What is the climate in the Caucasus. Climate - Caucasian mountains

general characteristics Caucasus climate

The climatic conditions of the Caucasus are determined not only by its geographical position, but also by its relief.

The Caucasus is located on the border of two climatic zones - temperate and subtropical. These climatic zones have internal differences, which are determined by the relief, air currents, local circulation of the atmosphere and the position between the seas.

Climate change is happening in three ways:

in the direction of increasing continentality, i.e. from west to east;
towards an increase in radiative heat, i.e. from North to South;
in the direction of increasing precipitation and decreasing temperatures, i.e. with height.

Territory gets a lot solar heat and during the summer radiation balance close to tropical, so the air masses here are transformed into tropical air.

AT winter period the radiation balance approaches positive values.

continental air temperate latitudes dominates the North Caucasus, subtropical air dominates the Transcaucasus. Altitude zones are influenced western directions.

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Transcaucasia, Ciscaucasia and the western part of the Greater Caucasus are under the influence of Mediterranean cyclones.

The mountains of the Greater Caucasus do not allow cold northern air masses to pass into the Transcaucasus, and in the same way they do not allow warm air masses to pass into the 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. 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, the sea air from the Atlantic intensifies in temperate latitudes and captures the Caucasus. The precipitation that sea air brings falls on the windward slopes of mountains.

In the second half of summer, the Caucasus captures the Azores high, which shifts to the north.

Summer and winter temperatures are higher on the southern slopes of the Caucasus. With height, the annual amount of precipitation increases, and decreases from west to east at all levels.

At an altitude of 2000 m, the western air transport plays a leading role, here there is an increase in the influence Atlantic Ocean and the Mediterranean Sea, 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 sea one.

Marine-type air masses cannot form over them due to the insufficient size of the Black and Caspian Seas. Continental air 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 located on the path of 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.

The climate of the Caucasus in winter

In winter, continental air of temperate latitudes dominates within Ciscaucasia, east and northeast winds. 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 height 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, there is a Novorossiysk bora - a strong cold wind. It arises in the Anapa-Tuapse section. The air temperature during the wind drops to -15 ... -20 degrees.

The western air transfer in winter is at an altitude of 1500-2000 m. The activity of cyclones at this time affects the formation of climatic conditions big influence.

Mediterranean cyclones cross the Caucasus in the western part and cause thaws, snow avalanches.

Föhn 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 January average temperature+2 degrees, +6.1 degrees in Sochi. 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 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 on the plains, a snow cover is established, with a thickness of 10-15 cm, which disappears during thaws.

Abundant precipitation falls on the southwestern slopes of the Greater Caucasus, and since thaws are much rarer 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.

The climate of the Caucasus in summer

Humid Atlantic and dry continental air masses coming from the east exert their influence on the formation of the climate in the Caucasus in summer.

The air of 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 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, the air masses are transformed, so there is less precipitation 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-Azov lowland is 550-600 mm, in the Stavropol Upland their amount increases to 700-800 mm, and within the Eastern Ciscaucasia it decreases to 500-350 mm.

The increase in precipitation from north to south is again 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 rainfall 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 +18 degrees.

Depending on the height of the mountains, temperature and precipitation change, thus forming a high-altitude climatic zoning - 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 positive mean annual temperature remains at an altitude of 2300-2500 m, and on Elbrus the temperature is already -10 degrees.

