Western Siberia- a country with a fairly severe, continental climate. Its large length from north to south determines a clearly pronounced climate zoning and significant differences in climatic conditions in the northern and southern parts of Western Siberia, associated with a change in the amount of solar radiation and the nature of the circulation of air masses, especially western transport flows. The southern provinces of the country, located inland, at a great distance from the oceans, are also characterized by a more continental climate.
IN cold period within the country, two baric systems interact: an area of relatively high atmospheric pressure located above southern part plains, an area of low pressure, which in the first half of winter stretches in the form of a hollow of the Icelandic baric minimum over the Kara Sea and the northern peninsulas. In winter, masses of continental air of temperate latitudes predominate, which come from Eastern Siberia or are formed on the spot as a result of air cooling over the territory of the plain.
Cyclones often pass in the border zone of areas of high and low pressure. Especially often they are repeated in the first half of winter. Therefore, the weather in the maritime provinces is very unstable; on the coast of Yamal and the Gydan Peninsula vouch strong winds, the speed of which reaches 35-40 m/s. The temperature here is even somewhat higher than in the neighboring forest-tundra provinces located between 66 and 69°N. sh. Further south, however, winter temperatures gradually rise again. In general, winter is characterized by stable low temperatures, there are few thaws here. The minimum temperatures throughout Western Siberia are almost the same. Even near the southern border of the country, in Barnaul, there are frosts down to -50 -52 °, i.e., almost the same as in the far north, although the distance between these points is more than 2000 km. Spring is short, dry and comparatively cold; April, even in the forest-marsh zone, is not yet quite a spring month.
In the warm season, low pressure sets in over the country, and an area of higher pressure forms over the Arctic Ocean. In connection with this summer, weak northerly or northeasterly winds predominate, and the role of western air transport noticeably increases. In May, there is a rapid increase in temperatures, but often, with the intrusions of arctic air masses, there are returns of cold weather and frosts. The warmest month is July, the average temperature of which is from 3.6° on Bely Island to 21-22° in the Pavlodar region. The absolute maximum temperature is from 21° in the north (Bely Island) to 40° in the extreme southern regions (Rubtsovsk). High summer temperatures in the southern half of Western Siberia are explained by the inflow of heated continental air here from the south - from Kazakhstan and Central Asia. Autumn comes late. Even in September, the weather is warm during the day, but November, even in the south, is already a real winter month with frosts up to? 20? 35 °.
Most of the precipitation falls in the summer and is brought by air masses coming from the west, from the Atlantic. From May to October, Western Siberia receives up to 70-80% of the annual precipitation. There are especially many of them in July and August, which is explained by intensive activity on the Arctic and polar fronts. The amount of winter precipitation is relatively low and ranges from 5 to 20-30 mm/month. In the south, in some winter months, snow sometimes does not fall at all. Significant fluctuations in the amount of precipitation in different years are characteristic. Even in the taiga, where these changes are less than in other zones, precipitation, for example, in Tomsk, falls from 339 mm in a dry year up to 769 mm into wet. Especially large differences are observed in the forest-steppe zone, where, with an average long-term precipitation of about 300-350 mm/year in wet years falls up to 550-600 mm/year, and in dry - only 170-180 mm/year.
There are also significant zonal differences in evaporation values, which depend on the amount of precipitation, air temperature, and the evaporative properties of the underlying surface. Moisture evaporates most of all in the rainy-rich southern half of the forest-bog zone (350-400 mm/year). In the north, in the coastal tundra, where the air humidity is relatively high in summer, the amount of evaporation does not exceed 150-200 mm/year. It is approximately the same in the south of the steppe zone (200-250 mm), which is already explained by the low amount of precipitation falling in the steppes. However, evaporation here reaches 650-700 mm, therefore, in some months (especially in May), the amount of evaporating moisture can exceed the amount of precipitation by 2-3 times. In this case, the lack of precipitation is compensated by the reserves of moisture in the soil accumulated due to autumn rains and thawing. snow cover.
The extreme southern regions of Western Siberia are characterized by droughts, which occur mainly in May and June. They are observed on average every three to four years during periods with anticyclonic circulation and increased frequency of arctic air intrusions. The dry air coming from the Arctic, when passing over Western Siberia, is warmed up and enriched with moisture, but its heating is more intense, so the air is more and more removed from the state of saturation. In this regard, evaporation increases, which leads to drought. In some cases, the cause of droughts is also the inflow of dry and warm air masses from the south - from Kazakhstan and Central Asia.
In winter, the territory of Western Siberia is covered with snow for a long time, the duration of which is northern regions reaches 240-270 days, and in the south - 160-170 days. Due to the fact that the period of precipitation in solid form lasts more than six months, and thaws begin no earlier than March, the thickness of the snow cover in the tundra and steppe zones in February is 20-40 cm, in the swampy zone - from 50-60 cm in the west up to 70-100 cm in the eastern Yenisei regions. In treeless - tundra and steppe - provinces, where strong winds and snowstorms occur in winter, snow is distributed very unevenly, as the winds blow it from elevated relief elements into depressions, where powerful snowdrifts form.
The harsh climate of the northern regions of Western Siberia, where the heat entering the soil is not enough to maintain a positive temperature rocks, contributes to the freezing of soils and the wide distribution permafrost. On the Yamal, Tazovsky and Gydansky peninsulas, permafrost is found everywhere. In these areas of its continuous (confluent) distribution, the thickness of the frozen layer is very significant (up to 300-600 m), and its temperatures are low (in the watershed spaces?4, -9°, in the valleys?2, -8°). Further south, within the limits of the northern taiga up to a latitude of about 64°, permafrost occurs already in the form of isolated islands interspersed with taliks. Its thickness decreases, temperatures rise to ?0.5?1°, and the depth of summer thawing also increases, especially in areas composed of mineral rocks.
The vast territory of Central Siberia is located between the valley of the Yenisei River and the western foot of the Verkhoyansk Range. It stretches from the shores of the Kara and Laptev Seas to the foothills of the mountains. 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 at the latitude of Yakutsk - 2500 km (about 45°). The area of Central Siberia is about 4 million km2.
Central Siberia is confined to the ancient Siberian platform. Most of the territory is represented by the deeply dissected Central Siberian Plateau, the height of which gradually decreases to the east, towards the Central Yakut Plain and the Lena Valley. The North Siberian Lowland separates the plateau from the Byrranga Mountains (1146 m), occupying the northern and central parts of the Taimyr Peninsula.
Central Siberia is characterized by a significant elevation and dissection of the surface, a sharply continental climate, an almost ubiquitous distribution of permafrost and a less distinct manifestation of zonal differentiation of natural conditions than in Western Siberia, dominance of larch taiga in most of the territory on peculiar permafrost-taiga soils. In a number of regions of Central Siberia, latitudinal zonality is complicated by altitudinal zonality.
In contrast to Western Siberia, the boundaries of Central Siberia do not coincide on different schemes of physical-geographical zoning. This is due to the greater contrast of nature within the country, with its less clear boundaries, the ambiguous interpretation of the actual data available to researchers, and the insufficient comprehensive physical and geographical knowledge of the border regions, characterized by a transitional landscape structure. The greatest disagreements arise regarding the northern and eastern borders of the country.
A great contribution to the study of the nature of Central Siberia was made by large expeditions organized back in the 18th century: the Great Northern Expedition (1733-1743) and its Academic Detachment led by I.G. Gmelin, Academic expeditions of the second half of the century (P.S. Pallas and others).
