent the penetration of warm and humid winds from the seas located south and east of the Asian mainland. Only from the north, from the Arctic Ocean, masses of dry and cold Arctic air reach far into the depths of Siberia.

Almost everywhere north of the Siberian line railway on the plains, plateaus and mountain ranges, a very cold winter continues for more than six months, in the middle of which frosts of 40–50 ° C, and in some places even 60 ° C, occur. However, summer in Siberia (with the exception of only its most northern regions) is warm, and in the southern half it is sometimes even hot and rather long. Already at the end of May, and in the north in June, under the bright rays of the sun, there is a strong warming of the land surface. Mercury in the thermometer rises during the day to 20–25°, and in early July, in the steppe zone, the heat often exceeds 30–35° for several days in a row. In almost the entire territory of Siberia, the summer is much warmer than in the corresponding latitudes of the European part of the Soviet Union. In Yakutsk, which lies at the same latitude as Leningrad, the temperature in July is on average 2–3° higher than on the shores of the Gulf of Finland; the temperature difference between Kyiv and Semipalatinsk is approximately the same.

The transitions from summer to winter and from winter to summer are rapid in Siberia. Therefore, the duration of the transitional seasons - spring and autumn - is generally short.

The climate of Siberia is sharply continental everywhere. The difference between the average temperatures of the coldest and warmest months in its various regions ranges from 35 to 65°, and the absolute temperature amplitudes in such areas as Eastern Yakutia reach 95–105°. The continental climate of Siberia is also manifested in rather sharp temperature fluctuations during the day and a relatively small amount of precipitation falling in most areas mainly in July and August.

Huge area and big differences relief is also determined by a significant variety of climates in individual regions of Siberia. This is primarily due to the great length of Siberia from north to south and therefore the unequal amount of incoming solar heat. Some southern regions of Siberia receive no less solar heat than the southern regions of Ukraine and the lower Volga region. It's different in the north. As you know, about a quarter of the territory of Siberia lies north of the Arctic Circle. In winter here for several weeks, and in the very north - two or even three months, the sun does not rise above the horizon at all and there is a "dark time" of the polar night. At the end of January, the length of the day begins to increase rapidly, and at the end of May - beginning of June, a multi-week polar day sets in. A huge disk of the sun during the day describes a full circle, not hiding behind the horizon.

Polar day and night are distinguished by very small fluctuations in daily air temperatures. In winter, both "day" and "night" are almost equally cold. With the onset of summer, with round-the-clock illumination and a continuous influx of solar heat, the melting of the snow cover and the development of plants are very rapid here.

The climatic differences between the western and eastern regions of Siberia are also very significant. The climate of Eastern Siberia is generally more continental than in the western part, to the plains of which air masses often reach from the Atlantic Ocean. True, when passing over Western Europe and the Russian Plain, they lose a lot of moisture, and in winter, in addition, they also get very cold. Nevertheless, the masses of Atlantic air over the territory of Western Siberia are still more humid than the continental air of Eastern Siberia. That is why in the western part there is more rainfall.

The difference between the climates of Western and Eastern Siberia is also explained by the different nature of their relief. In Eastern Siberia, with its high mountain ranges and plateaus separated by deep valleys, masses of heavier cold air accumulate and stagnate in depressions. This phenomenon is especially pronounced in winter. At this time, in clear and frosty weather, radiation from the surface is very a large number heat. Heavy supercooled air flows into the hollows, where it cools even more. It is this circumstance that explains the extremely low temperatures. winter months and the phenomena of so-called inversions (Usually, with height, there is a gradual decrease in temperature, averaging about 0.5–0.6 ° for every 100 m of ascent. But there are cases when the temperature rises to a certain height, and sometimes quite significantly. So, for example, at the Mangazeya mine, located in the Verkhoyansk ridge, at an altitude of about 1 thousand meters, the average temperature in January is -29 °, in Yakutsk, located at the foot of this ridge, -43 °, and in Verkhoyansk even -50 °. called temperature inversion), which are especially characteristic of intermountain depressions in Eastern Siberia.

The relief also has a very significant influence on the distribution of precipitation. It is known, for example, that slopes facing moist winds receive much more precipitation than opposite slopes of the same ridge. Thus, in Western Altai at an altitude of 1200–1500 m, sometimes more than 1500 mm of precipitation falls annually (In recent years, Siberian hydrologists, according to the amount of water flowing into rivers, have established that in some areas of Western Altai and Kuznetsk Alatau, up to 1800 and even 2 thousand mm of precipitation, i.e., almost as much as in the humid subtropics of the Black Sea coast of the Caucasus), and at the same height in the basins of Eastern Altai, only 200–300 mm. No less striking example in this respect is the Khamar-Daban ridge. Its northwestern slopes facing Baikal receive up to 800–1000 mm of precipitation per year, and the thickness of the snow cover in winter here reaches 1.5–2 m. On the opposite, southeastern slope, less than 300 mm falls per year; due to the lack of snow, it is far from possible to ride a sleigh there every winter.

