The average temperature of the Caucasus. Climatic conditions of the Caucasus

The climate of the Caucasus is very diverse. The northern part of the Caucasus is located within the temperate zone, Transcaucasia - in the subtropical. Such geographical position significantly influences the formation of the climate in various parts of the Caucasus.

The Caucasus is a vivid example of the influence of orography and relief on climate-forming processes. Radiant energy is distributed unevenly due to different angles of incidence and different heights of surface levels. Circulation air masses reaching the Caucasus, undergoes significant changes, encountering on its way the mountain ranges of both the Greater Caucasus and Transcaucasia. Climatic contrasts appear at relatively short distances. An example is the western, abundantly humidified Transcaucasia and the eastern, with a dry subtropical climate, the Kuro-Araks lowland. The significance of the exposure of slopes is great, which strongly affects the thermal regime and the distribution of precipitation. The climate is influenced by the seas washing the Caucasian Isthmus, especially the Black Sea.

Black and Caspian Sea they moderate the air temperature in summer, contribute to its more even daily course, moisten the parts of the Caucasus adjacent to them, increase the temperature of the cold season, and reduce temperature amplitudes. The plain eastern Ciscaucasia and the Kuro-Araks lowland, which extends deeply into the isthmus, do not contribute to the condensation of moisture coming from the Caspian Sea. Ciscaucasia is greatly influenced by continental air masses coming from the north, including the Arctic ones, which often significantly reduce the temperature of the warm season. The spur of high East Siberian barometric pressure often lowers the temperature of the cold season. There are cases when cold air, flowing around the Greater Caucasus from the east and west, spreads into Transcaucasia, causing a sharp drop in temperature there.

Air masses coming from the Atlantic Ocean and the Mediterranean ensure high humidity in the western parts of the Caucasus and the slopes of the western exposure ranges. Additional moisture is brought by air masses passing over the Black Sea. The influence of the Caspian Sea is less pronounced.

V in general terms The climate of the Caucasus changes significantly in three directions: from west to east towards increasing dryness and continentality, from north to south towards an increase in total radiation and radiation balance, and in height on mountain structures, on which altitudinal zonality is clearly manifested.

The total radiation within the Caucasus ranges from 460548 J/sq. cm in the north to 586 152 J / sq. see extreme south. Annual radiation balance from 146538 to 188406 J/sq. see The amount of solar radiation depends not only on latitude, but also on cloud cover. Many peaks of the Caucasus are characterized by persistent cloudiness, so direct solar radiation here is below the average norm. To the east, it increases due to a decrease in humidity. The exceptions are Lankaran and Talysh, where the relief contributes to the condensation of water vapor and an increase in cloudiness.

The value of the total radiation and the radiation balance in different regions of the Caucasus is not the same due to the contrasts of the orography, relief, different angles of incidence of the sun's rays and the physical properties of the underlying surface. In summer, the radiation balance in some regions of the Caucasus approaches the balance of tropical latitudes, so the air temperatures are high here (Ciscaucasia and Transcaucasian plains), and in abundantly humidified areas, high evapotranspiration and, accordingly, increased air humidity are observed.

air masses, taking part in circulation over the territory of the Caucasus are different. Basically, continental air of temperate latitudes dominates over Ciscaucasia, and subtropical air dominates in Transcaucasia. High-mountain belts are influenced by air masses coming from the west, and the northern slopes of the Greater Caucasus and the Arctic - from the north.

In Ciscaucasia, located south of the band of high barometric pressure, cold air often enters. Over the Black Sea and in the southern part of the Caspian Sea, low pressure remains. Pressure contrasts lead to the spread of cold air to the south. In such a situation, the barrier role of the Greater Caucasus is especially great, which serves as an obstacle to the wide penetration of cold air into the Transcaucasus. Usually its influence is limited to the Ciscaucasia and the northern slope of the Greater Caucasus up to about 700 m. It causes a sharp drop in temperature, an increase in pressure and an increase in wind speed.

Intrusions of cold air masses are observed from the northwest and northeast, bypassing the ridges of the Greater Caucasus along the shores of the Caspian and Black Seas. The accumulated cold air rolls over low ridges. and spreads along the western and eastern coasts to Batumi and Lenkoran, causing a drop in temperatures on the western coast of Transcaucasia to -12 ° C, on the Lankaran lowland to -15 ° C and below. A sharp drop in temperature has a disastrous effect on subtropical crops, and especially on citrus fruits. Baric gradients in these situations between Ciscaucasia and Transcaucasia are sharply contrasting, the spread of cold air from Ciscaucasia to Transcaucasia proceeds very rapidly. Cold winds of high, often catastrophic speeds are known as bora (in the Novorossiysk region) and norda (in the Baku region).