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

The climate of the Greater Caucasus is determined by its southern location, the proximity of Chernoy and mediterranean seas, as well as a significant height of mountain ranges. The Greater Caucasus is a barrier to the movement of masses of humid warm air from the west. More precipitation falls on the southern slopes, the maximum amount is in the western part, where more than 2500 mm per year falls in the highlands (most of all in our country). To the east, precipitation drops to 600 mm per year. The northern slope of the Greater Caucasus is generally drier than the southern one.
In the mountains of the Greater Caucasus, in a relatively small area, there is a wide range of climatic zones with pronounced zonality in height: humid subtropics of the Black Sea coast continental dry (in the east to semi-desert) climate with hot summers and short, but cold winter on the plains of the Ciscaucasia, there is a temperate continental climate of the foothills with significant precipitation (especially in the western part) and snowy winters (in the Krasnaya Polyana region, on the watershed of the Bzyb and Chkhalta rivers, the snow cover reaches 5 m and even 8 m). In the zone of alpine meadows, the climate is cold and humid, winter lasts up to 7 months, the average temperatures of August - the warmest month - range from 0 to + 10C. Above is the so-called nival belt, where the average temperature of even the warmest month does not exceed 0. Precipitation here falls mainly in the form of snow or grains (hail).

The average January temperatures at the foot of the mountains are -5С in the north and from +3 to +6С in the south at an altitude of 2000 m -7-8С, at an altitude of 3000 m -12С, at an altitude of 4000 m -17С. The average temperature in July at the foot of the mountains in the west is +24С, in the east up to +29С at an altitude of 2000 m +14С, at an altitude of 3000 m +8С, at an altitude of 4000 m +2С.

In the Greater Caucasus, the height of the snow line, rising from west to east, fluctuates between 2700 m - 3900 m above sea level. Its northern mark is different for the northern and southern slopes. In the Western Caucasus, these are 3010 and 2090 m, respectively, in the Central - 3360 and 3560 m, in the Eastern - 3700 and 3800 m. The total area of modern glaciation of the Greater Caucasus is 1780 km. The number of glaciers is 2047, their tongues descend to absolute levels: 2300-2700 m ( Western Caucasus) , 1950-2400 m (Central Caucasus), 2400-3200 m (Eastern Caucasus). Most of glaciation falls on the north side of the GKH. The distribution of the glaciation area is as follows: Western Caucasus - 282 and 163 sq. km Central Caucasus - 835 and 385 sq. km East Caucasus - 114 and 1 sq. km, respectively.
Caucasian glaciers are distinguished by a variety of forms. Here you can see grandiose icefalls with seracs, ice grottoes, "tables", "mills", deep cracks. Glaciers carry out a large amount of detrital material that accumulates in the form of various moraines on the sides and at the tongue of the glaciers.

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

Caucasus is a prime 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, meeting on its way mountain ranges 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 dry subtropical climate 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 moderate the air temperature in summer, contribute to its more even daily course, humidification of the parts of the Caucasus adjacent to them, increase the temperature of the cold season, reduce the 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 sharp decline temperature.

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.

AT 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 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 quantity 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 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 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 sunlight and physical properties 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 Transcaucasia 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 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 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 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. associated with them hot weather in spring- summer time. 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.

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, 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.

High rainfall, short warm season, dependency natural conditions from the height of the mountains and the exposure of the slopes, the distribution 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. Third difference high mountain climate- 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 altitudinal zonality 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, 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 Caucasus cannot be attributed to one climatic region. To the north of the axial belt of the Greater Caucasus - a temperate climate, in Transcaucasia - subtropical. Within them there are differences due to the nature of the relief, position in relation to air currents, position relative to the Black and Caspian Seas, and local circulation.

The climate of the Caucasus is changing in three directions:

from west to east - in the direction of increasing continentality,

from north to south - in the direction of increasing amounts of radiative heat

in the high-altitude direction - an increase in precipitation and a decrease in temperatures.

Cloudiness plays a special role - with an increase in the mountains and in the western regions of the Caucasus, due to its increase, the annual values of solar radiation are less than average.

AT summer months The radiation balance in the Caucasus is close to tropical; local VMs are transformed into tropical ones.

Circulation: continental air of temperate latitudes dominates in the North Caucasus, subtropical in Transcaucasia. Alpine zones under the influence of western directions.

