Eastern Siberia occupies a vast territory from the Yenisei to the Pacific Ocean. It is famous for its large number of natural resources and minerals. The features of the relief and this region made it so valuable in terms of raw materials. Mineral resources of Eastern Siberia are not only oil, coal and iron ores. A significant part of Russia's gold and diamonds, as well as valuable metals, is mined here. In addition, almost half of the country's forest resources are located in this region.

Eastern Siberia

Minerals are not the only feature of this region. Eastern Siberia covers an area of ​​more than 7 million square kilometers, which is about a quarter of the whole of Russia. It stretches from the valley of the Yenisei River to the most mountain ranges on the Pacific coast. The region borders the Arctic Ocean to the north and Mongolia and China to the south.

Eastern Siberia does not include as many regions and settlements as in the European part of Russia, because this area is considered sparsely populated. Here are the country's largest Chita and Irkutsk regions, as well as the Krasnoyarsk and Trans-Baikal regions. In addition, the autonomous republics of Yakutia, Tuva and Buryatia belong to Eastern Siberia.

Eastern Siberia: relief and minerals

The diversity of the geological structure of this region explains such a wealth of its raw materials. Due to their huge number, many deposits have not even been explored. What minerals are Eastern Siberia rich in? It is not only coal, oil and iron ores. The subsoil of the region contains rich reserves of nickel, lead, tin, aluminum and other metals, as well as sedimentary rocks necessary for industry. In addition, Eastern Siberia is the main supplier of gold and diamonds.

This can be explained by the features of the relief and geological structure of this region. Eastern Siberia is located on the ancient Siberian platform. And most of the territory of the region is occupied by the Central Siberian Plateau, elevated above sea level from 500 to 1700 m. The foundation of this platform is the oldest crystalline rocks, whose age reaches 4 million years. The next layer is sedimentary. It alternates with igneous rocks formed as a result of volcanic eruptions. Therefore, the relief of Eastern Siberia is folded, stepped. It contains many mountain ranges, plateaus, terraces, deep river valleys.

Such a variety of geological processes, tectonic shifts, deposits of sedimentary and igneous rocks led to the wealth of minerals in Eastern Siberia. The table allows you to find out that more resources are mined here than in neighboring regions.

Coal reserves

Due to geological processes since the Paleozoic and Mesozoic eras, the largest in Russia coal deposits of minerals in Western and Eastern Siberia are located in the lowlands of the region. These are the Lena and Tunguska basins. There are also a lot of smaller deposits. And although there is less coal in them, they are also promising. These are the Kama-Achinsk and Kolyma-Indigirsk basins, the Irkutsk, Minusinsk, South Yakut deposits.

Hard coal reserves in Eastern Siberia account for 80% of all coal mined in Russia. But many places of its occurrence are very difficult to develop due to the harsh climatic conditions of the region and the features of the relief.

Iron and copper ores

The main minerals of Eastern Siberia are metals. Their deposits are found in the most ancient rocks, even the Precambrian period. Most of all in the region are hematites and magnetites. Their deposits are located in the south of the Yakutsk region, in the basin on and also on the Angara, in Khakassia, Tuva and Transbaikalia.

The largest ore deposits are Korshunovskoye and Abakanskoye. There are also many of them in the Angara-Pitsky region. 10% of all Russian iron ore reserves are concentrated here. In Transbaikalia and in the north of the region there are also large deposits of tin and valuable metals.

The environs of Norilsk are famous for large deposits of copper-nickel ores. Almost 40% of Russian copper and about 80% of nickel are mined here. In addition, there is a lot of cobalt, there are also platinum, silver, tellurium, selenium and other elements. In other places, copper, mercury, manganese, antimony are mined. There are large deposits of bauxite.

Non-metallic minerals

Our country is the world's largest supplier of natural gas, and a lot of oil is produced here. And the first supplier of these minerals is the deposits of Eastern Siberia. In addition, geological processes have led to the emergence of rich deposits of sedimentary rocks.

Gold and diamonds of Eastern Siberia

The most valuable metal has been mined here for almost the second century. The oldest deposit is Bodaibo in the Irkutsk region. There are rich placer and bedrock deposits of gold in the Aldan, Yan, Allah-Yun regions. Deposits have recently begun to be developed in the region of the Yenisei Ridge, near Minussinsk and in the east of Transbaikalia.

Thanks to the special geological processes that have been going on in this region since the Mesozoic era, many diamonds are now being mined here. The largest deposit in Russia is located in Western Yakutia. They are mined from the so-called diatremes filled with kimberlites. Each such "explosion tube" in which diamonds are found even got its own name. The most famous are "Udachnaya-Vostochnaya", "Mir" and "Aikhal".

Natural resources

The complex topography of the region, vast undeveloped territories covered with taiga forests provide a wealth of natural resources. Due to the fact that the most full-flowing rivers of Russia flow here, the region is provided with cheap and environmentally friendly hydroelectric power. The rivers are rich in fish, the surrounding forests are rich in fur-bearing animals, of which sable is especially valued. But due to the fact that man has become more and more actively interfering with nature, many species of plants and animals are dying out. Therefore, many reserves and national parks have recently been created in the region to preserve natural wealth.

The richest areas

Eastern Siberia occupies almost a quarter of the territory of Russia. But there are not many people living here. In some places, there are more than 100 square kilometers per person. But Eastern Siberia is very rich in minerals and natural resources. Although they are unevenly distributed throughout the region.

• The richest in economic terms is the Yenisei basin. Krasnoyarsk is located here, in which more than half of the entire population of Eastern Siberia is concentrated. The richness of this area in minerals, natural and hydro resources led to the active development of industry.
• The wealth located in the upper reaches of the Angara River began to be used only in the 20th century. A very large polymetallic deposit has been discovered here. And the reserves of iron ore are simply huge. The best magnesites in Russia are mined here, as well as a lot of antimony, bauxites, nephelines, and slates. Deposits of clay, sand, talc and limestone are being developed.
• Evenkia has the richest resources. Here in the Tunguska basin there are such minerals of Eastern Siberia as stone and high-quality graphite is mined in the Noginsk deposit. Icelandic spar deposits are also being developed.
• Khakassia is another richest region. A quarter of East Siberian coal and all iron ore are mined here. After all, the Abakansky mine, located in Khakassia, is the largest and oldest in the region. There is gold, copper, a lot of building materials.
• One of the richest places in the country is Transbaikalia. Mostly metals are mined here. For example, it supplies copper ores, Ononskoye - tungsten, Sherlokogonskoye and Tarbaldzheyskoye - tin, and Shakhtaminskoye and Zhrikenskoye - molybdenum. In addition, a lot of gold is mined in Transbaikalia.
• Yakutia is a treasure trove of minerals in Eastern Siberia. Although only after the revolution, deposits of rock salt, coal and iron ore began to be developed. There are rich deposits of non-ferrous metals, mica. In addition, it is in Yakutia that the richest reserves of gold and diamonds have been discovered.

Problems of development of minerals

Huge, often unexplored territories of the region lead to the fact that many of its natural resources are not developed. There is a very low population density here, therefore, promising mineral deposits in Eastern Siberia are mainly developed in populated areas. After all, the lack of roads over a large area and the huge distance from the center make the development of deposits in remote regions unprofitable. In addition, most of Eastern Siberia is located in the permafrost zone. A sharply continental climate hinders the development of natural resources in the rest of the territory.

Northeastern Siberia and the Far East

Due to the peculiarities of the relief and climatic conditions, the minerals of North-Eastern Siberia are not so rich. There are few forests here, mainly tundra and arctic deserts. Most of the territory is dominated by permafrost and year-round low temperatures. Therefore, the minerals of North-Eastern Siberia are not very developed. Basically, coal is mined here, as well as metals - tungsten, cobalt, tin, mercury, molybdenum and gold.

The easternmost and northern regions of Siberia belong to the Far East. This area is also rich, but also more populated due to its proximity to the ocean and milder climate. Mineral resources of Eastern Siberia and the Far East are similar in many respects. There are also many diamonds, gold, tungsten and other non-ferrous metals, mercury, sulfur, graphite, mica are mined. The region has rich deposits of oil, coal and natural gas.

Central Siberia

Siberia has been and remains a unique part of the planet Earth. The unique scale of its territory, the diversity of natural and climatic conditions, flora and fauna located in the depths of mineral resources, the energy capacity of rivers and the purity of lake waters, the original history and culture of the peoples inhabiting it. It is no coincidence that Siberia was originally called a land or a country. The annexation of Siberia has become the most valuable acquisition of the Russian state for the entire time of its existence and the most important milestone on the way to the formation of the Russian Empire.

The first information about the nature of Central Siberia - its rivers, climate features and fur wealth - were obtained as a result of campaigns of Russian "service people" at the beginning of the 17th century. Their observations were used in the preparation of maps and drawings that contained a fairly accurate image of the most important geographical features of the country for that time. In the 19th century, reconnaissance scientific research was carried out in many regions of Central Siberia. At the beginning of the 20th century, mineral deposits of Central Siberia (gold, coal, iron ore), navigation conditions on rivers and climate were studied. Expeditions of the Resettlement Administration on a large scale undertook studies of soils and vegetation in the southern regions of the country.

At present, the nature and natural resources of Central Siberia have been relatively well studied. Deposits of various minerals have been discovered in the bowels of the region. Hydropower resources and conditions for the construction of powerful hydroelectric power stations on the Angara, Lena and other rivers have been studied.

Central Siberia has its own distinctive features of flora and fauna and its own contribution to the general structure of life on Earth.

The nature of the Central Siberian Plateau

Geographical position, geological structure, tectonics and history of the development of the territory

The Central Siberian Plateau is located between the Yenisei and Lena rivers. In the north, the plateau abruptly breaks off to the North Siberian Lowland, and in the south it comes to the foothills of the Eastern Sayan, the Baikal region and the North Baikal highlands. The average heights of the plateau reach 500 - 700 meters. The most elevated areas are 1500 - 1700 meters (Putorana Plateau).

The most ancient part of the plateau is the Siberian platform. The most important feature of the structure is the high position of the Argian and Lower Proterozoic folded basement and the Upper Proterozoic and Paleozoic sedimentary deposits overlying it, penetrated by volcanic rocks and outcropping on the ancient surface in most of the territory. Oscillatory movements on the platform created anteclises and syneclises, the depth of the foundation in the latter reaches 5000 - 7000 meters.

The Siberian platform has two large uplifts of the Argian basement, the Anabar and Aldan shields. The Anabar shield is located in the upper part of the Anabar river basin. The folded base is the most elevated in the central part and comes to the surface, and along the edges the basement surface descends under sedimentary deposits.

In the west of the Siberian platform, dislocated Riphean rocks (schists, teys, marbles, quartzites, all of which are cut through by intrusions) emerge, forming projections of the Baikal basement of the platform - the Yenisei and Turukhansk uplifts.

The subsided sections of the foundation form syneclises and deflections. In the basins of the Angara, Kureika, Nizhnaya and Podkamennaya Tunguska rivers, there is the Tunguska syneclise, which is filled with Cambrian deposits and marine lagoon sediments of the Devonian and Lower Carboniferous. Upper Paleozoic and Early Mesozoic rocks fill the entire Tunguska syneclise and consist of the so-called Tunguska suite, which is formed by thick continental deposits (sands, sandstones, gray clays and coal seams), tuffaceous suite and traps. Coal-bearing strata belong to the Carboniferous and Permian systems, forming the Tunguska basin. Its area is 1 million km2.

Effusions and intrusions of basic rocks (diabases and basalts) began in the Permian period and continued until the beginning of the Jurassic. Volcanic processes on the Central Siberian Plateau manifested themselves in the form of powerful effusions that formed colossal lava sheets, sheet intrusions and laccoliths in the thickness of the Upper Paleozoic rocks. The main distribution of traps is associated with the Tunguska syneclise, but they are also found beyond its borders. Under the influence of trap intrusions, part of the coals turned into high-quality graphite. The largest deposits of graphite are concentrated in the lower parts of the Kureika and Nizhnyaya Tunguska river basins.