Many of the features of the Siberian climate that we have noted are due to the distribution of atmospheric pressure and the circulation of air masses over the territory of Siberia and neighboring countries. It is known that the land during the cold period of the year cools faster and more intensively than the surface of the seas and oceans. For this reason, usually from the beginning of autumn, the air above it becomes colder and denser, and the so-called anticyclonic area of ​​high atmospheric pressure gradually forms. The Asian continent is one of the most significant and compact land masses in the world. Therefore, the process of formation of increased pressure in winter in the center of the mainland is extremely pronounced, and the pressure of the atmosphere here is much higher than in the seas surrounding the mainland.

Already at the end of September, the pressure of the atmosphere over the territory of North-Eastern Siberia becomes relatively high, and by the end of autumn, the area of ​​increased pressure gradually spreads to the whole of Eastern Siberia. The pressure is highest in Transbaikalia and the eastern part of Yakutia. In January, it reaches an average of 770–775 mm here. In connection with the emergence of an area of ​​high atmospheric pressure, the penetration of masses of moist air from neighboring territories stops here. This circumstance explains the prevailing winter in Eastern Siberia, clear, almost cloudless, but very cold and dry weather. Winds at this time are very rare and differ in very insignificant force.

Unlike Eastern Siberia, over the northern part West Siberian Lowland and especially over the seas of the Pacific Ocean, the pressure during the cold season is lower and sometimes does not exceed 760 mm. Due to the large difference in atmospheric pressure, cold and dry air from the East Siberian region high pressure spreads to the west and to the east. Its penetration causes a significant cooling in neighboring regions, which in the west extends even to the territory of the European part of the USSR.

In the warm season, when the land heats up more than the water surface, the pattern of pressure distribution over Siberia changes dramatically. Already in April, the pressure over the mainland begins to decrease rapidly and the Siberian anticyclone disappears. By the middle of summer, in North Asia, almost everywhere the air pressure becomes below normal and does not exceed 755–758 mm on average. In contrast to winter in the north, over the seas of the Arctic Ocean, and in the west - in the European part of the Union, the pressure at this time is somewhat higher. Therefore, air masses often come to Siberia in summer either from the north (arctic) or from the west (atlantic). The former are most often cold and dry, while the latter are more humid and bring a significant part of the summer precipitation.

The wind regime is also closely related to the seasonal distribution of pressure and air masses. The coldest months of the year (December, January and February) are characterized by comparatively calm weather throughout almost the entire territory of Eastern Siberia. Windy days in winter are usually accompanied by a noticeable increase in temperature and a small amount of precipitation.

In Western Siberia, where areas with relatively high pressure are located in the south in winter, and the region reduced pressure formed over the Kara Sea, southerly winds prevail. They reach their greatest strength in the middle of winter. It was at this time that snowstorms and blizzards rage in treeless regions in the south of Western Siberia and in the tundra zone on the shores of the Arctic Ocean. With a huge wind speed, sometimes reaching 30-40 m / s in the north, swept snow and ice crystals fill the surface layers of air so much that even five steps away you can no longer see anything; movement in a blizzard becomes almost impossible. It is especially dangerous to be caught in the tundra, far from settlements by the so-called "dark blizzard". It starts suddenly and often does not subside within five to ten days, only at times somewhat weakening. During a strong blizzard, the air temperature almost always rises by 10–20°C.

The winds during the warm Siberian summer have a completely different character. At this time, northwest and north winds prevail everywhere. The first of them are humid and bring a large amount of precipitation in the form of rains, and the relatively cold winds of the northern rhumbs cause a strong drop in temperature in summer, and in May, June and August are sometimes accompanied by frosts.

Due to the significant diversity of the surface in some places in Siberia, especially in mountainous regions, local winds are also observed. In Altai, the Sayan Mountains and the mountains of North-Eastern Siberia, they often take on the character of foehns (foehn is a relatively warm and dry wind blowing from the slopes of the mountains into the valleys. It occurs if different pressures are established over the opposite slopes of the ridge, or when over the crest of the ridge, the pressure is higher than on its sides. Descending from the slopes, the air, as a result of compression, becomes very hot and becomes dry. In the mountains of Siberia, this phenomenon is most often observed in winter. There are cases when, during a strong foehn, the air temperature in the valley increased by 20 and even 40°. So, for example, on the night of December 2-3, 1903, as a result of a foehn, the temperature in Verkhoyansk rose from -47 ° to -7 °. Foens often cause thaws, and in spring - rapid melting of the snow cover). In the basin of Lake Baikal, which is surrounded on all sides by mountain ranges, very peculiar winds blow. Many of them are remarkably consistent in direction. Such, for example, is the northeast wind "barguzin", the southwest, or "kultuk", and the north, called by the local population "angara", or "verkhovik". The very strong wind “sarma” blowing in autumn and winter in the middle part of the lake is especially famous. During the "sarma" on Baikal, a storm arises, sometimes lasting several days. On frosty days, clouds of wind-blown spray freeze in the air, and ships are often covered with a thick layer of ice. Sometimes, as a result of a storm caused by a "sarma", fishermen's boats die on Lake Baikal.