AT winter months the territory is located south of the "major axis"; areas of low pressure are formed over the Black and the south of the Caspian. The result is an outflow of dense cold masses of the "great axis" to the Caucasus. However, the mountain wall prevents penetration to the south, it is still possible to bypass along the coasts of the seas - "nords" and "boron". In the west, there is a lot of snow in the mountains. To the east, the influence of southwestern transport weakens and the influence of the Asian anticyclone intensifies, snowfall decreases. A local anticyclone forms over the Armenian Highlands in winter.

In summer time over Asia they form an area of low pressure. The western currents of sea air of temperate latitudes from the North Atlantic are intensifying, which capture the Caucasus. They give up precipitation on windward slopes. In the second half, the Azorean maximum shifts to the north and often captures the Caucasus.

The role of foehns, mountain-valley winds and breezes, the formation of a center of low pressure over the Armenian Highlands is noticeable. Sea basins moderate the temperature.

In general, the southern slopes are characterized by higher (summer and winter) temperatures. The annual amount of precipitation increases with elevation to the mountains and decreases at all levels from west to east.

The Caucasus is located on the border of the temperate and subtropical zones. The influx of solar radiation is so significant that in the summer a local center for the formation of tropical air masses is created in Transcaucasia. The boundary of the temperate and subtropical belts runs along the axial part of the Greater Caucasus. Radiation balance 2300 MJ / m 2 / year (west) - 1800 (east) MJ / m 2 / year.

In winter, the continental air of temperate latitudes (CLA) spreads to Ciscaucasia from the Voeikov axis. East and northeast winds prevail. Cold air entering Ciscaucasia lingers on the northern slopes of the Greater Caucasus, not rising above 700-800 m. And only in the northwestern part of the Black Sea chain, where the height of the ridges is less than 1000 m, cold air crosses them. Over the water area of the Black Sea in winter, low pressure is established, so cold heavy air rushes towards it at high speed, literally falling from the mountains. Strong cold winds arise, the so-called Novorossiysk bora. The air temperature during boron drops to -15...-20°С. Bora is observed in the Anapa-Tuapse section.

The upper parts of the mountains are located in the free atmosphere zone, where the prevailing role belongs to the western winds. In winter, the western transport dominates at an altitude of more than 1.5-2 km, and in summer - 3.5-4 km.

The formation of climatic conditions of the cold period is greatly influenced by cyclonic activity developing on the Mediterranean branch of the polar front. The trajectories of the Mediterranean cyclones are directed to the northeast of the Black Sea and cross the Caucasus in its western part. Their movement through the Caucasus leads to advection of tropical air, which causes intense thaws, snow cover, the occurrence of snow avalanches in the mountains and the formation of foehns on the northern slopes of the Greater Caucasus. With the development of hair dryers, the air temperature can rise to +15...+20°C. As the height of the mountains increases, the absolute maximum temperature decreases in winter and becomes negative at Elbrus station (-2...-3°C).

Frequent advection of heat and the influence of the sea determine the positive average monthly air temperature on the Black Sea coast of the Caucasus. The average January temperature in Novorossiysk is +2°С, in Sochi +6.1°С. In Ciscaucasia, the average air temperature is -1...-2°C in the western regions, dropping to -4...-4.5°C in the center and rising again to the Caspian Sea to -2...0°C. In the mountains, the temperature decreases with height, reaching -12 ... -14 ° C in the highlands, in the area of \u200b\u200bperpetual snow and glaciers.

When cold air masses break through from the north, the temperature in Ciscaucasia can drop to -30...-36°C. Even in Anapa absolute minimum is -26°C, and in Sochi - -15°C.

The intensification of cyclonic activity in the cold season causes the winter maximum precipitation on the Black Sea coast of the Caucasus. In the rest of the territory, the maximum precipitation occurs in the summer.

