Siberia is a huge territory located to the east of the Ural Mountains and extending to the most Pacific Ocean. Siberian expanses occupy the large territory of the Russian Federation. Of course, such an extensive land has a large natural and climate diversity, because in the north is the plague, and in the south is a hot Asian steppes and deserts. However, Siberia has some common climate features, which will be described.
Siberia is one of the coldest regions of the globe. This is due to the remoteness from the seas and the fact that from the West and the south, the territory is surrounded by mountain arrays that do not transmit warm air. Only in Western and South areas, the average annual temperature is positive, it is below zero on the rest of the territory. The climate is continental and sharp-continental with substantial (sometimes extremely high) vacancies of annual and daily temperatures. Winter in Siberia Long and frosty, summer - roast and dry, transition seasons - autumn and spring - short and little expressed.
Climate of Siberia (Novosibirsk) by months:
Spring
Spring almost all over the entire territory of Siberia is short, and in the north - rapid. In March, it is snow everywhere, the climatic spring is even in areas with a relatively mild climate begins only after March 20, and the snow cover comes down after mid-April. In the northern regions, where the eternal Merzlota, Spring comes only in June.
There are many clear days, but the weather is unstable, with sharp cooling and even frosts. Precipitation is not so much, although there may be short rains.
Summer
Depending on the region, the Siberian summer is very different. In the southern regions it is roast and dry, in the north - short and cool, although in Yakutia, for example, it is very warm and even hot.
Air humidity throughout Siberia is much lower than in other areas of Russia, rains and fogs less. Most of the sediments fall in July and August.
The average daily temperatures are approximately 20-25 degrees, often climbing up to 30 degrees and above.
The continental nature of the climate affects the fact that night frosts last longer (until mid-June) and returned before (already in August).
In the West of Siberia, the climatic summer ends in accordance with the calendar, that is, in the last few days, and in the tundra and in the east even earlier.
Fall
The transition from summer to winter takes place in Siberia much faster than in the European part of Russia. In September, the air quickly cools, atmospheric pressure increases dramatically. Even in the eastern regions, snowfall can begin at the end of September, and in the middle of October a snow cover is already installed. In areas with a more harsh climate, this happens before.
But in September, the weather is still pleased: many sunny days are issued, the temperature can rise to 20 degrees and above. Holds quickly, rains are replaced by mixed precipitation, and then snowfall. Winter comes to Siberia in the first decade of November.
Winter
Siberian winter is a real test for humans and nature. But there are here and its advantages: thanks to the reduced humidity of the air, the frost are transferred easier, many sunny days, blizzards and heavy snowfall are not so annoyed as in the European part.
The greatest frosts come for January. In the eastern regions with the most mild climate, the average monthly temperatures of January are minus 18 degrees, but in Yakutsk this indicator is minus 40 degrees, and this is not the limit for the North of Siberia.
Snow thickness in Siberia as a whole is small. Even in the snowproof areas, it does not exceed 70 cm, there are areas in which there is almost no snow, but at the same time very frosty.
The main factors of climatic formation on the territory of Eastern Siberia are: significant remoteness from the Atlantic Ocean, the location in high latitudes, isolation from the Pacific Ocean. Therefore, the climate is characterized by a sharp continentality, large seasonal and daily fluctuations in air temperature, minor moisture and low cloudiness.
Since the territory is open to the North Arctic Ocean, the Arctic air masses dominate here. In winter, a powerful bary maximum is installed with very low temperatures, which is formed to be stable, usually windless and cloudless weather. In the northern regions, due to low temperatures, excessive moisturizing is observed. And in the southern direction, the moisturizing is insignificant, which is especially characteristic of the Central Yakut depression. There are steppe landscapes, the development of which contributes a slight amount of atmospheric precipitation and isolation of mountain ranges located on the periphery.
In the warm period between Eastern Siberia, the surface of which is largely heated, and large temperature differences arise with the Arctic pool. As a result, cyclonic activity is developing in the front when contacting warm and cold air masses.
Within the mid-Siberian Plateau and Central Yakutsk, intense solar radiation, but due to the lengthy snow cover and the transparency of the atmosphere, a lot of heat is consumed for reflection and efficient radiation. In connection with the mountain relief, temperature inversion is clearly observed. So, in the valleys and basins in winter there is a sharp drop in temperature; On more elevated areas where cold air outflow is possible, warmer by 15-20 ° C.
On the territory of Eastern Siberia, the zonality of natural conditions is planned and, of course, climate,
In East Sibirsk Tundra in winter, very low temperatures. January isotherms are -30-40 ° C. The influence of an Asian baric maximum affects. The precipitation falls a little, in some places less than 200mm (Cape Chelyuskin, Delta Lena). Summer warmer than in West Siberian tundra. In Tundra Yakutia the growing season exceeds 75 days. This makes it possible to grow vegetable cultures. Agricultural sections are confined to southern slopes of valleys, protected from the penetration of cold air from the Arctic.