In Siberia, almost everywhere the average annual temperatures below 0°. In some northern regions, they even fall below –15–18° (Novosibirsk Islands – 19°, Sagastyr –17°, Verkhoyansk –16°). Only in the most southern parts In the West Siberian Lowland, already within the northern regions of the Kazakh SSR, the average temperature of the year rises to 2–3°C.

The severity of the Siberian climate is determined primarily by the very low temperatures of winter and its long duration. Nowhere else on the globe does winter get so cold, and only some areas in central Antarctica or the Greenland ice sheet can rival Siberia in the harshness of their winters. However, there have not yet been observed such cold weather as occurs in January in Oymyakon or Verkhoyansk.

Even in the relatively "warm" winters of the southern and western regions In the West Siberian Lowland, the average January temperature does not exceed -16–20°C. In Biysk and Barnaul, located almost at the same latitude as the capital of Ukraine, in January it is 10° colder than in Kyiv. On some days, temperatures of -45 ° can be everywhere in Siberia; Fifty-degree frosts were observed even in the south of Western Siberia - in Barnaul, Omsk, Novosibirsk.

Winter is especially cold in Eastern Siberia, over the territory of which at this time there is, as we already know, an area of ​​high air pressure. Throughout the winter, the weather here is clear, cloudless and absolutely windless. Under conditions of such weather, an exceptionally intensive cooling of the surface occurs, especially at night. Therefore, in winter in most of the territory of Yakutia long time temperatures are kept below -40° and there are no thaws. Especially strong colds are in closed basins, in the region of Verkhoyansk and Oymyakon. The average temperature in January here is lower - 50°C, and on some days frosts even almost reach 70°C.

Winter in the eastern part of Siberia is on average twenty degrees colder than in the western part. Even the northernmost sections of Western Siberia, located on the coast of the Kara Sea, at this time sometimes turn out to be warmer than some regions of Eastern Siberia, which lie almost 2 thousand km south of them. So, for example, in Chita the air temperature in January is much lower than on the banks of the Gulf of Ob.

Due to the constancy of the weather, the great dryness of the air, the abundance of clear, sometimes even sunny days and the absence of winds, low air temperatures in winter are relatively easily tolerated by the local population. An invigorating thirty-degree frost is considered by a resident of Krasnoyarsk or Yakutsk to be as common as a 10-degree frost in Leningrad. Stepping off a train that arrived from Moscow or Leningrad, in a large Siberian city you will not even immediately feel that the temperature here is 20–25 ° lower. The unwinter bright sun floods the snow-covered surroundings with its rays, the air does not stir, there is not a cloud in the sky. From the roofs, sometimes already in early March, drops begin, and a person who is not accustomed to the peculiarities of the Siberian climate looks with distrust at a thermometer showing -15, or even -20 °.

Especially often clear and sunny days are observed in winter in Eastern Siberia. The number of sunny days and the duration of hours of sunshine in many areas of Southern Transbaikalia are much greater than, for example, in Odessa or the Crimea.

As we have already said, summer in Siberia is warm, and in the south, in the steppe zone and in Transbaikalia, it is hot. The average temperature is the most warm month, July, even in the forest zone varies from 10–12° at its extreme northern limit to 18–19° in the south. Even higher temperatures were observed in the steppe regions, where July is warmer than in Ukraine. Only in the north, in the coastal tundra and on the coast of the Arctic Ocean, July and August are cool, for example, in the area of ​​​​Cape Chelyuskin, the average temperature in July is only + 2 °. True, on some, the warmest days, the temperature in the tundra can sometimes rise to 20-25 °. But there are few such days in the north in general.

At the beginning of summer, even in the southernmost regions of Siberia, short-term night frosts are possible. In some areas, crops of grain crops and vegetables often suffer from them. The first autumn frosts usually occur already at the end of August. Spring and autumn frosts significantly reduce the duration of the frost-free period. In the north, this period is everywhere shorter than two months, in the taiga zone it lasts from 60 to 120–130 days, and only in the steppes from late May to mid-September, frosts are usually not observed or are extremely rare.