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The Vilyui syneclise is located between the Anabar and Aldan shields. At its base is the Urinsky aulacogen filled with Proterozoic rocks. In place of the aulacogen, the Vilyui syneclise developed with a thick stratum of Paleozoic and Mesozoic deposits, among which there are deposits of Cambrian salt, Jurassic and Cretaceous coals.

In the Carboniferous and Permian, the northwestern part of the platform was lowered and the Tunguska syneclise was formed. Its surface was covered with lakes and swamps, and coal accumulated.

In the Jurassic period, in connection with tectonic activity, the formation of the main morphostructures occurs; in the zones of stable subsidence, negative morphostructures were outlined (Vilyui syneclise, Angara-Vilyui and Sayan troughs), and in the zones of uplifts - positive (straight lines - Anabar anteclise; inverted ones arose in the Tunguska syneclise, the Putorana plateau, etc.).

From the end of the Paleogene to the beginning of the Pleistocene, due to neotectonic movements, further changes in the relief and the formation of modern morphostructures take place.

By the beginning of the development of the mainland branch, the Central Siberian Plateau rose again, in connection with which the rivers cut and lower basement and accumulative terraces formed in their valleys. In the valleys of large rivers, there are up to 8-10 terraces. Simultaneously with the incision of the rivers, the ledges of the Byrranga and Putorana plateaus were formed, facing the North Siberian Plain, which sagged and was flooded by the waters of the borgal transgression. Marine Quaternary deposits of this transgression are now at altitudes of 200-220 meters.

In the Pleistocene, under the influence of glacial exaration and accumulation, erosion, nivation, frost weathering, solifluction, and permafrost, morphosculpture was formed. The northwestern part was covered by the Middle Pleistocene and Late Pleistocene glaciations, the centers of which were in the Byrranga, Putorana and Anabar shield mountains. To the south of the glaciation boundaries there were severe perigmatic conditions.

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In general, Central Siberia, confined to the Central Siberian Plateau, is a country of traps and Tunguska coals. It has a fire-breathing past, although now there are no active or extinct volcanoes here. At the beginning of the Mesozoic era, the nature was different: interstratal and vein intrusions of igneous masses penetrated the body of the platform and the structures of adjacent troughs, and in some places lavas poured onto the surface. A complex system of solidified volumes of magma survived in the depths; erosion separated them in the form of armoring layers on vast plateaus up to a million km2 in area. Where the reservoir intrusions were located in several tiers, stepped slopes arose (these lava layers are called traps - from the Swedish. "ladder"). The vents of many Mesozoic volcanoes are explosion tubes; during their formation, rare conditions arose that are necessary for the birth of diamond crystals. Two outcrops of the deep basement of the Siberian Platform - the Anabar Shield and the Yenisei Ridge - were built by Precambrian rocks, and the Anabar structures are older than the Yenisei. In other areas, the platform is two-tiered - the foundation is covered by horizontally lying Paleozoic sedimentary strata, the extensive basement trough is the Tunguska depression. Here, in a thick stratum of continental strata, in the Upper Paleozoic and the beginning of the Mesozoic, the coal-bearing Tunguska suite was concentrated. Thus, one of the richest coal basins in the country, the Tunguska, arose.

In the south, the Pre-Sayan trough borders the platform, in the north there is the North Siberian depression. Only in the east is the boundary devoid of certainty - the platform structures gradually sink towards the Vilyui depression, and the relief of the plateau just as imperceptibly passes into the plain.

Millions of years of erosion would long ago have turned the territory into a residual plain, but the latest uplifts, breaking open, humping and tilting the surface, enlivened the incisions of the valleys, and karst was powerfully formed in the salt-bearing and limestone strata in vast spaces - caves, tunnels with underground rivers arose.

The geographical position of the Central Siberian plateau on the ancient Siberian platform determined the complexity and diversity of the geological structure, the development of physical and geographical processes, the nature of minerals and the formation of natural complexes. The territory of the region is composed of rocks of the Precambrian (Archaean, Proterozoic), Paleozoic, Mesozoic and Cenozoic age, that is, starting from the most ancient and ending with modern formations.

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Relief

Against the background of the rest of the predominantly mountainous High Siberia, Middle Siberia seems to be relatively even, as if an intermediate step between the plain of the west and the mountains of the south and east. But its surface is rarely called a plain. More than a quarter of the territory is characterized by intricately dissected mountainous terrain. The very word "plateau" here is rather a tribute to tradition. The acquaintance of geographers with this country began with its flat parts, and horizontally lying layers were visible in the cliffs of the outskirts.

Along the meridian, Central Siberia is elongated, like Western Siberia, but the differences between the latitudinal zones recede into the background here. Almost the entire plateau is dominated by a variety of landscapes, this is facilitated by differences in the structure of the bowels, the recent uplift of the protrusions of the ancient basement and the high mobility of the younger outskirts of the plateau. Its northern and middle parts are more stable - the platform is stable here, while the south lies beyond its borders - these are ancient foothill troughs. Beddings in them are disturbed by old processes of folding, and the latest erosion creates not only table and stepped plateaus, but also sloping ridges, and even ridges in the Cis-Baikal trough.

The Central Siberian Plateau 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 height within it ranges from 150-200 to 1500-1700 meters. The average height is 500-700 meters. A distinctive feature of the plateau is the combination of a predominantly flat or gently undulating stepped relief of the 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. The plateau reaches its maximum heights in the northwest, where the Putorana plateau (up to 1701 meters) and Syverma (more than 1000 meters) rise. They are adjoined by the Anabar plateau, the Vilyui and Tunguska plateaus with heights up to 850-950 meters.

From the Central Yakut Plain, located to the east of the Central Siberian Plateau, and confined to the Vilyui syneclise and the Predverzhoyansky trough, a lowered strip (300-500 meters) stretches through the territory of the plateau to the foot of the Sayan. Within its limits are the Angara and Central Tunguska plateaus. To the southeast of this band, the surface rises. Here are the Angarsk Ridge and the Lena-Angara Plateau with a height of up to 1000-1100 meters. To the northeast, they pass into the Prilenskoye plateau, limiting the Central Yakut plain from the south. Thus, according to the altitudinal position, the Central Siberian Plateau is clearly divided into three parts: the northwestern - the most elevated, the central - lowered, the southeastern - elevated.

The Central Siberian Plateau is characterized by the development of a multi-tiered stepped relief, the formation of which is due to the structural features of the Siberian Platform, long-term continental denudation since the pre-Jurassic, the lithology of the constituent rocks - dense traps and less stable sedimentary rocks of the Pamozoic and Mesozoic age, and the latest tectonic movements that have intensified the denudation process. Dividing spaces have the appearance of either isolated mesas or elongated ridge-like hills. In some places, individual ridges, composed of volcanic rocks (diabases and basalts), rise up under uniformly leveled surfaces. The flat areas are swampy in some places. In the northwest is the Putorana Plateau, composed of traps and volcanic tuffs. In its middle part, in the upper reaches of the Katanga River, the maximum heights (1701 meters) are concentrated. To the west and east, the height of the mountains gradually decreases to 600-700 meters. Traces of ancient glaciations are widespread in the mountains. The bottom of the intermountain depressions is occupied by rivers (upper reaches of the Pyasina, Kheta and others) and lakes (Keta, Khantayskoe). In the upper reaches of the Anabar and Olenek rivers, there is the Anabar plateau with glacial processing. Its maximum heights reach 700-900 meters. From the southwest, the Central Siberian Plateau borders the Yenisei Ridge, it extends from the mouth of the Podkamennaya Tunguska River almost to the Eastern Sayan, which is separated by a tectonic depression. The highest height of the Yenisei Ridge is Mount Epashimsky Polkan (1104 meters).

Thus, the relief of the Central Siberian region was formed under the influence of internal and external forces that manifest themselves on our planet. Certainly, it is quite unique.

At the base of the Central Siberian plateau lies a hard massif of ancient crystalline rocks that are weakly compressible, which determined the nature of the relief of the plateau. From above, these rocks are covered with traps.

Climate of Central Siberia

The climate of the territory is sharply continental. The continentality of the climate is determined by the geographical position and relief. The territory is located in the center of the northern part of Asia, elevated, removed from the warm seas, fenced off from them by mountain barriers. In most of the territory, except for the south, the radiation balance has a negative value from October to March. Orographic conditions have a significant influence on climate formation. Large mountain ranges and deeply incised river valleys determine local climatic differences, uneven distribution of precipitation during winter temperature inversions. In terms of the annual number of hours of sunshine, the southern part surpasses many of the southern regions of the country: in Irkutsk it reaches 2099 hours. Compared with the climate of other territories located at the same latitudes, the continentality of the climate is expressed in the coldest and coldest winters, the warmest summers and the least annual precipitation. Therefore, the climate is characterized by a large temperature amplitude and negative annual air temperature (Bratsk -2.60C).

Precipitation falls mainly in summer, 4-5 times more than in winter, which is twice as long as summer. On the Central Siberian Plateau, the annual precipitation is 300-400 millimeters. The continentality of the climate increases towards the east, which is expressed in a decrease in the amount of precipitation, and in the mountains the amount of precipitation increases.

In winter, the entire territory is very cool, which contributes to the development of a stable powerful anticyclone from October to March. From the center of the Asian anticyclone to the north and northeast, a high-pressure spur actually extends, filling almost the entire territory. Cold continental arctic and temperate air masses dominate. The weather is mostly clear, windless, with low temperatures.

In winter, precipitation is occasionally brought by cyclones coming from the west. The long stay of inactive anticyclones over the territory causes a strong cooling of the surface and the ground 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 and low moisture content. Therefore, January temperatures are 6-200C lower than the mid-latitude ones. The lowest January temperatures are typical for the northeastern part of the Central Siberian Plateau (-42…-430C). There is little precipitation in winter, about 20-25% of the annual amount.

Summer is relatively warm. The total solar radiation in July in the north reaches 12-13 Kcal/cm2, in most of the territory - 13-14 Kcal/cm2.

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In summer, due to warming up, a lower pressure is established over the territory. 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 run sublatitudinally within the Central Siberian Plateau, this pattern 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 14-160С and only in the southern outskirts it reaches 18-190С (Irkutsk 17.60С). With an increase in the height of the terrain, summer temperatures decrease, that is, on the territory of the plateau, a vertical differentiation of temperature conditions can be traced, which is especially pronounced on the Putorana Plateau.

The continentality of the climate naturally increases in an easterly direction, and especially in the northern part. Thus, the average air temperature in January at the northwestern limit of the zone is -320C, and at the eastern limit -380C, the average July temperatures are +14 and +180C. at the southern border, the average January temperature is 260C, and the average July temperature is +180C. The average temperatures for the year are negative everywhere: at the northern border - about -100C, and at the southern border - about -40C. To the east, the amount of precipitation decreases from 500 to 250 mm, as well as evaporation from 250 in the southwest to 150 mm in the northeast.

The cooling of the mainland in winter creates stable anticyclonic weather with severe frosts, low wind speeds and an abundance of calms with moderate, and in some years even thin snow cover. In October, an anticyclone begins to form, it reaches its maximum in January, and collapses from March. Surface layers of air are intensively cooled and sometimes become colder than arctic air masses. Throughout the territory, they can drop annually to -50, and sometimes even to -620C, once every 15-20 years in January they rise to 3 and even to 00C, but there is no thaw.

Winter moves from the northeast to the southwest, where it lasts a total of 5 months. Characterized by stable temperature inversions with an increase of 1-30C for every 100 meters of altitude. In this regard, "lakes" of cold are formed in depressions not only in winter, but also in transitional seasons. Therefore, the plants in the depressions suffer from frost, and on the uplands and slopes more productive and species-rich forests grow in comparison with the forests in the depressions.

When the temperature drops below -350C, frosty fogs usually appear over settlements - water vapor condenses. Fogs rise up to 40-50 meters, and sometimes up to 100 meters. The maximum annual cloudiness differs in November up to 25 cloudy days. The sunniest is March, when there are no more than 14-15 cloudy days.