The average annual facilities of the forest zone of Eastern Siberia are negative (- 7-16 ° C), the average January is very low (- 30-44 ° C). The direct effect of anticyclone affects. Summer is short, but relatively warm. For example, the average temperature of July from +14 to + 19 ° C, which is explained by significant insolation. The growing season is short, from 90 days in the north to 140 - in the south. Annual atmospheric precipitation here is significantly less than in Western Siberia. Thus, 300-450 mm falls on the main territory of Eastern Siberia, and in the closed blades of Yakutia only 250-150 mm. As a result, steppe landscapes are developing. And only on the western slopes of the mountains, the amount of precipitation increases to 500-700 mm per year (Plateau Pouotos, Yenisei ridge).
Due to the dryness of the climate, the taiga zone is distinguished by a low-power snow cover. An insignificant snow cover and low winter temperatures contribute to the deep freezing of the soil and preservation of many years of permanent. The sandy soil pulls up to 250 cm.
The long-term permafrost has a negative effect on the soil formation, causing strong soil cooling and the processes of fevering. However, in the arid areas of Eastern Siberia, it plays a positive role, since when thawing has plants in moisture.
Eastern Siberia includes Verkhoyansky and Kolyma ridges, the mining system of the black and elevation of Chukotka, as well as the tundra flat part of the lower pools of the Yana rivers, indigrants and kolyma. The formation of a sharp continental climate has an influence primarily geographical position. Due to the high length of the territory in the meridional direction (73-55 ° C. sh.) There are three climatic belts: arctic, subarctic (occupies the main territory) and moderate.
An important climate-forming factor is also relief. For the mining part of this region, the temperature of the temperature regime is characterized depending on the orographic conditions. In the semi-shined mountain basins, valleys and plateau penetrate the cold continental air from the Arctic, contributing to the formation of extremely low temperatures. The absolute minimum sometimes reaches -65-70 ° C. This is the lowest temperature in the northern hemisphere ("Polyus of the Cold" - on the Oymyakon Plateau). In winter, an anticyclonal weather type is installed, while in summer airs on certain days is heated to + 30 ° C. Thus, the maximum annual temperature amplitude reaches 100 ° C. The influence of the Pacific Ocean, unlike the Northern Ice, on the formation of the North-Eastern Siberian climate is limited coastal ridges. Therefore, cyclonal processes are traced only on the coast of the Sea of \u200b\u200bOkhotsk and Chukotka.
For the inland areas of Northeast Siberia, temperature inversion is characterized. For example, in the foothills of the Verkhoyansky ridge 64 ° C. sh. where there is an outflow of cold air, registered the mid-gauge temperature -29 ° C; Approximately on the same latitude, but in the basins, where the cold air is caressed, the same isotherm is -44-50 ° C.
In the flat part of the region, the climate is arctic with relatively high humidity. The North Arctic Ocean has a direct impact on its formation. Winter here is cold, windy and long (260 days); Summer short, moderately cold; The medium temperature is from + 4-6 in the north to 11-14 ° C in the south.
The Chukotka mountain-tundra area refers to the Arctic and subarctic climate, some softening effect on which the Pacific Ocean has. Thanks to the influence of the Eastern Esibirsk high on one side and the Aleutian minimum on the other, there is a significant baric difference in the winter with the other between the Western and Eastern districts in winter. As a result, severe cold winds with a purgy arise. Winter period lasts about 8 months. The average January temperature rises in the eastern direction from -35 to -20 ° C; Accordingly, the annual amount of precipitation increases (from 200 to 700 mm); The power of snow cover increases from 35 to 80 cm.
Summer short, the growing season does not exceed 70 days. The average temperature of the warmest month does not exceed + 10 ° C.
The formation of the harsh climate of the Okhotsk coast is influenced by the Cold Okhotsk Sea, as well as a winter cold and dry monsoon. Summer is cool, the average temperature of the warmest month does not exceed 15 ° C. Annual precipitation 500-700 mm, excessive moisture.
Moderate climate in the territory of Western Siberia is characterized by a greater continentality compared to ETP. The influx increases, the annual amplitude of air increases, in the southern regions the climate becomes arid. East of the ridge, the effect is completely weakened and continental is dominated here. The climate of Western Siberia is more uniform than on the other side of the Urals in the European territory.
In the cold period, cyclonic activity in the north is resumed and cold continental air comes from central Siberia, which makes the temperature regime unstable. In January, for the most part of Western Siberia, temperature fluctuations from day to day are an average of 5 °. (Such a phenomenon in other regions of the globe is almost no observed.) Winter is cold, the average temperature in January varies from - 18 ° in the south, to -28, -30 ° in the northeast. With small winter sediments in the southern regions, the height is less than 30 cm. In the northeast, in the region of the Upper-Tazhskaya and the Nizhny-Yenisei hills, where it is frequent, it increases to 80 cm.
Summer over the entire territory of Western Siberia, cyclones are developing. The number of them decreases from north to south. Cyclones from the European part of Russia and the Atlantic are invaded to the northern regions. Cyclones from the West and South-West come to the southern regions (with low-levels, with and seas). The most intense cyclonic activity is observed between 54 and 60 ° C. sh. During the summer period here drops from 300 to 400 mm precipitation. North and south of this territory decreases. In the summer, the Arctic air comes, which turns into continental. Air flow increases dryness and enhances continentality to the south.