Air masses coming from the west and southwest from the Atlantic Ocean and the Mediterranean, greatest influence have on the western coast of Transcaucasia. When moving further to the east, they, overcoming the ridges located on their way, adiabatically heat up and dry up. Therefore, Eastern Transcaucasia is distinguished by a relatively stable thermal regime and low precipitation.

The mountain structures of the Lesser Caucasus and the Javakheti-Armenian Highlands contribute to the formation of a local anticyclone in winter, which causes a strong drop in temperature. In summer, low pressure sets in over the highlands.

In the second half of summer, the Caucasus experiences the influence of the spur of the Azores barometric maximum, located within the Russian Plain between 50 and 45°N. sh. It determines the decrease in summer cyclonic activity. It is associated with a decrease in precipitation in the second half of summer (compared to the first). At this time, the importance of local convective precipitation increases due to the daily variation of air temperatures.

In the Caucasus, föhns are actively manifested, which are common for mountains with a dissected relief. They are associated with hot weather in spring and summer. Mountain-valley winds and breezes are also characteristic.

On the plains of Ciscaucasia and Transcaucasia average temperature July 24--25 ° C, its increase is observed to the east. The coldest month is January. In the Ciscaucasia, the average January temperature is -4, -5 ° C, in the western Transcaucasia 4-5 ° C, in the eastern 1-2 ° C. At an altitude of 2000 m, the temperature is 13 ° C in July, -7 ° C in January, in the highest zones - 1 ° C in July, and from -18 to -25 ° C in January.

The annual amount of precipitation increases with elevation and at all levels decreases noticeably from west to east (most evenly in high belts). In the Western Ciscaucasia, the amount of precipitation is 450-500 mm, in the foothills and on the Stavropol Upland at an altitude of 600-700 m - up to 900 mm. In the east of Ciscaucasia - 250-200 mm.

In the humid subtropics of Western Transcaucasia on the coastal plains, the annual precipitation reaches 2500 mm (in the Batumi region). Maximum in September. In the Sochi region, 1400 mm, of which 600 mm falls in November-February. On the western slopes of the Greater and Lesser Caucasus, the amount of precipitation increases to 2500 mm, on the slopes of the Meskheti Range up to 3000 mm, and on the Kuro-Araks lowland it decreases to 200 mm. The Lankaran lowland and the eastern slopes of the Talysh ridge are abundantly moistened, where 1500-1800 mm of precipitation falls.

The climate of the Caucasus is very diverse. The northern part of the Caucasus is located within the temperate zone, Transcaucasia - in the subtropical. This geographical position significantly affects the formation of the climate in various parts of the Caucasus.

The Caucasus is a vivid example of the influence of orography and relief on climate-forming processes. Radiant energy is distributed unevenly due to different angles of its incidence and different heights of surface levels. The circulation of air masses reaching the Caucasus undergoes significant changes, encountering on its way the mountain ranges of both the Greater Caucasus and Transcaucasia. Climatic contrasts appear at relatively short distances. An example is the western, abundantly humidified Transcaucasia and the eastern, with a dry subtropical climate, the Kuro-Araks lowland. The significance of the exposure of slopes is great, which strongly affects the thermal regime and the distribution of precipitation. The climate is influenced by the seas washing the Caucasian Isthmus, especially the Black Sea.

The Black and Caspian Seas moderate the air temperature in summer, contribute to its more even daily course, moisten the adjacent parts of the Caucasus, increase the temperature of the cold season, and reduce temperature amplitudes. The plain eastern Ciscaucasia and the Kuro-Araks lowland, which extends deeply into the isthmus, do not contribute to the condensation of moisture coming from the Caspian Sea. Ciscaucasia is greatly influenced by continental air masses coming from the north, including the Arctic ones, which often significantly reduce the temperature of the warm season. The spur of high East Siberian barometric pressure often lowers the temperature of the cold season. There are cases when cold air, flowing around the Greater Caucasus from the east and west, spreads into Transcaucasia, causing a sharp drop in temperature there.

Air masses coming from the Atlantic Ocean and the Mediterranean ensure high humidity in the western parts of the Caucasus and the slopes of the western exposure ranges. Additional moisture is brought by air masses passing over the Black Sea. The influence of the Caspian Sea is less pronounced.

In general terms, the climate of the Caucasus changes significantly in three directions: from west to east towards an increase in dryness and continentality, from north to south towards an increase in total radiation and radiation balance, and in height on mountain structures, on which altitudinal zonality is clearly manifested.

The total radiation within the Caucasus ranges from 460548 J/sq. cm in the north to 586 152 J / sq. see extreme south. Annual radiation balance from 146538 to 188406 J/sq. see The amount of solar radiation depends not only on latitude, but also on cloud cover. Many peaks of the Caucasus are characterized by persistent cloudiness, so direct solar radiation here is below the average norm. To the east, it increases due to a decrease in humidity. The exceptions are Lankaran and Talysh, where the relief contributes to the condensation of water vapor and an increase in cloudiness.