One of the remarkable events in the geographical study of Central Siberia in the first half of the XIX century. was the Siberian expedition of the naturalist and geographer A.F. Middendorf (1843-1844), organized on behalf of the Academy of Sciences. The researcher was given the task of studying permafrost and life in high latitudes away from the seas. Middendorf was the first scientific explorer of the Taimyr Peninsula. He not only studied organic world of this territory, established the patterns of distribution of tree species on their northern limit, but also characterized the geology and relief of the North Siberian Lowland and the Byrranga Mountains. Middendorf was the first to determine the boundaries of permafrost distribution in Siberia, established a number of temperature gradients by studying permafrost in wells and wells in Yakutsk, and calculated the thickness of permafrost in Yakutsk (204 m), which was later practically confirmed by drilling (214 m).
In the last quarter of the 19th century, a number of expeditionary studies were carried out in Central Siberia, covering the northern and central regions. The expedition of A.L. Chekanovsky (1873-1875), which illuminated, geologically and geographically, the vast expanses of the Central Siberian Plateau from the Lower Tunguska to the mouths of the Olenek and Lena. Chekanovsky was the first to give a description of the Siberian traps.
At the beginning of the 20th century, deposits of Vilyui salt, gold, coal, iron ores were studied. Geologist I.P. Tolmachev (1905-1906) discovered the Anabar plateau and singled out the Anabar massif as a separate unit of the Siberian platform. In 1909-1914 reconnaissance soil and botanical studies were carried out by detachments of the long-term expedition of the Resettlement Administration in the southern part of Central Siberia (in the Angara basin, the upper reaches of the Lena and Lower Tunguska, on the interfluve of the Lena and Vilyui). Materials were gradually accumulated on the climate, the conditions of navigation on rivers, the effect of permafrost on vegetation, etc.
In 1914, the Resettlement Administration published a three-volume work - "Asian Russia" with an atlas of maps, which reflected a fairly complete idea of the nature of Central Siberia for that time.
The main task of research in the Soviet years was to study natural resources 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 searched for minerals. Already in the first post-revolutionary years, S.V. Obruchev (1917-1924) discovered the world's largest Tunguska coal basin, covering an area of over 1 million km2. Since 1925, the Yakut Complex Expedition of the USSR Academy of Sciences has been conducting long-term research. In the postwar years, expeditions of the Council for the Study of Productive Forces worked here to study the resources of the Krasnoyarsk Territory and Yakutia. In 1959, the Institute of Geography of Siberia and the Far East of the Siberian Branch of the USSR Academy of Sciences was established in Irkutsk, conducting various geographical research (now the Institute of Siberian Geography of the Siberian Branch of the Russian Academy of Sciences).
To date, numerous deposits of various minerals have been discovered in the bowels of Central Siberia, the cartographic image of the Central Siberian Plateau, especially its western part, and the Central Yakut Lowland has changed quite significantly, hydropower resources have been studied largest rivers and conditions for the construction of hydroelectric power stations on them. Much has been done to study the relief, climatic conditions and agro-climatic resources, permafrost and its influence on other components of nature and the features of the development of the territory, soils and vegetation, including forest and fodder resources.
Geological structure and history of the development of the territory
Tectonic basis Central Siberia is served by the ancient Siberian platform, the boundary of which is usually drawn along the northern outskirts of the Central Siberian Plateau. The tectonic position of the northern part of Central Siberia is determined ambiguously. For a long time, the territory of Taimyr and the North Siberian Lowland was considered an area of Hercynian folding, then areas of Caledonian, Baikal and Mesozoic folding began to be distinguished within its boundaries. All this was reflected in tectonic maps (1952, 1957, 1969 and 1978). However, the latest works on the tectonics of Taimyr have established that its structure, as well as the structure of the Anabar massif, includes metamorphic basement complexes overlain by Proterozoic deposits. This gave rise to M.V. Muratov (1977) to classify Taimyr as a shield, including it in the Siberian Platform. A growing number of researchers support this view.
Thus, the territory of Central Siberia practically coincides with the Siberian platform. Only the southeastern part of the platform, its Aldan Shield, which underlies the Aldan Highlands, a number of researchers (S.S. Voskresensky, 1968; N.I. Mikhailov, 1961; N.I. Mikhailov, N.A. Gvozdetsky, 1976 and etc.) is not included in the composition of Central Siberia. The reason for this is the significant differences in the modern nature of the Aldan Highlands and Central Siberia, due to the fact that its development over a long Meso-Cenozoic history differs significantly from the development of the rest of the platform and approaches the North Baikal highlands.
Foundation The platform is composed of Archean and Proterozoic folded complexes and has a dissected relief. In the Anabar and Taimyr massifs, basement rocks (gneisses, quartzites, marbles, granites) come to the surface. Areas of shallow basement (up to 1-1.5 km) are located on the outskirts of the Anabar massif, the northern slope of the Aldan shield, on the western margin of the platform (the Turukhan uplift, the slope of the Yenisei massif) and cross the territory from northeast to southwest from the lower reaches of the Lena to the Eastern Sayan. The folded structures of the Yenisei uplift were created in the Late Proterozoic (Baikalian folding).
The basement uplifts are separated by extensive and deep depressions: the Tungusskaya, Pyasinsko-Khatanga, Angara-Lena and Vilyuiskaya, which merges with the Predverkhoyansk marginal trough in the east. The depressions are filled with sedimentary strata of great thickness (8-12 km). Only in the Angara-Lena trough the thickness of the cover does not exceed 3 km.
Formation sedimentary cover The Siberian platform began in the Lower Paleozoic with a general subsidence that caused a major marine transgression. The Cambrian deposits are characterized by high facies variability and breaks in sedimentation, indicating a fairly high mobility of the territory. Along with conglomerates, sandstones, and limestones, red-colored strata containing salts and gypsum accumulated along the margins of the platform in sea lagoons.
But limestones and dolomites predominate among the Lower Paleozoic deposits, which come to the surface in vast areas.
IN late Silurian almost the entire area experienced uplift, which was an echo of the Caledonian folding in the territories adjacent to the platform. The maritime regime has been preserved only in the Pyasa-Khatanga depression and in the northwestern part of the Tunguska syneclise. During Devonian the platform area continued to remain dry land. In the Early Devonian, the South Taimyr aulacogen was laid down, where a complete section of Devonian deposits accumulated.
IN Upper Paleozoic in conditions slow dive on the vast territory of the Tunguska and Pyasa-Khatanga syneclise, a lacustrine-marsh regime is established. Thick layers of the Tunguska suite have accumulated here. The lower part of this suite is represented by the so-called productive strata alternation of sandstones, argillaceous and carbonaceous shales, siltstones and coal interlayers. The thickness of this sequence is up to 1.5 km. It is associated with industrial coal seams spread over a vast territory.
The productive coal-bearing stratum is penetrated by numerous intrusions of basic igneous rocks and is overlain volcanogenic stratum, consisting of tuffs, tuff breccias, lava covers with layers of sedimentary rocks. Its formation is associated with the manifestation of platform fissure magmatism at the end of the Permian - Triassic, due to the activation of faults and the crushing of the basement, which coincided with tectonic movements in the neighboring Ural-Mongolian belt. The effusive and intrusive formations of the basic composition created by him are called traps, and magmatism itself is called trap magmatism.
trapps a characteristic feature of the geological structure of the Siberian platform, which sharply distinguishes it from the Russian platform, the forms of occurrence of traps are diverse. There is a clear pattern in their distribution. Thick basalt (lava) sheets predominate in the Kurey depression, the most deeply subsided northwestern part of the Tunguska syneclise. Transverse intrusions(dykes, veins, stocks) dominate in the central part of the syneclise. Laccoliths and sheet intrusions(sills) are most characteristic of its western, eastern, and southern margins, where the main fault zones pass, separating the syneclise from other structures. The bulk of the explosion tubes (ring structures) is also concentrated here. Outside the Tunguska syneclise, traps are much less common (in Taimyr, along the northern outskirts of the Anabar massif).
The erupted and intruded basaltic magma permeated the rocks of the platform, creating an even more rigid and stable frame, so the western part was hardly subjected to subsidence in the future.