During the long almost semi-annual cold period, only about 15% of the annual precipitation falls. Snow lasts from October to May (from 250 days in the northwest to 230 days in the northeast and 185 in the south). Its distribution largely depends on the relief. If in the valleys its thickness does not exceed 30-40 centimeters, then on a hill it reaches 60-80 centimeters. In general, the greatest thickness of snow cover is observed in the Katanga basin in accordance with the November snowfalls. The growth of snow cover continues until January, then slows down. It depends on the increase in the evaporation of snow on sunny days. Persistent and severe frosts with a small snow cover create conditions for the preservation, and in some places for an increase in permafrost soils.

The transition from winter to spring in the southern part of the zone is usually abrupt with a significant difference between low nighttime and high daytime air temperatures, especially on cloudless days. Sometimes, during the transfer of warm air masses from Central Asia, positive average daily temperatures are observed already in the first ten days of April. However, frosts occur until June.

In spring, air humidity is minimal (50-60%) and the least cloudy in the year. In combination with low rainfall (about 12% of the annual amount), droughts occur, especially in the southern part. This contributes to the dominant distribution of larch. Spring is also the windiest time of the year with changeable winds that change direction. Their speed often exceeds 15m/s. Fairly evaporated during sunny March, the snow melts quickly, with the exception of elevated shady places. But constant night frosts slow down the thawing of soils, which excludes their moistening with melted snow water, which quickly rolls into rivers without benefit for future crops.

The predominant transfer of air masses in the warm part of the year is from the west. Less often cold masses of it come from the north. Cyclonic activity develops. Usually cyclones bring rains, except for those that originate in Central Asia. However, the influence of the last sharp cyclones is limited only to the southern part of the zone. Cold arctic air flows into the rear of the western cyclones, causing cooling down to frost.

The frost-free period naturally decreases from west to east and from south to north. Its average duration in the valleys of the southern rivers is 90-100 days, in the northwest - 70 days, and in the northeast - no more than 60 days. Daytime temperatures in summer are quite high everywhere and often exceed 300C. evaporation is greatly increased. Cyclonic activity dramatically increases the amount of precipitation. For 2-3 months they fall more than half of the annual amount, maximum in July - the first half of August.

Autumn, like spring, is very short and comes immediately, passing from warm summer days to constant night frosts. Everywhere in the beginning of autumn the weather is usually dry and clear. By the end of autumn, cyclonic activity fades. An anticyclone begins to form. Frequent frosts occur at the end of August. In the valleys of small rivers, frost occurs at the end of August. In the valleys of small rivers, frost occurs at the end of August. In the valleys of small rivers, frosts begin almost a month earlier than in the valleys of large ones. In October-November, the cloudiness is the highest for the year, but fogs decrease, the maximum of which occurs in August-September. In different years, the change of seasons of the year deviates up to two weeks in one direction or another.

As a result, we can conclude that the climate of the Central Siberian Plateau is formed under the influence of solar radiation entering the earth's surface, the circulation of air masses and moisture circulation, as well as the underlying surface. The close interaction of these factors determined the formation of a sharply continental climate with long cold winters, low precipitation, relatively hot and humid summers, short transitional hot and humid summers, and short transitional periods from winter to summer.

Inland waters

The largest rivers of Russia - the Lena, the Yenisei and their numerous tributaries - flow through Central Siberia.

The watershed between the Yenisei and the Lena runs along the Central Siberian Plateau from south to north. In the northern part of the plateau, a watershed extends from west to east, separating the Pyasina, Khatanga, Anabar and Olenek rivers from the upper reaches of the tributaries of the Nizhnyaya Tunguska, Kureika and Vilyui rivers. All rivers carry their waters to the Laptev and Kara seas. Some rivers begin in the mountains, in the middle reaches their valleys have a transitional character, and finally, in the lower reaches, they enter the plains and become typical lowland rivers. These include the Yenisei, Lena and the left tributaries of the Angara, Uda, Oka, Irkut and others. Other rivers - and most of them - begin on the Central Siberian Plateau. Their upper sections approach the flat rivers. In the middle reaches, they cut deeply into the plateau, flowing through a narrow rapids valley, and in the lower reaches they become flat (for example, Podkamennaya and Lower Tunguska, Vilyui).

Large rivers flow within the permafrost through the taiga. The upper reaches of the rivers are located in the southern regions: here they have many tributaries, bringing a large amount of water to the main rivers. The rivers are fed by rain and snow, part of the water in the rivers comes from the melting of ice and permafrost. Ground feeding is negligible. Spring-summer flood. During 4-6 warm months, more than 90-95% of the annual runoff occurs. The minimum flow of all rivers is observed in winter. Due to the long cold winter, the ice cover on the rivers is very long. For example, in the northern part of the Irkutsk region, rivers freeze in the first half of November, and break up at the end of April. In winter, as a result of the weakening of the flow and low temperatures, some rivers freeze through. Water flows from the upper reaches of the frozen sections of the rivers and spreads over the surface of the ice, forming powerful icings. At the same time, there are polynyas at the places where powerful ground sources emerge, for example, on the Lena below Kachug. The freezing of the Central Siberian rivers occurs in a very peculiar way. Ice first forms not on the surface of the water, but at the bottom on supercooled pebbles, and then rises to the surface. Freezing on the rivers occurs in October, and on the southern rivers - in early November. The ice thickness on the rivers reaches 1-3 meters. Small rivers freeze to the bottom.

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All major rivers are important transport routes and are used for navigation and timber rafting. The Angara River is navigable from Lake Baikal to the city of Bratsk and in the lower reaches - from the mouth up at a distance of 300 km. The Lower Tunguska is a raftable river, navigable from the village of Turukhansk to the village of Tura. Podkamennaya Tunguska is navigable only in the lower reaches.

Rivers have enormous reserves of electricity. A cascade of powerful hydroelectric power stations has been built and is being built on the Angara and Yenisei, but these large stations also have huge reservoirs, although with a relatively large depth and narrowness of the valleys, they flood even less land than their "colleagues" on the plains of the West. And yet, about 5 1/2 thousand went under the waters of the Bratsk Sea, and a little less than 2 thousand km2 under the waters of the Ust-Ilimsk. The Bratsk Sea stretched along the river for almost 550 km, and its bays, penetrating up the Oka and its tributary, stretched for another 370 and 180 km, respectively. The Ust-Ilimsk reservoir raised the Angara by 300 km. in length, and the bay in the lower reaches of the Angarsk tributary of the Ilim turned out to be shorter by only 1 km. Nevertheless, the width of the new "seas" is also significant. It was possible to save large stocks of timber from flooding, primarily combat timber, - more than 3 thousand km2 of timber was removed. But the part of the forest that has not been cut down harms water bodies. Decaying wood impoverishes the water, the lack of oxygen increases the winter kills of fish.

The Central Siberian Plateau has a well-developed river network. This is due to the significant elevation and uneven heights of the territory, rock fissuring, a long period of continental development, the water-resistant effect of permafrost, and deep and prolonged ozone freezing of soils.

Permafrost not only prevents moisture from seeping into the ground, but also reduces evaporation due to the low temperature of river and groundwater. All this determines the features of the water balance - an increase in the table and, above all, its surface component and a decrease in evaporation compared with similar latitudes of the Russian Plain and Western Siberia.

The rivers are rich in various fish. Sterlet, sturgeon, omul, whitefish, and grayling are of primary commercial importance. Salmon fish make up 97% of the catch. The largest number of these fish is concentrated in the mouths of the Yenisei and Lena rivers.

Soils, vegetation and wildlife

In connection with the appearance of perennial soils of the eastern Yenisei Ridge, soil formation differs markedly from the western territories. The soil profile is more often loosened from the western territories. The soil profile is often loosened by the seasonal intrusion of ice, causing its mobility.

The podzolic process is suppressed and occurs mainly on deep-thawing sandy-clay soils, especially on river terraces. In the interfluves, soils are formed on massively crystalline or tree-saddle stony rocks. As a result of orthoeluvia, the usually stony amount of fine earth quickly decreases with depth and height, becoming strongly gravelly.

Due to the low-temperature substrate, litter humification proceeds extremely slowly, and the organic-cumulative horizon A1 becomes coarse-humus and often peaty. Easily soluble substances, and especially fulvic acids, are quickly washed out of it. Looseness and gravelly soil profile accelerate the migration of most substances, including silica. Humus is found throughout the soil profile, although in lower proportions. If in the upper part its content reaches 8-10%, then at a depth of 50 cm - about 5%, and at a depth of 1 meter there may be 2-3% of humus.

The A2 podzolic horizon is by no means always formed, especially in the northern half of the Central Siberian taiga. In general, podzolization is typical here on those parent rocks that include light, weathering-resistant minerals - quartz, feldspar, micaceous silicates, i.e. mainly on sands and Mesozoic sandstones, developed just in the southern half of the plateau. But a podzolic or simply lightened horizon is never thicker than 3-5 cm; it is usually underlain by a bright brown horizon. This is due to the leaching of iron and fulvic acids. With depth, humic substances are gradually deposited around the mineral grains in the form of humus-iron-oxide compounds, coloring the soil brown. The brightness of the color decreases downward, although the glandular compounds increase. The permafrost screen, which moistens the soil during the growing season, affects the small differentiation of the soil profile. The high content of fulvic acids causes a strongly acid reaction of soils with a pH of water extract of 4-6. A small amount of humus and high acidity do not provide soil fertility.

In the south, in the Angara River basin, clayey slightly podzolic and soddy-forest soils without a podzolic horizon are more common. A dark gray upper humus horizon and a transitional one to the parent rock stand out. In soils on traps rich in sesquioxides, where humic acids predominate over fulvic acids, calcium and magnesium are leached, and a ferruginous film is formed around the primary minerals, which inhibits podzolization. Such soils are called sod-iron-aluminum.

On carbonate rocks of the lower Paleozoic plain, soddy-calcareous soils with a weakly differentiated profile, but with a dark gray humus horizon, containing 5-6% humus and about 9% calcium carbonate. Humic acids predominate in humus. The reaction is neutral or even slightly alkaline.

In the northern taiga, a new type of soil on traps, granuzems, has recently been studied. They are formed in the conditions of a sharply continental climate on a rock that, when weathered, produces minerals with framework structures, pyroxenes, glasses, in which clay minerals do not transform. Rapid physical crushing contributes to the accumulation of amorphous compounds of iron, aluminum and the rapid removal of the products of the interaction of humic acids with minerals. A thin soil (about 20 cm) is formed with an unexpressed differentiation into genetic horizons in chemistry close to the parent rock, but with a high humus content of the fulvic composition and unsaturation of the absorbing complex.

Vegetation.

The vegetation cover of the taiga zone, which occupies more than 70% of the territory, has the most peculiar character. Despite this relative homogeneity and the vast expanses occupied by the taiga, it is not always the same. Differences in the thickness of the permafrost layer, in appearance, in drainage and other factors create some diversity in the plant world.

Within the boundaries of Central Siberia, light coniferous forests of Siberian larch (in the west) and Daurian larch (in the east) predominate. The dark coniferous taiga is pushed back to the extreme western regions. Warm and not very humid summers are the reason for the more significant advancement of forests to the north than anywhere else.

Animal world

The fauna of Central Siberia differs from the fauna of Western Siberia: it is more ancient; the sharp continentality of the climate contributes to the large movement of taiga species to the north in the summer; in harsh climatic conditions, the hairline of fur-bearing animals acquires a special splendor, tenderness and silkiness.

The taiga has a more diverse and rich animal world. Of the predators, the brown bear, wolverine, fox, Siberian weasel, ermine, and sable are common. Wolverine lives everywhere. This nocturnal predator settles under tree roots, in rock crevices, in soft ground and in snow. Kolonok with brown fluffy silky fur. It is distributed in the Vimoya basin in dense taiga with undergrowth. Sable is rare and spread over stony placers in dense taiga. The lynx is the only animal from the cat family, its habitat is dense taiga forests. Of the ungulates in the taiga, elk and musk deer are common, and on the Putorana plateau there is a bighorn sheep. Maral and roe deer are common in the southern part of the Cis-Yenisei taiga.