Most of the precipitation that falls in the form of rain and snow in Siberia is brought by air masses coming here from the west and northwest. Wet east winds from the seas of the Pacific Ocean, fenced off from the territory of Eastern Siberia by a strip of rather high mountain ranges, they occasionally penetrate only into the eastern regions of Transbaikalia. Unlike the rest of the territory of Siberia, only here at the end of summer heavy rains fall, brought from the east by monsoon winds.

The amount of precipitation falling in Siberia generally decreases markedly towards the east. Even in the forest regions of Western Siberia, which are richest in precipitation, they are somewhat less than in the middle zone of the European part of the Soviet Union. Even less precipitation falls in Eastern Siberia, where in the taiga zone the population of some regions is forced to resort to artificial irrigation of their fields and hayfields (Central Yakutia).

There is also a significant change in the amount of precipitation in different geographical areas. Relatively few of them are received by the northernmost, tundra regions of Siberia. In the tundra of the West Siberian Lowland, no more than 250–300 mm falls annually, and in Northeastern Siberia, 150–200 mm. Here, on the coast of the Chukchi and East Siberian Seas, as well as on the New Siberian Islands, there are places that receive less than 100 mm of precipitation per year, that is, less than some desert regions of Central Asia and Kazakhstan. A little more (from 300 to 400 mm) precipitation is received by the forest-tundra regions of Western Siberia and the taiga of the Central Siberian Plateau.

The greatest amount of precipitation in the plain areas falls on the taiga zone of Western Siberia. Within its limits, more than 400 mm of precipitation falls throughout the year, and in separate places even more than 500 mm (Tomsk 565, Taiga 535 mm). A lot of precipitation (500-600 mm per year) also falls on the western slopes of the Central Siberian Plateau - in the Putorana Mountains and on the Yenisei Ridge.

In the south, in the forest-steppe and steppe zones, the amount of precipitation decreases again, and less than 300 mm fall on the driest regions in the middle reaches of the Irtysh and southern Transbaikalia.

Throughout Siberia, precipitation falls mainly in the summer as rain. The warm period of the year in some places accounts for up to 75–80% of the annual precipitation. The maximum amount of precipitation in most of Siberia falls in July and August. Only in the south, in the steppes of the West Siberian Lowland, June is usually the rainiest month.

The predominance of precipitation in the form of summer rains is generally favorable for the development of vegetation and Agriculture. In most parts of Siberia, rains bring moisture to plants just at the time when they need it most. In connection with the relatively small evaporation from the soil surface, this moisture is almost everywhere quite sufficient. However, some southern steppe regions of Siberia, where the maximum precipitation occurs in June and where strong winds noticeably increase evaporation in spring, sometimes suffer from drought. On the contrary, in those regions where there is a relatively high amount of summer rains, they sometimes make haymaking and harvesting difficult. Summer precipitation falls mainly in the form of long continuous rains, and only in the most eastern regions there are often heavy showers. The maximum amount of precipitation falling per day usually does not exceed 30–50 mm. However, there are cases when up to 120-130 mm fell per day (Kamen-on-Obi, Babushkin). Heavy showers are especially characteristic of the eastern part of Transbaikalia, where they occur at the end of summer almost every year. These showers often cause significant summer floods here.

With regard to the precipitation regime in many regions of Siberia, "year after year does not occur." This applies both to the annual amount of precipitation and to the precipitation of the warm season. So, for example, in forest-steppe regions, the annual amount of precipitation can vary from 600 mm in an exceptionally rainy year to 175 mm in a dry year, with an average annual amount of about 275 mm. The difference between the maximum and minimum amount of precipitation in the summer months is also very large.

In winter, due to low air humidity and clear weather, the amount of precipitation is relatively low almost everywhere. In the tundra zone, as well as in Transbaikalia and Yakutia, no more than 50 mm of them fall during the entire cold period of the year; even in the most humid winter regions of the middle part of the West Siberian Lowland, the period with negative air temperatures accounts for only about one fifth of the annual precipitation, i.e., slightly more than 100 mm.

The entire territory of Siberia at the beginning of winter is covered with snow for a long time. First of all, it is installed in the extreme northern regions - on the New Siberian Islands and Severnaya Zemlya. Here the snow that fell in late August no longer melts. During September, snow cover appears everywhere on the coast of the Arctic Ocean, in the tundra zone, high-mountain regions in the east and south of Siberia, as well as in the northern and middle parts of the Central Siberian Plateau. At the end of October, snow covers the whole of Siberia, with the exception of only some areas of southern Transbaikalia.

The duration of the period with stable snow cover ranges from 300 days on the islands of the seas of the Arctic Ocean to 150–160 days in the south of Siberia. Only in the snowless regions of Transbaikalia and in the southwestern part of the West Siberian Lowland is the time during which the snow cover lies somewhat shorter. However, even here it is held for more than four or five months.

