The climate of the Caucasus is influenced by many factors. The most important of them are latitudinal zoning and vertical zonation. However, the actions of these main factors are largely corrected by the features of the geographical position and topography.
In addition, the climate of different parts of the Caucasus is greatly influenced by the proximity of the Black and Azov Seas in the west and the Caspian Sea in the east. All these factors have created a variety of climatic and forest growing conditions in the Caucasus.
High mountain ranges in the Caucasus influence the promotion and distribution of baric phenomena. So, the main Caucasian ridge protects the territory of Transcaucasia from the invasion of cold air masses approaching from the north. These air masses flow around the ridge and enter Transcaucasia from the west and east, becoming wet due to contact with the Black and Caspian Seas and warming somewhat under the influence of the warm land surface.
Mountains that cut across the territory of Transcaucasia in different directions, and solar radiation continue to modify the climate of the Caucasus, affecting the direction and speed of movement of air masses, their rise, etc.
All this creates the complexity and diversity of climate elements - air and soil temperature, amount, intensity and distribution of precipitation, relative air humidity, wind direction and speed, etc.
The intensity of solar radiation increases with increasing altitude. However, the main role belongs not to the sum of heat and solar radiation, but to the temperature of air and soil. Due to the intensity of solar radiation in the mountains, large fluctuations in air temperatures are observed during the day.
The soil is very warm on sunny days, especially on the slopes of the southern exposure. As a result, the temperature of the soil changes less with increasing height than the temperature of the air, and the difference between the temperatures of the air and the soil becomes very insignificant. At night, the surface soil layer on the slopes noticeably cools, but in deeper layers its temperature exceeds air temperature.
According to the degree of moisture in the Caucasus, the following are distinguished: humid subtropical regions of the Black Sea coast of the Krasnodar Territory, Western Georgia and Southeast Azerbaijan; humid areas of the North and West Caucasus; dry regions of Eastern Georgia, Western Azerbaijan, Armenia, Dagestan.
The climate of the Caucasus can be traced with each increase in altitude, according to scientists, for every 100 meters of rise the amount of precipitation increases by 20%, in the Crimea by 14-15%.
Rainfall and rainy days are greatly influenced by local geographic factors. Thus, under the influence of the Black Sea, in the adjacent regions of Western Georgia and the Krasnodar Territory, the average annual rainfall exceeds 1000 mm, reaching 3000 mm in the coastal zone of Adjara. In dry mountainous areas, the average annual rainfall is 300-350 mm, decreasing to 100 mm in some years.
Summer is hot except for the highlands. So, the average temperature on the plain in the summer is about 25 ° C, and in the upper reaches of the mountains - 0 ° C.
The abundance of heat and light ensures the development of vegetation in the steppe zone for seven months, foothills - eight, and on the Black Sea coast - up to eleven. (T not lower than +10).
Winters in the Ciscaucasia are quite warm (the average temperature in January is -5єС). Warm from the Atlantic Ocean contribute to this. air masses. On the Black Sea coast, the temperature rarely drops below zero (the average January temperature is + 3 ° C). In mountainous areas, the temperature is naturally below -4 - 8 ° C.
Precipitation.
The decisive influence on the distribution of precipitation is exerted by dry Central Asian winds, penetrating through the Caspian Sea, and wet Black Sea.
Precipitation this territory comes mainly from coming from the west cyclonesas a result of which their number to the east is gradually decreasing. Most precipitation falls on the southwestern slopes of the Greater Caucasus. (2600mm) (most of all in our country) To the east, rainfall drops to 600 mm per year.
Their number on the Prikubanskaya Plain is approximately 400 mm. The Stavropol Plateau serves not only as a watershed, but also as a barrier restricting the influence of the Black Sea winds in the east of the region. Therefore, the southwestern regions of the North Caucasus are quite humid (1410 mm of precipitation falls annually in Sochi), and the eastern ones are arid (Kizlyar - 340 mm).
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 climate formation of various parts of the Caucasus.
