The main factors influencing the climate of the Caucasus. Describe the climate of the Greater Caucasus, explain how the climate of the foothills differs from the high-mountain regions. Finished works on a similar topic
home The climate of the Caucasus is very diverse. The northern part of the Caucasus is located within temperate zone Transcaucasia is subtropical. This geographical position
significantly influences the formation of the climate of various parts of the Caucasus. The Caucasus is a shining example 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. Circulation air masses reaching the Caucasus undergoes significant changes, encountering mountain ranges like Greater Caucasus , and Transcaucasia. Climatic contrasts appear at relatively short distances
. An example is the western, abundantly moistened Transcaucasia and the eastern, dry subtropical climate of the Kura-Araks lowland. The exposure of the slopes is of great importance, greatly influencing the thermal regime and the distribution of precipitation. The climate is affected 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 diurnal variation, moistening the adjacent parts of the Caucasus, increase the temperature of the cold season, and reduce temperature amplitudes. The flat eastern Ciscaucasia and the Kura-Araks lowland, which protrudes deeply into the isthmus, do not contribute to the condensation of moisture coming from the Caspian Sea. The Ciscaucasia is greatly influenced by continental air masses coming from the north, including the Arctic, which often significantly reduce the temperature of the warm season. Spur of the high East Siberian barometric pressure
often lowers the temperature of the cold season. There are cases when cold air, flowing from the east and west of the Greater Caucasus, spreads into Transcaucasia, causing a sharp drop in temperature there. Air masses coming from Atlantic Ocean and Mediterranean, provide high humidity western parts
Caucasus and slopes of ridges of western exposure. Additional moisture is brought by air masses passing over the Black Sea. The influence of the Caspian Sea is less pronounced. IN 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 altitude on mountain structures, where altitudinal zonation is clearly manifested.
Total radiation within the Caucasus ranges from 460548 J/sq. cm in the north to 586,152 J/sq. cm in the extreme south. Annual radiation balance from 146538 to 188406 J/sq. cm. The amount of solar radiation depends not only on latitude, but also on cloudiness. Many peaks of the Caucasus are characterized by persistent cloudiness, so direct solar radiation is lower here average norm. To the east it increases due to decreased humidity. The exception is Lankaran and Talysh, where the topography promotes condensation of water vapor and increased cloudiness.
The amount of total radiation and radiation balance in different regions of the Caucasus is not the same due to contrasts in orography, relief, different angles falling sunlight and physical properties underlying surface. In summer, the radiation balance in some areas of the Caucasus approaches the balance of tropical latitudes, so the air temperatures here are high (the Ciscaucasia and Transcaucasian plains), and in abundantly humidified areas there is high evaporation and, accordingly, increased air humidity.
air masses, taking part in circulation over the territory of the Caucasus are different. Mainly continental air of temperate latitudes dominates over the Ciscaucasia, and subtropical air dominates in the Transcaucasus. 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 the Ciscaucasia, located south of the band of high barometric pressure, cold air often enters. Low pressure remains over the Black Sea and in the southern part of the Caspian Sea. Pressure contrasts cause cold air to spread southward. In such a situation, the barrier role of the Greater Caucasus is especially great, serving as an obstacle to the widespread penetration of cold air into Transcaucasia. Typically, its influence is limited to the Ciscaucasia and the northern slope of the Greater Caucasus to approximately an altitude of about 700 m. It causes a sharp decrease in temperatures, an increase in pressure and an increase in wind speed.
Intrusions of cold air masses from the northwest and northeast are observed, bypassing the Greater Caucasus ridges along the shores of the Caspian and Black Seas. The accumulated cold air flows over the low ridges. and spreads along the western and east coast to Batumi and Lenkoran, causing temperatures to drop on the western coast of Transcaucasia to -12°, in the Lenkoran Lowland to -15° C and below. A sharp drop in temperature has a disastrous effect on subtropical crops and especially citrus fruits. The pressure gradients in the above situations between the Ciscaucasia and the Transcaucasus are sharply contrasting, and the spread of cold air from the Ciscaucasia to the Transcaucasia is very rapid. 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 are exerted 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 out. Therefore, Eastern Transcaucasia is characterized 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, causing a strong decrease in temperature. In summer, low pressure sets in over 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° N. w. It determines the decrease in cyclonic activity in summer. This 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, due to the daily variation of air temperatures, increases.
In the Caucasus, foehns, which are common in mountains with dissected relief, actively appear. Associated with them 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, and 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 Transcaucasia 1-2° C. At an altitude of 2000 m, the temperature in July is 13°C, in January -7°C, in the highest zones - in July 1°C, in January from -18 to -25°C.