The value of the total radiation and the radiation balance in different regions of the Caucasus is not the same due to the contrasts of the orography, relief, different angles of incidence of the sun's rays and the physical properties of the underlying surface. In summer, the radiation balance in some regions of the Caucasus approaches the balance of tropical latitudes, so the air temperatures are high here (Ciscaucasia and Transcaucasian plains), and in abundantly humidified areas, high evapotranspiration and, accordingly, increased air humidity are observed.

The air masses that take part in the circulation over the territory of the Caucasus are different. Basically, continental air of temperate latitudes dominates over Ciscaucasia, and subtropical air dominates in Transcaucasia. High-mountain belts are influenced by air masses coming from the west, and the northern slopes of the Greater Caucasus and the Arctic - from the north.

In Ciscaucasia, located south of the band of high barometric pressure, cold air often enters. Over the Black Sea and in the southern part of the Caspian Sea, low pressure remains. Pressure contrasts lead to the spread of cold air to the south. In such a situation, the barrier role of the Greater Caucasus is especially great, which serves as an obstacle to the wide penetration of cold air into the Transcaucasus. Usually its influence is limited to the Ciscaucasia and the northern slope of the Greater Caucasus up to about 700 m. It causes a sharp drop in temperature, an increase in pressure and an increase in wind speed.

Intrusions of cold air masses are observed from the northwest and northeast, bypassing the ridges of the Greater Caucasus along the shores of the Caspian and Black Seas. The accumulated cold air rolls over low ridges. and spreads along the western and eastern coasts to Batumi and Lenkoran, causing a drop in temperatures on the western coast of Transcaucasia to -12 ° C, on the Lankaran lowland to -15 ° C and below. A sharp drop in temperature has a disastrous effect on subtropical crops, and especially on citrus fruits. Baric gradients in these situations between Ciscaucasia and Transcaucasia are sharply contrasting, the spread of cold air from Ciscaucasia to Transcaucasia proceeds very rapidly. Cold winds of high, often catastrophic speeds are known as bora (in the Novorossiysk region) and norda (in the Baku region).

Air masses coming from the west and southwest from the Atlantic Ocean and the Mediterranean have the greatest impact on the western coast of Transcaucasia. When moving further to the east, they, overcoming the ridges located on their way, adiabatically heat up and dry up. Therefore, Eastern Transcaucasia is distinguished by a relatively stable thermal regime and low precipitation.

The mountain structures of the Lesser Caucasus and the Javakheti-Armenian Highlands contribute to the formation of a local anticyclone in winter, which causes a strong drop in temperature. In summer, low pressure sets in over the highlands.

In the second half of summer, the Caucasus experiences the influence of the spur of the Azores barometric maximum, located within the Russian Plain between 50 and 45°N. sh. It determines the decrease in summer cyclonic activity. It is associated with a decrease in precipitation in the second half of summer (compared to the first). At this time, the importance of local convective precipitation increases due to the daily variation of air temperatures.

In the Caucasus, föhns are actively manifested, which are common for mountains with a dissected relief. They are associated with hot weather in spring and summer. Mountain-valley winds and breezes are also characteristic.

On the plains of Ciscaucasia and Transcaucasia, the average July temperature is 24--25 ° C, its increase is observed to the east. The coldest month is January. In the Ciscaucasia, the average January temperature is -4, -5 ° C, in the western Transcaucasia 4-5 ° C, in the eastern 1-2 ° C. At an altitude of 2000 m, the temperature is 13 ° C in July, -7 ° C in January, in the highest zones - 1 ° C in July, and from -18 to -25 ° C in January.

The annual amount of precipitation increases with elevation and at all levels decreases noticeably from west to east (most evenly in high belts). In the Western Ciscaucasia, the amount of precipitation is 450-500 mm, in the foothills and on the Stavropol Upland at an altitude of 600-700 m - up to 900 mm. In the east of Ciscaucasia - 250-200 mm.

In the humid subtropics of Western Transcaucasia on the coastal plains, the annual precipitation reaches 2500 mm (in the Batumi region). Maximum in September. In the Sochi region, 1400 mm, of which 600 mm falls in November-February. On the western slopes of the Greater and Lesser Caucasus, the amount of precipitation increases to 2500 mm, on the slopes of the Meskheti Range up to 3000 mm, and on the Kuro-Araks lowland it decreases to 200 mm. The Lankaran lowland and the eastern slopes of the Talysh ridge are abundantly moistened, where 1500-1800 mm of precipitation falls.

The hydrographic network of the Caucasus is represented by numerous rivers and lakes, the distribution of which over the territory is associated not only with climatic conditions, but also with orography and relief.