For most of the territory of Western Siberia, the climate is wet. The zero isolated of the difference in precipitation and evaporation, which is the southern border of the forest, runs about the line - Novosibirsk (56 ° C. sh.). The region of Western Siberia is the most overwhelmed territory of Russia. There is a significant accumulation of surface waters, the forests of the bundle. The precipitate, the annual sum of which is 600 mm, most of the territory exceeds the evaporation by 100 - 200 mm. Many solar heat is spent on evaporation. Average varies from north to south from 14 to 18 °. South of 56 ° C. sh. Cyclonic activity weakens and the annual amount of precipitation decreases to 350 - 400 mm. Possible evaporation exceeds the amount of precipitation, the climate becomes arid. Dominate.
Siberian summer is characterized by a sharp continental climate. Since Siberia spread over very long distances, the climate varies depending on the regions. The territory of Siberia is divided into Western, East and Northern Siberia regions. Therefore, to the question of what summer in Siberia is unambiguously replied.
What summer is in Siberia
For example, in the eastern part of the Siberian Earth, summer is quite warm. The average temperature may vary from 150c and up to 350c. It all depends on cyclones going on the northern side or south. Siberians are not surprised if during the period of two days, the air temperature may change from 300C heat, and the next day heavy rains can go and warm air can sharply.
Often there are such situations when after hot days, there can be sharply to cut black clouds and degrees to the ground, the dimensions of which can reach a chicken egg. Grad, as a rule, is not long, but there may be serious damage to sow.
This is July. Rivers and lakes are warming up for a comfortable bathing than Siberian children are happy with pleasure. In the morning and until late in the evening they can spend on the rivers: and fish home caught.
On the territory of the Buryat Territory and the region of Lake Baikal, mainly prevails. Weather conditions in these areas are rather soft. Mountain air clean and fresh. Many people are specially going to relax in these areas. It was in these areas a lot of sanatoriums, resorts and various recreation databases are built.
In Buryatia, for example, there are many sources with mineral water of various composition. People with various diseases of the gastric intestinal tract. 
Olkhon Island is located on the territory of Lake Baikal. The weather on the island is quite interesting, the rains go very rarely, mostly the sun shines. Water in the lake is warming up for a very long time, time for a comfortable bathing occurs only in August.
Therefore, on questions and doubts of people, what summer in Siberia is worth it, the answer is unequivocal - worth it!
Everyone, no matter where he lives: in Moscow, Crimea or Volgograd should at least once in his life visit the Siberian region. Look at the legendary Lake Baikal, the biggest lake on the whole globe. Visit the famous waterfalls in Buryatia, climb on the highest point of the mountains, visit the monuments of ancient architecture, which are located in Siberia a large number.
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The extensive territory of the Central Siberia is located between the Valley of the Yenisei River and the Western foot of the Verkhoyansky ridge. It extends from the shores of the seas of Kars and Laptev before the foot of the mountains of Southern Siberia. The maximum length of Central Siberia from north to south, from Cape Chelyuskin to Irkutsk, exceeds 2800 km (about 25 °), and from west to east on the latitude of Yakutsk 2500 km (about 45 °). The area of \u200b\u200bCentral Siberia is about 4 million km 2.
The average Siberia is timed to the ancient Siberian platform. Most of the territory is represented by a deeply dismembered medium-grained plateorem, the height of which is gradually decreasing to the east, towards the Centraliakuta Plain and the Lena Valley. The North-Siberian lowland separates the plateore from the Mountains of Byrranga (1146 m), which occupy the northern and central parts of the Taimyr Peninsula.
For medium Siberia, a significant elevation and dismemberment of the surface is characterized, a sharply continental climate, almost the widespread distribution of permissal and less distinct than in Western Siberia, the manifestation of zonal differentiation of natural conditions, domination for most of the territory of the larch taiga on peculiar permanent taiga soils. In a number of regions of medium Siberia, the latitudinal zonality is complicated by a high-dimensional explanancy.
Unlike Western Siberia, the boundaries of medium Siberia in different schemes of physico-geographical zoning do not coincide. This is due to the greater contrast of nature within the country, with the less clear boundaries, an ambiguous interpretation of the actual data from researchers and with an insufficient complex physico-geographical study of border areas characterized by the transitional landscape structure. The greatest differences arise in relation to the northern and eastern borders of the country.
In the study of the nature of Central Siberia, a large contribution was made by major expeditions, organized in the XVIII century: the Great Northern Expedition (17331743) and its academic detachment under the direction of I.G. Gmlin, academic expeditions of the second half of the century (P.S. Pallas, etc.).
One of the wonderful events in the geographical study of Middle Siberia in the first half of the XIX century. There was a Siberian expedition of naturalist and geographer A.F. Middondorf (1843-1844), organized on behalf of the Academy of Sciences. In front of the researcher, the tasks of studying many years of marzlot and life in high latitudes away from the seas were delivered. Middendorf was the first scientist researcher of the Taimyr Peninsula. He not only studied the organic world of this territory, set the patterns of spreading wood species on their northern limit, but also described the geology and relief of the North-Siberian lowland and the Mountains of the Borranga. Middendorf first determined the borders of the spread of the permissal in Siberia, set a number of temperature gradients, studying with a thread in the wells and wells of Yakutsk, and calculated the power of the permotor in Yakutsk (204 m), which was later practically confirmed by drilling (214 m).