The Caucasus is a prime example of the influence of orography and topography on climate-forming processes. Radiant energy is distributed unevenly due to different angles of incidence and different heights of surface levels. The circulation of air masses reaching the Caucasus undergoes significant changes, encountering mountain ranges of both the Greater Caucasus and Transcaucasia on their way. Climatic contrasts occur at relatively short distances. An example is the western, abundantly moistened Transcaucasia and the eastern one with a dry subtropical climate of the Kuro-Araksin lowland. The exposure of the slopes is very significant, which strongly affects the thermal regime and the distribution of precipitation. The climate is affected by the seas washing the Isthmus of the Caucasus, especially the Black Sea.
The Black and Caspian Seas moderate air temperature in summer, contribute to a more even diurnal course, moisturize parts of the Caucasus adjacent to them, increase the temperature of the cold season, and reduce temperature amplitudes. The plains eastern Ciscaucasia and the Kuro-Araksin lowland, deeply extending into the isthmus, do not contribute to the condensation of moisture coming from the Caspian Sea. The Ciscaucasia is heavily influenced by continental air masses coming from the north, including the Arctic, which often significantly reduce the temperature of the warm season. A spur of high East Siberian barometric pressure often lowers the temperature of the cold season. There are times when cold air flowing from the east and west of the Greater Caucasus spreads to the Transcaucasus, causing a sharp drop in temperature there.
The air masses coming from the Atlantic Ocean and the Mediterranean provide high humidity of 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 apparent.
In general terms, the climate of the Caucasus changes significantly in three directions: from west to east in the direction of increasing dryness and continentality, from north to south in the direction of increasing total radiation and radiation balance, and in height in mountain structures where altitudinal zonation is clearly manifested.
The total radiation within the Caucasus ranges from 460,548 J / sq. cm in the north to 586 152 J / sq. see in the extreme south. The annual radiation balance is from 146538 to 188406 J / sq. see. The magnitude of solar radiation depends not only on latitude, but also on cloud cover. Many peaks of the Caucasus are characterized by stable cloud cover; therefore, direct solar radiation is below 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 increased cloud cover.
The magnitude of the total radiation and radiation balance in different regions of the Caucasus is not the same due to contrasts in orography, topography, different angles of incidence of sunlight and the physical properties of the underlying surface. In summer, the radiation balance in some areas of the Caucasus approaches the balance of tropical latitudes, therefore, air temperatures are high (Ciscaucasia and Transcaucasian plains), and in highly humid areas there is a high evaporation rate and, accordingly, increased air humidity.
The air masses participating in the circulation over the territory of the Caucasus are different. Basically, the continental air of temperate latitudes dominates over the Ciscaucasia, while in the Caucasus it is subtropical. Alpine zones are influenced by air masses coming from the west, and the northern slopes of the Greater Caucasus and Arctic ones from the north.
In the Ciscaucasia, located south of the high barometric pressure band, cold air often arrives. Over the Black Sea and in the southern part of the Caspian Sea, reduced pressure remains. Pressure contrasts lead to the spread of cold air to the south. In this 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 Caucasus. Usually its influence is limited to the Ciscaucasia and the northern slope of the Greater Caucasus to approximately 700 m. It causes a sharp decrease in temperature, an increase in pressure, and an increase in wind speed.
There are incursions of cold air masses 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 passes through the low ridges. and spreads along the western and eastern coasts to Batumi and Lankaran, causing a decrease 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 disastrously affects subtropical crops and especially citrus fruits. Baric gradients in these situations between Ciscaucasia and Transcaucasia are sharply contrasted, the distribution 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 “north” (in the Baku region).
Air masses coming from the west and southwest from the Atlantic Ocean and the Mediterranean have the greatest influence on the western coast of Transcaucasia. When moving further east, they, overcoming the ridges located on their way, adiabatically heat up and dry out. Therefore, Eastern Transcaucasia is characterized by a relatively stable thermal regime and insignificant amount of 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 decrease in temperature. In summer, low pressure is set above the highlands.