Almost all the rivers of the Caucasus originate in the mountains, where a huge amount of moisture accumulates in the form of liquid and solid precipitation and glaciers. With the rise upward due to an increase in precipitation, a decrease in evaporation losses, the annual surface runoff increases, and the density of the river network increases. Rivers originating in the mountains, within the plains of Ciscaucasia and Transcaucasia, play a transit role.

The watershed ridge of the Greater Caucasus delimits the basins of the rivers of the Black, Azov and Caspian Seas.

The flat rivers of Ciscaucasia stand out with a slow flow and a small flood. Some of them originate on the slopes of the Stavropol Upland. Their spring floods are associated with the melting of snow. In summer they either dry up or form chains of lakes (Western and Eastern Manych).

At rivers of mixed nutrition, the upper reaches are located in the mountains, and the lower sections are within the plains. These include Kuban, Kuma, Rioni, Terek, Kuri and Arax.

Typically mountainous are the Bzyb, Kodor, Inguri and the upper sections of most of the rivers of the Caucasus. Their sources are located in the nival zone, the rivers flow in deep, often canyon-like gorges (Sulak, Terek, etc.). They are characterized by high flow rates, rapids, waterfalls.

Depending on the relief, amount and regime of precipitation, the density of the river network of the Caucasus ranges from 0.05 km / sq. km in the east of Ciscaucasia d6 1.62 km/sq. km in the mountains.

The nutrition of rivers starting in the high-mountain belt is snowy, snow-glacial (Kuban, Terek, Rioni, Kodor, etc.). In the rivers of snow-glacier feeding, the maximum discharges are observed not only in spring due to snow melting, but also in summer, as snow and glaciers melt in the upper altitudinal belts.

The rivers of the humid subtropics are predominantly rain-fed, they are characterized by a sharp fluctuation in flow. During heavy rainfall, they turn into stormy powerful streams, carrying a mass of coarse-grained material and unloading it in the lower reaches. In the absence of rain, such rivers turn almost into streams; they belong to the Mediterranean type (rivers between Tuapse and Sochi).

The sources of the rivers of the Lesser Caucasus are located in the belt of 2000-3000 m. Groundwater plays an important role in their nutrition. Snowmelt in spring contributes to a sharp increase in levels and discharges, with minimum discharges in June and July (Kura, Araks).

The turbidity of the waters depends on the nature of the eroded rocks and sediments. Many rivers of the Caucasus, especially Dagestan, are characterized by high turbidity - 5000 - 7000 g / cu. m (clays, shales, sandstones, limestones). The turbidity of the Kura and Terek is high. Rivers flowing in crystalline rocks have the least turbidity.

The hardness and salinity of river waters varies considerably. In the Kura basin, hardness reaches 10–20 mg/l, and mineralization is 2000 kg/l.

The transport value of the rivers of the Caucasus is small. Only in the lower reaches are the Kura, Rioni and Kuban navigable. Many rivers are used for timber rafting and especially widely for irrigation. Hydroelectric power stations have been built on many rivers of the Caucasus (Zangezur cascade, etc.).

There are relatively few lakes in the Caucasus - about 2000. Their area is usually small, with the exception of the mountain lake Sevan (1416 sq. km). On the plains of the Caucasus along the coasts of the Azov and Caspian Seas, lakes of the lagoon and estuary type are common. The Manych lakes are peculiar, forming a whole system. In summer, the mirror of the lakes of the Kuma-Manych depression. sharply reduced, and some dry up. There are no lakes on the lower slopes of the mountains and in the foothills, but higher in the mountains they are quite widespread.

The largest lake is Sevan. Until recently, it occupied an area of ​​1416 sq. km, its maximum depth was 99 m at an absolute height of the water table of 1916 m. The discharge of the lake water in connection with hydropower construction lowered its level by more than 18 m, due to which its depth and area decreased. This caused serious changes in the hydrological regime of the lake and was reflected in other sides. natural conditions the lake basin itself and the surrounding area. In particular, the masses of birds that nested and rested during flights on the group of daughter lakes of Sevan - Gilli disappeared. In connection with the descent of the waters of Sevan, this area turned into vast exposed peat bogs. Dozens of species of animals and birds disappeared, fish resources were catastrophically reduced, especially the resources of the most valuable Sevan trout - ishkhana.

The lake is located in a mountain basin, which is a complex synclinal trough, which in some places has experienced fault dislocations. A well-known role in the formation of the basin was played by the damming of the tectonic valley by a lava flow. A project was developed to utilize this huge reservoir as a powerful source of hydropower and water for irrigation. To increase the flow of the river flowing from the lake. Hrazdan began to drain the upper layer of lake waters, which then passed through 6 hydroelectric stations of the Sevan-Hrazdan cascade. The surface runoff in the upper reaches of the Hrazdan stopped - the Sevan water went through the tunnel to the turbines of the Sevan HPP.