In the last quarter of the XIX century, in Central Siberia, a number of expeditionary studies have been conducted that engulfed the northern and central regions. Especially important was the Expedition A.L. Chekanovsky (1873-1875), freshen in geological and geographical terms, the huge spaces of the medium-grained plateau from the lower Tunguska to the mouth of Olenek and Lena. Chekanovsky first gave a description of Siberian trapps.
At the beginning of the XX century, the deposits of the Vilyuic salt, gold, stone coal, iron ore were studied. Geologist I.P. Tolmachev (1905-1906) Anabar plateau was opened and an anabar array was allocated as a separate unit of the Siberian platform. In 1909-1914 Recognitive soil-botanical studies were carried out by the detachments of a multi-year expedition of the migrant department in the southern part of Central Siberia (in the Angara basin, the top flow of Lena and the lower Tunguska, on the interfluent Lena and Vilyuya). The materials on the climate, the conditions of shipping on the rivers, the influence of permafrost to vegetation, and so on, were gradually accumulated.
In 1914, a three-volume work was published by a three-volume work. "Asian Russia" with the atlas of cards, which reflected quite complete the idea of \u200b\u200bthe nature of Medium Siberia.
The main objective of research in the Soviet years was the study of the natural resources of the Central Siberia and the conditions for their development in order to develop the productive forces of this large region. Numerous expeditions of the Ministry of Geology conducted the search for minerals. Already in the first post-revolutionary years S.V. Obruchev (1917-1924) opened the world's largest Tungusky coal pool, which occupies an area over 1 million km 2. From 1925, the Yakut Integrated Expedition of the USSR Academy of Sciences was led since 1925. In the postwar years, the expeditions of the Council on the study of the productive forces on the study of the resources of the Krasnoyarsk Territory and Yakutia worked here, in 1959, in Irkutsk, the Institute of Geography of Siberia and the Far East from the USSR Academy of Sciences, leading various geographical research (now the Institute of Siberia Geography Siberian RAS).
To date, numerous deposits of various minerals were found in the depths of Central Siberia, the map image of the medium-librian plateau, especially its western part, and the Central Lowland, was studied quite significantly, the hydropower resources of the largest rivers and the conditions for the construction of HPP were studied. A lot was made to study the relief, climatic conditions and agroclimatic resources, many years of permissal and its influence on other components of nature and the features of the development of the territory, soil and vegetation, including forest and feed resources.
Geological structure and history of development of the territory
Tectonic basis Medium Siberia is an ancient Siberian platform, the boundary of which is usually carried out along the northern outskirts of the medium-grained plateau. The tectonic position of the northern part of the average Siberia is determined ambiguously. For a long time, the territory of Taimyr and the North-Siberian lowland was considered the area of \u200b\u200bthe Gercino folding, then within its limits began to allocate sections of the Caledonian, Baikal and Mesozoic folding. All this is reflected on tectonic maps (1952, 1957, 1969 and 1978). However, metamorphic foundation complexes, overlapped with proteozoic deposits, are established by the last works on Tactonika Taimyra that in its structure, as in the structure of the Anabar massif, metamorphic complexes of the foundation are involved. This gave the basis of M.V. Muratov (1977) attribute Taimyr to the category of shields, including it in the Siberian platform. An increasing number of researchers support this point of view.
Thus, the territory of Middle Siberia practically coincides with the Siberian platform. Only the south-eastern part of the platform, its Alandanian shield underlying the Alandanian Highlands, a number of researchers (S.S. Voskresensky, 1968; N.I. Mikhailov, 1961; N.I. Mikhailov, N.A. Gvozdetsky, 1976 and Dr.) is not included in the composition of medium Siberia. The basis for this is the significant differences in the modern nature of the Alandanian Highlands and Central Siberia, due to the fact that its development for long-term mesocynezoic history is significantly different from the development of the rest of the platform area and comes closer to Severobaician highlands.
Foundation Platforms are complicated by the Archean and Proterozoic folded complexes and has a dismembered relief. In the Anabar and Taimyr arrays of the formation of the foundation (GNECA, quartzites, marbles, granites) overlook the surface. The area of \u200b\u200bshallow occurrence of the foundation (up to 1-1.5 km) is located on the outskirts of the Anabar massif, the northern slope of the Alandanian shield, on the western outskirts of the platform (Turukhan raising, the slope of the Yenisei massif) and cross the territory from the northeast to the south-west from the lowerland of Lena To the eastern Sayan. The folded structures of the Yenisei raising were created in Late Proterozoa (Baikal folding).
The raising of the foundation is divided by extensive and deep depressions: Tunguskaya, Pyanesko-Khatanga, Angaro-Lena and Vilyuyskaya, which in the east closes with the beforeproyan regional deflection. The depressions are filled with sedimentary thickness of high power (8-12 km). Only in the Angar Lena deflection the power of the cover does not exceed 3 km.
Formation a sedimentary case The Siberian platform began in the Nizhny Paleozoa with a common immersion, which caused a large marine transgression. For sediments, Cambrian is characterized by a large facial variability and breaks in sedimentation, indicating a fairly large mobility of the territory. Along with conglomerates, sandstones and limestones in the outskirts of the platform in marine lagoons, red-color stals containing salts and plaster were accumulated.
But they prevail among the Nizhneepaleozoic sediments of limestone and the dolomites overlooking the surface on extensive spaces.