At the turn of the Paleozoic and Mesozoic block movements, ruptures and folding occurred in the South Taimyr aulacogen.
IN Late Mesozoic most of Central Siberia experienced uplift and was a demolition area. The Kurey depression rose especially intensively, turning into an inverted morphostructure - the Putorana plateau, the Anabar arch and the northern part of the Yenisei uplift. Sagging occurs in the Pyasinsko-Khatanga syneclise, along the eastern and southern margins of the platform. It is accompanied by a short-term marine transgression, which did not go far to the south; therefore, among the Jurassic deposits, continental coal-bearing strata with commercial coal reserves sharply predominate. Cretaceous deposits are distributed only in the Pyasinsko-Khatanga syneclise (alluvial-lacustrine low-carbonaceous facies), the Vilyui syneclise, and the Predverkhoyansk trough, where they are represented by a thick (up to 2000 m) alluvial coarse clastic sequence.
TO the end of the Mesozoic the entire territory of Central Siberia was a compact land, which was an area of denudation and the formation of leveling surfaces and weathering crust.
Cenozoic characterized by differentiated oscillatory movements with a general tendency to rise. As a result, erosion processes dominated sharply. The surface was divided by a river network. Paleogene deposits are rare, represented by alluvial clays, sands and pebbles, and are associated with the remains of ancient river valleys. IN the end of the Neogene and in the Quaternary, against the background of a general uplift, the differentiation of vertical movements increased. The Byrranga, Putorana, Anabar and Yenisei massifs rose most intensively. The eastern part of the Vilyui syneclise experienced subsidence, where during the Neogene a sequence of large-clastic red-colored pebbles 3–4 km thick accumulated.
In general, the Siberian platform is characterized by a large activation neotectonic movements compared to Russian. This was reflected in its higher hypsometric position, as well as in the predominance of high plateaus and plains among the morphostructures. As a result of the latest tectonic movements, the ancient hydrographic network was restructured. This is evidenced by the remains of river systems preserved on the watersheds. The general uplift of the territory caused a deep incision of the rivers and the formation of a series of river terraces.
IN early quaternary period land occupied nai large areas and extended north to the boundaries of the modern shelf. Against the background of a general cooling that began in the Neogene, this caused an increase in the continentality and severity of the climate of Central Siberia, a decrease in precipitation. During the Middle Pleistocene boreal transgression The North Siberian lowland and the sunken outskirts of Taimyr were flooded with sea waters. The Byrranga Mountains and Severnaya Zemlya were low islands. The sea came close to the northern and northwestern foothills of the Central Siberian Plateau. This caused an increase in precipitation and the development glaciation. The glaciation centers were the Putorana and Taimyr Plateaus. It is currently established that maximum (Samarovskoye) glaciation was cover. Its border is quite clearly visible only in the southwestern part: the mouth of the Podkamennaya Tunguska, the upper reaches of the Vilyui and Markha and further to the Olenek valley. The eastern segment of the border is not traceable.
After short-term regression sea, during which not only Taimyr, but also Severnaya Zemlya joined the land, begins new maritime transgression. The Zyryansk (Upper Pleistocene) glaciation develops. Ice accumulation took place in Taimyr, the Putorana Plateau and the Anabar massif. The boundary of the maximum distribution of ice during the Zyryansk glaciation passed from the mouth of the Lower Tunguska to the upper reaches of the Moyero River (the right tributary of the Kotui), went around the Anabar massif from the south, went to the lower course of the Anabar River and to the eastern tip of Taimyr. The last phase of the degradation of the Upper Pleistocene glaciation is considered to be the mountain-valley Sartan stage, traces of which have been recorded in the central part of the Putorana Plateau, in Taimyr.
The main feature of the Pleistocene glaciation in Central Siberia was the low thickness, and hence the low mobility of the glacier. The sea approaching the foot of the Central Siberian Plateau was cold, so the air formed above it contained little moisture. Most of the precipitation fell in the northwestern part - on Taimyr and the Putorana Plateau. To the south and east, the amount of precipitation rapidly decreased, and the thickness of the glacier also sharply decreased. These glaciers were "passive". With low mobility of glaciers, their destructive activity was also small. Consequently, the body of the glaciers contained little moraine material and was weakly rounded, i.e., similar to slope deluvial deposits. The small relief-forming role of the Central Siberian glaciers also led to a much weaker preservation of traces of their existence than on the Russian Plain, and even in Western Siberia. Therefore, many issues related to the nature, number, boundaries and age of glaciations in Central Siberia are still debatable.
Huge areas internal parts Central Siberia were in the conditions of the periglacial regime. The cold dry climate contributed to the deep freezing of soils and soils. Permafrost formed, and in some places underground ice. The formation of permafrost was especially intensive at the end of the Middle Pleistocene, during the period of sea regression, when, due to the increase in land area in northern latitudes the continentality and dryness of the climate of Central Siberia sharply increased.
The trend towards climate cooling that has been preserved since the Neogene led to a gradual depletion of vegetation in Central Siberia. Pliocene coniferous-broad-leaved forests, rich in species composition, were replaced in the Lower Pleistocene by depleted Beringian dark coniferous taiga with an admixture of broad-leaved species (linden, oak, hornbeam, hazel) in the southern regions.
Further cooling and the development of glaciation led to the wide distribution of tundra and forest-tundra, and in the southern regions - peculiar cold forest-steppes, represented by an alternation of larch-birch-pine forests with open tundra-steppe spaces. The general warming of the climate during the interglacial favored the advancement of forests to the north.
In the late and post-glacial times, a general uplift of the territory took place, the climate had several warm and cold phases, dry and wet periods associated with changes in circulation conditions (the predominance of meridional circulation, or western transport). This led to a significant mobility of natural zones in the territory of Central Siberia. The increase in the continentality of the climate contributed to the widespread development of herbaceous vegetation of the steppe type and the accumulation of salts in soils. The decrease in continentality and some increase in precipitation led to the replacement of steppe vegetation by forests and forest-steppes.
Relief
Most of the territory is occupied by the Central Siberian Plateau, which was formed in the western part of the Siberian Platform, the structures of which were rigidly soldered as a result of trap magmatism. All this territory in the Meso-Cenozoic steadily rose as a single structure and is represented in the relief by the largest orographic unit. The Central Siberian Plateau is characterized by a significant elevation and relief contrast. The heights within it range from 150-200 to 1500-1700 m. The average height is 500-700 m. hallmark Plateau is a combination of predominantly flat or gently undulating stepped relief of interfluves with deeply incised steep-slope (often canyon-like) river valleys.
By the nature of the distribution of heights and dismemberment, the Central Siberian Plateau is very heterogeneous. Within its limits, more fractional orographic units are distinguished. Max Heights the plateau reaches in the northwest, where the Putorana plateau (up to 1701 m) and Syverma (more than 1000 m) rise.
The close relationship between orographic elements and tectonic structures makes it possible to single out large morphostructures that can be combined into four groups: 1) plateaus, ranges, low- and medium-mountain massifs on ledges of the crystalline basement; 2) bedded uplands and plateaus on sedimentary Paleozoic rocks; 3) volcanic plateaus associated with powerful manifestations of trap magmatism; 4) accumulative and reservoir-accumulative plains. The first three groups combine morphostructures, in the formation of which denudation processes played a predominant role against the background of stable or predominant uplifts, the fourth - morphostructures created by the accumulation of loose material in territories that lagged behind in uplift and experienced recent subsidence.
Among the morphostructures of Central Siberia dominated by inherited(straight lines). This is due to the fact that the latest tectonic movements have updated ancient structures. However, the direction of the latest movements did not coincide everywhere with the direction of earlier tectonic movements. In such places, there is a discrepancy between ancient structures and modern device surfaces. Reversed morphostructures are represented exclusively by elevations in place of negative structures: Putorana, Siverma and the Tunguska plateau correspond to the deepest depressions of the Tunguska syneclise. There are also complex semi-straight and semi-reversed morphostructures in Central Siberia (the Prilenskoye Plateau, the Central Tunguska Plateau, etc.).