In winter, snow cover sets in on the plains and in the mountains of the Caucasus. It first appears on the plains with relatively warm winter only in the second half of December. In some winters, stable snow cover does not form. Snow falls repeatedly during cooling and melts during thaws. The thickness of the snow cover on the plains is 10-15 cm. On the southwestern slopes of the Greater Caucasus Mountains (Achishkho), due to the abundance of winter precipitation and the decrease in the frequency of winter thaws, the snow thickness reaches 3-4 m. In the mountains of the eastern part of the Caucasus, it is reduced to 1 m (Myachkova N.A., 1983). The number of days with snow cover on the Stavropol Upland is 70-80, decreasing to the west and east of it to 50-40 and increasing in the mountains to 80-110 days due to the long cold period. On the lower border of the highland zone, snow lies 120 days a year.

In the Javakheti-Armenian Highlands, an area of high pressure is formed at this time. From here, the cold continental air of Asia Minor (temperature -12°C) is taken out, penetrating into the middle part of the Riono-Kura corridor, but quickly transforming as it moves east. Colchis is filled with sea air masses of temperate latitudes, coming here with Mediterranean cyclones (t 4-6o). In winter, they constantly cross the Black Sea, where the pressure is low, and, as it were, fall into a trap between the B. and M. Caucasus ranges. The greatest amount of precipitation falls in late summer (August-September), as well as in late autumn - early winter. In other regions of the Caucasus, there is no precipitation at this time, with the exception of the Kuro-Araks lowland. Here, autumn-winter precipitation and partly spring precipitation are associated with a branch of the Iranian polar front, along the line of which cyclonic activity develops. It increases significantly on the slopes of Talysh and along the outskirts of this lowland.

In summer, the formation of the climate in the Caucasus is significantly affected by the frequency of humid Atlantic air masses and dry continental air masses, which form over the spaces of the interior regions of Eurasia and come from the east. In connection with this, the importance of the submeridional climate division (the transverse uplift of the Stavropol Upland - the Central Caucasus) is enhanced. On the Black Sea coast of the Caucasus and in the Western Ciscaucasia, the air warms up to 22-23°C. In the highest parts of the Stavropol Upland and in the Mineralovodchesky region, the average temperature in July is 20-21°C. In the east of Ciscaucasia, the air warms up to 24-25°C. In the mountains, the air temperature decreases with height, reaching 10°C at an altitude of about 2500 m and 7°C at an altitude of 3000 m. At the Elbrus station (altitude 4250 m), the average July temperature is only 1.4°C.

In the first half of summer in Ciscaucasia, the influence of Atlantic cyclones, which determine the June maximum precipitation, increases. Later, the transformation of air masses over the southeast of the Russian Plain increases, therefore, already in the middle of summer, the amount of precipitation decreases, and conditions are often created for the formation of dry winds and droughts, the frequency of which increases in the east.

The annual amount of precipitation increases from the foothills to the mountains and with the rise up the slopes, but at the same time it noticeably decreases when moving from west to east. On the Kuban-Azov lowland, the annual amount of precipitation is 550-600 mm, on the Stavropol Upland it increases to 700-800 mm and decreases to 500-350 mm in the Eastern Ciscaucasia. On the Black Sea coast, the amount of precipitation increases rapidly from north to south (from 700 mm northwest of Novorossiysk to 1650 mm in the Sochi region). In the highlands of the western part of the Greater Caucasus, 2000-3000 mm of precipitation falls, and in the eastern part - only 1000-1500 mm. The amount of precipitation also decreases in the depression between the Rocky and Lateral Ranges, especially in the "shadow" of the Rocky Range, amounting to 650-700 mm. The largest annual amount of precipitation is observed on the windward southwestern slopes of the Greater Caucasus. At the Achishkho station, it is over 3700 mm per year. It - the largest number precipitation not only in the Caucasus, but throughout Russia.