In the second half of summer, the Caucasus is influenced by the spur of the Azores barometric maximum, located within the Russian Plain between 50 and 45 ° C. w. It determines the decrease in summer cyclonic activity. It is associated with a decrease in precipitation in the second half of summer (compared with the first). At this time, the value of local convective precipitation due to the daily course of air temperatures increases.
In the Caucasus, hairdryers, which are usual for mountains with dissected relief, are actively manifesting themselves. 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 ° С, 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 Transcaucasus 4-5 °, in the eastern 1-2 ° C. At an altitude of 2000 m, the temperature in July is 13 °, in January -7 ° C, in the highest zones - in July 1 °, in January from -18 to -25 ° C.
The annual precipitation increases with rising upward 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 the 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 region of Sochi, 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 Meskhetian ridge to 3000 mm, on the Kuro-Araksin lowland, it decreases to 200 mm. The Lankaran Lowland and the eastern slopes of the Talysh Range, where 1,500-1800 mm of rainfall, are abundantly moistened.
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 climate formation of various parts of the Caucasus.
The Caucasus is a prime example of the influence of orography and topography on climate-forming processes. Radiant energy is distributed unevenly due to different angles of incidence and different heights of surface levels. The circulation of air masses reaching the Caucasus undergoes significant changes, encountering mountain ranges of both the Greater Caucasus and Transcaucasia on their way. Climatic contrasts occur at relatively short distances. An example is the western, abundantly moistened Transcaucasia and the eastern one with a dry subtropical climate of the Kuro-Araksin lowland. The exposure of the slopes is very significant, which strongly affects the thermal regime and the distribution of precipitation. The climate is affected by the seas washing the Isthmus of the Caucasus, especially the Black Sea.
The Black and Caspian Seas moderate air temperature in summer, contribute to a more even diurnal course, moisturize parts of the Caucasus adjacent to them, increase the temperature of the cold season, and reduce temperature amplitudes. The plains eastern Ciscaucasia and the Kuro-Araksin lowland, deeply extending into the isthmus, do not contribute to the condensation of moisture coming from the Caspian Sea. The Ciscaucasia is heavily influenced by continental air masses coming from the north, including the Arctic, which often significantly reduce the temperature of the warm season. A spur of high East Siberian barometric pressure often lowers the temperature of the cold season. There are times when cold air flowing from the east and west of the Greater Caucasus spreads to the Transcaucasus, causing a sharp drop in temperature there.
The air masses coming from the Atlantic Ocean and the Mediterranean provide high humidity of 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 apparent.
In general terms, the climate of the Caucasus changes significantly in three directions: from west to east in the direction of increasing dryness and continentality, from north to south in the direction of increasing total radiation and radiation balance, and in height in mountain structures where altitudinal zonation is clearly manifested.
The total radiation within the Caucasus ranges from 460,548 J / sq. cm in the north to 586 152 J / sq. see in the extreme south. The annual radiation balance is from 146538 to 188406 J / sq. see. The magnitude of solar radiation depends not only on latitude, but also on cloud cover. Many peaks of the Caucasus are characterized by stable cloud cover; therefore, direct solar radiation is below 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 increased cloud cover.
The magnitude of the total radiation and radiation balance in different regions of the Caucasus is not the same due to contrasts in orography, topography, different angles of incidence of sunlight and the physical properties of the underlying surface. In summer, the radiation balance in some areas of the Caucasus approaches the balance of tropical latitudes, therefore, air temperatures are high (Ciscaucasia and Transcaucasian plains), and in highly humid areas there is a high evaporation rate and, accordingly, increased air humidity.
The air masses participating in the circulation over the territory of the Caucasus are different. Basically, the continental air of temperate latitudes dominates over the Ciscaucasia, while in the Caucasus it is subtropical. Alpine zones are influenced by air masses coming from the west, and the northern slopes of the Greater Caucasus and Arctic ones from the north.