Central Siberia has experienced a long period of continental development; therefore, its territory is dominated by denudation relief. The latest uplifts and the alternation of rocks of different stability that make up the surface caused it layering, or gradation. The surface is dissected by a dense network of river valleys. The maximum depth of valley incision (up to 1000 m) is typical for the western part of the Putorana Plateau, and the minimum (50-100 m) for the Central Tunguska Plateau, the Central Yakut and North Siberian lowlands. Most of the valleys are canyon-like, asymmetrical.
The most important distinguishing feature of the river valleys of Central Siberia is a large number of terraces (six to nine), indicating both antiquity and repeated tectonic uplifts of the territory. The height of the upper terraces reaches 180-250 m. Only Taimyr and the North-Siberian lowland are characterized by weak terracing and youthful river valleys. Even large rivers have no more than three or four terraces here.
Almost the entire territory of Central Siberia is characterized by cryogenic(permafrost) morphosculpture. forms of permafrost relief reveal regional confinement. In the West, where dense bedrocks predominate, and the cloak of Quaternary deposits is not continuous and thin, developed thermal denudation, thermal planning associated with subsidence, leveling of the surface during seasonal thawing of frozen soils and ice in them, and solifluction. In the north and east, where loose deposits are widespread, thermokarst, solifluction forms, heaving mounds and hydrolaccoliths (bulgunnyakhs).
Permafrost hinders modern erosion processes and prevents the development of karst, therefore karst forms relief in Central Siberia are much less widespread than might be expected due to the abundance of karst rocks. They are more widely developed in the southern part of the country, where there is no continuous permafrost. So, on the Leno-Angara and Leno-Aldan plateaus there are a lot of karst funnels, wells, blind valleys, etc.
Active physical weathering in a sharply continental climate is associated with an abundance of blocky-stony placers, stone streams Kurumov and talus in mountain ranges, on the surfaces of plateaus and slopes of river valleys.
Despite the large extent of the territory from north to south, there is no clear zoning in the placement of morphosculptures, in contrast to Western Siberia. Erosive and cryogenic morphosculptures dominate throughout the space of Central Siberia. This is due to the nature of tectonic movements and the peculiarities of the harsh climate throughout the entire Quaternary period. In the northern part of the country, the dominant morphosculptures are joined by a relic ancient glacial, and on the south more common karst forms.
Climate
The main feature of the climate of Central Siberia is sharp continentality, due to the position of the territory in the middle part North Asia. It is located at a great distance from the warm seas of the Atlantic Ocean, is protected by mountain ranges from the influence of the Pacific and is subject to the influence of the Arctic Ocean. The continentality of the climate increases from west to east and from north to south, reaching the highest degree in Central Yakutia.
The climate of Central Siberia is characterized by large annual amplitudes of average monthly (50-65°С) and extreme (up to 102°С) temperatures, short transition periods(one-two months) with large daily amplitudes (up to 25-30°C), very uneven intra-annual distribution of precipitation and their relatively small amount. The large differences between winter and summer air temperatures in Central Siberia are primarily due to the strong overcooling of the surface in winter.
Total radiation varies within the country from 65 kcal/cm 2 per year in the northern part of Taimyr to 110 kcal/cm 2 per year in the Irkutsk region, and the radiation balance varies from 8 to 32 kcal/cm 2 per year, respectively. From October to March, the radiation balance in most of the territory is negative. January in the northern part of the country solar radiation practically does not enter, in the Yakutsk region it is only 1-2 kcal / cm 2, and in the extreme south it does not exceed 3 kcal / cm 2. IN summer time the influx of solar energy depends little on latitude, since the decrease in the angle of incidence of the sun's rays towards the north is almost compensated by the increase in the duration of sunshine. As a result, the total radiation throughout the entire territory of Central Siberia is about 15 kcal/cm 2 per month; only in Central Yakutia does it increase to 16 kcal/cm 2 .
in winter Central Siberia is in the sphere of influence of the Asian High, the spur of which runs along the southeastern outskirts of the country, capturing Central Yakutia. The pressure gradually decreases to the northwest, towards a trough extending from the Icelandic low. Almost throughout the entire territory, with the exception of the northwest, anticyclonic clear, almost cloudless, frosty and dry, often windless weather prevails in winter. Winter lasts five to seven months. The long stay of low-moving anticyclones over the territory of Central Siberia causes a strong cooling of the surface and the surface layer of air, the occurrence of powerful temperature inversions. This is also facilitated by the nature of the relief: the presence of deep river valleys and basins, in which masses of cold heavy air stagnate. The continental air of temperate latitudes prevailing here is characterized by very low temperatures (even lower than the Arctic air) and a low moisture content. Therefore, the January temperatures in Central Siberia are 6-20°C lower than the mid-latitude ones.
The stability of winter anticyclonic weather decreases in the direction from the east and southeast to the west and northwest as one moves away from the high pressure axis. The frequency of cyclonic weather especially increases in the northwest due to active cyclogenesis on the Taimyr branch of the Arctic front. Cyclones cause an increase in wind, an increase in cloudiness and precipitation, and an increase in air temperature.
Lowest averages January temperatures characteristic of the Central Yakut lowland (-45°С) and the northeastern part of the Central Siberian plateau (-42...-43°С). On some days the thermometer drops down to -68°С in the valleys and basins of these regions. To the north, temperatures rise to -31°C, and to the west to -26...-30°C. This is due to the less stable anticyclonic weather and the more frequent intrusion of Arctic air, especially from the Barents Sea. But temperatures increase most significantly towards the southwest due to an increase in the arrival of solar energy. Here, in Pre-Sayanye, the average January temperatures are -20.9°C (Irkutsk), -18.5°C (Krasnoyarsk).
Due to the great dryness of the air, the abundance of clear sunny days and the constancy (low variability) of the weather, low air temperatures are relatively easily tolerated not only by the old-timers of Siberia, but also by visitors. However, the exceptional severity and duration of winter require large expenditures to maintain comfortable conditions (heat) in dwellings, and increase the cost of capital construction and heating.
precipitation little rain falls in winter, about 20-25% annual amount. This is about 100-150 mm in most of the territory, and less than 50 mm in Central Yakutia. Therefore, despite the long winters, as well as the almost complete absence of thaws, the thickness of the snow cover in Central Siberia is small. In Central Yakutia and in the Pre-Sayan region, at the end of winter, the thickness of the snow cover is less than 30 cm; in the far north, due to an increase in cyclonic activity, it increases to 40–50 cm. In most of the territory, the thickness of the snow cover is 50–70 cm; area of the Lower and Podkamennaya Tunguska, - more than 80 cm.
Spring in Central Siberia late, friendly and short. Almost throughout the entire territory, it occurs in the second half of April, and in the north - at the end of May and beginning of June. The melting of snows and the increase in temperatures proceed rapidly, but returns of cold weather are often observed due to breakthroughs of arctic air to the southern outskirts of Central Siberia.
In summer in connection with the heating of the surface over the territory of Central Siberia, a reduced pressure is established. Air masses rush here from the Arctic Ocean, the western transfer is intensifying. But the cold Arctic air, entering the land, very quickly transforms (warms up and moves away from the state of saturation) into the continental air of temperate latitudes. July isotherms pass sublatitudinally. This is especially clearly seen within the North Siberian Lowland.