According to the new project for the use of Sevan waters, further lowering of their level is suspended. It will remain at around 1898 m, and the picturesque reservoir will remain within the boundaries close to natural. Through a 48-kilometer tunnel in the Vardenis Range, water is supplied to Sevan from the upper reaches of the river. Arpy. A recreation area with a national park is being created on the shores of the lake, and a strip of land released from the waters of the lake is being afforested. The main problem lake and its basin is currently the preservation and restoration of largely unique natural conditions and endemic species of flora and fauna, in particular the named Sevan trout, which is also of great commercial importance. In the future, measures should be taken to raise the level of the lake by 4–5 m.

The basins of mountain lakes are tectonic, karst, volcanic, and cirque. Some occupy depressions in the moraine relief. Volcanic lakes are predominantly dammed, common on the Karabakh plateau and the Armenian Highlands. There are many karst lakes in Western Georgia. Glacial lakes are well preserved in the Teberda basin - Baduksky, Murudzhinsky, Klukhorskoye (on the pass of the same name). There are lakes in the floodplains of the plains of the Caucasus. The dammed lake Ritsa is peculiar and very beautiful. The lakes of Colchis were formed during the formation of the lowland itself, the largest of them is Lake Paleostomi.

Caucasus. They are significant in terms of reserves and diverse in terms of chemical composition and degree of mineralization. Their formation is associated with geotectonic structures and infiltration of atmospheric precipitation. Fissure and formation-fissure waters are common in folded geostructures. The movement of water occurs along the cracks of tectonic faults, faults and overthrusts, along the strike of folds into river valleys.

The mineral composition of groundwater is determined by the composition of rocks. Crystalline rocks are sparingly soluble, so the groundwater circulating in them is relatively little mineralized. Groundwater in sedimentary deposits is often saturated with readily soluble compounds and highly mineralized. The underground waters of the Caucasus are predominantly cold - up to 20°C. There are subthermal - above 20 and hot - above 42 ° C (the latter are not uncommon within the Greater and Lesser Caucasus).

The chemical composition of the underground waters of the Caucasus is very diverse. Carbonic mineral springs are especially characteristic; There are also chloride waters, hydrogen sulfide waters (Matsesta, Chkhalta), thermal radon waters up to 35°C (Tskhaltubo springs). The mineral waters of the Caucasus are used by numerous resorts.

The climate, orography and relief determine the modern glaciation of the Caucasus. total area its glaciers are about 1965 sq. km. (about 1.5% of the entire territory of the Caucasus). The Greater Caucasus is the only one of the mountainous regions of the Caucasus with a wide development of modern glaciation. The number of glaciers is 2047, the area of ​​glaciation is 1424 sq. km. About 70% of the number of glaciers and the area of ​​glaciation falls on the northern slope and about 30% on the southern slope. The difference is explained by orographic features, blizzard transport of snow by western winds beyond the barrier of the Dividing Range, increased insolation on the southern slope. The most glaciated is the Central Caucasus, where 5 glaciers (Dykhsu, Bezengi, Karaugom on the northern slope, Lekhzir and Tsanner on the southern) have an area of ​​​​approximately 40 square kilometers. km. Their length is more than 12 km. The modern snow boundary of the Greater Caucasus in the southwest lies at an altitude of 2800-3200 m, in the east it rises to 3600 m. The area of ​​glaciers in Transcaucasia is small - a little over 5 sq. km. km (Zanzegur Ridge, Aragats peak). The glaciers of the Caucasus play big role in the nutrition of the rivers of the Caucasus, causing their full flow and the nature of the alpine-type water regime.

Together they bring this product to the consumer. The most picturesque product they sell is the vacation travel agents who sell dreams. Based on world practice, as well as articles 128-134 of the Civil Code of the Russian Federation, a tourist product is not only a set of services, and even less the right to it, but a more complex and yet unfamiliar product for us, consisting of a complex of “things, rights , works and services, information, intellectual property and intangible benefits”. “A tourist product is a set of material (consumables), intangible (in the form of a service) use values ​​necessary to meet the needs of a tourist that arose during his trip.”

The Caucasus is one of the southern regions of Russia. Its extreme points lie within 50.5 ° N. sh. (northern extremity of the Rostov region) and from the village. sh. (on the border of Dagestan). The territory of the North Caucasus receives a lot of solar radiation - approximately one and a half times more than, for example, the Moscow region. Its annual amount for the plains and foothill regions is 120-140 large calories (kilocalories) per square centimeter of surface.

In different seasons of the year, the radiation flux is different. In summer, each square centimeter of the surface receives 17-18 kcal per month. At this time, the heat balance is positive. In winter, the flow of sunlight is sharply reduced - up to 3-b kcal per 1 sq. km. cm per month and a lot of heat reflects the snowy earth's surface. Therefore, the radiation balance becomes negative for some time in the middle of winter.