Average annual precipitation: Colchis, southern slope of the Western Caucasus - 1.5-2 thousand mm, Western and Middle Ciscaucasia 450-600 mm, Eastern Ciscaucasia, Terek-Kuma lowland -200-350 mm, Kuro-Araks lowland - 200-300 mm, Javakheti-Armenian highland 450-600 mm, Lankaran lowland - 1200 mm. It is warmest in summer in the Kuro-Araks lowland (26-28°C), in the rest of the territory 23-25°C, in the Javakheti-Armenian Highlands 18°C. However, temperature and precipitation are subject to change depending on the height of the mountains, forming altitudinal climatic zonality. So, the average annual temperature on the Black Sea coast is 12-14°С, in the foothills of the Caucasus it is 7-8°С, at an altitude of 2-3 thousand m -3-0°С. In summer, despite the increase in solar radiation with height, the temperature drops by an average of 0.5-0.6 ° C every 100 m, and by 0.3-0.4 ° C in winter. When climbing the mountains, the average annual positive temperature persists only up to a height of 2300-2500 m. On Elbrus it is -10°C. Similar regularities are preserved for average monthly air temperatures. Thus, the average temperature in January in the Ciscaucasia is -2-7 ° С, in the middle and high mountains - from -8 to -13°C; on Elbrus -19°С; in Novorossiysk 3°С, Sochi 5°С. In July, the temperature is 23-25°С everywhere, at an altitude of 2-2.5 thousand m -18°С, 4000 m -2°С.

The amount of precipitation also changes with altitude. If in the northeastern Ciscaucasia they fall less than 300 m, further to the west 300-400 mm, and in the Western Ciscaucasia 400-500 mm, then already in the low-mountain regions of Stavropol - Nalchik 500-800 mm, at the latitude and height of Vladikavkaz - 800-1000 m (1.5 thousand m), at an altitude of 2 thousand m, an average of 1000-1500 mm; higher the amount of precipitation decreases: Terskol - (3050 m) - 930 mm.

The height of the snow line is 2800-3000 m, in the western part - 3200-3500 m, in the eastern part of the Greater and Lesser Caucasus glaciation is negligible - 3 square meters. km. On B.K. - 1420 km 2, their total- 2200. Of these, 70% is located on the northern slope, 30% - on the southern. Types of glaciers - mountain-valley (20% of the area), cirque and hanging. Glaciation centers - Elbrus, Kazbek, other peaks of the Central Caucasus in M.K. - Aragats, Zangezur ridge, Javakheti ridge. All glaciers are in retreat (10-20 m/year).

The climate and features of the relief of the Caucasus determine its modern glaciation. There are 1498 glaciers in the Caucasus within Russia with total area glaciation 993.6 km 2, which is 70% of the total number of glaciers and the area of glaciation of the Greater Caucasus. The sharp predominance of glaciers on the northern slope is due to orographic features, snow drift westerly winds beyond the barrier of the Dividing Range and somewhat less than on the southern slope, insolation. The snow limit lies at 2800-3200 m in the western part of the Caucasus and rises to 3600-4000 m in the east.

The greatest glaciation is concentrated in the Central Caucasus. The largest massif of modern glaciation is the Elbrus glacial complex (area 122.6 km 2). The two-headed Elbrus is covered with a firn-ice cap about 10 km in diameter, which feeds more than 50 glacial streams radially diverging from it. The largest complex valley glacier in the Caucasus is the Bezengi glacier (length 17.6 km, area 36.2 km 2), located at the foot of the Bezengi wall and feeding the Cherek-Bezengi river. It is followed by the Dykh-Su glaciers (length 13.3 km, area 34.0 km2) and Karaugom (length 13.3 km, area 26.6 km2).

In the Western Caucasus, due to the low height of the mountains, glaciation is small. Its largest areas are concentrated in the Kuban basin near the highest mountain peaks - Dombai-Ulgen, Pshish, etc. The glaciation of the Eastern Caucasus is less significant due to the great dryness of the climate and is mainly represented by small glaciers - cirque, hanging, caro-valley.

The total area of glaciers is 1965 km2. greatest development glaciation reaches between Elbrus and Kazbek, from here it gradually decreases to the west and sharply to the east. The most common car and hanging. 20% - valley glaciers. Everyone regresses.