The annual amount of precipitation increases with elevation and at all levels decreases noticeably from west to east (most uniformly in high zones). 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 Sochi area 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 to 3000 mm, on the Kura-Araks Lowland it decreases to 200 mm. The Lenkoran Lowland and the eastern slopes of the Talysh Range are abundantly moistened, where 1500-1800 mm of precipitation falls.
The climate of the Caucasus is very diverse, which is explained primarily by the influence of relief.
The Caucasus is located on the border of temperate and subtropical climate zones. The differences between them are amplified by the Greater Caucasus Mountains, which impede the transfer of cold air masses from the north to Transcaucasia and warm air masses from the south to Ciscaucasia. The North Caucasus belongs to the temperate zone, Transcaucasia - to the subtropical zone. The differences between them are especially noticeable in air temperature.There is a lot of heat everywhere in the North Caucasus, with the exception of the highlands. On the plains, average July temperatures everywhere exceed 20°, and summer lasts from 4.5 to 5.5 months. Average January temperatures range from -10° to +6° in different areas, 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 an altitude of approximately 2000 m, and in the Transcaucasian Plateau somewhat higher, the role of western air transport plays a role, and therefore the influence of the Atlantic and Mediterranean Sea. Therefore, in the highlands the climate is more humid.
The complex mountainous terrain creates a wide variety of local climates in the Caucasus, and the previously outlined large geomorphiclogical units differ in climate.
The diversity of the climate of the Caucasus determines the differences in the agricultural use of its territory. Particularly large economic importance Transcaucasian subtropical regions protected by the mountain barrier of the Greater Caucasus, where a whole range of subtropical climates are observed, ranging from humid, allowing for the cultivation of tea and citrus fruits, to dry, suitable for growing cotton and other crops that require an abundance of sunlight.
General characteristics of the climate of the Caucasus
The climatic conditions of the Caucasus are determined not only by its geographical location, but also by its topography.
The Caucasus is located on the border of two climatic zones - temperate and subtropical. These climatic zones have internal differences that are determined by relief, air currents, local atmospheric circulation and position between the seas.
Climate change occurs in three directions:
- towards increasing continentality, i.e. from west to east;
- towards increasing radiative heat, i.e. from North to South;
- towards 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 temperate 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 under the influence of Mediterranean cyclones.
The Greater Caucasus Mountains do not allow cold northern air masses to pass through in Transcaucasia, and they also do not allow warm air masses to pass through to Ciscaucasia, therefore 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 summer, temperature differences are smoothed out, but there is a difference in temperatures between the western and eastern parts of the mountains. The July temperature in the west is +23, +24 degrees, and in the east +25, +29 degrees.
In winter, an area of low 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 low pressure forms over Asia, as a result, sea air from temperate latitudes from the Atlantic intensifies and invades the Caucasus. The precipitation that sea air brings falls on the windward slopes of the mountains.
In the second half of summer, the Caucasus is captured by the Azores high, which moves north.
Summer and winter temperatures the southern slopes of the Caucasus are higher. The annual amount of precipitation increases with height and decreases from west to east at all levels.
At an altitude of 2000 m, westerly air transport plays a leading role, here the influence of the Atlantic Ocean and the Mediterranean Sea increases, and the upper “floor” is located in conditions where a free atmosphere circulates.
Since the mountain topography ensures this exchange, the climate of the highlands is more humid and resembles a sea climate.
Air masses marine type due to the insufficient size of the Black and Caspian Seas, they cannot form above them. Continental air mainly circulates above the surface of the seas, in the lower layer of which changes in temperature and humidity occur.
The Black Sea is located in the path of western air currents and evaporation from its surface reaches the mountains, depositing a significant part of the precipitation on the southern slope of the western part.
Climate of the Caucasus in winter
In winter, continental air of temperate latitudes and easterly and northeasterly winds dominate within the Ciscaucasia region. The northern slopes of the Greater Caucasus trap cold air, and it does not rise above 700-800 m, but in the northwestern part, where the altitude is less than 1000 m, cold air manages to cross the mountain range.
At this time, low pressure is established over the Black Sea, and cold air falls from the mountains, rushing to the sea.
As a result, Novorossiysk bora arises - a strong cold wind. It arises in the Anapa-Tuapse section. When there is wind, the air temperature drops to -15...-20 degrees.
Western air transport in 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 and avalanches.
Foehn winds form on the northern slopes of the Greater Caucasus. The temperature during this period rises to +15…+20 degrees.