In the middle and end of April, under the rays of the warming spring sun, all the southern regions of Siberia are relatively quickly freed from snow. In the taiga zone, snow cover persists as early as early May, and in the tundra even in June. The last, at the end of June and even in July, the coasts and islands of the Arctic Ocean are freed from seasonal snow.

Despite the very significant duration of the snow cover and almost complete absence thaws in the winter months, the thickness of the snow cover in Siberia is generally relatively small and in most areas varies from 30 to 70 cm. in early April it reaches 100 and even 120 cm.

But the snow cover is especially thick in certain areas in the mountainous regions of Siberia. Soft, blown by strong mountain winds in winter, fluffy snow fills here the upper reaches of river gorges, accumulates in the crevices of mountain peaks and on wooded slopes. Its power in such shelters in some places reaches several meters. A lot of solar heat is needed in order to melt these many-meter-long snow faces, and the high mountain belt does not always receive the amount of heat required for this. In cooler summers, along the shaded depressions on the northern slopes and at the bottom of narrow valleys, one can often find here, even at the end of August, significant fields of “flying” snow that has not had time to melt.

Of course, there are places in Siberia where there is very little snow, for example, in the southern foothills of the Altai, in the Minusinsk Basin and in Southern Transbaikalia. In a number of districts of the Chita region and the Buryat-Mongolian Autonomous Soviet Socialist Republic, the thickness of the snow cover does not exceed 10 cm, and in some areas it is only 2 cm. locals they ride carts. It is not surprising that in March, when the sun begins to warm up like a spring, you will not find snow anywhere else in open places. Thin snow cover disappears here completely without a trace, without forming spring streams. The small thickness of the snow cover in Southern Transbaikalia and its early disappearance in the spring are explained both by the insignificant amount of winter precipitation and by frequent strong winds that "dry" the snow.

Differences in the thickness of the snow cover have a significant impact on the economic activity of the local population. So, in many areas of the forest belt of Western Siberia in winter, the population is forced to fight against heavy snow drifts on the roads, and in the steppes and forest-steppe, where there is little snow, one has to resort to special measures to keep snow on the fields. In those areas where the thickness of the snow cover in winter is small, and the summer is not very hot, permafrost is often found.

We got acquainted with the most characteristic features of the Siberian climate. There are few places on the globe that can compete with it in terms of such a distinct continental climate. It is quite natural that the conditions of the continental climate give some specific features to the geographical landscapes of Siberia.

They affect primarily the nature of vegetation, soil formation and weathering processes. So, for example, in a continental climate with its very cold winter broad-leaved trees are almost completely absent in Siberia, and coniferous species of the Siberian taiga dominate in the forest zone. On the other hand, a warm and not very humid summer is the reason for a more significant movement of forests to the north than anywhere else on the globe, and in the mountains - high up. Forests on Taimyr, for example, reach almost 72 ° 30 "N. (On the Commander Islands, lying almost 2 thousand km south (54 ° N. Lat.), there are no forests at all. Even on the mainland in the northern part of the Far East, the southern the boundary of the tundra zone lies at about 60°N), and in Altai their upper boundary sometimes rises to 2300–2400 m.

The relatively warm summer is also one of the reasons for the more northerly position of the border of agriculture - in Siberia, vegetables are sometimes grown north of the 72nd parallel, and cereals - at the latitude of the Arctic Circle. Distribution within the taiga, often near the Arctic Circle, significant islands of steppe vegetation on chernozem soils and even halophytes on solonchaks (Central Yakutsk Lowland) is associated with the characteristics of the continental climate, and typical steppe grasses are found even in the mountains near Verkhoyansk.

Spring in areas with the most continental climate passes quickly. Sometimes its duration does not exceed three or four weeks. Under the warm rays of the sun, the snow cover unanimously disappears, and the vegetation develops with cinematic speed. That is why, for example, in the vicinity of Yakutsk, during a short but hot summer, many vegetables and even watermelons ripen; barley sown in May is harvested already in mid-July, before the onset of frost. This time coincides with the harvesting of barley in the Kuban and in the northern regions of Central Asia.

Sharp temperature fluctuations characteristic of Siberian climate are associated with intensive destruction rocks occurring under the influence of physical weathering processes. The processes of chemical weathering, typical for areas with a maritime climate, are relatively poorly developed here.