Lowest temperature in summer it is observed at Cape Chelyuskin (2°C). When moving south, July temperatures rise from 4°C at the foot of the Byrranga Mountains up to 12°C near the ledge of the Central Siberian Plateau and up to 18°C in Central Yakutia. On the low plains of Central Siberia, the influence of the inland position on the distribution of summer temperatures is clearly traced. Here, the average July temperature is higher than at the same latitudes in Western Siberia and the European part of Russia. For example, in Yakutsk, located near 62°C north latitude, the average July temperature is 18.7°C, and in Petrozavodsk, located at the same latitude, it is almost 3°C lower (15.9°C). Within the limits of the Central Siberian Plateau, this regularity is obscured by the influence of the relief. The high hypsometric position causes less heating of the surface, therefore, in most of its territory, the average temperature in July is 14-16 ° C and only in the southern outskirts does it reach 18- 19°С(Irkutsk 17.6°, Krasnoyarsk 18.6°). With an increase in the height of the area, summer temperatures decrease, i.e., on the territory of the plateau, a vertical differentiation of temperature conditions is traced, which is especially clearly expressed on the Putorana Plateau.
In summer increases sharply cyclone frequency. This entails an increase in cloudiness and precipitation, especially in the second half of summer. The beginning of summer is dry. IN July-August usually falls 2-3 times more precipitation than for the entire cold period. Precipitation falls more often in the form of long continuous rains. Cyclones of the Arctic front pass over most of Central Siberia, and cyclones of the Mongolian branch of the polar front pass over the south.
The end of August for most of the territory can be considered the beginning of autumn. Autumn is short. Temperatures are dropping very quickly. In October, even in the extreme south, the average monthly temperature is negative and high pressure is formed.
The bulk of precipitation in the form of rain and snow is brought by air masses coming from the west and northwest. Therefore, the largest annual precipitation (more than 600 mm) is characteristic of the western, Yenisei part of Central Siberia. The aggravation of cyclones and an increase in precipitation in these areas is also facilitated by the orographic barrier - the ledge of the Central Siberian Plateau. Here, on the highest plateaus of the northwestern part (Putorana, Siverma, Tunguska), the maximum amount of precipitation for Central Siberia falls - over 1000 mm. To the east, the annual precipitation decreases, amounting to less than 400 mm in the Lena basin, and only about 300 mm in Central Yakutia. Here evaporation is 2.5 times higher than the annual amount of precipitation. The moisture coefficient in the area of the lower reaches of the Aldan and Vilyui is only 0.4. In the Pre-Sayan region, humidification is unstable, the moisture coefficient is somewhat less than unity. In the rest of the territory of Central Siberia, the annual amount of precipitation is greater or close to evaporation, so moisture is excessive.
The amount of precipitation varies greatly from year to year. In wet years, it is 2.5-3 times higher than the amount of precipitation in dry years.
Insufficient moisture in Central Yakutia, the regions located at 60-64° N, is one of the consequences of the sharp continental climate, which reaches its greatest extent here. In large areas of Central Siberia, the excess of annual amplitudes over the average for latitudes is 30-40°C.
There are almost no places on the globe (in Russia - only the North-East) that can compete with Central Siberia in terms of the degree of continental climate. Many features of the nature of Central Siberia are associated with the sharp continentality of its climate, with its characteristic great contrasts of the seasons of the year. This significantly affects the processes of weathering and soil formation, the hydrological regime of rivers and relief-forming processes, the development and distribution of vegetation, and the entire appearance of the natural complexes of Central Siberia.
Siberia is a huge picturesque territory, which occupies more than 60% of the area of the whole of Russia. It lies in three climatic zones (temperate, subarctic and arctic), so the natural conditions and weather differ markedly in different regions of the Federation. This article only describes general information and climate features of the region.
Climate of Western Siberia
Western Siberia stretches from the Ural Mountains to the Yenisei River. Most of its territory is occupied by the West Siberian Plain. The climate in this area is continental.
Climate features are formed from the indicators of weather regimes of all subjects of the Russian Federation located in this part of Siberia. Completely in the expanses of Western Siberia lie the Trans-Urals, Omsk, Kemerovo, Novosibirsk and Tomsk regions, as well as the Altai Territory and the Republic of Khakassia. Partially included here are the Chelyabinsk, Sverdlovsk, Tyumen and Orenburg regions, Krasnoyarsk region, the Republic of Bashkortostan, as well as Khanty-Mansi Autonomous Okrug and YNAO.
Precipitation, wind
The climate of Siberia in its western part is not affected by the Atlantic air masses, since this territory is well protected Ural mountains.
From April to September, Western Siberia is dominated by winds brought from the Arctic Ocean and from the east. In the form of cyclones and anticyclones, arctic ones come bringing coolness with them.
Dry Asian winds blow from the south and southwest (Uzbekistan, Kazakhstan) and bring clear and frosty weather with them in cold weather.
The weather in Siberia is stable, so the average annual rainfall rarely changes in one direction or another. Approximately 300-600 mm of atmospheric moisture falls annually, with most of it falling on summer period and autumn. This is meteorological precipitation in the form of rain. Snow falls about 100 mm in almost the entire space of Western Siberia. Of course, this is an average. For example, in autonomous regions snow cover reaches a level of 60-80 cm. By comparison, in the Omsk region this mark barely reaches 40 cm.
Temperature regime
Features of the climate of Siberia in its western part is that most of the territories there are occupied by swamps. They have a huge impact on air humidity, which entails a decrease in the influence of the continental climate.
Winter in the north of Western Siberia lasts about nine months, in the center - about seven. The south was a little more fortunate, there climatic winter reigns for five months. These calculations are directly related to the average air temperature in each region. In this way, South part Western Siberia has an average winter temperature of -16°C, while northern Siberia has an average of -30°C.
Summer also does not please these regions, since the average temperature ranges from +1°C (in the north) to +20°C (in the south).
The lowest mark on the thermometer was recorded at -62 ° C in the valley
Climate of Eastern Siberia
Located on the territory from the Yenisei to the watershed ranges Pacific Ocean. Features are determined by its position in the temperate and cold zones. That is why it can be described as harsh and dry. Unlike Western Siberia, Eastern Siberia is sharply continental.
Of great importance for natural conditions is the fact that Eastern Siberia is located mainly in elevated and mountainous areas. There are no marshes here, and lowlands are rare.
The following regions are located in its expanses: the Krasnoyarsk and Trans-Baikal Territories, the republics of Yakutia, Tuva, Buryatia, and the Irkutsk Region. Siberia (Russia) in this part is quite severe, even unpredictable.
Precipitation, wind
IN winter time in Eastern Siberia, the south dominates, bringing with it anticyclones from Asia. The result is the establishment of clear and frosty weather.
In spring and summer, dry Asian air also prevails in Eastern Siberia, but despite this, south winds often replaced by air masses from the east, which are carried by the sea winds of the Pacific Ocean. And the cold Arctic air is brought here by the northern ones.
The weather in Siberia decreed that precipitation over the area of Eastern Siberia is unevenly distributed. Their smallest number is in Yakutia: only 250-300 mm per year in almost all areas of the republic. The Krasnoyarsk Territory is in some way a champion. It accounts for the largest number precipitation: from 600-800 mm (west) to 400-500 mm (east). In the rest of Eastern Siberia, the annual amount of precipitation is 300-500 mm.
Temperature regime
The winter months are extremely cold in Eastern Siberia. The temperature amplitude changes dramatically depending on the transition of the continental climate in the west to the sharply continental climate of Siberia in the east. If in the south of the Krasnoyarsk Territory the average temperature of the second month of winter is about -18°C, then to the north it drops to -28°C, and not far from the city of Tura it reaches -36°C.
The northwest of Eastern Siberia has an average January temperature of about -30°C, and on the way to Norilsk and further east it drops to -38°C. Northern Yakutia, where the average temperature is extremely low, -50°C, set a record in 1916, when the thermometer showed -82°C.