The influence of the sea and frequent advection of heat determine the positive average temperature, so in Novorossiysk the average January temperature is +2 degrees, in Sochi +6.1 degrees. In the mountains, with 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 precipitation to the Black Sea coast. In the mountains and plains, a snow cover of 10-15 cm thick is established, which disappears during thaws.
Heavy precipitation falls on the southwestern slopes of the Greater Caucasus, and since thaws occur much less frequently 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 the area of high atmospheric pressure is formed 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 influence the formation of the climate of the Caucasus in the summer.
The air on the Black Sea coast and 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.
Towards the middle summer period over the southeast of the Russian Plain, air masses are transformed, so precipitation becomes less and conditions for the formation of droughts and hot winds appear.
The amount of precipitation increases from the foothills to the mountains and in the mountains, but decreases when moving from west to east. Thus, the annual amount of precipitation in the Kuban-Azov lowland is 550-600 mm, in the Stavropol Upland its amount increases to 700-800 mm, and within the Eastern Ciscaucasia it decreases to 500-350 mm.
Precipitation increases from north to south again 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 3700 mm during the year - this is the most a large number of precipitation in the country.
The highest summer temperatures are observed in the Kura-Araks lowland +26…+28 degrees. The temperature in the rest of the territory is +23…+25 degrees, and in the Javakheti-Armenian Highlands is +18 degrees.
Depending on the height of the mountains, temperature and precipitation change, thus forming an altitudinal climatic zonation - 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.
Positive with altitude average annual temperature persists at an altitude of 2300-2500 m, and on Elbrus the temperature is already -10 degrees.
Summer is hot everywhere, with the exception of the highlands. Thus, the average temperature on the plain in 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, in the foothills for eight, and on the Black Sea coast for up to eleven. (T not lower than +10).
Winters in the Ciscaucasia are quite warm (the average temperature in January is -5ºC). This is facilitated by warm temperatures coming from the Atlantic Ocean. air masses. On the Black Sea coast, the temperature rarely drops below zero (the average January temperature is +3ºC). In mountainous areas, the temperature is naturally below -4 - 8° C.
Precipitation.
Dry Central Asian winds penetrating through the Caspian Sea and humid Black Sea winds have a decisive influence on the distribution of precipitation.
Precipitation they enter this territory mainly thanks to those coming from the west cyclones, as a result of which their number gradually decreases to the east. Most precipitation falls on the southwestern slopes of the Greater Caucasus. (2600mm) (most of all in our country). To the east, precipitation drops to 600 mm per year
Their number on the Kuban Plain is approximately 400 mm. The Stavropol Plateau serves not only as a watershed, but also as a barrier limiting the influence of the Black Sea winds in the east of the region. Therefore, the southwestern regions North Caucasus quite humid (in Sochi there is 1410 mm of precipitation per year), 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 zone. This geographical location significantly influences the formation of the climate of various parts of the Caucasus.
The Caucasus is a striking 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. The circulation of air masses reaching the Caucasus undergoes significant changes, meeting on its way the mountain ranges of both the Greater Caucasus and Transcaucasia. Climatic contrasts occur over relatively short distances. An example is the western, abundantly moistened Transcaucasia and the eastern, dry subtropical climate of the Kura-Araks lowland. The exposure of the slopes is of great importance, greatly influencing the thermal regime and the distribution of precipitation. The climate is affected by the seas washing the Caucasian Isthmus, especially the Black Sea.
The Black and Caspian seas moderate the air temperature in summer, contribute to a more even diurnal variation, moisten the adjacent parts of the Caucasus, increase the temperature of the cold season, and reduce temperature amplitudes. The flat eastern Ciscaucasia and the Kura-Araks lowland, which protrudes deeply into the isthmus, do not contribute to the condensation of moisture coming from the Caspian Sea. The Ciscaucasia is greatly 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 cases when cold air, flowing from the east and west of the Greater Caucasus, spreads into Transcaucasia, causing a sharp drop in temperature there.
Air masses coming from the Atlantic Ocean and the Mediterranean provide high humidity in the western parts of the Caucasus and the slopes of the western-facing ridges. 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 increasing dryness and continentality, from north to south towards increasing total radiation and radiation balance, and in altitude on mountain structures, where altitudinal zonation is clearly manifested.
Total radiation within the Caucasus ranges from 460548 J/sq. cm in the north to 586,152 J/sq. cm in the extreme south. Annual radiation balance from 146538 to 188406 J/sq. cm. 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 average. To the east it increases due to decreased humidity. The exception is Lankaran and Talysh, where the topography promotes condensation of water vapor and increased cloudiness.