The peculiarities of the continental climate also explain the very wide distribution of permafrost in Siberia. This very peculiar phenomenon was already noticed in Siberia by its first explorers - explorers. When they took out soil during the construction of "forts" or dug a well, in many places at a shallow depth, even on hot summer days, they encountered hard frozen soil. This was so unusual even for the inhabitants of the northern regions of European Russia that the Yakut governors found it necessary to specifically “write off” this to the tsar himself. “And in Yakutsk, sir,” they wrote, “according to the tale of trade and industrial service people, do not look for grain arable land - the land is de, sir, and in the middle of summer it does not grow at all.”

Soviet scientists studied this phenomenon in detail and in detail, which was called permafrost, or permafrost. They established the boundaries of its distribution by showing on special maps areas where, at a more or less significant depth, there is a layer of soil or rock, in which the negative temperature persists continuously for many years.

It turned out that permafrost occupies especially large areas in the northern and eastern regions of Siberia. The southern border of the distribution of permafrost in western Siberia begins south of the mouth of the Ob, goes from here to the east to the upper reaches of the river. Taz, then enters the Yenisei approximately at the mouth of the Podkamennaya Tunguska, and then sharply turns southeast to the northern tip of Lake Baikal. The northern regions of Transbaikalia and the entire territory of the Yakut Autonomous Soviet Socialist Republic also lie in the permafrost zone. Permafrost is sometimes found much to the south of this border, but already in the form of separate, sometimes, however, very large "islands" of permafrost soils among areas where there is no permafrost in summer. The distribution area of ​​this "island permafrost" includes the northern part of the taiga zone of Western Siberia, the southwest of Zayenisei Siberia, and the southern and southeastern regions of Transbaikalia.

A layer of permafrost soil is usually found at a certain depth, since even in the most northern and coldest regions of Siberia in summer the upper soil horizons thaw and have a positive temperature. This soil horizon that thaws in warm weather is called the active layer. In different parts of Siberia, its thickness varies from 10–20 cm (in the Far North and islands of the Arctic Ocean) to several meters (near the southern limit of permafrost distribution). The thickness of the active layer is of great importance for the life of plants and animals, as well as for the formation of soil. Plant roots develop only in thawed soil (In recent years, it has been proven that the roots of many plants penetrate into the frozen layers of the soil. (V.P. Dadykin. Features of the behavior of plants on cold soils, M "1952), animals dig their holes, processes breakdown of organic matter.

The thickness of the permafrost layer is very significant in places. Its maximum thickness reaches several hundred meters (Nordvik 600 m, Ust-Port 325 m). But to the south it, of course, decreases. Already near the southern border of the distribution of continuous permafrost, its thickness is 35–60 m, and on the “islands” of frozen soils found in the south of the Krasnoyarsk Territory, the Irkutsk Region and the Buryat-Mongolian Autonomous Soviet Socialist Republic, it does not exceed 5–10 m.

Permafrost is common in areas with particularly harsh climates average annual temperature below -2°. Its existence is possible only in places that are distinguished by a very long and extremely cold winter, as well as a short, usually not very warm summer, during which the soil does not have time to thaw even at a certain depth. Permafrost is especially widely developed in those regions of Siberia where little snow falls in winter and its cover does not reach significant thickness, for example, in the southern regions of Transbaikalia.

However, it is not always possible to explain the causes of the emergence and very large thickness of permafrost only by the conditions of the modern climate. Seasonal freezing does not extend to a depth of several hundred meters; it is difficult to explain only by this also the findings in the frozen strata of well-preserved corpses of long-extinct animals (mammoth, rhinoceros). Moreover, in a number of regions of Siberia, even the thawing and retreat (degradation) of permafrost is currently observed. Therefore, there is reason to consider permafrost an ancient formation associated with the conditions of an even more severe climate that was here during periods of glaciation or in the late glacial period (Recently, in many regions of Siberia, facts have been established that indicate the possibility, in the conditions of the modern Siberian climate, not only of conservation, but also formations of permafrost.Thus, in the lower reaches of the Yenisei, permafrost is found in young (post-glacial) river sediments, in the Tunka basin (Buryat-Mongolian ASSR) it was formed after the appearance of a person here, and in Eastern Yakutia, dumps of rock worked out by miners in a few years turn out to be firmly bound by permafrost).

Permafrost in the areas of its distribution has a great influence on all elements of geographical landscapes. One can point, for example, to the specific nature of the coast of the New Siberian Islands, composed of layers of fossil ice several tens of meters thick, to sinkholes (the so-called "thermokarst") lake basins that are widespread in the tundra zone and the Vilyui basin, to hillocks characteristic of the northern part of Siberia. with an ice core (“bulgunnyakhi”), etc.

Permafrost to a large extent also determines the features of the regime of surface and ground waters. Preventing the penetration of water into the soil, it is the reason for the large swampiness of many plain spaces in Siberia. In spring, meltwater quickly rolls down the frozen ground into the valleys and causes a high level rise in the rivers; in summer, water formed due to the slow thawing of the upper horizons of frozen soil serves as a source of water supply for watercourses. But in winter, when frost fetters the moisture of the active layer, the flow of water almost stops and many small rivers freeze to the bottom. Permafrost is associated with the formation of river and ground icings, as well as the phenomena of heaving and cracking of the soil, etc.