In the south and southwest, frosts noticeably weaken. In Yakutsk itself, this is almost imperceptible, but in the Trans-Baikal Territory and Buryatia, the average January temperature rises to -24 ... -28 ° C.
average temperature of the warmest month of the year varies from +1...+7°C in the north of the Krasnoyarsk Territory and the Republic of Yakutia to +8...+14°C in the central part and up to +15...+18°C in the south. The zone of mountain ranges and elevations, characteristic of such regions as the Irkutsk region, Buryatia, and the Trans-Baikal Territory, causes an uneven distribution of heat. Thus appear significant differences in the average monthly temperatures of the spring-summer period. On average, in July the thermometer stops at +13 to +17°C. But in some places the temperature range can be much larger.
Siberia (Russia) in its eastern part is characterized by a cold climate. Winter lasts from 5-6 months (Baikal region) to 7-8 months (the center of Yakutia and the Krasnoyarsk Territory). In the far north, summer is almost impossible to wait for, since winter reigns there for about 11 months. In the central and southern parts of Eastern Siberia, the warm season (including spring and autumn) lasts from 1.5-2 to 4 months.
The climate of the northern regions of Siberia
The northern regions are located in the zone of the Arctic and subarctic belts. Territory Arctic deserts- these are continuous glaciers and impenetrable snow. Almost no vegetation can be found there. The only oases in this ice realm are mosses and lichens that can withstand low temperature fluctuations.
The climate of Siberia in this part is greatly influenced by albedo. From the surface of the snow and the edge of the ice are constantly reflected Sun rays, i.e. heat is repelled.
Although the average number annual precipitation few (about 400 mm), the soil is saturated with moisture and snow very deeply and freezes.
Harsh aggravate terrible hurricanes and snowstorms, which sweep across the entire territory at great speed and leave behind traces of giant snowdrifts.
Also, this part of Siberia is characterized by frequent fogs in the summer, as the ocean water evaporates from its surface.
During the summer, the earth does not have time to warm up, and the snow melts very slowly, because the average temperature ranges from 0 to + 3 ° C.
Here you can see such unusual natural phenomena like polar night and northern lights.
Permafrost
Surprisingly, more than 60% of Russia's area is permafrost. This is mainly the area of Eastern Siberia and Transbaikalia.
Permafrost is characterized by the fact that the ground never thaws completely. In some places it is frozen a thousand meters down. Yakutia recorded a record for the depth of permafrost - 1370 meters.
In Russia, it exists with its own dungeon, in which you can consider this amazing phenomenon.
Climate of Southern Siberia
The mountainous relief, located in Southern Siberia, was the reason for the contrast of the climate.
Continentality increases towards the east, where precipitation is plentiful on the slopes. It is because of them that numerous snows and glaciers are so common. Western Altai.
In winter, the climate of Siberia in this part is characterized by cloudless, sunny weather with low temperatures. Summer is cool and short everywhere, only in the intermountain basins it is dry and hot (the average temperature in July is about +20 o C).
It is very interesting to answer the question of how the oceans influence the climate of Southern Siberia. Despite the fact that Russia does not have direct contact with the Atlantic Ocean, it is he who has the greatest impact on the climate of this territory of the country. In southern Siberia, it brings heavy snowfalls and, at the same time, a decrease in frost and thaw.
The climate of the Siberian part of Russia is quite severe, but this fact does not prevent it from being the heart of our country.
Department of Education of the Administration of the City District Sukhoi Log Municipal Autonomous educational institution"Secondary school No. 5"
Features of the nature of Central Siberia
Performer: geography teacher Listratova O.I.
Sukhoi Log 2016
Significant height amplitudes and a strongly rugged relief determine a distinct altitudinal zonality, which is especially typical for the most elevated northern provinces of the country. So, in the mountains of the lower reaches of the Lower Tunguska at an altitude of up to 250-400 m dark coniferous taiga is located, which is replaced by light coniferous larch forests higher up. At an altitude of 500-700 m they pass into mountain larch sparse forests or thickets of shrubby alder; tops of arrays rising above 700-800 m , are occupied by mountain rocky tundra.
The soils and vegetation of Central Siberia develop in a sharply continental, harsh climate. Precipitation here is less than in the more western regions of the USSR, the thickness of the snow cover is usually small, and permafrost is almost universal. In contrast to Western Siberia, soils are formed mainly on rubble and loamy eluvium of bedrocks; they are usually stony and have small power. There are few swamps, and they are found mainly within the lowlands and on flat, poorly drained interfluves.
In the northern half of the Central Siberian taiga, gley-permafrost-taiga and permafrost-taiga soils are formed. Their main features are related to the permafrost horizon lying close to the surface, which creates conditions for a non-leaching water regime and hinders the removal of salts. Permafrost-taiga soils are characterized by an acidic reaction and the presence of traces of soil mass movement under the influence of permafrost phenomena: bulging as a result of hydrodynamic stresses, slumping and slumping. These processes contribute to the constant mixing of the material and cause weak differentiation of soil profile horizons. However, in its upper part there is usually a thin horizon of coarse light humus, and below there are numerous traces of gleying - the result of periodic summer waterlogging experienced by the soil mass. On the loess-like loams of Central Yakutia, soddy-forest and permafrost-taiga pale (neutral) solodized soils are formed, which have no analogues anywhere on the globe.
Significant areas are also occupied by soils that form in mountainous terrain - mountain-tundra (in the mountains of Byrranga, Putorana and in the Anabar massif), mountain-frost-taiga and mountain-forest carbonate. In the south, in the Angara region, zonal sod-podzolic and sod-forest browns dominate, and in the forest-steppe "islands" - gray forest soils and black earth.
It has a peculiar character vegetation cover taiga zone, which occupies more than 70% of the territory of Central Siberia. Within its boundaries, light coniferous forests of Siberian larch (in the west) and Daurian larch (in the east) predominate. The dark coniferous taiga has been pushed back to the extreme western regions and to the elevated areas of the southern provinces. Warm and not very humid summers are the reason for the more significant advancement of forests to the north than anywhere else: in Taimyr, woody vegetation occurs at 72 ° 50 ′ N. sh.
The existence in the taiga, often even near the Arctic Circle, of steppe islands and areas of halophyte vegetation on solonchaks (Central Yakut Lowland) is associated with the peculiarities of the continental climate. The duration of spring here is no more than three or four weeks; under the warm rays of the sun, the snow cover unanimously disappears, and vegetation develops with cinematic speed. That is why in the vicinity of Yakutsk, during a short but hot summer, many vegetables and even watermelons ripen; Central Siberia is one of the parts richest in various natural resources. Soviet Union. However, due to the poor development of the territory, its wealth is still far from being fully used.
In the first place among the natural wealth of the country are various minerals, the deposits of which are associated with Precambrian, Paleozoic and Mesozoic rocks. In Central Siberia there are the largest coal basins, deposits of iron ores, non-ferrous metals, gold, graphite, diamonds, various raw materials for chemical industry and production building materials. Mining is the most important sector of the economy of Central Siberia. (See Figure 10)
Fig.10 Natural resources
The fauna of Central Siberia is richer and more diverse than the fauna of the West Siberian Plain. More mammals and birds live here; many of them are important commercial value(squirrel, Siberian weasel, ermine, muskrat, arctic fox (see Appendix 10), etc.). Animals such as musk deer appear(Moschus moschiferus) (see annex 12), northern pika(Ochotona hyperborea) and bighorn sheep (Ovis nivicola) ; more often than in Western Siberia, there are sable (see Appendix 9) and reindeer(See Annex 11). In some taiga regions of Yakutia, lying even near the Arctic Circle, such steppe animals live as the long-tailed ground squirrel (“Eurazhka” - Citellus undulatus ) and black-capped marmot(Marmota camtschatica) . Some southern birds also penetrate far to the north: bittern(Botaurus stellaris) , rock pigeon(Columba livia) , field lark. There are also many taiga birds that are not typical for Western Siberia: stone capercaillie(Tetrao urogalloides), black crow (Corvus corone orientalis) , killer whale and several species of passerines. The diversity of the fauna of Central Siberia is associated with the relatively ancient age of the country and with the differences in its modern natural conditions.