The amount of total radiation and radiation balance in different regions of the Caucasus is not the same due to contrasts in orography, relief, different angles of incidence of solar rays 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, so the air temperatures here are high (the Ciscaucasia and Transcaucasian plains), and in abundantly humidified areas there is high evaporation and, accordingly, increased air humidity.
The air masses that take part in the circulation over the territory of the Caucasus are different. Mainly continental air of temperate latitudes dominates over the Ciscaucasia, and subtropical air dominates in the Transcaucasus. 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 the Ciscaucasia, located south of the band of high barometric pressure, cold air often enters. Low pressure remains over the Black Sea and in the southern part of the Caspian Sea. Pressure contrasts cause cold air to spread southward. In such a situation, the barrier role of the Greater Caucasus is especially great, serving as an obstacle to the widespread penetration of cold air into Transcaucasia. Typically, its influence is limited to the Ciscaucasia and the northern slope of the Greater Caucasus to approximately an altitude of about 700 m. It causes a sharp decrease in temperatures, an increase in pressure and an increase in wind speed.
Intrusions of cold air masses from the northwest and northeast are observed, bypassing the Greater Caucasus ridges along the shores of the Caspian and Black Seas. The accumulated cold air flows over the low ridges. and spreads along the western and eastern coasts to Batumi and Lenkoran, causing temperatures to drop on the western coast of Transcaucasia to -12°, on the Lenkoran lowland to -15° C and below. A sharp drop in temperature has a disastrous effect on subtropical crops and especially citrus fruits. The pressure gradients in the above situations between the Ciscaucasia and the Transcaucasus are sharply contrasting, and the spread of cold air from the Ciscaucasia to the Transcaucasia is very rapid. 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 out. Therefore, Eastern Transcaucasia is characterized 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, causing a strong decrease in temperature. In summer, low pressure sets in over 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° N. w. It determines the decrease in cyclonic activity in summer. This 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, due to the daily variation of air temperatures, increases.
In the Caucasus, foehns, which are common in mountains with dissected relief, actively appear. 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, and 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 Transcaucasia 1-2° C. At an altitude of 2000 m, the temperature in July is 13°C, in January -7°C, in the highest zones - in July 1°C, in January from -18 to -25°C.
The annual amount of precipitation increases with elevation and at all levels decreases noticeably from west to east (most uniformly in high zones). 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 Sochi area 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 to 3000 mm, on the Kura-Araks Lowland it decreases to 200 mm. The Lenkoran Lowland and the eastern slopes of the Talysh Range 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 throughout the territory is associated not only with climatic conditions, but also with orography and relief.
Almost all rivers of the Caucasus originate in the mountains, where they accumulate great amount moisture in the form of liquid and solid precipitation and glaciers. As it rises upward due to an increase in precipitation and a decrease in evaporation losses, the annual surface runoff increases and the density of the river network increases. Rivers originating in the mountains play a transit role within the plains of Ciscaucasia and Transcaucasia.
The Greater Caucasus watershed ridge delimits the river basins of the Black, Azov and Caspian seas.
Stand out lowland rivers Ciscaucasia with a slow current and small floods. Some of them originate on the slopes of the Stavropol Upland. Their spring floods are associated with melting snow. In summer they either dry up or form chains of lakes (Western and Eastern Manych).
In mixed-fed rivers, the upper reaches are located in the mountains, and the lower sections are located within the plains. These include Kuban, Kuma, Rioni, Terek, Kuri and Araks.
Typically mountainous are the Bzyb, Kodor, Inguri and the upper sections of most rivers of the Caucasus. Their sources are located in the nival belt, the rivers flow in deep, often canyon-like gorges (Sulak, Terek, etc.). They are characterized by high flow speeds, rapids, and waterfalls.
Depending on the topography, amount and regime of precipitation, the density of the Caucasus river network ranges from 0.05 km/sq. km in the east of Ciscaucasia d6 1.62 km/sq. km in the mountains.
Rivers starting in the high mountain zone are fed by snow, snow-glaciers (Kuban, Terek, Rioni, Kodor, etc.). In rivers fed by snow and glacier, maximum flow rates are observed not only in spring due to snow melting, but also in summer as snow and glaciers melt in the upper altitudinal zones.
The rivers of the humid subtropics are predominantly rain-fed and are characterized by sharp fluctuations in flow. During rainfall, precipitation turns into turbulent powerful streams, carrying a mass of coarse 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 zone of 2000-3000 m. Groundwater plays a large role in their nutrition. Melting snow in the spring contributes to a sharp increase in levels and flows, with minimal flows in June and July (Kura, Araks).