In the Ciscaucasia, located south of the high barometric pressure band, cold air often arrives. Over the Black Sea and in the southern part of the Caspian Sea, reduced pressure remains. Pressure contrasts lead to the spread of cold air to the south. In this 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 Caucasus. Usually its influence is limited to the Ciscaucasia and the northern slope of the Greater Caucasus to approximately 700 m. It causes a sharp decrease in temperature, an increase in pressure, and an increase in wind speed.
There are incursions of cold air masses 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 passes through the low ridges. and spreads along the western and eastern coasts to Batumi and Lankaran, causing a decrease 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 disastrously affects subtropical crops and especially citrus fruits. Baric gradients in these situations between Ciscaucasia and Transcaucasia are sharply contrasted, the distribution 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 “north” (in the Baku region).
Air masses coming from the west and southwest from the Atlantic Ocean and the Mediterranean have the greatest influence on the western coast of Transcaucasia. When moving further east, they, overcoming the ridges located on their way, adiabatically heat up and dry out. Therefore, Eastern Transcaucasia is characterized by a relatively stable thermal regime and insignificant amount of 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 decrease in temperature. In summer, low pressure is set above the highlands.
In the second half of summer, the Caucasus is influenced by the spur of the Azores barometric maximum, located within the Russian Plain between 50 and 45 ° C. w. It determines the decrease in summer cyclonic activity. It is associated with a decrease in precipitation in the second half of summer (compared with the first). At this time, the value of local convective precipitation due to the daily course of air temperatures increases.
In the Caucasus, hairdryers, which are usual for mountains with dissected relief, are actively manifesting themselves. 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 ° С, 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 Transcaucasus 4-5 °, in the eastern 1-2 ° C. At an altitude of 2000 m, the temperature in July is 13 °, in January -7 ° C, in the highest zones - in July 1 °, in January from -18 to -25 ° C.
The annual precipitation increases with rising upward 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 the 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 region of Sochi, 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 Meskhetian ridge to 3000 mm, on the Kuro-Araksin lowland, it decreases to 200 mm. The Lankaran Lowland and the eastern slopes of the Talysh Range, where 1,500-1800 mm of rainfall, are abundantly moistened.
The hydrographic network of the Caucasus is represented by numerous rivers and lakes, the distribution of which over the territory is connected 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 a rise upwards due to an increase in precipitation, a decrease in evaporation loss, the annual surface runoff increases, and the density of the river network increases. Rivers originating in the mountains, within the plains of the Ciscaucasia and Transcaucasia, play a transit role.
The dividing ridge of the Greater Caucasus delimits the river basins of the Black, Azov and Caspian Seas.
Plain rivers of the Ciscaucasia with a slow course and a small flood stand out. Some of them originate on the slopes of the Stavropol Upland. Their spring floods are associated with melting snow. In summer, they either dry out 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 located within the plains. These include the Kuban, Kuma, Rioni, Those Rivers, Kuri and Araks.
Typically mountainous are Bzyb, Kodor, Inguri and the upper sections of most rivers of the Caucasus. Their sources are located in the nival belt, rivers flow in deep, often canyon-shaped gorges (Sulak, Terek, etc.). They are characterized by high flow rates, rapids, waterfalls.
Depending on the topography, amount and mode 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 food of the rivers starting in the alpine zone is snowy, snow-glacial (Kuban, Terek, Rioni, Kodor, etc.). In rivers of snow-ice nutrition, maximum costs are observed not only in spring due to melting snow, but also in summer as snow and glaciers melt in the upper altitude zones.
The rivers of humid subtropics have mainly rain nutrition, they are characterized by sharp fluctuations in flow. During rainfall, they turn into violent powerful streams that carry a mass of coarse material and discharge 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 in the belt of 2,000--3,000 m. Groundwater plays a great role in their nutrition. Melting snow in the spring contributes to a sharp increase in levels and costs, minimum spending in June and July (Kura, Araks).
Turbidity of waters depends on the nature of eroded rocks and sediments. Many rivers of the Caucasus, especially Dagestan, are characterized by high turbidity of -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 mineralization of river waters varies significantly. In the Kura basin, hardness reaches 10--20 mg / l, and mineralization is 2000 kg / l.