There are numerous rodents in the taiga, especially the squirrel, which occupies a prominent place in the fur trade; it is found throughout the territory, but its main habitat is the central dark coniferous taiga. Of the other rodents, chipmunk, white hare, and vole are common. Of the birds, hazel grouses, white partridges and many others are common.

Beginning in 1930, the muskrat was released into the territory of the Irkutsk region. Its habitats are reservoirs, slowly flowing rivers, where there is a lot of wetland vegetation. In the western part of the Irkutsk region, the acclimatization of the hare and the American mink was carried out.

It is important to note that many animals of Central Siberia are wrapped in warm coats of fur and feathers, which are especially necessary in winter, they are much larger than their relatives living in a milder climate, which is an advantage in conditions when it is necessary to keep warm (the larger the animal, the less surface that loses heat relative to its size).

Thus, the formation and distribution of soils, flora and fauna over the territory of the plateau is greatly influenced by its specific harsh sharply continental climate and the almost universal distribution of permafrost associated with it. The conservation of permafrost is favored by low average annual temperatures and the peculiarities of the cold period inherent in this climate: low temperatures, low cloudiness, which contributes to night radiation.

The diversity of the soil cover of the Central Siberian Plateau is closely dependent on the heterogeneity of rocks, topography, moisture conditions, temperature regime and the nature of vegetation. The species composition of animals, their number, lifestyle, external coloration depend on the characteristics of the surrounding geographical environment.

Natural resources

The territory of the Central Siberian Plateau is rich in natural resources, it is especially provided with minerals, hydropower and forest resources.

So, in the west of the Siberian Platform, there are dislocated Riphean rocks (crystalline schists, gneisses, marbles, quartzites), here is one of the largest iron ore basins in Siberia - the Angara-Pitsky - located in the Yenisei Ridge; it is confined to a large synclinorium. Iron ores of sedimentary origin are noticed in the upper Proterozoic sequence.

Here is one of the largest coal basins in Russia, its coal-bearing strata are attributed to the Carboniferous and Permian systems. Under the influence of trap intrusions, part of the coals turned into high-quality graphite. The largest deposits of graphite are concentrated in the lower parts of the Kureika and Nizhnyaya Tunguska river basins.

The Lena coal basin is located in the Vilyui syneclise and in the Verkhoyansk trough.

Most of the Central Siberian Plateau is covered with taiga, including the Angara region belongs to the forest surplus zone.

The fauna is rich in game and fur animals, for the production of which Central Siberia occupies a leading position.

The rivers of the Central Siberian Plateau have a significant hydropower potential, for example, the Ust-Ilimskaya HPP (4.3 million kW) and the world's largest Bratskaya HPP (4.5 million kW) are located on the Angara River, as well as the Vilyuiskaya HPP on the Vilyui River.

Thus, the territory of the Central Siberian Plateau is provided with all types of natural resources, as a result, the following industries are developed in the economy of the region: fuel, non-ferrous, forestry, energy, fur and fur.

The current state of landscapes and geoecological problems, possible solutions

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 the last decade, more and more centers of local changes in nature have appeared in the course of mining in the course of transport and energy construction.

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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. The Angara basin is a striking representative of the areas of human impact on nature. 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 ​​​​about 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 conserve 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 regulating CO2 reserves in the Earth's atmosphere. This has become apparent as a result of recent 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 plants, 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.

Physical-geographical zoning of Central Siberia

natural areas

Throughout the entire length of Central Siberia, 3 zones are distinguished: tundra, forest-tundra and taiga. The taiga is most fully represented, occupying 70% of the area. The Central Siberian Plateau includes only the forest-tundra and taiga.

The forest-tundra stretches in a narrow strip (up to 50-70 km); the boundary of the zone runs along the northern ledge of the Central Siberian Plateau.

The climate of the zone was assigned to B.P. Alisov to subarctic with a predominance of continental air of temperate latitudes in the cold period and transformed arctic air in summer. The combination of the polar position with continentality with insignificant radiation and the dominance of anticyclone weather determines the severity of the winter period, which lasts about 8 months, from October to May. Snow cover lasts 250-260 days. Its thickness is 30-50 cm, slightly increasing towards the west. In summer, the soil and the surface layer of air warms up intensively. The average July temperature is 12-13oC.

Sufficiently high temperatures during the growing season, a decrease in the strength of winter winds, favor the growth of not only herbaceous and shrubby vegetation, but also trees. Of the tree species, Dahurian larch dominates here. The vegetation cover of the forest-tundra is dominated by shrub thickets of birch, alder, and willow. Trees are scattered in individual specimens or groups.

The taiga zone stretches from north to south for more than 2000 km from the northern edge of the Central Siberian Plateau.

The specific features of the Central Siberian taiga, which sharply distinguish it from the taiga of Western Siberia, are the sharply continental climate and the almost universal distribution of permafrost, slight swampiness, the dominance of monotonous deciduous taiga and permafrost-taiga soils.

The climate of the zone is sharply continental, with severe winters with little snow and moderately warm and cool, moderately humid summers. Cold winter with persistent and severe frosts lasts 7-8 months. On the western slopes of the Central Siberian Plateau, the greatest amount of precipitation falls, which contributes to the formation of snow cover up to 70-80 cm thick. The relief and features of atmospheric circulation determine the variegated distribution of precipitation in the zone.

The zonal soils of the taiga are permafrost-taiga. In the central part of the taiga, the density of the tree layer and the height of the trees increase. In the undergrowth, in addition to shrubs, birch, there are bird cherry, mountain ash, elderberry, juniper, honeysuckle. The grass-moss cover is typically taiga. Acid permafrost-taiga soils develop under the forests. In the southern taiga, the diversity of coniferous forests is increasing. In the space of the taiga zone, intrazonal differences associated with the nature of the lithogenic base are clearly traced.

The increase in the severity of winter and the decrease in the thickness of snow cover from west to east have the greatest influence on the distribution of forests across the territory. In this regard, dark coniferous spruce-cedar forests predominate in the Yenisei part. To the east, they are replaced by dark coniferous-larch and pine-larch.

Physiographic provinces and regions

There are two main provinces on the territory of Central Siberia:

1. The province of mountain-glacial tundra and forest-tundra middle mountains and moraine-sea plains occupies the northern part of Central Siberia. The province is characterized by a significant differentiation of neotectonic uplifts. The greatest uplifts were manifested in the folded-block mountains of Byrranga, where, in connection with the uplift of the territory, local centers of ancient and modern glaciation arose. The moraine-marine accumulative plains were formed on the site of territories with insignificant subsidence and rises. The province is located within the northern part of the Krasnoyarsk Territory and the northwest of the Yakut Autonomous Soviet Socialist Republic.

The arctic deserts and tundras of Taimyr are the northernmost physiographic continental region of the Soviet Union. It occupies the northern half of the Taimyr Peninsula. The Byrranga Mountains stretch from the Yenisei Bay to the Laptev Sea for almost the length of the Caucasus (1000 km) and are divided into three parts: the western one, located between the Yenisei Bay and the Pyasina River with heights up to 400 m; central between the rivers Pyasina and Lower Taimyr with heights up to 700 m; the eastern part is the highest, the highest height reaches 1146 m. ​​The mountains gradually descend to the shores of the seas of the Arctic Ocean, forming a series of low elevations, and fall steeply to the North Siberian Lowland. The ridges and massifs are separated by deep longitudinal and transverse river valleys. The mountains are composed mainly of Paleozoic rocks: in the north of the highlands there are outcrops of Precambrian (Proterozoic metamorphic shales) and acid intrusions of pre-Paleozoic and Paleozoic age. The northern part of the highlands was created in the Caledonian folding, and the southern - in the Hercynian.

The relief is characterized by a wide development of stone placers and a complex of exaration ("ram's foreheads", cara, troughs) and permafrost-solifluction forms. In the central and western parts, the peaks of the mountains are dome-shaped, and in the eastern part, a dissected glacial relief prevails: moraines and sands are common, located in low areas - highlands. There are numerous large snowfields and modern glaciers in the Byrranga mountains.

The winter is severe with a negative radiation balance (from mid-September to April) and a predominance of severely frosty weather types. The duration of the cold period is about 290 days. The average January temperature is -30, -35 ° C. The snow cover lasts from September 15-20 to June 27, and its height in the middle of winter is 20-60 cm.

Summer is short and cold. The total radiation in July reaches 16 kcal/cm2. The average July temperature at Cape Chelyuskin is +1°С. The annual rainfall is about 200-300 mm. They fall approximately evenly throughout the year, the ratio of precipitation to evaporation is more than 1.33. The entire territory is located in the permafrost zone with insignificant seasonal thawing of the soil during the warm period and to the north of the bullet isoline of the sum of active temperatures.

In the highest part of the mountains, northeast of the lake. Taimyr, where up to 700 mm of precipitation falls at an altitude of 900 m, modern glaciation is developed. The area of ​​all glaciers is about 50 km2. The existence of glaciers and snowfields on the Byrranga highlands, apparently, should be considered as an altitudinal belt of perennial snow and ice, since this is the highest part of the mountains, where "level 365" comes close to the surface of the ridges.

At the foot of the mountains there are arctic tundras on hidden gley (in the northern foothills) and arctic tundra (in the southern foothills) soils. In the southwestern foothills, moss, lichen, and shrub tundras are developed on tundra gley soils.

The altitudinal zonality is expressed in the Byrranga mountains as follows: at the foot of the northern slopes - the Arctic tundra, and the southern slopes - the Arctic tundra and moss, lichen and shrub tundra; along the southern slopes, moss-herbaceous tundras rise to a height of 200 m. Higher up the slopes of the mountains there are arctic deserts on cryptogley arctic soils. Even higher - sparse vegetation of talus and rocks, glaciers. Numerous finds of stumps and trunks of trees (larches, birches, willows, spruces) in the Quaternary deposits along the rivers of the Upper and Lower Taimyr, at the mouth of the Pyasina and at Cape Chelyuskin (to the north of 76 ° N) indicate that forest vegetation covered almost the entire territory of the Taimyr Peninsula and the northern border of the forest-tundra was 4-5 ° north of the modern one.

The North Siberian moraine-marine tundra lowland is located between the tectonic ledges of the Byrranga, Putorana and Central Siberian plateaus. In the west, the lowland merges with the West Siberian Plain, and in the east, with the Lena Delta. The hilly surface of the lowland has a height of 50-100 m. The maximum heights are about 225-260 m. From the side of the Byrranga mountains, individual ridges and hills with heights of 400-650 m enter the lowland. m) and Chekanovsky (up to 529 m).

Coast to the west of the mouth of the river. Olenek continues to descend. This is evidenced by the estuaries of the Anabar and Khatanga rivers. To the east of the mouth of the Olenek, the rivers form deltas at their confluence, which indicates the rise of the coast. The area of ​​the river delta Lena is 28500 km 2. Many islands of the delta have developed peatlands, polygonal vein ice and hydrolaccoliths.

The North Siberian Lowland was formed on the site of the submerged Hercynian structures of the Taimyr Peninsula, Mesozoic structures extending from the Pre-Verkhoyansk marginal foredeep. The lowered folded structures form the marginal Khatanga trough, which is filled with Paleozoic, Meso-Cenozoic and Quaternary sedimentary deposits. Mesozoic deposits are coal-bearing. Among the sedimentary rocks there are salt domes composed of Permian, Triassic sandstones, Devonian rock salt (Nordvik).

The climate is arctic with moderately severe long winters and short cool summers. In winter, anticyclonic weather prevails. The duration of the cold period is about 290 days. The average January temperature is about -30, -36°C, the minimum is -61°C. The average temperature in July is from +4°C in the north of the lowland to +12°C in the south. The maximum temperature reaches +30° C. Annual precipitation decreases from west to east from 300-350 to 200-220 mm, and about 100 mm falls in the delta of the Lena River. The zone is excessively humid: the ratio of annual precipitation and evaporation is more than 1.33. The sum of active temperatures is 0-400°С, N=0-3.