From the nature of the blurred rocks and sediments depends on the turbidity of the water. Many rivers of the Caucasus, especially Dagestan, are characterized by high turbidity - 5000-7000 g / cubic meter. m (clays, shales, sandstones, limestones). The turbidity of the Kura and Terek rivers is high. Rivers flowing in crystalline rocks have the lowest turbidity.
The hardness and mineralization of river waters varies widely. In the Kura basin, hardness reaches 10-20 mg/l, and mineralization 2000 kg/l.
The transport significance of the Caucasus rivers 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 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 unique, forming an entire system. In summer, the mirror of the lakes of the Kuma-Manych depression. is 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 square meters. km, maximum depth it was 99 m with an absolute height of the water surface of 1916 m. The release of the lake's water in connection with hydropower construction lowered its level by more than 18 m, which is why its depth and area decreased. This caused serious changes in the hydrological regime of the lake and affected other aspects natural conditions the lake basin itself and the surrounding area. In particular, the masses of birds that nested and rested during migration on the group of daughter lakes of Sevan, Gilli, disappeared. Due to the drainage of Sevan's waters, this area turned into vast exposed peatlands. Dozens of species of animals and birds have disappeared, fish resources have 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 trough that has experienced fault dislocations in places. 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. In Hrazdan they began to drain the upper layer of lake waters, which then passed through 6 hydroelectric stations of the Sevan-Hrazdan cascade. The surface flow in the upper reaches of Hrazdan stopped - Sevan water went through a tunnel to the turbines of the Sevan hydroelectric station.
According to the new project for the use of Sevan waters, further lowering of their level has been suspended. It will remain at 1898 m, and the picturesque reservoir will remain within boundaries close to natural. Through a 48-kilometer tunnel in the Vardenis ridge, water is supplied to Sevan from the upper reaches of the river. Arps. A recreation area with a national park is being created on the shores of the lake, and the strip of land freed from under the waters of the lake is being afforested. The main problem of the lake and its basin at present is the preservation and restoration of the largely unique natural conditions and endemic species of flora and fauna, in particular the aforementioned Sevan trout, which is also of great commercial importance. In the future, measures should be taken to raise the lake level by 4-5 m.
The basins of mountain lakes are tectonic, karst, volcanic, cirque. Some occupy depressions in the moraine relief. Volcanic lakes are predominantly dammed and are 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 - Badukskie, Murudzhinskie, Klukhorskoe (at the pass of the same name). There are lakes in the floodplains of the rivers of the Caucasus plains. The dammed Lake Ritsa is unique and very beautiful. The lakes of Colchis were formed during the formation of the lowland itself, the largest of them being Lake Paleostomi.
Caucasus. They are significant in reserves and varied in chemical composition and degree of mineralization. Their formation is associated with geotectonic structures and infiltration atmospheric precipitation. Fissure and strata-fissure waters are common in folded geostructures. The movement of water occurs along the cracks of tectonic faults, faults and thrusts, along the strike of folds into river valleys.
The mineral composition of groundwater is determined by the composition of rocks. Crystalline rocks are poorly soluble, therefore The groundwater, circulating in them, are relatively little mineralized. Groundwater located in sedimentary deposits is often saturated with easily soluble compounds and highly mineralized. The underground waters of the Caucasus are predominantly cold - up to 20°C. There are subthermal ones - above 20 and hot ones - above 42 ° C (the latter are not uncommon within the Greater and Lesser Caucasus).
The chemical composition of the groundwater in the Caucasus is very diverse. Carbon dioxide is especially characteristic mineral springs, 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 waters (Matsesta, Chkhalta), radon thermal waters up to 35 ° C (Tskhaltubo springs). Mineral water The Caucasus is used by numerous resorts.
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 mountain region of the Caucasus with widespread development of modern glaciation. The number of glaciers is 2047, the glaciation area is 1424 sq. km. About 70% of the number of glaciers and glaciation area is on the northern slope and about 30% on the southern slope. The difference is explained by orographic features, snowstorm transport of snow by westerly winds beyond the barrier of the Dividing Range, and increased insolation on the southern slope. The most glaciated is the Central Caucasus, where 5 glaciers (Dykhsu, Bezengi, Karaugom on the northern slope, Lekhzyr and Tsanner on the southern) have an area of approximately 40 square meters. km. Their length is more than 12 km. Modern snow border of the Greater Caucasus on southwest lies at an altitude of 2800-3200 m, in the east it rises to 3600 m. The area of Transcaucasian glaciers is small - a little more than 5 square meters. km (Zanzegur Ridge, peak of Aragats). The glaciers of the Caucasus play a large role in feeding the rivers of the Caucasus, determining their full flow and the nature of the alpine-type water regime.
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