In the North Caucasus, everywhere, with the exception of the highlands, there is a lot of heat. On the plains, the average temperatures in July everywhere exceed 20°, and summer lasts from 4.5 to 5.5 months. Average January temperatures fluctuate in different regions from -10° to +6°, and winter lasts only two or three months. The rest of the year is occupied by transitional seasons - spring and autumn.

Due to the abundance of heat and light, vegetation in the Caucasus has the opportunity to develop in the northern parts of the region for seven months, in Ciscaucasia - eight months, and on the Black Sea coast, south of Gelendzhik - up to 11 months. This means that with an appropriate selection of field and garden crops, one can get one and a half crops a year * in the north of the region, and even two crops in the entire Ciscaucasia.

The movement of air masses and their transformation in the territory of the North Caucasus are exceptionally complex and diverse. The area is located on the border of temperate and subtropical latitudes, not far from the warm mediterranean sea. As far north as the Arctic Ocean, there are no significant orographic obstacles. In the south, on the contrary, high chains of mountains rise. Therefore, in all seasons of the year, North Caucasus various masses of air can penetrate: either the cold dry air of the Arctic, then the moisture-saturated masses formed over the Atlantic Ocean, then the humid tropical air of the Mediterranean, and finally, although very rarely, also tropical, but dry and heavily dusty air from the desert highlands of Western Asia and the Middle East. Replacing each other, various air masses create great diversity and diversity. weather conditions that distinguishes the North Caucasus. But the main amount of precipitation is associated with westerly winds that carry moisture from the Atlantic. Their moisture is intercepted by the slopes of mountains and hills facing to the west, while to the east the dryness and continentality of the climate increases, which affects the entire landscape.

The nature of the circulation of air masses in different seasons of the year has noticeable differences. And, of course, the conditions of the plains and mountains are sharply different.

On the plains in winter, the cold dense air of Siberia and Kazakhstan (the Siberian, or Asian, anticyclone) collides with each other and the relatively warm rarefied air that sets over the Black Sea (the Black Sea depression). Under the influence of the Siberian anticyclone, streams of dry, strongly cooled air are constantly directed towards Ciscaucasia. Due to the significant difference in pressure, the air flows quickly, forming strong, often stormy easterly and northeasterly winds. These winds dominate throughout the winter in the Caspian region and in the eastern parts of Ciscaucasia. Due to the dryness of the air they bring, there is almost no precipitation here, and the thickness of the snow cover is small - 5-10 cm, in some places there is no snow at all.

Further to the west, the air of the Siberian anticyclone rarely penetrates. The entire Western Ciscaucasia is under the influence of the Black Sea depression: cyclones come from there, bringing sharp warming and a lot of precipitation. The snow cover in the west is 2-3 times thicker than in the east, the winter is unstable: frequent thaws sometimes last for a week or more, with temperatures rising to 6-12° in the north and up to 20° in the south of the region.

The Stavropol Upland is a kind of climatic boundary between the Eastern and Western Ciscaucasia. Here there are very heterogeneous in their physical properties air masses. In this case, the winds usually increase sharply; variable wind regime - main feature winters in Stavropol.

Arctic air usually comes to the North Caucasus from the northwest. In the Lower Don and Ciscaucasia, this cold air, as a rule, is delayed for a long time by the dense air of the Siberian anticyclone and mountain ranges. Then, it would seem that low temperatures are not at all characteristic of these southern places. Thus, in Pyatigorsk and Maykop, the absolute minimums, that is, the lowest of the observed temperatures, are -30°, and in Krasnodar even -33°. The average lows are also quite severe: -16°, -20°.

The cold Arctic air, as if clinging to the ground, usually does not rise high and does not cross the mountain ranges that protect the Transcaucasus from destructive northern cold. But cold intrusions can bypass Caucasian mountains along their eastern outskirts along the Caspian coast, reaching Baku and its environs, often having a detrimental effect on the coastal regions of Dagestan along the way.

In the west, on a small section of the coast from Novorossiysk to Gelendzhik, where the mountain range is low, cold and dense air accumulating in the foothills sometimes rises to the saddle of the Markotkhsky pass. Then a bora falls on the city of Novorossiysk and the Tsemess Bay, in the local north-east - a wind of hurricane strength and speed, moreover, extremely cold. It often brings serious destruction to the urban economy and causes severe storms in the coastal parts of the sea.

In spring, air masses heated from the earth's surface rush upwards and the pressure weakens. Then conditions are created for the active invasion of warm Mediterranean air. Under its influence, the unstable snow cover melts together, the average daily temperatures rise rapidly, and already in early May, summer conditions are established throughout the entire territory of the North Caucasus, except for the highlands.

In summer, the incoming air is actively transformed under the influence of a strongly heated earth's surface, and its own air, close to the tropical type, is formed on the territory of the region. On the plains everywhere, often for many weeks, an anticyclone sets in with its characteristic weather features: hot days prevail, with weak winds, low clouds and strong warming of the surface layers of air, almost without rain.