The rivers Pyasina, Upper Taimyr and the lower reaches of the Khatanga, Anabar and Olenek flow through the lowlands. Among the hilly-morainic sea plains and on the islands of the Lena delta, there are many shallow glacial and thermokarst lakes. Swamps are common in places: their depth is small, since the top layer of frozen soil thaws by 30-60 cm during the warm period.

In the North Siberian Lowland, moss-lichen and shrub tundras predominate; to the south, shrubs of dwarf dwarf and willow forests are common. The main soils are tundra gley. In the south of the lowland, swampy larch sparse forests appear on gley-frozen-taiga soils. Siberian larch comes from the west only to the sources of the Pyasina, and to the east of it, Dahurian larch is common. Dahurian larch moves along the river valleys far to the north: in the valley of the river. Khatangi - up to 72 ° N. sh. The northernmost forest area on the globe is located on the terrace of the Lukunskaya River (72 ° 34 "N. Lat.). The northern border of the forest on the North Siberian Lowland during the period of the post-glacial thermal maximum was much north of the modern one, approximately at the foot of the Barranga Mountains. For To preserve the northernmost forests on Earth, it is necessary to organize a nature reserve in the Khatanga River basin.

The northern taiga and mountain-tundra plateau of Putorana is located on the northwestern polar margin of the Central Siberian Plateau: its western and northern boundaries pass along tectonic ledges, in places forming rocky walls 300-500 m high. The southern and eastern boundaries of the Putorana region are drawn along the border of the Zyryansk glaciation. Putorana is a huge dome-shaped mid-mountain uplift of the Central Siberian Plateau, the highest heights of which are concentrated in the center (1701 m). All rivers begin there (Kotui, Kureika, upper reaches of the Kheta), creating a centrifugal pattern of the hydro network and emphasizing the dome-shaped structure of the mountain system.

The Putorana Plateau was formed on the site of the lowered part of the Tunguska syneclise, the anticline zone and the marginal foredeep of the Baikal folding as a result of intense Quaternary uplifts. The plateau is composed of horizontally deposited Paleozoic sedimentary rocks and traps - volcanic rocks of Upper Permian and Lower Mesozoic age. The determining factor in the creation of the modern relief was tectonic movements: pre-Quaternary and Quaternary splits of the latitudinal and meridional directions, as well as arched uplifts and in some areas of subsidence.

The main relief forms are numerous raised blocks along the lines of splits of the massif - ridges with flat stony watersheds, separated by wide intermountain depressions, young erosional and glacial valleys. The slopes of the mountains abruptly break off to deep intermountain depressions and to valleys created as a result of the activity of rivers and glaciers along the lines of Neogene, Paleogene and Quaternary splits. The depth of dissection of the mountains reaches 800-1500 m. Thick ice sheets developed on the Putorana Plateau in the Pleistocene, which had a great influence on the formation of morphosculpture. Intermountain depressions are filled with glacial deposits and have a hilly-morainic relief with a large number of lakes dammed by moraines, as well as tectonic ones (lakes Lamo, Keto, Khantai, Glubokoe, etc.). On the slopes of the valleys, circuses and caravans filled with snow are characteristic.

The Putorana Plateau is located in the west of the Siberian region of the subarctic climatic zone and is influenced by the Atlantic and Arctic air masses and the Asian anticyclone. Therefore, there are significant differences in the climate of the western and eastern parts of the plateau. In the west of the Putorana, there is more precipitation and cooler summers than in its eastern half. Winter is long and very cold: the average temperature of the coldest month reaches -30, -38°С, the absolute maximum temperatures in the north are -58°С, and in the east -59°С. The snow cover lies for about eight months. Summer is short, but moderately cool, in lower areas the average temperature of the warmest month is from +12 to +14°C, and in the mountains, at an altitude of 600-1500 m, from +6 to +12°C. The maximum temperature was +28°С in the north, and +31°С in the east, in most of the region the sum of active temperatures was less than 400°С. The annual precipitation in the west is 504 mm, and in the east - 300 mm. Moisture coefficient - 1.33, N = 3.

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The Putorana Plateau is located in the northern taiga subzone, where the western dark coniferous taiga is in contact with the eastern larch taiga. Dark coniferous taiga with larch occupies intermountain basins and valleys, rising up to a height of 250-450 m.

Higher up are larch forests, which, from a height of 450-500 m, are replaced by larch woodlands and thickets of dwarf pine. Soils are mountain permafrost-taiga, gleyic-acid with signs of podzolization. Above 700-750 m, the alder belt follows, turning into mountain shrub tundra. From a height of 800-900 m, mountain tundras (lichen and stony) are widespread. Below continuous stony placers, mountain tundra and mountain arctic soils are developed.

The Anabar socle taiga and mountain-tundra upland is located in the upper reaches of the Anabar and Olenek rivers, on the Anabar Shield, which is expressed in relief as a dome-shaped uplift. Its maximum heights reach 905 m in the center. The watersheds look like numerous massifs with smooth domed tops.

The folded Archean crystalline basement of the Anabar shield is elevated in the central part, and the basement surface descends along the edges, overlapping mainly with limestones and sandstones of the Cambrian and Ordovician. In the south-west of the region there are outcrops of sedimentary Silurian and Permian deposits and covers of traps. Between the Anabar Upland and the Putorana Plateau is the Kotuy swampy trap plateau. On the Anabar Upland and the Kotui Plateau, traces of ancient glaciations were found in the form of narrow ridges composed of boulder loam and sand and gravel material. Glaciation was inactive. The watersheds are flat with domed tops; valleys carved in easily eroded rocks, floodplains with ancient terraces, and in some areas (where crystalline rocks emerge) the valleys are narrow with rapids and rifts. The main relief types of the Anabar shield are basement plateaus with glacial and nival processing; along the edges of the Anabar shield, in the area of ​​development of Paleozoic rocks, erosional layered-tiered, water-glacial lacustrine and alluvial plains and a trap plateau were formed.

The climate is subarctic with long cold winters. The average January temperature is -38, -43°С. In the basin of Lake Essey, the minimum inversion temperature was recorded at about -70°C. The summer is moderately cool: the average temperature in July is +12, +14°C. The sums of active temperatures are 700-400°C and less (in the mountains). Moisture coefficient - 1.33-1.00. The annual rainfall is about 300 mm. The area is excessively humid.

The main part of the territory is covered with northern taiga forests of Daurian larch and mountain larch sparse forests on gley-permafrost-taiga and mountain-permafrost-taiga soils. In the south, in the upper reaches of the river. Olenek, permafrost-taiga carbonate rubble soils are developed on sedimentary rocks of the Lower Paleozoic. Forests rise along the slopes of valleys and mountain ranges up to a height of 500-700 m. Higher mountain tundras are developed on mountain-tundra soils.

The Tunguska trap north and middle taiga plateau occupies the basin of the Lower Tunguska and the upper reaches of the Olenek and Vilyui between the boundaries of the Samarovo and Zyryansk glaciations. The heights of the watershed plateaus are up to 981 m (N. Tunguska basin). The river valleys are deeply incised. The surface of the basement of the Tunguska syneclise and the southwestern slope of the Anabar massif subsides to depths of 1000 to 4000 m and is overlain by a thick sequence of Paleozoic and Triassic sedimentary rocks penetrated by traps. During the maximum and Taz glaciations, the region was a marginal glacial zone, and on the surfaces of the trap plateau and stratified-stage plains, bottom and terminal moraine glacial-glacial deposits were formed. During the Zyryansk and Sartan glaciations, the territory was a periglacial area: in a cold climate, permafrost and treelessness, deluvial and permafrost processes took place; a microrelief was formed - mounds, polygonal forms, etc.

The region lies in the subarctic and temperate zone. The climate is sharply continental, humid. The average January temperature is around -28°C in the southwest and -38°C in the northeast. The average roofing temperature is +15, +16° C. The greatest amount of precipitation in the west is 400-500 mm; in the east, they gradually decrease to 300 mm. The sum of active temperatures is 600-1000 ° C. The coefficient of moisture is 1.33-1.00, N = 6-10.

The increase in precipitation and proximity to the West Siberian Plain predetermined the development of a more diverse species composition of the middle and north taiga forests in the southwest of the region. They consist of larch (Daurian and Siberian), spruce, pine, cedar with an admixture of birch. In the east, the forest is formed by larch with an admixture of birch. Permafrost-taiga, mountain permafrost-taiga carbonate and podzolic soils have formed under forests under permafrost conditions; The highest watersheds (de-800-900 m high) are covered with mountain tundra.

2. The province of non-glacial erosional plateaus and uplands and alluvial-lacustrine lowlands of the forest zone is located in the southern half of Central Siberia, beyond the limits of maximum glaciation. The province is characterized by intense differentiated neotectonic movements. Permafrost and related permafrost-solifluction landforms are widespread. The province lies mainly in the southern part of the Krasnoyarsk Territory and in the southwest of the Yakut Autonomous Soviet Socialist Republic.

The Leno-Olenyok northern taiga plateau is located in the northeast of the Central Siberian plateau, between the border of maximum glaciation and the mountains of the Verkhoyansk ridge. The plain is located on the eastern slope of the Anabar massif, which consists of the Olenyok trough, the Olenyok and Mun uplifts. The depth of the basement in the trough is about 1500 m, and in the uplifts - from 500 to 1000 m. The platform cover is formed by Cambrian and Ordovician carbonate deposits. Of the Quaternary rocks on the watersheds, deluvial - solifluction and eluvial strata predominate, and along the river valleys - alluvial and deluvial-colluvial. The plateau is dissected by deep valleys with flat watersheds. In areas of fractured rocks, the valleys sharply change their directions. The surfaces of carbonate rocks are dissected by modern ancient karst forms. Permafrost-solifluction forms are widespread throughout the territory.

The climate is subarctic with a cold long winter: the average January temperature is -40, -42°C. The duration of snow cover is from 220 days in the south of the region and more than 240 days in the north. The average temperature in July is from +12 to +16°C. The sum of active temperatures is 400-1000°C. The territory is slightly arid, the humidity coefficient is 1.00-0.77. The annual rainfall is over 200 mm.

The region is located in the northern taiga subzone of sparse larch forests. The sparse larch stand in the north - in the forest tundra - is distributed evenly. On the Olenyok uplift, on elevated plateaus north of 70 ° N. latitude, altitudinal zonality is manifested: from about a height of 350 m, the tops of the plateau are covered with mountain tundra on mountain-tundra soils, and along lower watersheds and river valleys, larch sparse forests go far to the north. In the southern part of the Leno-Olenyok watershed, on the slopes of the southern and southwestern exposure, relic steppe grass-forb areas have been preserved.

The main soils of the region are gley-permafrost-taiga soils and at the outcrops of carbonate Lower Paleozoic permafrost-

noteazh carbonate.

The Angara-Tunguska trap middle and southern taiga plateau is located in the basins of the Angara, Podkamennaya and Nizhnyaya Tunguska rivers and the upper reaches of the Lena, in the southern part of the Tunguska syneclise. The plateau is composed of Paleozoic and Lower Mesozoic sedimentary rocks with a wide distribution of traps. The Quaternary cover is formed by eluvial-deluvial, deluvial-solifluction and alluvial processes.

The relief is dominated by erosive layer-tier and trap plateaus separated by deep valleys. In readily soluble rocks, karst forms are developed, especially in the southern Angara region, where funnels, caves, dry and blind valleys arose in gypsum, limestone and dolomite. The traps had a great influence on the landforms of the entire territory: on the watersheds they form an elevated plateau, in the valleys they form canyon-like forms and rapids.

The large fracturing of the traps contributes to the accumulation of groundwater, which comes out in the slopes of the river valleys.

The climate is moderate, continental. Winter is very cold and moderately severe. The average January temperature is from -20 to -30°C, and the minimum is -58°C. The summer is warm: the average temperature in July is +16, +18°C. The sum of active temperatures is 1000-1600°C. The moisture coefficient is 1.00-0.77. The greatest amount of precipitation (about 400 mm) falls in the west of the region, to the east they decrease to 300 mm, N=10-16.