Where the thickness of the soil thawing in summer is small, it is characterized by low temperature and high humidity, which slows down the processes of soil formation, since the decomposition of plant residues occurs extremely slowly under these conditions. Therefore, soils in permafrost areas are usually thin, contain a lot of undecomposed plant remains, and are highly moistened. The hard surface of the upper permafrost horizon and low temperatures even in thawed soil limit the ability of plant roots to penetrate deep into the soil. Therefore, the roots here are most often forced to spread in a horizontal direction, and during strong winds the trees are often uprooted. This explains the large number of fallen trunks that form the “windblows” known to every Siberian in the East Siberian taiga.

The Siberian summer is distinguished by a sharply continental climate. Since Siberia is spread over very long distances, the climate also varies depending on the regions. The territory of Siberia is subdivided into Western, Eastern and Northern regions of Siberia. Therefore, the question of what summer is in Siberia cannot be unambiguously answered.

What is summer like in Siberia?

For example, in the Eastern part of the Siberian land, summer is quite warm. The average temperature can range from 150C to 350C. It all depends on the cyclones coming from the north side or south. Siberians are not surprised if, over a period of two days, the air temperature can change from 300C heat, and the next day it can be heavy rains and warm air can drastically.

Often there are situations when, after hot days, black clouds can suddenly run up and hail will fall on the ground, the size of which can reach a chicken egg. Hail, as a rule, does not last long, but it can cause serious damage to crops.

It's July. Rivers and lakes warm up for comfortable swimming, which Siberian children enjoy doing. From morning until late evening they can spend on the rivers: and they will catch fish at home.

On the territory of the Buryat Territory and the region of Lake Baikal, it mainly prevails. Weather in these areas are quite mild. The mountain air is clean and fresh. Many people go on holiday to these areas. It is in these areas that many sanatoriums, resorts and various recreation centers have been built.

In Buryatia, for example, there are many sources with mineral water of various composition. people with various diseases of the gastrointestinal tract.

Olkhon Island is located on the territory of Lake Baikal. The weather on the island is quite interesting, it rains very rarely, mostly the sun shines. The water in the lake warms up for a very long time, the time for comfortable swimming comes only in August.

Therefore, to the questions and doubts of people, what kind of summer is in Siberia, is it worth it, the answer is unequivocal - it is worth it!

Every person, regardless of where he lives: in Moscow, the Crimea or Volgograd, should visit the Siberian Territory at least once in his life. View the legendary Lake Baikal, the largest lake in the world. Visit the famous waterfalls in Buryatia, climb the highest point of the mountains, visit the monuments of ancient architecture, which are located in Siberia in a large number.

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Climate of Western Siberia

The climate in most of the territory of Western Siberia contributes to the widespread development of permafrost, in the distribution of which zonality is clearly traced.
Permafrost is found everywhere on the peninsulas. Its thickness is 300 - 600 m. To the south, approximately to the Siberian Ridges, permafrost with talik islands is distributed. The monolithic permafrost here is replaced by a two-layer one: the upper layer of modern permafrost with a thickness of 50 - 100 m in the north to 10 - 50 m in the south is separated by a layer of thawed rocks from the lower, relict layer, starting at a depth of 80 - 140 m and having a thickness of up to 200 - 250 m. m.
Separate islands of modern permafrost are found up to the latitude of the mouth of the Demyanka River (the right tributary of the Irtysh) - Somewhat to the south (up to the sublatitudinal segment of the Irtysh), relict permafrost is widespread (it is absent only on the floodplains of large rivers), occurring at a depth of 100 - 120 to 250 m and having a thickness from 150 to 250 m. In the direction from west to east, an increase in thickness and a decrease in the temperature of frozen soils are observed.

moisture circulation

Among the geographical problems of Western Siberia, an important place is occupied by the study of its moisture management, elucidation of its influence on natural features and conditions for the development of the territory, as well as consideration of possible ways of its transformation. The study of the water balance of Western Siberia or its individual parts helps to assess the different sources of water resources, allows you to identify possible ways to optimize moisture circulation.
To study the moisture cycle in the territory of Western Siberia, it is necessary to trace the spatial change in the components of the water balance: precipitation (as already mentioned above) and evaporation. Evaporation capacity increases following an increase in temperature from 150 mm near the northern borders of the plain to 650-700 mm in the steppe zone.
At the southern border of the forest zone, the amount of precipitation and evapotranspiration are almost equal to each other (about 500 mm), here the evaporation is greatest (350 - 400 mm), and the moisture coefficient is equal to one.
"(In addition to the moisture coefficient, this ratio in climatology is characterized by the difference in precipitation and evaporation. In the northern part of the plain it is positive (up to 200-250 mm), and in the southern part it is negative (up to 300-350 mm))
To the north and south of this boundary, the structure of the water balance is heterogeneous.