Only from time to time anticyclonic conditions are replaced by periods of passage of cyclones. They usually invade from the Atlantic through Western Europe, Belarus and Ukraine, and much less frequently from the Black Sea. Cyclones bring cloudy weather: heavy rains fall on their leading fronts, often accompanied by thunderstorms. Occasionally, long drizzling rains fall in the rear of passing cyclones.

Cyclones almost always come from the west or northwest, and as they move east and southeast, the air masses they bring lose their moisture reserves. Therefore, not only in winter, but also in summer, the western plain Ciscaucasia is more abundantly moistened than the eastern one. In the west, the annual precipitation is 380-520 mm, while in the Caspian region it is only 220-250 mm. True, in the foothills and on the Stavropol Upland, precipitation increases to 600-650 mm, but on the plains east of the upland, it is not enough to make full use of the abundance of solar heat in agriculture and horticulture. The situation is further complicated by the extreme unevenness of precipitation over time.

In fact, the entire territory of the Lower Don and the plain Ciscaucasia is not guaranteed against the possibility of droughts with their constant companions - dry winds - a cruel, inexorable enemy of field and horticultural plants. However, not all areas are equally prone to these formidable natural phenomena. So, for the period from 1883 to 1946, that is, for 64 years, droughts occurred 21 times in the Caspian region, 15 times in the Rostov region, and only 5 times in the Kuban.

During droughts and dry winds, especially in the east, dusty or black storms often occur. They occur when the upper layers of dry soil, still loosely held together by newly emerged plants, are blown away by strong winds. A cloud of dust rises into the air, covering the sky with a thick veil. Sometimes the dusty cloud is so dense that the sun barely shines through it and appears as a hazy, blood-red disk.

Measures of protection against black storms are known. The main ones are properly planned forest shelterbelts and high agricultural technology. Much has already been done in this direction. However, until now, in the fields of the Ciscaucasia, it is often necessary to re-sow (re-sow) several tens of thousands of hectares, from which the most fertile soil layer is demolished during dust storms.

In autumn, the influx of solar heat weakens. Initially, the features of the summer circulation are still preserved. Anticyclonic weather prevails with a weak movement of air masses. Subsequently, the earth's surface begins to noticeably cool, and from it the lower layers of air. In the mornings, thick milky-white fogs spread over the ground that has cooled overnight. The already strongly cooled air of the Siberian anticyclone comes more and more often, and in November a winter type of circulation is established over the entire territory of the North Caucasus.

The climate of the mountainous territories of the North Caucasus (from 800-900 m and above) is very different from the adjacent plains, although it repeats some of the most common features.

One of the main differences is that the mountain slopes, delaying the flow of air masses, make them rise up. At the same time, the temperature of the air mass decreases rapidly, and moisture saturation increases, which leads to precipitation. Therefore, the mountain slopes are much better moistened: in the mountains of the Western Caucasus at altitudes above 2000 m, 2500-2600 mm falls annually; to the east their number decreases to 900-1000 mm. The lower zone of the mountains - from 1000 to 2000 m - receives less precipitation, but still enough for the growth of lush forest vegetation.

Another difference is due to the decrease in temperature with increasing altitude: for every 100 m you rise, it drops by about 0.5-0.6°. In this regard, a belt distribution of climate is clearly manifested on the mountain slopes, and already at an altitude of 2700 m on the northern slopes of the mountains of the Western Caucasus, 3700-3800 m in the Central and 3500 m in the Eastern, there is a snow line, or the border of "eternal" snow. Above it, the warm season with positive temperatures lasts no more than 2.5-3 months, and at altitudes above 4000 m, even in July, positive temperatures are observed very rarely.

Due to the abundance of precipitation in the mountains of the Western Caucasus during the winter, 4–5 and snow accumulates, and in the mountain valleys, where it is blown away by the wind, up to 10–12 m. even a sharp sound, so that a thousand-ton mass of accumulated snow, breaking off a steep ledge, flew down with a terrible roar, destroying everything in its path. In the mountains of the Eastern Caucasus, due to the general dryness, the snow cover is much less.

The third difference between the mountain climate is that the chilled air of the highlands often, as it were, rushes down the comparatively narrow intermountain valleys. For every 100 m lowered, the air heats up by about 1°. Falling from a height of 2500 m, when it reaches the lower parts of the mountains and foothills, it heats up by 25 °, that is, instead of cold, it will become warm and even hot. Such winds are called foehns. They blow at all times of the year, but especially often in the spring, when the intensity of the general circulation of air masses increases sharply.