Thus, the flora and fauna are greatly influenced by its specific harsh sharply continental climate and the almost universal distribution of permafrost associated with it. Permafrost conservation is favored by low average annual temperatures and the features of the cold period inherent in this climate: low temperatures, low clouds, contributing to night radiation. (see fig. 12).
Rice. 12 Animal world Central Siberia
Chapter 3. Ecological features of the nature of Central Siberia
3.1. Anthropogenic changes nature
INXV - XVIcenturies in Central Siberia, small peoples and tribes lived, scattered over a vast territory. Only the Yakuts, who inhabited the Lena-Vilyui (Central Yakut) plain and the adjacent river valleys, were engaged in cattle breeding (horse breeding), hunting and fishing, the rest - hunting and fishing. Some tribes had deer.
After the annexation of the territory to Russia, the economic structure of the population essentially does not change, the development of fur resources only intensifies. Already at the beginning of the 18th century, 40% of the population lived in Pre-Sayanye, and by late XIX in. - 80% of the population of Central Siberia. By the middle of the XVIII century. here the Moscow (Siberian) tract was laid to the Pacific coast, and in 1893 - 1899. railroad part Trans-Siberian Railway. This contributed to the further increase in population and development Agriculture to meet the needs of the entire local population. Fur trade continues to develop throughout the rest of the territory.
FROM mid-nineteenth in. pockets of gold mining appear in the Yenisei Ridge, and in last years century, when coal was needed in connection with the exploitation railway, its production began in the Cheremkhovo basin. In Pre-Sayanye and in some places near the Angara, logging begins. All this led to changes in nature in the southwestern, pre-Sayan, part of Central Siberia. In the rest of the territory, the changes affected only the animal world. Due to immoderate hunting, the main object of hunting - sable - has almost completely disappeared in many places. The number of squirrels has also significantly decreased.
The current direction of the economy in Central Siberia is preserved in the post-revolutionary years. At the same time, focal agriculture is moving to more northern regions, the number of livestock is increasing, and the volume of logging in the Angara basin and in the upper reaches of the Lena is increasing. In Soviet times, new centers of industrial development of Central Siberia arose on the basis of the use of its mineral resources in the regions of Norilsk and Mirny. All this entailed an increase in human impact on nature, but at the same time, the local nature of the impact itself was preserved. Only unintended impact on vegetation covered large areas. This is due to the spread of forest fires, most often caused by human faults. 
Rice. 13 Forest fire of 1915 (according to V.B. Shostakovich)
Fires sometimes covered vast areas. For example, the catastrophic fire of 1915 spread from the Sayans to the lower reaches of the Yenisei and from the Ob to the upper reaches of the Podkamennaya Tunguska. During this fire, about half of the forests in the Yenisei basin within Central Siberia were destroyed. (see fig. 13)
economic basis development of the economy of Central Siberia at the present time is the approximation of industry to the sources of raw materials. But the development of natural resources in the harsh Siberian climate is costly and careful attitude to nature in the process of exploiting its resources. In recent decades, more and more foci local change nature in the course of mining, transport and energy construction.
Man actively invades nature and often changes the regime of permafrost, which entails not only a change in the soil and vegetation cover, but often also in the relief. These changes are often irreversible, although they do not yet cover large areas. The main areas of human impact on nature are the Angara basin, the regions of Norilsk, Western Yakutia and the Central Yakut Plain.
3.2. Economic and environmental prospects for the development of the territory of Central Siberia
On the map Irkutsk region or the Krasnoyarsk Territory, huge undeveloped massifs of the Siberian taiga are depicted; an abundance of plain green spaces, disturbed only by thin blue threads of rivers, is striking. Only the Sayan region can be considered inhabited, where the majority of the population lives and the main enterprises are concentrated. It is here that the seven main industrial centers of the region are located: Angarsk, Bratsk, Zima, Irkutsk, Krasnoyarsk, Cheremkhovo and Shelekhov. Unfortunately, all of them were included in the list of cities with the highest level of air pollution in Russia. Hazardous waste threatens human health, causing significant damage to forests and soils. The environmental problems of the region will become more acute with the further development of its huge natural resources.
The economic basis for the development of the economy of Central Siberia is the approach of industry to the sources of raw materials. But the development of natural resources in the harsh Siberian climate costs a lot and respect for nature in the process of exploiting its resources. IN last decade there are more and more centers of local changes in nature in the course of mining in the course of transport and energy construction.
Man actively invades nature and often changes the regime of permafrost, which entails not only a change in the soil and vegetation cover, but often also in the relief. These changes turn out to be irreversible, although they do not yet cover large areas. bright representative areas of human impact on nature is the Angara basin. In order to preserve unique and typical natural complexes, to protect animals, in 1985, the Ust-Lena Reserve was created in the lower reaches of the Lena on an area of \u200b\u200babout 1.5 million hectares, and in the Tunguska province - the Central Siberian Reserve with an area of slightly less than 1 million hectares.
It is important to preserve and preserve as far as possible the Central Siberian taiga, not only for ethical and moral reasons, as a unique habitat, but also because, apparently, coniferous forest plays a significant role in the regulation of CO2 reserves in the Earth's atmosphere. This became apparent as a result latest research. The regeneration of the taiga is painfully slow. When layers of soil are removed, permafrost rises to the surface and prevents new trees from growing. It is now obvious that it is human impact that causes the most dramatic changes in the taiga ecosystem.
Large-scale mining of iron ore, gold and minerals has left its mark on large areas of the region. Roads, settlements and all infrastructure have completely changed the local environment. Moreover, metallurgical plants and pulp and paper mills seriously pollute the air.
Influencing factors include:
- deforestation;
- water and air pollution;
- Forest fires;
- roads, dams, hydroelectric power stations, pulp and paper mills, metallurgical plants, mining and so on.
Of particular value are the pine and pine-deciduous forests of the Angara basin, where over 35 million hectares are concentrated. Pine forests.
The forest is an important physical and geographical factor that creates a special climate, retains moisture, and reduces wind speed. The vast majority of the territory of the Central Siberian Plateau belongs to the forest areas.
Today, the anthropogenic pressure on the fauna of Central Siberia has increased many times over, although today one can be proud of the leadership in the world in the extraction of valuable fur animals, many birds and river fish, then soon without the organization of cultural hunting and fishing and fish farms, without the creation of reserves and wildlife sanctuaries, nothing of this will not.
Conclusion
Target term paper: to reveal the features of the nature of Central Siberia has been successfully achieved. The main components of nature were characterized. It was possible to study and analyze archival materials on this topic. The characteristics of the territory of Central Siberia are given, the features of its nature are revealed. Contribution shown scientific researchers in the study and research of this territory.
The work done allowed us to draw the following conclusions:
1. Central Siberia is a complex formation in terms of relief and history of formation. On its territory there are both plateaus and mountains with steep river valleys and narrow watershed ridges. So, the Putorana Plateau is the highest part of the Central Siberian Plateau.
2. The territory of Central Siberia is characterized by river valleys with well-defined terraces and numerous small valleys. The presence of terraces testifies to the slow movements of the earth's crust that took place on the territory of the plateau.
3. The climate is sharply continental. Permafrost is ubiquitous. The formation of permafrost took place in ice Age. Permafrost is a legacy of the Ice Age.
4. The Central Siberian region has a rich material and raw material base, sufficiently prepared for industrial development.
5. Water resources of the Central Siberian Plateau are one of the most valuable natural resources. Resources groundwater can be renewed in accordance with the natural cycles characteristic of a particular climatic zone, the geological structure and landscape features of the territory.