Northern and central parts Western Siberia (more than 80% of its area) has a moisture coefficient of more than 1. These are waterlogged and extremely humid territories. Evaporation here is limited solely by the amount of evaporation. The study of the water balance of this territory, carried out by the staff of the Institute of Geography of the Academy of Sciences of the USSR, showed that only due to atmospheric precipitation, a layer of moisture from 5 to 10 mm annually lingers and accumulates here (Vendrov et al., 1966). It is used to replenish groundwater and lakes, to moisten the soil, but it is mainly preserved in the thickness of continuously growing peat tracts. To retain this moisture, the annual growth of peat should be between 0.5 and 1.0 cm over the entire area. In fact, much more water accumulates here every year, since part of the moisture brought from the surrounding territories by river runoff is also conserved. The northern and central parts of the plain are among the most waterlogged spaces on the entire surface of the Earth. This stimulates the continuous growth of swamps, an increase in the thickness of the peat and the expansion of the swamp area. Many areas are practically inaccessible to land and water transport, which makes it difficult for the economic development of the territory.
The study of the structure of the water balance showed that the main reason for waterlogging lies in the low amount of runoff in relation to precipitation, in the insufficient level of training of the plain.
In the forest-bog zone of Western Siberia, the runoff varies from 100 to 300 mm, which corresponds to a runoff coefficient of 0.2–0.4. At the same latitudes of the Russian Plain, it is 1.5 - 2.0 times greater. In this way. waterlogging, slow moisture circulation in Western Siberia are associated primarily with its lithogenic basis.
The flat relief and the presence of numerous depressions in the interfluve spaces that contribute to stagnation of water, weak infiltration of atmospheric precipitation due to the alternation of sandy-clay deposits, small surface slopes, the fall and longitudinal slopes of rivers, a weak incision of river valleys, a rare river flow - all this complicates the processes of runoff , significantly reduces river runoff in comparison with other regions and slows down the moisture cycle.
To combat waterlogging, it is necessary to increase surface runoff. This can be achieved by straightening the channels of the rivers and thereby increasing the descent. The carrying capacity on the straightened sections of the rivers increases by l.5 - 2.0 times, which makes it possible to drain large land masses. Forests and peat resources will become more accessible, it will be easier to develop the subsoil. The accelerated flow will wash the riverbeds, ensure their better self-cleaning, prevent fish kills, and improve the conditions for their feeding and spawning. Small water intakes in the upper parts of the Ob, Irtysh and their tributaries, the laying of canals and field water pipelines will make it possible to partially compensate for the lack of moisture in the southern regions and reduce its inflow into the central part of the plain.
The southern part of Western Siberia belongs to the region of insufficient and unstable moisture; the moisture coefficient here is less than 1. Evaporation is limited by the amount of precipitation and decreases towards the south. In the same direction, the moisture deficit is growing due to a decrease in precipitation and a simultaneous rapid increase in evaporation. From 85 to 98% of the annual precipitation is spent on evaporation; the runoff layer in the forest-steppe does not exceed 10 - 15 mm, and in the extreme south - 5 - 10 mm. The runoff coefficient decreases to the south from 0.1 to 0.02. The rivers that start here are shallow. Transit rivers almost do not receive tributaries. Many rivers are fed by snow waters. In the spring, high and short floods form on them, but already in the middle of summer the rivers dry up.
Surface runoff in the area of ​​insufficient and unstable moisture leads to moisture loss, therefore, it is an unfavorable element of the water balance. The surface remains without moisture for most of the growing season, since summer precipitation evaporates very quickly and almost does not enter the soil.
In years when rainfall is less than normal, droughts occur in the southern part of the country, reducing crops. Droughts recur on average every 3-4 years and occur most often in May-June. As in the Russian Plain, they are usually associated with the intrusion of Arctic air. Sometimes the cause of drought is the arrival of very warm and dry air masses from Central Asia and Kazakhstan. Strong winds cause dust storms in summer. Number of days since dust storms is 10 - 15. In dry years, it increases by 2 times. The occurrence of dust storms is facilitated by the presence of light sandy and light loamy soils, carbonate soils plowed without special anti-deflation measures, low forest cover in the north and treelessness in the south.
The limited water resources require additional moistening of agricultural lands, forcing one to resort to measures to accumulate and conserve moisture (snow retention, creation of backstage, etc.), in some places and to irrigate land masses

Water