Finally, another important distinguishing feature of the climate of the mountains is its amazing diversity from place to place, which is due to the rugged relief with numerous bends of the slopes, differently oriented with respect to the illumination of the sun and the directions of the prevailing winds. On the plains, differences in the orientation of the slopes are less pronounced due to their low steepness.

For all the importance of each of the noted features of the climate of the mountains, the height, which determines the vertical division into climatic zones, is still of leading importance.

1) What features of the nature of mountains do you know from the 7th grade geography course.

For mountains, the characteristic altitudinal zonality in change natural areas. In mountains, pressure and temperature decrease with height.

Questions in a paragraph

* Remember how much the air temperature drops when you rise for every 100 m. Calculate how much the air will cool when you rise to a height of 4000 m, if its temperature at the earth's surface is + 200C. What happens to the moisture in the air.

For every 100 m you rise, the air temperature drops by 0.60C. The temperature at an altitude of 4000 m will be -40C. The moisture in the air will begin to condense.

*Explain why there are no avalanches in the mountains of the Eastern Caucasus.

Due to the dryness of the climate, there is very little snow.

*Think about what differences will be observed in the change of altitudinal zones on the western and eastern slopes.

There are altitudinal belts of the Caucasus related to two types of vertical zonality: continental and coastal (coastal). The second one is represented in the mountains of the Western Caucasus, which are influenced by the Atlantic and humid sea air. In the east, somewhat different altitudinal belts of the Caucasus are observed, which are often called the continental, or Dagestan type of vertical zonality.

Questions at the end of the paragraph

1. Name the main features of the nature of the highlands and explain their reasons.

A large amount of precipitation, a short warm season, the dependence of natural conditions on the height of mountains and the exposure of slopes, the spread of glacial landforms, altitudinal zonality.

2. Give a description of the climate of the Greater Caucasus, explain how the climate of the foothills differs from the highlands.

With the exception of the highlands, the climate in the North Caucasus is mild and warm; on the plains, the average temperature in July exceeds 20 ° C everywhere, and summer lasts from 4.5 to 5.5 months. Average January temperatures range from -10 to +6°C, and winter lasts only two to three months. The city of Sochi is located in the North Caucasus, where the warmest winter in Russia is with a January temperature of +6.1 ° С. The climate of the highlands is very different from the plains and foothills. The first main difference is that much more precipitation falls in the mountains: at an altitude of 2000 m - 2500-2600 mm per year. The second difference in the climate of the highlands is a decrease in the duration of the warm season due to a decrease in air temperature with height. The third difference of the alpine climate is its amazing diversity from place to place in connection with the height of the mountains, the exposure of the slope, proximity or distance from the sea. The fourth difference is the peculiarity of atmospheric circulation.

3. Using Figure 102, explain the features of the altitudinal zonation of the Greater Caucasus.

There are altitudinal belts of the Caucasus related to two types of vertical zonality: continental and coastal (coastal). The second one is represented in the mountains of the Western Caucasus, which are influenced by the Atlantic and humid sea air. We list the main altitudinal belts from the foothills to the peaks:

1. Meadow steppes, interrupted by curtains of oak, hornbeam, ash (up to 100 m).

2. Forest belt.

3. Subalpine crooked forests and tall grass meadows (at an altitude of 2000 m).

4. Low-grass alpine meadows, rich in bluebells, cereals and umbrella plants.

5. Nival zone (at an altitude of 2800–3200 m).

The climate of the Caucasus is very diverse, which is primarily due to the influence of the relief.

The Caucasus is located on the border of the temperate and subtropical climatic zones. The differences between them are intensified by the mountains of the Greater Caucasus, which hinder the transfer of cold air masses from the north to Transcaucasia and warm ones from the south to Ciscaucasia. The North Caucasus belongs to temperate zone, Transcaucasia - to subtropical. The differences between them are especially noticeable in air temperature.In the North Caucasus, everywhere, with the exception of the highlands, there is a lot of heat. On the plains, the average temperatures in July everywhere exceed 20°, and summer lasts from 4.5 to 5.5 months. The average January temperatures fluctuate in different areas from -10° to +6°, and winter lasts only two to three months. The rest of the year is occupied by transitional seasons - spring and autumn.


In the Greater Caucasus, starting from a height of about 2000 m, and in the Transcaucasian Highlands, the role belongs to the western air transport, in connection with which the influence of the Atlantic and the Mediterranean Sea increases. Therefore, the climate is more humid in the highlands.

Complex mountainous relief creates in the Caucasus big variety local climates, and previously outlined large geomorphological units differ in climatic terms.

The diversity of the climate of the Caucasus determines the differences in the agricultural use of its territory. The economic importance of the Transcaucasian subtropical regions, protected by the Greater Caucasus mountain barrier, is especially great, where a whole range of subtropical climates is observed, ranging from humid, which allows the cultivation of tea and citrus fruits, to dry, suitable for growing cotton and other crops that require an abundance of sunlight.

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