According to morphology, the Angara valley is divided into three parts: the upper one - from the lake. Baikal before the confluence of the river. Oka, 680 km long, where the river flows in a narrow valley with rocky banks; the middle one - from the Oka river to the confluence of the Ilima river, 290 km long, where the Angara passes through the traps, forming the Podkamenny, Padunsky, Dolgiy and other rapids; the lower one - from the Ilma River to the Yenisei, 860 km long, where the Angara River also flows through traps, but the rapids in these areas are much smaller. The regime of the Angara largely depends on the regime of the lake. Baikal. The Angara is characterized by high water content, smooth level fluctuations, especially in the upper reaches. In the spring, the Angara is not flooded, but a decline in water. With the onset of freeze-up, the water level rises and remains high throughout the winter. In the spring, when the ice jams disappear, the water level begins to decrease.

The water temperature in summer at the source (in August) is about + 8.4 ° C. Downstream it rises, reaching + 16.7 ° C near Bratsk (in August). ambient air, and warmer in autumn. In the north of the district, larch forests grow with an admixture of spruce, cedar and pine on permafrost-taiga acidic soils. To the south of the latitudinal segment of the Angara stretches the southern light coniferous taiga, dominated by pine with an admixture of larch, cedar, spruce and birch on soddy-podzolic soils, among which there are soddy-calcareous.

The Yenisei socle taiga ridge consists of separate ridges and massifs with heights of 800-1100 m. The maximum peak is Enashimsky Polkan (1104 m). This range is formed by anticlinal and synclinal structures of the Baikal folding and is composed of Precambrian shales - gneisses and granites. In the northern part of the ridge, sandstones and limestones of the Lower Paleozoic occur on Precambrian rocks. Above the mouth of the Podkamennaya Tunguska, the Yenisei ridge is sawn up by the Yenisei. To the west of the Yenisei valley, it plunges under the sedimentary deposits of the West Siberian Plain. In places of breakthrough, the Yenisei valley is narrow, and there are Osinovsky rapids in the channel. The largest river of the Yenisei Ridge - the Big Pit - cuts it in the south and flows in a narrow deep valley. The socle watershed elevations of the ridge are flat-ridged, swampy in places, many rivers flow from the swamps. The slopes are strongly dissected by river valleys, the depth of which often reaches 180-200 m.

The climate is characterized by cold winters with high snow cover (up to 90 cm) and moderately warm summers. The average temperature in January is about -20, -25°С, and in July +16°С. The sum of active temperatures is 1200-1600°C. Annual rainfall 550-700 mm; the territory is humid, the moisture coefficient is 1.33-1.00. The ridge is covered with dark coniferous mountain taiga forests, consisting of spruce, fir, cedar with an admixture of larch, pine and birch. Mountain permafrost-taiga soils are formed under the forests.

The Leno-Vilyui accumulative and stratified middle taiga plain occupies the subsidence zone of the Siberian platform basement: the eastern part of the Angara-Lena trough, the Vilyui syneclise and the Verkhoyane trough. The largest rivers of Central Siberia - Lena, Aldan, and Vilyui - flow on the surface of the plain in terraced valleys. The highest heights are located on the outskirts of the region and reach 400-700 m, and the lowest - in the valleys of Vilyui and Lena - about 50 m and below.

The Vilyui syneclise and troughs are filled with terrigenous, salt-bearing and carbonate deposits of the Cambrian, Ordovician and Silurian, a thick sequence of continental and marine Jurassic and Cretaceous deposits (sands, loose sandstones, clay shales with interlayers of brown coal), in the Lower Aldan depression there are coal-bearing and sandy lacustrine-alluvial neogene deposits. Particularly widespread coal accumulation occurred in the Lower Cretaceous. The thickness of the Mesozoic rocks reaches 200-300 m. Among the loose Quaternary deposits (lacustrine-marsh, loess-like, etc.), lenses of fossil firn or lacustrine ice have been preserved, they thaw and subsidence filled with water is formed.

A large number of lakes are scattered throughout the Leno-Vilyui lowland, on watersheds and in valleys. For the purpose of economic use, the local population lowers lakes into rivers. Beautiful meadows used for mowing and pastures, the so-called alas, form in the lake basins.

The climate is sharply continental. In winter, cold air flows into the Leno-Vilyui lowland, here the air cools and an anticyclone weather regime develops. Therefore, the winter is very severe and cruel, with the temperature of the coldest month -35 -45°C, moderately snowy. The duration of the snow cover is about 220 days, and the height is -20-40 cm. Summer is warm, slightly dry and arid; the average temperature in July reaches +18°C in Vilyuisk, and +18.8°C in Yakutsk. The sum of active temperatures is 1200-1400°C. The annual amount of precipitation decreases from west to east: in Vilyuisk 2.46 mm falls, and in Yakutsk - 192 mm, the moisture coefficient is -0.77 -0.55, N=15 - 26.

The entire territory is covered with larch forests, under which predominantly permafrost-taiga carbonate soils are developed, which are formed on carbonate rocks. on the Leno-Vilyui lowland, forests are often swampy. Larch-pine and pine forests are widespread on the sandy terraces of the valleys. Permafrost-taiga fawn (neutral) and solodized soils have formed under the forests. On the terraces of the valleys of the Lena and Vilyui rivers, among the larch taiga, there are patches of meadows, among which alasses are especially peculiar. Alas vegetation consists of fescue, bluegrass, sedge and a large amount of herbs. Some of the alasses are covered with solonchak meadows (turans) formed on the site of lakes.

The vegetation of saline meadows consists of saltworts. There are salt licks and solods. Steppe meadows with dark-colored meadow-chernozem loamy soils containing up to 12-17% of humus are common on the floodplain terraces of the Lena. Their vegetation cover is formed by hairy feather grass, fescue, thin-legged, xerophytic forbs: Siberian edelweiss and speedwell. Among wall species, there are local Siberian species, whose origin is associated with the mountainous regions of Siberia, and Mongolian species, which came mainly from Central Asia during one of the xerothermic periods.

The Aldan socle taiga mountain-tundra plateau occupies the southeastern part of Central Siberia, between the Lena and the Stanovoy Range. In the Aldan Highlands, the ridges rise up to 1800-2300.

The Aldan socle plateau is a reflection in the relief of the Aldan shield, which is composed of crystalline and metamorphic rocks of the Archean. They are covered from the surface by sedimentary rocks of the Lower Cambrian and continental sediments of the Jurassic and Lower Cretaceous. The Aldan Shield is riddled with intrusions of various ages. Mesozoic deposits on the shield occur in the Predstanovoy trough, which is a zone of deep basement subsidence, where the thickness of Mesozoic coal-bearing sediments reaches up to 750 m. A large fault passes in the south of the trough, separating the Stanovoy Range from the Aldan Highlands. In the relief, the fault line is expressed as a ledge.

To the north, the Archean rocks submerge under the predominantly carbonate sequences of the Lower Cambrian, gently dipping to the north. There are patches of Jurassic deposits on the surface of the Cambrian. The slope of the Aldan shield in the relief is expressed by the Lena-Aldan erosion layer-tier plateau, on which heights of 500-600 m prevail, reaching 700-1000 m in some areas. Ancient and modern karst processes occurring in Cambrian rocks are widespread on the plateau. In the Pliocene-Quaternary, the Aldan Highlands experienced a greater uplift than the Lena-Aldan Plateau. Uplifts caused a revival of erosion and dismemberment of the territory.

The rivers are deeply incised: they have up to 4-8 accumulative and socle terraces (Olyokma, Lena, Aldan). Within the region, four leveling surfaces are distinguished (the highest is 1000-1300 m, the lowest is Lenskaya-300-400 m). Traces of ancient glaciations are expressed on the ridges of the Aldan Highlands with absolute elevations above 1200-1300 m.

The climate is cold and cold-temperate with an average January temperature of -32, -40°C, with a long snow cover of 220-240 days. Summer on the Leno-Aldan plateau is warm, humid and semi-humid, the average July temperature is above +16°C; in the Aldan Highlands - cool and excessively humid; the average July temperature is about +12°C. The sum of active temperatures is 1200°-1400°C, the humidification coefficient is 1.33-1.00. Annual precipitation is 200-300 mm on the Lena-Aldan Plateau and 400-500 mm on the Aldan Highlands, N = 9-4.

On the Lena-Aldan plateau, larch middle taiga forests on permafrost-taiga pale (neutral) and solodized soils predominate. Along the river valleys there are larch-pine forests and patches of meadow steppes (Amga valley). The Aldan Highlands are dominated by mountain-larch and larch-cedar forests on mountain permafrost-taiga soils and mountain permafrost-taiga carbonate soils. Forests rise along the slopes of the ridges to a height of 1200-1300 m. Above the slopes and peaks are covered with mountain tundra on mountain-tundra soils.

The Sayan southern taiga and forest-steppe erosional plateau with a cover of loess-like rocks lies in the foothills of the Eastern Sayan. The plateau reaches its highest height in the foothills (550-760 m). To the north and northeast, the territory drops to 500 m. The lowest parts of the region (200-240 m) are located in the area of ​​the city of Kansk. The region is located on the southern outskirts of the Siberian platform - in the Irkutsk amphitheater, where three geostructures are distinguished: the Sayano-Prienisei and Baikal-Lena syneclises and the Angarsk anteclise separating them. Along the northern foot of the Eastern Sayan stretch the Mesozoic depressions - the Cape and Irkutsk, filled mainly with terrigenous coal-bearing deposits of the Jurassic age; The Cape depression continues to the west, beyond the Yenisei, and is united by the common name of the Kansk-Achinsk depression.

The coal and lignite deposits of the Kansk-Achinsk and Irkutsk basins form the Kansk-Irkutsk coal-bearing province.

The climate is sharply continental, semi-arid: the amplitude of absolute temperatures is about 84°С (-51°С +33°С). Winter is very cold, quite snowy in the west and moderately snowy in the east with an average January temperature of -20, -25 ° C. Summer is warm, the sum of active temperatures is 1400-1600 ° C, the duration of the frost-free period is from 72 days in the northeast of the region to 106 -111 days in the Cape forest-steppe. Precipitation per year is 300-400 mm, the moisture coefficient is 1.00-0.77. Permafrost islands are rare.

Among the southern taiga pine forests there are areas of steppes and steppe meadows: their distribution is associated with a dissected relief and degree of moisture. Significant areas are covered with larch-pine forests on soddy-podzolic soils. Spruce-fir forests of the southern taiga type occupy the northern territories and are found along the valleys. Pine forests of forest-steppes on watersheds and slopes are sparse and with a high grass cover, birch forests with an admixture of larch cover the slopes of the northern exposure, and sometimes watersheds.

The forest-steppes occupy the lower parts of the plateau (the Cape Basin) and the slopes of the valleys of the Oka and Angara rivers (the Irkutsk and Balagan forest-steppes). The steppes are dominated by perennial turf grasses (fine-legged fescue, hairy feather grass, wormwood) and herbs (veronica and cinquefoil). The species composition of the steppes of Central Siberia is somewhat different from the steppes of Western Siberia: many species are absent, for example, tavolzhanka, but mountain-steppe ones appear, for example, edelweiss. Leached chernozems predominate, and on the outskirts - gray forest slightly podzolic soils. Meadow saline soils are developed in logs.

Conclusion

On the basis of the studied material, it can be concluded that the Central Siberian Plateau is a formation that is complex 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.

The Central Siberian Plateau is characterized by river valleys with well-defined terraces and numerous shallow valleys. The presence of terraces testifies to the slow movements of the earth's crust that took place on the territory of the plateau.

The climate is sharply continental. Permafrost is ubiquitous. The formation of permafrost occurred during the Ice Age. Permafrost is a legacy of the Ice Age. The Central Siberian region has a rich material and raw material base, sufficiently prepared for industrial development. The water resources of the Central Siberian Plateau are one of the most valuable natural resources. Groundwater resources can be renewed in accordance with the natural cycles characteristic of a particular climatic zone, the geological structure and landscape features of the territory.