The transport significance of the rivers of the Caucasus is small. Only in the lower reaches are navigable Kura, Rioni and Kuban. Many rivers are used for rafting and especially widely for irrigation. Hydroelectric power stations (Zangezur cascade, etc.) were built on many rivers of the Caucasus.
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, lagoon and estuary-type lakes are common. Manych lakes are peculiar, forming a whole system. In summer, the mirror of the lakes of the Kumo-Manych depression. sharply reduced, and some dry up. On the lower slopes of the mountains and in the foothills of the lake are absent, but higher in the mountains they are quite widespread.
The largest lake is Sevan. until recently, it occupied an area of \u200b\u200b1416 square meters. km, its maximum depth was 99 m with an absolute height of the water mirror of 1916 m. The descent 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 on other sides of the natural conditions of the lake basin itself and the adjacent territory. In particular, the masses of feathered, nesting and resting during the flights on the group of subsidiary lakes of Sevan - Gilly disappeared. In connection with the descent of the water of Sevan, this area turned into extensive naked peatlands. Dozens of species of animals and birds disappeared, fish wealth catastrophically decreased, especially the resources of the most valuable Sevan trout - ishkhan.
The lake is located in a mountain basin, which is a complex synclinal deflection, which in some places experienced fault dislocations. A well-known role in the formation of the basin was played by the loading of the tectonic valley with a lava flow. A project was developed to utilize this huge reservoir as a powerful source of hydropower and irrigation water. To increase runoff flowing from the lake p. The upper layer of lake waters, which then passed through 6 hydroelectric stations of the Sevan-Hrazdan cascade, began to be distributed Hrazdan. The surface runoff in the upper Hrazdan stopped - Sevan water went through the tunnel into the turbines of Sevan Hydroelectric Power Station.
Under the new project for the use of Sevan waters, further lowering of their level is suspended. It will remain at the level of 1898 m, and the picturesque reservoir will remain within the boundaries close to natural. Through the 48-kilometer tunnel in the Vardenis ridge in Sevan water is supplied from the upper river. Arps. A recreation area with a national park is being created on the shores of the lake; afforestation of the land strip freed from under the waters of the lake is underway. The main problem of the lake and its basin at present is 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 increase the lake level by 4-5 m.
The hollows of mountain lakes are tectonic, karst, volcanic, and kar. Some occupy lowering moraine topography. Volcanic lakes are mainly dammed, distributed 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, Muruzhinsky, Klukhorsky (on the pass of the same name). There are lakes in the floodplains of the plains of the Caucasus. Peculiar and very beautiful dammed lake Ritsa. Colchis lakes were formed in the process of the formation of the lowland itself, the largest of them is Lake Paleostomi.
Of the Caucasus. They are significant in stocks and diverse in chemical composition and degree of mineralization. Their formation is associated with geotectonic structures and atmospheric precipitation infiltration. Fractured and formation-fissured waters are common in folded geostructures. The movement of water occurs along the cracks of tectonic faults, faults and thrusts, along the stretching of folds into river valleys.
The mineral composition of groundwater is determined by the composition of the rocks. Crystalline rocks are difficult to dissolve; therefore, the groundwater circulating in them is relatively poorly mineralized. Groundwater occurring in sedimentary deposits is often saturated with readily soluble compounds and highly mineralized. The underground waters of the Caucasus are mostly 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 soda-type Borjomi, salt-alkaline-type Essentuki, sulfate-hydrocarbonate-type Kislovodsk narzan (in the Ardon, Chkhalta basin, etc.). There are also chloride waters, hydrogen sulfide (Matsesta, Chkhalta), thermal radon up to 35 ° C (sources of Tskhaltubo). Mineral waters of the Caucasus are used by numerous resorts.