IN end of Silouralmost all the territory experienced raising, which was an extension of Caledonian folding on neighboring areas of the territories. Marine regime has been preserved only in the Pyan-Hatang Wpadin and in the northwestern part of the Tungusky syneclide. During devon The territory of the platform continued to remain sun.. In the early Devon, Yuzhnayimirsky Avlacogen laid, where a complete incision of Devonian deposits has accumulated.
IN upper Paleozoa in conditions slow dive On the extensive territory of the Tungus and Pyan-Khatanga syneclide, the lake-marsh mode is established. There are powerful layers of the Tungusian suite. The lower part of this suite is represented by the so-called productive thickness alternating sandstones, clay and angry slates, aleurolites and stained coal. The power of this thickness is up to 1.5 km. Industrial coal layers are confined to it, common in a huge territory.
The productive coalous thickness is permeated with numerous intrusions of the main magmatic rocks and blocked volcanogenic thickconsisting of tuffs, tube, lava cover with precipitation of sedimentary rocks. Its formation is associated with the manifestation of platform fractured magmatism at the end of Perm TRIAS, due to the activation of faults and the crushing of the foundation, which coincided with tectonic movements in the neighboring Ural-Mongolian belt. Effusion and intrusive formation formations created by them are the names of the trappers, and the magmatism itself is trapps magmatism.
Trappes A characteristic feature of the geological structure of the Siberian platform, sharply distinguishing it from the Russian platform, the shape of the location of the trappers is diverse. In their distribution, a clear pattern is traced. In Kurenskaya Vpadina, the most deeply lowered north-western part of Tungusky syneclide is predominated by powerful basalt (lava) cover. Singing intrusion (dikes, veins, rods) dominate the central part of the syneclide. Lacolites and reservoir intrusion (Silly) is most characteristic of its western, eastern and southern outflows, where the main zones of faults separating syneclizes from other structures pass. The main mass of the explosion tubes (annular structures) is also concentrated. Outside the Tungusian syneclide, the trapps are much less common (on Taimyr, along the northern outskirts of the anabar massif).
The repulsive and introduced basalt magma permeashed the breed of the platform, created an even tougher and steady framework, so the western part was almost never incremented.
At the turn of Paleozoic and Mesozoic There were block movements, gaps and folds in South Mir Avlacogenes.
IN late Mesozoe Most of the Central Siberia experienced raising and was a demolition area. Kuresskaya Vpadina, which turned into an overlooking morphostructure Plateau Puratorna, Anabar Code and the northern part of the Yenisei raising, was particularly intensely reigned. There is a flexing in Pyan-Hatanga syneclise, along the eastern and southern outskirts of the platform. It is accompanied by a short-term sea transgression that did not go far to the south, therefore, among Jurassic deposits, continental coal stones with industrial deposits of coal are sharply dominated. Cretaceous sediments are distributed only in the Pyan-Hatanga syneclide (alluvial-lake wegethugal fats), Vilyuy syneclide and before-up to-200, which are represented by a powerful (up to 2000 m) alluvial threats.
TO end of Mesozoy The entire territory of Middle Siberia was a compact land, which is the area of \u200b\u200bdenudation and the formation of alignment surfaces and the weathelation bark.
Cenozoa It was characterized by differentiated oscillatory movements with a general trend towards raising. In this regard, the erosion processes sharply prevailed. The surface dismemberment of the river network took place. Paleogenic deposits are rare, represented by alluvial clays, sands and peccles and are associated with the remnants of the ancient river valleys. IN end Neogene And in quaternary time, against the background of a general lift increased the differentiation of vertical movements. The most intensively rose to the grains, Puratorna, Anabar and Yenisei arrays. The eastern part of Vilyuic syneclide was launing, where the thickness of the large-grass red-colored pebbles with a capacity of 3-4 km had accumulated during the neogen.
In general, the Siberian platform is characterized by a large activation non-projectonic movementscompared to Russian. This is reflected in its higher plaster meter, as well as in predominance among high plateaus and plains among morphostructures. As a result of the newest tectonic movements, the ancient hydrographic network occurred. This is evidenced by the remains of river systems remaining on the watersheds. The overall raising of the territory led to deep cutting of the rivers and the formation of a series of river terraces.
IN the beginning of a quaternary period Susha occupied the greatest square and stretched to the north to the borders of the modern shelf. Against the background of the general cooling started in Neogene, it caused the strengthening of the continentality and the severity of the climate of medium Siberia, a decrease in the amount of precipitation. During medium-powerlycene boreal transgression North-Siberian lowland and the lowered outskirts of the Taimyr were flooded with marine waters. The Mountains of the Graduate and the Northern Earth were the low islands. The sea is close to the northern and northwestern footages of the Medium-Big Plateau. It caused an increase in precipitation and development glaciation. The center of the glaciation was Plateau Pouotnian and Taimyr. Currently it is established that maximum (Samarovskoye) The glaciation was covered. His border is clearly visible quite clearly only in the southwestern part: the mouth of the subframe Tunguska, the rover of vilyuya and the marchs and further to the Valley of the Olenek. Oriental segment of the boundary is not traced.