6. Physical and geographical conditions, the considerable length of the Central Siberian Plateau, the complexity and dissection of the relief determine the diversity of natural zones. natural areas, represented by the forest tundra and taiga are integrated ecological complexes that arise when plants and animals interact with the environment. Each of the zones is characterized by its own set of plant life forms and a specific dominant form.
These findings confirm that the nature of Central Siberia is unique.
In this way, this work can be used in the practical activities of teachers, students during teaching practice.
Rakovskaya E. M., Davydova M. I. physical geography Russia: Proc. for stud. higher textbook establishments. - M .: Humanit. ed. center "Vlados", 2009
Okladnikov A.P. "Discovery of Siberia" 2014
V.P. Dronov, I.I. Barinova, V.Ya. Rom, A.A. Lozhbanidze Geography of Russia. Economy and geographic areas. Moscow "Drofa" 2010
Voskresensky S.S. Geomorphology of Siberia 1962.
Golovachev P.Sh. "Economic geography of Siberia" 2009
Paramuzin Yu.L. Secret of Siberia. M.: Thought, 1985.
Rakovskaya E.M., Davydov M.I. Physical geography of Russia. Proc. For students of pedagogical higher educational institutions. Part 2. M.: VLADOS, 2001.
Great Soviet Encyclopedia. Volume 23. M.: Soviet Encyclopedia, 1976.
Mikhailov N.I., Gvozdetsky N.A. "Physical geography of the USSR", 1987.
Prokaev V.I. "Physical-geographical zoning" Uch. Allowance for students Ped. Institutes for Geography. Ed. Enlightenment, 1983.
Popov A.I. Permafrost phenomena in the earth's crust. Ed. Moscow University 2005.
Central Siberia Ed. Moscow "Nauka", 2007
Babushkin V.A. "Practicum"
Geocryology of the USSR. Central Siberia 1989
Climatic conditions and microclimate of the taiga geosystems of Siberia. Novosibirsk: Nauka, 1980.
Tushinsky G.K., Davydova M.I., Physical Geography of the USSR. M .: "Enlightenment", 1976. https://en.wikipedia.org
Annex 11 Reindeer
Annex 12 Musk deer
In the vast territory of Eurasia, more than ten million square kilometers is occupied by boundless Siberia. Depending on the territorial location and relief features, the climate of Siberia cannot be called homogeneous. Yes, the climate Central Siberia will be sharply continental, that is, very cold in winter and very hot in summer, and in the south of Western Siberia, the natural conditions are no longer so severe and allow the cultivation of many heat-loving crops.
Endless expanses
In the geographical concept, Siberia is considered the territory on the western side of the end of the Ural chain of mountains and in the East - the coast of the Pacific Ocean. Natural northern border- the ocean, and Southern Territory includes regions of Kazakhstan and Mongolia.
The whole vast Siberia according to its relief and climatic features can be divided into such geographical zones as Western, Middle, Eastern and the mountains of Southern Siberia. Each zone has its own climatic features, strongly dependent on the oceans, mountain ranges, many rivers and lakes, as well as the movement of air masses.
West Siberia
The borders of Western Siberia in the north extend to the Kara Sea, in the south - to the mountainous terrain of Kazakhstan and Altai, from the west it is bordered by the Ural Mountains, and from the east - the Yenisei River.
The climate of Western Siberia is temperate continental, in the north - arctic and subarctic, depending on the formation of air masses emanating from the Arctic. The continentality of the climate is expressed by a significant fluctuation in average daily temperatures and a relatively scarce amount of precipitation falling over most of the territory mainly at the end of summer.
The relief of Western Siberia is mostly flat, with many large lakes and swamps. Thanks to this relief, Atmosphere pressure and air masses from the north and from the south move freely and mix with each other.
In the winter months in Western Siberia, frosts are characteristic within -20 ° ... -25 °, but lower temperatures are also observed in the Yenisei valley up to -30 °. The minimum recorded winter temperature is -55°. Also, the winter months do not pass without blizzards, mainly from the south. Precipitation at the level of 20-30%. Permanent snow cover in the north of Western Siberia is observed already in September, and in November in the south.
During the summer months, the direction of the winds changes to the north, and atmospheric pressure tends to decrease towards the southeast. The spread of July average temperatures in different regions of Western Siberia is large: from +4 ° in the north to +22 ° in the south. The absolute maximum in extreme southern points was +45°. In summer, the amount of precipitation is 70-80%, and drought is often possible in the southern regions.
Siberia Central
Moving east of Western Siberia, one can observe an increase in the continentality of weather conditions. The climate of Central Siberia is characterized as sharply continental. Its borders stretch from the Yenisei Valley in the west to the Verkhoyansk Range in the east.
The main feature of the climate of Central Siberia is the large amplitude of the difference between summer and winter.
In winter, almost the entire part of Central Siberia has clear, sunny, frosty weather with almost no winds and precipitation. This climate is facilitated by a relief characterized by deep basins and river valleys, in which frosty air stagnates and cools even more. The average temperature in the cold months can reach up to -42 ° ... -45 ° (in the northeastern basins of the Central Siberian Plateau), and closer to southern zones will be -19 °...-21 °.
Summer temperatures are caused by the movement of air masses from the Arctic Ocean.They also fluctuate considerably and depend on the terrain. When moving north, the average summer temperature remains within +4 °...+6 ° (Cape Chelyuskin), and to the south it can reach +15 °...+18 ° (Central Yakutia).
East
The climate of Eastern Siberia is distinguished by its severity, and throughout its territory, from the Yenisei River to the Pacific Ocean, it is sharply continental.
The formation of the climate in Eastern Siberia is significantly influenced by the remoteness of the Atlantic Ocean and the Asian anticyclone, which is caused by dry air and low precipitation.
The vast taiga occupies almost the entire territory of Eastern Siberia. The winter period can last from 5 to 8 months, but the days are mostly sunny, clear and calm.
Winter temperatures are mostly in the range of -40 °...-50 °, but the temperature was recorded below -70 °. Frosty air without thaws is preserved here thanks to relief depressions and hollows.
Summer, especially in the southern part, cannot be called cold. After all, July temperatures here can be higher than in European latitudes. They can reach +38...+39 degrees, but usually they are +27°...+31°.
South and mountainous south
The southern part of Siberia is predominantly mountainous. Beginning in the west with the Altai Mountains, forming a vast mountain complex, it ends up to the Amur region.
The region is considered seismically dangerous, earth vibrations can reach 5-7 points.
The climate of Southern Siberia is greatly influenced by the Asian anticyclone. It also affects the mixing of air masses from the Atlantic and North arctic oceans. Due to this, the climate of the mountains of Southern Siberia is continental and sharply continental.
So, winters here are mostly with little snow, on average, the thickness of the snow cover is only 10-12 cm. winter weather sunny, clear and with low temperatures, especially they appear in the basins and can reach -50 ° ... -60 ° due to the accumulation of cold air from the mountains. But in Altai, winters are milder, thanks to western cyclones, which bring clouds and precipitation with them.
Summer in Southern Siberia is short. Both in early June and from mid-August, night frosts are quite likely. summer months in the mountains are mostly dry, with an average July temperature of +20 °.
Almost the entire vast territory of Siberia (except for the southern regions) is subject to such a phenomenon as "permafrost". Max Depth it in the soil in the northern regions can reach more than one hundred meters, and decrease to the south - 35-60 meters. But even in the southern regions there are "islands" of permafrost, 10-15 meters deep. For scientists, it is of scientific value, because in its conditions the remains of long-extinct animals have been perfectly preserved.
Thanks to the cloudless, windless, sunny winter climate with dry air, locals perfectly adapted to the bitter cold. A fairly low temperature of -35 ° is easier to bear here than -15 °, for example, in humid St. Petersburg.
The duration of the off-season - spring and autumn in Siberia is very short. So, in the eastern regions, the snow that fell at the end of August may no longer melt, and the snowmelt that began in early April can rapidly end in 1.5-2 weeks.
Loading...