Climate, orography and relief determine the modern glaciation of the Caucasus. The total area of \u200b\u200bits glaciers is about 1965 square meters. km (about 1.5% of the entire territory of the Caucasus). The Greater Caucasus is the only mountain region of the Caucasus with the widespread development of modern glaciation. The number of glaciers is 2047, the area of \u200b\u200bglaciation is 1424 square meters. km About 70% of the number of glaciers and the area of \u200b\u200bglaciation falls on the northern slope and about 30% on the southern. The difference is explained by orographic features, snowstorm snow transfer by westerly winds beyond the barrier of the Dividing Range, increased insolation on the southern slope. The most icy is the Central Caucasus, where 5 glaciers (Dykhsu, Bezengi, Karaugom on the northern slope, Lehzyr and Zanner on the southern) have an area of \u200b\u200bapproximately 40 square meters. km Their length is more than 12km. The modern snow border 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 \u200b\u200bglaciers of Transcaucasia is small - a little more than 5 square meters. km (Zanzegursky Range, peak of Aragats). The glaciers of the Caucasus play a large role in the nutrition of the rivers of the Caucasus, determining their full flow and the nature of the water regime of the alpine type.
Together they bring this product to the consumer. The most picturesque of all was determined by the product they sell travel agents specializing in recreation - they 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, moreover, not a right to it, but a more complex and not yet familiar product for us, consisting of a set of “things, rights , works and services, information, intellectual property and intangible goods. ” “A tourist product is a combination of material (consumer goods), non-material (in the form of services) consumption values \u200b\u200bnecessary to meet the needs of a tourist arising during his travel.”
General characteristic of the climate of the Caucasus
The climatic conditions of the Caucasus are determined not only by its geographical position, but also by the relief.
The Caucasus lies on the border of two climatic zones - temperate and subtropical. These climatic zones have internal differences, which are determined by the topography, air currents, local atmospheric circulation and the position between the seas.
Climate change occurs in three directions:
- in the direction of increasing continentality, i.e. from west to east;
- in the direction of increasing radiation heat, i.e. from North to South;
- in the direction of increasing precipitation and decreasing temperatures, i.e., with height.
The territory receives a lot of solar heat and in summer the radiation balance is close to tropical, so the air masses here are transformed into tropical air.
In winter, the radiation balance approaches positive values.
Continental air of moderate latitudes dominates in the North Caucasus, subtropical air dominates in Transcaucasia. Altitude zones are influenced by western directions.
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Transcaucasia, Ciscaucasia and the western part of the Greater Caucasus are influenced by Mediterranean cyclones.
The mountains of the Greater Caucasus do not allow the cold northern air masses to pass through the Transcaucasus, and the warm air masses in the Ciscaucasia do not pass the same way, so the northern and southern parts of the Caucasus have large temperature differences.
Average annual temperatures vary from +10 degrees in the north to +16 degrees in the south.
In the summer, temperature differences are smoothed out, but a difference appears in the temperatures of the western and eastern parts of the mountains. July temperature in the west is +23, +24 degrees, and in the east +25, +29 degrees.
In winter, an area of \u200b\u200blow pressure forms over the Black Sea and the south of the Caspian Sea, and a local anticyclone forms over the Armenian Highlands.
In summer, an area of \u200b\u200blow pressure is formed over Asia, as a result, sea air of temperate latitudes from the Atlantic intensifies and captures the Caucasus. Precipitation that sea air brings falls on the windward slopes of the mountains.
In the second half of summer, the Caucasus captures the Azores maximum, shifting to the north.
Summer and winter temperatures of the southern slopes of the Caucasus are higher. The annual precipitation increases with height, and decreases from west to east at all levels.
At an altitude of 2000 m, western air transport plays a leading role, the influence of the Atlantic Ocean and the Mediterranean Sea is intensified here, and the upper "floor" is located in conditions where a free atmosphere circulates.
Since the relief of the mountains provides this exchange, the climate of the highlands is more humid and resembles a marine one.
Due to the insufficient size of the Black and Caspian Seas, airborne masses of the marine type cannot form above them. Continental air mainly circulates above the surface of the seas, in the lower layer of which there is a change in temperature and humidity.
The Black Sea is on the way of the western air currents and evaporation from its surface comes to the mountains, giving a significant part of the precipitation on the southern slope of the western part.