After short-term regressionthe sea, during which not only the Taimyr, but also the Northern Earth launched towards land, begins new marine transgression. Zyryansk (Verkhnevostocena) is developing glaciation. The accumulation of ice took place on Taimyr, Pouotnian Plateau and anabar array. The border of the maximum spread of ice during the Zyrian glaciation was held from the mouth of Lower Tunguska in the upper and the Moyero River (the right influx of Kotuua), enveloped from the south anabar array, went to the bottom flow of the Anabar River and to the eastern tip of Taimyr. The last phase of the degradation of Verkhnestocecene glaciation is the mining and valve sartan stage, traces of which are fixed in the central part of the Pouotnian Plateau, on Taimyr.
The main feature of the Pleistocene glaciation in the middle Siberia was a small power, and from here and the small mobility of the glacier. The sea, approached to the foot of the medium-grained plateau, was cold, so the air that had a little moisture contained above it. The bulk of precipitation fell in the north-western part on Taimyr and Plateau Pouotnian. To the south and east, the amount of precipitation quickly decreased, the capacity of the glacier decreased dramatically. These glaciers were "passive". With a small mobility of glaciers, their destructive activities were small. Consequently, in the body of glaciers kept a little frozen material and it was weakly anger, that is, it was similar to the sloping deluvial sediments. A small relief-forming role of medium-term glaciers led to a significantly weaker preservation of their existence of their existence than in Russian plain, and in Western Siberia. Therefore, many issues related to the character, the number, borders and age of the glaciation of Central Siberia are still discussion.
The huge areas of the inner parts of the medium Siberia were in the conditions of periglacial regime. A cold dry climate contributed to a deep freezing of soils and soils. A long-term permafrost was formed, and in places and underground ice. The formation of a permafrost at the end of the middle Pleistozer was particularly intensively intensively, during the regression of the sea, when, due to the increase in land area in the northern latitudes, the continentality and dryness of the climate of medium Siberia increased dramatically.
The tendency to cool the climate has led to the gradual depletion of the vegetation of medium Siberia to the gradual depletion of the vegetation. The rich in the species composition of the coniferous-wide forests of the Pliocene was replaced in the lower Pleistocene depleted beringian Darkness taiga with admixture of broad rock (linden, oak, grab, flavory) in southern regions.
Further cooling and development of glaciation led to the wide distribution of TundR and Foreturotund, and in the southern regions peculiar cold forest-steppes represented by alternating larch-berezo-pine forests with open tundrov-steppe spaces. The overall warming of climate in the interledstial favored the promotion of forests to the north.
In the late- and postradite time, there was a general raising of the territory, the climate had several warm and cold phases, dry and wet periods associated with a change in circulation conditions (the predominance of meridional circulation, or western transfer). This led to a significant mobility of natural zones on the territory of Central Siberia. Increasing the continentality of the climate contributed to the widespread development of the herbal vegetation of steppe type and the accumulation of salts in the soils. Reducing continentality and some increase in precipitation led to the change of steppe vegetation by forests and forest-steppes.
Relief
Most of the territory occupies a medium-term plateau, formed in the western part of the Siberian platform, the structures of which were tightly soldered as a result of trapping magmatism. All this territory in the mesocyneosis was raised steadily as a single structure and in the relief is represented by the largest orographic unit. For the medium-grained plateau, a significant elevation and contrast of the relief is characteristic. Heights within its limits range from 150-200 to 1500-1700 m. The average height is 500-700 m. The distinctive feature of the plateaus is a combination of a predominantly flat or high-end step relief of the transferee with deeply embedded steep-robber (often canyon-shaped) river valleys.
According to the character of the distribution of heights and dismemberment, the medium-grained plateau is very inhomogeneously. It distils more fractional orographic units. The maximum heights of the plateaus reaches in the north-west, where the Plateau of Poootan (up to 1701 m) and Somber (more than 1000 m) rise.
The close relationship between the orographic elements and tectonic structures makes it possible to select large morphostructures that can be combined into four groups: 1) of platea, rods, low- and middle array on the protrusions of the crystalline foundation; 2) reservoir hills and a plateau on sedimentary paleozoic rocks; 3) volcanic plateau associated with powerful manifestations of trapping magmatism; 4) accumulative and reservoir-accumulative plains. The first three groups combine morphostructures, in the formation of which denudation processes played a preferential role against the background of stable or predominant raises, the fourth morphostructures created by the accumulation of loose material in the territories lagging behind in the raise and experiencing the latest lowering.
Among the morphostructures of Central Siberia dominated inherited (straight). This is due to the fact that the newest tectonic movements updated the ancient structures. However, not everywhere the focus of the latest movements coincided with the focus of earlier tectonic movements. In such places there is a discrepancy between ancient structures and a modern surface device. Converted morphostructure Presented exclusively elevations on the spot of negative structures: Pooutan, Somomm and Tunguso Plateau meet the deepest pots of Tungusky syneclide. They are found in Middle Siberia and complex semi-simplicable and semi-varying morphostructures (adherent plateau, central nerd plateau, etc.).
The average Siberia experienced a long period of continental development, so it prevails on its territory denudation relief. The newest raising and alternation of various breed resistance, the stem, led to him liursery, or speed. The surface is dissected by a thick network of river valleys. The maximum cutting depth of the valleys (up to 1000 m) is characteristic of the western part of the Pouotnian plateau, and the minimum (50-100 m) for the Central Tungus plateau, the Centraliakut and North-Siberian lowlands. Most canyon-shaped valleys, asymmetrical.