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. The natural zones 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.

Weekly tour, one-day hiking trips and excursions combined with comfort (trekking) in the mountain resort of Khadzhokh (Adygea, Krasnodar Territory). Tourists live at the camp site and visit numerous natural monuments. Rufabgo Waterfalls, Lago-Naki Plateau, Meshoko Gorge, Big Azish Cave, Belaya River Canyon, Guam Gorge.

A vast territory lying to the east of the lower reaches of the Lena, north of the lower reaches of the Aldan and bounded in the east by the mountain ranges of the Pacific watershed, forms the country of North-Eastern Siberia.

Territory S-V. Siberia in the Paleozoic and the first half of the Mesozoic was a site of the Verkhoyansk-Chukotka geosynclinal marine basin. This is evidenced by tectonic movements that created the folded structures of the country and the large thickness of Paleozoic and Mesozoic deposits. Especially typical are deposits of Permian, Triassic, Jurassic sandstones and shales, usually intensively dislocated and cut through by young intrusions.

The most ancient structural elements are the Kolyma and Omolon median massifs. Their foundation is composed of Precambrian and Paleozoic deposits.

The remaining elements are of a younger age, predominantly Upper Jurassic and Cretaceous. These include the Verkhoyansk folded zone and the Sete-Dabansky anticlinorium, the Yana and Indigirsko-Kolyma synclinal zones, as well as the Tas-Khayakhtakhsky and Momsky anticlinoria. The extreme s-eastern regions are part of the Anyui-Chukotka anticline, separated from the median massifs by the Oloy tectonic depression. Mesozoic fold-like movements, as a result of which these structures were formed, were accompanied by ruptures, outpourings of rocks, intrusions, which are associated with various mineralization - gold, tin, molybdenum.

By the end of the Cretaceous, S-V. Siberia was elevated above the neighboring regions .. The processes of denudation led to the alignment of the relief and formation of flat layers.

The formation of the modern mountain relief is due to differentiated tectonic substrata of the Neogene and Quaternary time (100-200m). In areas of the most intense uplifts, especially high ridges arose.

During the Pliocene the climate was warm and humid. Early Quaternary uplifts were accompanied by a noticeable cooling of the climate. The forests that covered the southern regions of the country at that time consisted of dark coniferous species. From the middle of the Quaternary, glaciation began. Large valley glaciers appeared, and firn fields formed on the plains. In the far north in the second half of the quarter. Glaciation began the formation of permafrost.

That. glaciation of the plains was passive. The glaciers were mostly inactive, carrying little loose material, and their movement had little effect on the terrain.

In the outlying mountain ranges, forms of glacial exaration in the form of kars and trough valleys are well preserved. The length of valley glaciers reached 200-300 km. There were glaciations in Siberia: Middle Quaternary - Tobychanskoe and Upper Quaternary - Elga and Bokhapcha.

Fossil flora testifies to the increase in the severity and continent of the climate. Already after the first oleding, Siberian coniferous trees appeared, including the Daurian larch, which is now dominant.

There are the following types of relief:

Accumulative plains - occupy areas of tectonic subsidence and accumulation of sediments. Characterized by a slightly rugged relief and slight fluctuations in elevation. Forms are widespread: thermokarst depressions, permafrost heaving mounds, frost cracks and polygons, and high ice cliffs intensively collapsing on the sea coasts (Oyegossky Yar more than 70 km). They occupy vast areas of the Yano-Indigirskaya, Sredneindigirskaya and Kolyma lowlands, some islands of the seas of the Arctic Ocean (Fadddeevsky, Lyakhovsky, etc.). In the depressions of the Momo-Selenyakhskaya and Semchanskaya basins, the Yanskoye and Elga plateaus.

Erosion-denudation plains - at the foot of some northern ridges (Anyuysky, Momsky, Kharaulakhsky, Kulara), in the peripheral sections of the Polousny ridge, the Ulakhan-Sis ridge, the Alazeysky and Yukagirsky flats up to 200, in places 400-500m. They are composed of bedrocks of various ages - therefore, there are rubble placers, low hills, solifluction terraces, and other formations associated with the processes of permafrost relief formation.

Plateau relief in the strip between the systems of the Verkhoyansk and Chersky ridges (Yanskoye, Elginskoye, Oymyakonskoye and Nerskoye flats), as well as the Upper Kolyma highlands, Yukagirskoye and Alazeya flatlands. Most of them are composed of Mesozoic rocks and represent denudation leveling surfaces from 400 to 1200-300 m.

The lowlands are spread along the outskirts of high ridges and are dissected by a dense network of deep river valleys. Characteristic forms of nival-solifluction and glacial processing, an abundance of stony placers and rocky peaks.

Mid-mountain relief - for most massifs of the Verkhoyansk Range, Yudomo-Maya Highlands, Chersky, Tas-Khayakhtakh and Momsky Ranges, in the Kolyma Highlands and the Anyui Range from 800-1000 to 2000-2200 m, on interfluve spaces 200-300 m. Forms created by glaciers, permafrost and solifluction processes are developed. River valleys are usually deep, sometimes canyon-like gorges.

The high-mountainous alpine relief is associated with areas of the most intense Quaternary sublands at an altitude of more than 2000-2200 m. These are the ridges of the highest ridges (Suntar-Khayata, Tas-Khayakhtakh, the Chersky ridge, Tas-Kystabyt, Ulakhan-Chistai), the central regions of the Verkhoyansk ridge. They arose as a result of the latest uplifts of denudation plains on top of its alignment. It is characterized by deep dissection and large amplitudes of heights, the predominance of narrow rocky ridges, punishments, cirques and other glacial landforms.

Minerals - ore deposits are especially important. In the mountains of the Yano-Kolyma Territory there are gold-bearing regions - Verkhneindigirsky, Allah-Yunsky and Yansky. A large tin-bearing province has been explored within the Yana-Indigirka interfluve. The largest deposits of tin - Deputatskoe, Ege-Khaiskoe, Kesterskoe, Ilintas, etc. - are associated with the Upper Jurassic and Cretaceous granite intrusions: a lot of tin is also found here in alluvial placers. Deposits of polymetals, tungsten, mercury, molybdenum, antimony, cobalt, arsenic, coal and various building materials have great knowledge. In the intermountain depressions and on the coastal lowlands, prospects for the discovery of oil and gas fields have been identified.

(((There is also material in cheat sheets for the northeast of Siberia .. but here it is the main thing. You can take it extra if you have time))) ...

Question 20 Inland waters of Russia: concept, characteristics, patterns of distribution over the territory. The problem of water resources in Russia.

Inland waters (land waters) include waters of:

Ø Lakes (reservoirs)

Ø Glaciers and permafrost

Ø Underground and ground water

Ø Void waters and soil

Ø Air water vapor

At present, water is the most important natural resource, g.p., a limiting factor in the development of civilization. It puts a limit to the development of certain forms of farming.

Water is the most abundant liquid on earth, but also the most scarce. This is a true miracle of nature, a one-of-a-kind liquid that cannot be replaced by anything. All holy waters are an exception. It strikes with its heat capacity: it is enough to cool it by 1 0 C 1m 3 of water, while so much heat will be released that will allow it to be heated by 3 0 C 1 thousand m 3 of air.

The main source of water on Earth is atmospheric precipitation and juvenile water. If the large moisture circulation ceased, a person would have exhausted all the water on Earth in 84 years.

Inland waters are predominantly fresh waters. They make up about 3% of all V water on Earth, i.e. their V is insignificant ® the attitude towards them must be careful.

The main, most significant waters are waters rec.

Water supply in:

Ø rivers is 0.005% of the total V fresh water of the USSR

Ø lakes - 2.7%

Ø reservoirs - 0.03%

Ø groundwater (basic water) - 96%

Ø glaciers - 0.35%

In terms of the total V of river runoff (more than 45 thousand km 3), the Russian Federation surpasses other countries of the world, but the water supply per unit S (specific water supply) is 1.5 less than the average on the earth's land.

The CIS is inferior in terms of water supply:

Ø US 2 times

Ø France - 3 times

Ø Norway - 6 times

In general, the Russian Federation is a camp of great river systems. The significance of rivers in the life of nature and man, in their history is diverse. Rivers are closely related to relief and climate. Depending on the influence of the relief, the rivers are divided into:

2. Flat

In the Russian Federation, there are those and those. On the flat rivers there are both rapids (Dnepr, Onega) and waterfalls: vdp. Ivach on the river. Suna, which flows into the lake. Onega.

The influence of relief on rivers is manifested in their length and fall (difference in the absolute heights of the source and mouth), slope (ratio of fall to river length in cm/km). For example, the Ob River has a drop of 4 cm, the Volga - 7 cm, the Yenisei - 37 cm, near the Terek - several meters.

most long the Lena is considered a river 4400 km, there is evidence that the Ob (if the source of the Ob is the Irtysh) is 5410 km.

In the aisles of the Russian Federation there are more than 20 rivers with a length of more than 1 thousand km.

The river is characterized annual flow - the amount of water that flows through the channel per year. The most abundant river is the Yenisei River (annual flow 600 km 3 / year), Lena (500 km 3 / year), Amur (350 km 3 / year).

The largest S of the pool is near the Ob.

The ice regime is of great importance for the practical use of rivers. The rivers of the Russian Federation are characterized by a long-term stable ice regime. For Russia, this is very important, because. during the long winter, rivers and wetlands provide excellent roads.

The rivers of the Russian Federation are unevenly distributed over the ocean basins:

Ø 65% of the territory of the Russian Federation falls on the bass. Sev.Ice. ocean

Ø 20% - Quiet

Ø 3% - Atlantic

Ø 10% - Caspian Inland Basin

In addition to the rivers of the Russian Federation, it is rich lakes. There are more than 3 million of them on the territory of the Russian Federation, among which the unique one is Lake. Baikal. This is the deepest lake in the World = 1637 m. Its width increases annually by 3-5 mm, in some years by 10 or more mm ® the lake is located in the modern growing depth. The crustacean apeshura lives in this lake, constituting 97% of the fifth biomass. It purifies the water (the water is exceptionally pure). Baikal is fed by the waters of the layers of the earth - juvenile.

3 more large lakes (out of 140 of the world): Aral, Balkhash, Ladoga. S more than 10 thousand km2.

For practical purposes, it is not so much the number of lakes that is important, but the S occupied by them - lacustrine . The lake content of the USSR is 2%.

The largest northern lake in the world is Lake. Taimyr, located at the foot of the Byrranga mountains.

Lakes of God S-Z RF. This is the country of 1000 lakes. The lakes are unevenly distributed over the territory of the Russian Federation. With the movement to the south, their number ¯, and a great many of them in the north. Lakes, like rivers, are closely related to climate.

permafrost– a layer of GB that does not thaw for a period of several years to many thousand years. Occupied by S more than 50% of the CIS.

In present time its degradation (climate warming) is observed. All in. parts of continuous permafrost. South of the Arctic Circle - island. Covers the entire North West. Sib., all East. Sib. and the edge of the north of the Russian Equal.

It sharply complicates the household. Requires special construction. Any object will sink into the ground in 1-2 years.

Preserves the northern configuration of the coastline of the Russian Federation.

It is an additional source of moisture. Central Siberian forests would not be able to grow (300 mm of precipitation)

Powerful refrigerator.

ground water- an integral part of inland waters, the upper horizon of groundwater.

Soil formation and the development of vegetation cover depend on their nature.

In its distribution, groundwater obeys the law of zonality. In the northern part, they are ultra fresh and occur almost from the surface. With the movement to the south, they sink, their chemistry increases. On Wednesday. Asia have the greatest depth of immersion and chlorides in terms of chemistry.

swamps. More than 50% of the territory of the Russian Federation is swampy. On the territory of the Russian Federation there is a world phenomenon - the Vasyugan swamps. Meaning: water accumulator. In the swamps Zap. Sib. More than 1 thousand km 3 of water. Wetlands regulate river flow. Rivers West. Sib. full-flowing.