Climate of the Caucasus in winter
In winter, the continental air of temperate latitudes dominates, and the winds are eastern and northeast. The northern slopes of the Greater Caucasus retain cold air, and it does not rise above 700-800 m, but in the north-western part, where the altitude is less than 1000 m, the cold air can be crossed over the mountain range.
At this time, reduced pressure over the Black Sea sets in, and cold air collapses from the mountains, rushing toward the sea.
As a result, a Novorossiisk boron arises - a strong cold wind. It appears on the Anapa-Tuapse site. The air temperature in the wind drops to -15 ... -20 degrees.
Western air transport in the winter is at an altitude of 1500-2000 m. The activity of cyclones at this time has a great influence on the formation of climatic conditions.
Mediterranean cyclones cross the Caucasus in the western part and cause thaws, avalanches.
On the northern slopes of the Greater Caucasus, foehn winds form. The temperature during this period rises to + 15 ... + 20 degrees.
The influence of the sea and frequent advection of heat determine a positive average temperature, for January in Novorossiysk the average temperature is +2 degrees, in Sochi + 6.1 degrees. In the mountains with a height it will drop to -12 ... -14 degrees.
On the coast of the Caspian Sea -2 ... 0 degrees.
Sometimes cold northern air masses can reach the Ciscaucasia and lower the air temperature to -30 ... -36 degrees. The absolute minimum in Anapa is -26 degrees, in Sochi -15 degrees.
Winter cyclones bring an abundance of rainfall to the Black Sea coast. In the mountains and plains, snow cover is established with a thickness of 10-15 cm, which disappears during thaws.
Heavy rainfall occurs on the southwestern slopes of the Greater Caucasus, and since thaws are much less frequent here, the snow thickness reaches 3-4 m.
In the eastern part of the mountains, the thickness of the snow cover is reduced to 1 m. On the Stavropol Upland, snow lasts 70-80 days, and in the mountains up to 80-110 days.
At this time, a region of high atmospheric pressure forms on the Javakheti - Armenian Highlands, and the cold continental air of Asia Minor enters. As you move east, it quickly transforms.
Climate of the Caucasus in summer
Wet Atlantic and dry continental air masses coming from the east exert their influence on the climate of the Caucasus in summer.
The air of the Black Sea coast and the Western Ciscaucasia warms up to +22, +23 degrees.
The high parts of the Stavropol Upland warm up to +21 degrees, and the temperature in the east of the Ciscaucasia rises to +24, +25 degrees.
The June maximum precipitation in the first half of summer is enhanced by the influence of Atlantic cyclones.
By the middle of the summer period over the southeast of the Russian Plain, air masses are being transformed, so precipitation becomes less and conditions for the formation of droughts and dry winds appear.
The amount of precipitation from the foothills to the mountains and in the mountains increases, but decreases when moving from west to east. So, the annual amount of precipitation in the Kuban-Priazovskaya lowland is 550-600 mm, in the Stavropol Upland their amount increases to 700-800 mm, and in the Eastern Ciscaucasia decreases to 500-350 mm.
An increase in precipitation from north to south again occurs on the Black Sea coast from 700 mm in the Novorossiysk region to 1650 mm in Sochi.
In the west of the Greater Caucasus, 2000-3000 mm falls, and in the east - 1000-1500 mm. The windward southwestern slopes of the Greater Caucasus receive more than 3,700 mm during the year - this is the largest amount of rainfall in the country.
The highest summer temperatures are observed on the Kuro-Araksin lowland + 26 ... + 28 degrees. The temperature in the rest of the territory is + 23 ... + 25 degrees, and in the Javakheti-Armenian Highlands +18 degrees.
Depending on the height of the mountains, temperature and precipitation change, thus forming a high-altitude climatic zonality - on the Black Sea coast +12, +14 degrees, in the foothills already +7, +8 degrees, and 0, -3 degrees at an altitude of 2000-3000 m
With height, the positive average annual temperature remains at an altitude of 2300-2500 m, and on Elbrus the temperature is already -10 degrees.