The most important distinctive feature of the river valleys of Central Siberia is a large number of terraces (six-nine), indicating ancient times and repeated tectonic raising of the territory. The height of the upper terraces reaches 180-250 m. Only Taimyr and North-Siberian lowland are characterized by weak terracement and the youth of river valleys. Even large rivers have no more than three-four terraces here.
Almost for the entire territory of Central Siberia is characterized by cryogenic (Merzloid) Morphoskulface. Forms of mercury Relief detect regional deritrancy. In the Westwhere dense indigenous breeds predominate, and quaternary sediment cloaks are disaster and low-power, developed thermal denudation, thermal planningassociated with sedimentation, alignment of the surface during seasonal pulling of frozen soils and ice in them, and solifluction. In the north and eastwhere rubbed sediments are common, thermal, solifluctional forms, bugs and hydrolylaccolite (Bulgunnyah).
Perennial Merzlota makes it difficult to modern erosion processes and prevents the development of karst, so karst forms The relief in Middle Siberia has a much smaller spread than it could be expected due to the abundance of cursors. They are more widely developed in the southern part of the country where there is no solid merzlot. So, on the Leno-Angarsk and Leno-Alandan plateau there is a mass of karst funnels, wells, blind valleys, etc.
With active physical weathering in conditions of a sharp continental climate, an abundance of chill-stony rossely, stone streams kurumov and Oseos In mountain ranges, on the surfaces of the plateau and the slopes of river valleys.
Despite the large length of the territory from north to south, a clear zonality in the placement of morphoschool, unlike Western Siberia, is not traced here. On the entire space of medium Siberia, dominant morphoschools are erosion and cryogenic. This is due to the nature of the tectonic movements and the characteristics of the harsh throughout the quaternary period of climate. In the northern part of the country, the Relief Morphoskults is joined ancientlennikova, A. on the south wider common karstforms.
Climate
The main line of the climate of Central Siberia is sharp continentalitydue to the position of the territory in the middle part of North Asia. It is located at a high distance from the warm seas of the Atlantic Ocean, is fenced with mountain chains from the influence of quiet and exposed to the Northern Ocean. The continentality of the climate increases from the west to the east and from north to south, reaching the highest degree in Central Yakutia.
For the climate of medium Siberia, large annual amplitudes of average monthly (50-65 ° C) and extreme (up to 102 ° C) temperatures, short transitional periods (one or two months) with large daily amplitudes (up to 25-30 ° C), very uneven Introductory precipitation distribution and their relatively small amount. Large differences between the winter and summer air temperatures in the middle Siberia are primarily due to the strong undercoilment of the surface in winter.
Total radiation Changes within the country from 65 kcal / cm 2 per year in the northern Taimyr up to 110 kcal / cm 2 per year in the Irkutsk area, and the radiation balance , respectively, from 8 to 32 kcal / cm 2 per year. From October to March, the radiation balance for most of the territory is negative. In January, in the northern part of the country, solar radiation practically does not receive, in the Yakutsk area, only 1-2 kcal / cm 2, and in the extreme south does not exceed 3 kcal / cm 2. In the summer, the inflow of solar energy depends only on the latitude, since the decrease in the angle of falling the sun's rays towards the north is almost compensated by an increase in the duration of solar radiance. As a result, the total radiation throughout the medium Siberia is about 15 kcal / cm 2 per month, only in central yakutia it increases to 16 kcal / cm 2.
Winter The average Siberia is in the field of exposure to the Asian maximum, the spur of which passes along the southeast outskirts of the country, capturing central yakutia. The pressure is gradually reduced to the northwest, towards a hollow descending from an Icelandic minimum. Almost throughout, with the exception of the North-West, the anticyclonal clear clear, almost cloudless, frosty and dry, often hailless weather dominates in winter. Winter lasts five to seven months. A long stay of little moving anticyclones over the territory of Middle Siberia determines the strong heating of the surface and the surface layer of air, the occurrence of powerful temperature inversions. This contributes to the nature of the relief: the presence of deep river valleys and kitelins, in which the masses of cold heavy air are forced. The dominant continental air of moderate latitudes is distinguished by very low temperatures (even lower than arctic air) and low moisture content. Therefore, January temperature in medium Siberia is 6-20 ° C below the medium-wide.
The stability of winter anticyclonal weather decreases in the direction from the east and southeast to the West and the North-West as the high pressure is removed from the axis. The repeatability of cyclonal weather in the north-west is especially increasing due to the active cyclogenesis on the Taimyr branch of the Arctic Front. Cyclones cause wind enhancement, increasing cloudiness and precipitation, an increase in air temperature.
The lowest averages temperature January Characteristic for the Central-Cool lowland (-45 ° C) and the northeastern part of the medium-grained plateau (-42 ...- 43 ° C). On certain days, the thermometer is lowered in the valleys and the basins of these areas to -68 ° C. To the north of temperatures increase to -31 ° C, and west to -26 ...- 30 ° C. This is due to the smaller resistance of anticyclonal weather and more frequent invasion of the Arctic air, especially from the Barents Sea. But most significantly temperatures increase to the southwest due to the increase in the arrival of solar energy. Here, in the preyaginy, the average temperatures of January are -20.9 ° C (Irkutsk), -18.5 ° C (Krasnoyarsk).