Modern glaciation. 75% of the modern glaciation of the Russian Federation falls on the islands of the North. Ice. ocean. Cover glaciers prevail there, and in the mountains - mountain-valley (Altai, Caucasus).

By V soil water= V glaciers.

Problem water in the Russian Federation is acute. It is a unique solvent ® that gets dirty quickly. This is an anthropogenic factor. And natural - the flow of rivers is not distributed uniformly over time (80% of the flow in spring). The rivers are fed predominantly by precipitation® when there is a problem with water in dry years.

Rivers are characterized by a large fluctuation in flow: low-water and with increased flow. In low-water rivers, the water content is 1% of the high water content.

What will save us! The earth is a kind of generator of water, which produces 2/3 V, which can produce. Currently, geology is undergoing evolution in terms of the internal structure of the Earth. On Earth, rocks approach the earth's surface. And if you drill into one well and pump some kind of water, then you can get clean water from another.

Eastern Siberia is part of the Asian territory of the Russian Federation. It is located from the borders of the Pacific Ocean to the Yenisei River. This zone is characterized by an extremely harsh climate and limited fauna and flora.

Geographic Description

Eastern and occupy almost two-thirds of the territory of Russia. They are located on the plateau. The eastern zone covers an area of ​​about 7.2 million square meters. km. Its possessions extend up to the Sayan mountain ranges. Most of the territory is represented by the tundra lowland. The mountains of Transbaikalia play a significant role in the formation of the relief.

Despite the harsh climatic conditions, there are quite a lot of large cities in Eastern Siberia. The most attractive from an economic point of view are Norilsk, Irkutsk, Chita, Achinsk, Yakutsk, Ulan-Ude, and others. Within the zone are the Zabaikalsky and Krasnoyarsk Territories, the republics of Yakutia, Buryatia, Tuva and other administrative regions.

The main type of vegetation is the taiga. It will be washed from Mongolia to the borders of the forest-tundra. Occupies over 5 million sq. km. Most of the taiga is represented by coniferous forests, which make up 70% of the local vegetation. Soils develop unevenly relative to natural zones. In the taiga zone, the soil is favorable, stable, in the tundra - rocky, frozen.

Within the interfluve and lowlands, insignificant swamps are observed. However, they are much less than in the same Western Siberia. But in the eastern region, arctic deserts and deciduous plantations are often found.

Terrain characteristics

Eastern Siberia of Russia is located at a high level above the sea. All the fault of the plateau, which is located in the middle part of the zone. Here the height of the platform varies from 500 to 700 meters above sea level. The relative averageness of the region is noted. The highest points are the interfluve of the Lena and the Vilyui plateau - up to 1700 meters.

The base of the Siberian platform is represented by a crystalline folded basement, on which there are huge sedimentary layers up to 12 kilometers thick. The north of the zone is determined by the Aldan shield and the Anabar massif. The average thickness of the soil is about 30 kilometers.

To date, the Siberian platform contains several main types of rocks. These are marble, and schist, and charnockite, etc. The oldest deposits date back to 4 billion years. Igneous rocks were formed as a result of eruptions. Most of these deposits are located in and also in the Tunguska depression.

The modern relief is a combination of lowlands and uplands. Rivers flow in the valleys, swamps form, coniferous trees grow better on the hills.

Features of the water area

It is generally accepted that the Far East faces the Arctic Ocean with its "facade". The eastern region borders on such seas as the Kara, Siberian and Laptev. Of the largest lakes, it is worth highlighting Baikal, Lama, Taimyr, Pyasino and Khantayskoye.

Rivers flow in deep valleys. The most significant of them are the Yenisei, Vilyui, Lena, Angara, Selenga, Kolyma, Olekma, Indigirka, Aldan, Lower Tunguska, Vitim, Yana and Khatanga. The total length of the rivers is about 1 million km. Most of the inland basin of the region belongs to the Arctic Ocean. Other external water areas include such rivers as Ingoda, Argun, Shilka and Onon.

The main source of food for the inner basin of Eastern Siberia is the snow cover, which melts in large volumes under the influence of sunlight from the beginning of summer. The next most important role in the formation of the continental water area is played by rains and groundwater. The highest level of the basin's runoff is observed in the summer.

The largest and most important river in the region is the Kolyma. Its water area occupies more than 640 thousand square meters. km. The length is about 2.1 thousand km. The river originates in the Upper Kolyma Highlands. Water consumption exceeds 120 cubic meters per year. km.

Eastern Siberia: climate

The formation of meteorological features of the region is determined by its territorial location. The climate of Eastern Siberia can be briefly described as continental, consistently severe. There are significant seasonal fluctuations in cloudiness, temperature, and precipitation levels. The Asian anticyclone forms vast areas of high pressure in the region, especially this phenomenon occurs in winter. On the other hand, severe frost makes air circulation changeable. Because of this, temperature fluctuations at different times of the day are more significant than in the west.

The climate of North-Eastern Siberia is represented by changeable air masses. It is characterized by increased precipitation and dense snow cover. This area is dominated by continental flows, which are rapidly cooling in the ground layer. That is why in January the temperature drops to a minimum. Arctic winds prevail at this time of the year. Often in winter, you can observe air temperatures down to -60 degrees. Basically, such minima are inherent in depressions and valleys. On the plateau, the indicators do not drop below -38 degrees.

Warming is observed with the arrival of air flows from China and Central Asia to the region.

winter time

No wonder it is believed that Eastern Siberia has the heaviest and most severe. The table of temperature indicators in winter is proof of this (see below). These indicators are presented as average values ​​for the last 5 years.

Due to the increased dryness of the air, the constancy of the weather and the abundance of sunny days, such low rates are easier to tolerate than in a humid climate. One of the defining meteorological characteristics of winter in Eastern Siberia is the absence of wind. Most of the season there is a moderate calm, so there are practically no blizzards and snowstorms here.

Interestingly, in the middle part of Russia, a frost of -15 degrees is felt much stronger than in Siberia -35 C. Nevertheless, such low temperatures significantly worsen the living conditions and activities of local residents. All living quarters have thickened walls. Expensive fuel boilers are used to heat buildings. The weather begins to improve only with the onset of March.

warm seasons

In fact, spring in this region is short, as it comes late. The eastern one, which changes only with the arrival of warm Asian air currents, begins to wake up only by mid-April. It is then that the stability of positive temperatures during the daytime is noted. Warming comes in March, but it is insignificant. By the end of April, the weather begins to change for the better. In May, the snow cover completely melts, the vegetation blooms.

In summer, the weather becomes relatively hot in the south of the region. This is especially true for the steppe zone of Tuva, Khakassia and Transbaikalia. In July, the temperature here rises to +25 degrees. The highest rates are observed on flat terrain. It is still cool in the valleys and highlands. If we take the whole of Eastern Siberia, then the average summer temperature here is from +12 to +18 degrees.

Climate features in autumn

Already at the end of August, the first frosts begin to envelop the Far East. They are observed mainly in the northern part of the region at night. During the day the bright sun shines, it rains with sleet, sometimes the wind intensifies. It is worth noting that the transition to winter is much faster than from spring to summer. In the taiga, this period takes about 50 days, and in the steppe area - up to 2.5 months. All these are characteristic features that distinguish Eastern Siberia from other northern zones.

The climate in autumn is also represented by an abundance of rains coming from the west. Moist Pacific winds blow most often from the east.

Precipitation level

Relief is responsible for atmospheric circulation in Eastern Siberia. Both the pressure and the speed of air mass flows depend on it. About 700 mm of precipitation falls annually in the region. The maximum indicator for the reporting period is 1000 mm, the minimum is 130 mm. The level of precipitation is not clearly defined.

On the plateau in the middle lane, it rains more often. Due to this, the amount of precipitation sometimes exceeds the mark of 1000 mm. The most arid region is Yakutsk. Here the amount of precipitation varies within 200 mm. The least rain falls between February and March - up to 20 mm. The western regions of Transbaikalia are considered the optimal zones for vegetation with respect to precipitation.

Eternal Frost

Today there is no place in the world that could compete in terms of continentality and meteorological anomalies with a region called Eastern Siberia. The climate in some areas is striking in its severity. In the immediate vicinity of the Arctic Circle lies the permafrost zone.

This area is characterized by low snow cover and low temperatures throughout the year. Because of this, mountain weather and the ground lose a huge amount of heat, freezing to whole meters in depth. The soils here are mostly stony. Groundwater is underdeveloped and often freezes for decades.

Vegetation of the region

The nature of Eastern Siberia is mostly represented by taiga. Such vegetation extends for hundreds of kilometers from the Lena River to the Kolyma. In the south, the taiga borders on the local possessions are untouched by man. However, due to the arid climate, the threat of large-scale fires always hangs over them. In winter, the temperature in the taiga drops to -40 degrees, but in summer the figures often rise to +20. Rainfall is moderate.

Also, the nature of Eastern Siberia is represented by the tundra zone. This zone is adjacent to the Arctic Ocean. The soils here are bare, the temperature is low, and the humidity is excessive. Flowers such as cotton grass, gravel, poppy, saxifrage grow in mountainous areas. From the trees of the region, one can distinguish spruces, willows, poplars, birches, pines.

Animal world

Almost all regions of Eastern Siberia are not rich in fauna. The reasons for this are permafrost, lack of food and underdevelopment of deciduous flora.

The largest animals are the brown bear, lynx, elk and wolverine. Sometimes you can meet foxes, ferrets, stoats, badgers and weasels. Musk deer, sable, deer and bighorn sheep live in the central strip.

Due to the eternally frozen soil, only a few species of rodents are found here: squirrels, chipmunks, flying squirrels, beavers, marmots, etc. But the feathered world is extremely diverse: capercaillie, crossbill, hazel grouse, goose, crow, woodpecker, duck, nutcracker, sandpiper, etc. .

It occupies an area of ​​about 7 million square kilometers. Eastern Siberia is called the area located east of, to the mountains that form the watershed between and. It occupies the largest area. In the north and east there are two lowlands: North Siberian and Central Yakut. In the south and west there are mountains (, Yenisei Ridge). The length of this region from north to south is about 3 thousand kilometers. In the south there is a border with and, and the northernmost point is Cape Chelyuskin.

During the Mesozoic period, most of Central Siberia experienced uplift. It is no coincidence that the highest point of the Central Siberian Plateau is located in this area (its height is 1700 meters above sea level). In the Cenozoic, surface uplift continued. At the same time, a river network was being created on the surface. In addition to the Putorana plateau, the Byrranga, Anabar and Yenisei massifs rose most intensively. Subsequently, active tectonic processes that took place in this area led to a change in the river system. Traces of river systems that existed in ancient times have survived to our time. At the same time, river terraces and deep river valleys of the central part of Siberia were formed.

Cape Chelyuskin

The vast majority of river valleys in Central Siberia are canyon-like and asymmetrical. Their characteristic feature is also a large number of terraces (six to nine), which indicates repeated tectonic uplifts of the territory. The height of some terraces reaches 180-250 m. On and in the North Siberian lowland, the river valleys are younger, and the number of terraces is somewhat less. Even the largest rivers have here three or four terraces.

Four relief groups can be distinguished on the territory of the Central Siberian Plateau:

• plateaus, ridgesplateaus, ridges, and mid-mountain massifs on ledges of the crystalline basement
• bedded uplands and plateaus on sedimentary Paleozoic rocks;
• plateau
• and reservoir-accumulative

Most of the tectonic processes that took place in antiquity and in modern times, on the territory Eastern Siberia matched in direction. However, this did not happen throughout the entire territory of the Central Siberian Plateau. As a result of these discrepancies, depressions similar to the Tunguska were formed. There is no permafrost (the Lena-Angara and Lena-Aldan plateaus). But the main small relief forms on the territory of the Central Siberian plateau are still erosive and cryogenic.

Due to the strongest monsoons, sharply continental, characteristic of Eastern Siberia, here you can find a large number of stony placers and screes in mountain ranges, on the slopes of river valleys and on plateau surfaces.