Due to the heavy dryness of air, the abundance of clear sunny days and the constancy (low variability) of the weather is low air temperatures are transferred relatively easily not only by the old-timers of Siberia, but also arriving. However, the exceptional severity and duration of winter require large costs of maintaining comfortable conditions (heat) in housing, increase capital construction and heating.
Ospalkov In winter, a little falls around 20-25% annual amount. This is at most of the territory of about 100-150 mm, and in central Yakutia less than 50 mm. Therefore, despite long winter, as well as on almost complete lack of thaws, the power of snow cover in the middle Siberia is small. In Central Yakutia and in the subwinding at the end of winter, the power of snow cover is less than 30 cm, in the extreme north due to an increase in cyclonic activity, it increases to 40-50 cm. For most of the territory of the power of snow cover 50-70 cm, in the princing part, in The area of \u200b\u200bthe lower and submembering Tunguska is more than 80 cm.
Spring In the middle Siberia late, friendly and short. Almost throughout, she comes in the second half of April, and in the north at the end of May early June. Melting of snow and temperatures rise quickly, but often there are refunds of cold weather due to the breakthroughs of arctic air to the southern outskirts of Middle Siberia.
In summer Due to the warming of the surface over the territory of the Central Siberia, low pressure is established. Air masses from the Arctic Ocean rushes here, Western transfer is enhanced. But the cold Arctic air, entering dry, is very quickly transformed (heated and removed from the saturation state) into the continental air of moderate latitudes. The isotherms of July pass subshir. It is especially clear that it can be seen within the limits of Northcombirsk lowland.
Lowest temperature Summer is observed at Cape Chelyuskin (2 ° C). When moving to the south, July temperatures are growing from 4 ° C. At the foot of the cheerranga mountains up to 12 ° C near the ledge of the medium-grained plateau and up to 18 ° C in central Yakutia. On the low-lying planes of medium Siberia, the influence of the intramaterial position on the distribution of summer temperatures is clearly traced. Here the average temperature of July is higher than on the same latitudes in Western Siberia and in the European part of Russia. For example, in Yakutsk, located near 62 ° C, S.Sh., the average temperature of July is 18.7 ° C, and in Petrozavodsk, located on the same latitude, almost 3 ° C below (15.9 ° C). Within the medium-grained plateau, this pattern is simply influenced by the relief. The high plaster maker determines the smaller surface heating, so at most of its territory the average temperature of July is 14-16 ° C and only the southern colors reaches 18- 19 ° C. (Irkutsk 17.6 °, Krasnoyarsk 18.6 °). With an increase in the height of the summer temperature, it is also decreased, that is, on the territory of the plateau, the vertical differentiation of temperature conditions is traced, especially pronounced at the Puratorna plateau.
In summersharply increasing repeatability of cyclones. This entails an increase in cloudiness and precipitation especially in the second half of summer. Beginning of summer arid. IN july-August usually falls 2-3 times more ospalkovthan for the whole cold period. The sediments fall more likely in the form of prolonged covered rains. Over most part of the middle Siberia, the cyclones of the Arctic Front pass, and above the south of the cyclones of the Mongolian branch of the polar front.
The end of August for most of the territory can be considered the beginning of autumn. Autumn short. The decrease in temperatures is very fast. In October, even in the extreme south, the average monthly temperature is negative and increased pressure is formed.
The main mass of precipitation in the form of rain and snow brings air masses from the West and the North-West. Therefore, the largest annual amount of precipitation (more than 600 mm) is characteristic of the Western, ninesession part of the Central Siberia. The exacerbation of cyclones and the increase in precipitation in these areas contributes to the orographic barrier leaf of the medium-protein plateau. Here at the highest plateaus of the northwestern part (Pouotnian, Somber, Tungusky) drops the maximum amount of precipitation for medium Siberia. Over 1000 mm. To the east, the annual amount of precipitation decreases, in the pool of Lena less than 400 mm, and in central Yakutia, only about 300 mm. Here, evaporation 2.5 times exceeds the annual amount of precipitation. The coefficient of moisture in the area of \u200b\u200bthe lower Aldan and Vilyuya is only 0.4. In the preyassium, the moisturizing is unstable, the humidification coefficient is somewhat less than one. On the rest of the territory of Central Siberia, the annual amount of precipitation is greater or close to evaporation, so the moisture is excessive.
From year to year, the amount of precipitation varies very significantly. In the wet years it is 2.5-3 times higher than the amount of precipitation of dry years.
Insufficient moistening in central Yakutia, areas located at 60-64 ° C.Sh., One of the consequences of a sharp continentality of the climate, reaching the greatest extent. On large spaces of Central Siberia, the excess of annual amplitudes over averages for latitudes is 30-40 ° C.
There are almost no places on the globe (in Russia one northeast), which can compete with medium siberia to the degree of continentality of the climate. Many features of the nature of medium Siberia are associated with a sharp continentality of its climate, with the large contrasts of the season characteristic of it. This is significantly reflected in the processes of weathered and soil formation, on the hydrological regime of rivers and relief-forming processes, on the development and placement of vegetation, on the whole appearance of natural complexes of Central Siberia.
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