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The climate of the Eurasian continent. In what climatic zones is Eurasia located?

Eurasia is the largest continent on the planet. The climate of the continent is very diverse. What is causing this? In what climatic zones is the continent of Eurasia located? Let's try to answer all these questions in our article.

Description of the mainland

Three quarters of the world's population live in Eurasia. This is not surprising, because in terms of its size, the mainland is the largest on Earth. It occupies 35% of the earth's land, and its area is about 54 million square meters. km.

The main part of Eurasia belongs to the Northern Hemisphere, while some islands that belong to the mainland are located in the southern half of the planet. In ancient times, two parts of the continent - Europe and Asia - were perceived separately. They were even considered different continents. Now the division between the European and Asian parts of the continent is carried out only conditionally. The boundaries for this are mountains (Ural mountain range), rivers (Emba, Kuma, Manych), seas (Caspian, Black, Mediterranean, Aegean), as well as straits (Gibraltar, Bosphorus, Dardanelles).

The continent is washed by the Atlantic, Pacific, Indian, Arctic oceans. The extreme points of the mainland are the Russian Cape Chelyuskin in the north, the Malaysian Cape Piai in the south. The Portuguese Cape Roca is the extreme point in the west, and in the east is the Russian Cape Dezhnev.

Factors of climate formation in Eurasia

The climatic zones in which Eurasia is located were primarily influenced by: a significant length and geographical location. From north to south, the continent stretched for 8 thousand km, while covering a significant territory.

So, in what climatic zones is Eurasia located? Due to its location between the Arctic Circle and the Equator, all the belts of the Northern Hemisphere are present on the mainland. The elongation of the mainland from west to east is main reason amazing variety of natural and climatic zones.

Relief is an important climate-forming factor. The continent contains some of the world's most extensive plains. Winters are cold in these areas, while summers are hot and dry. Numerous mountain systems of the mainland create barriers to air masses, preventing warm south winds to the north, and cold and dry - to the south.

A significant role in the formation of the Eurasian climate is played by oceanic basins and indented coastlines. Along the edges of the continent, the marine type of climate prevails, in the interior - continental. Warm and cold currents in the oceans affect annual changes in coastal temperatures, as well as the amount precipitation.

In what climatic zones is the territory of Eurasia located?

We found out the main reasons for the formation of climate on the mainland. Now let's talk in more detail about the climatic zones in which Eurasia is located.

Arctic belt. It is located in the extreme north of the mainland, including the islands that are located in the Arctic Ocean. Dry frosty air, biting winds and high Atmosphere pressure- this is typical features arctic climate zone. Air temperatures here throughout the year rarely rise above zero, precipitation is about 250 mm.

subarctic belt. It is distinguished by milder climatic conditions, it acts as a kind of buffer zone between the arctic and temperate zones. It occupies a strip of the northern part of the continent, including Iceland and part of Scandinavia. In summer it is affected moderate winds and the temperature does not exceed +20. In winter, cold arctic winds blow here, the temperature can drop to -50 degrees.

Temperate zone. It runs along the entire continent below the subarctic zone. It occupies most of Europe and Central Asia. Within its boundaries, various types of climate have formed, which largely depend on the proximity to the World Ocean. The seasons clearly follow each other, the temperature fluctuations during the year are very significant.

subtropical belt. It covers China and the Japanese islands, Iran, Armenia, Italy, Greece, etc. Winters are mild, cool and humid, and summers are hot and dry.

Tropical belt. Includes southwestern Asia and absent from Europe. It is characterized by hot summers and very warm winters.

Sat equatorial belt. Covers the Indochina peninsula, the Philippines and the northern part of Sri Lanka. Humid air masses in summer are replaced by dry ones in winter.

equatorial belt. It occupies the southern part of Sri Lanka, the Malay Islands. It is dominated by high temperatures and heavy rainfall, and the winds bring humid sea air.

Conclusion

Most of the Eurasian continent is located in the Northern Hemisphere. This had a significant impact on the climatic zones in which Eurasia is located. So, on the territory of the mainland there are arctic, subarctic, temperate, subtropical, tropical, subequatorial and equatorial belts.

Analysis of meteorological indicators and their changes during the year give an idea of ​​the wide variety of climates within Eurasia. Eurasia lies in all climatic zones of the Northern Hemisphere, and within each zone climatic regions have formed:

arctic belt. The northernmost islands of Eurasia, and in the east the strip of the mainland adjacent to the Arctic Ocean, are within the Arctic zone. In the Arctic belt, a marine arctic climate west of the European sector of the Arctic: Svalbard and small oceanic islands in the western part of the Arctic Ocean. The maritime climate of these islands is due to the influence of the warm North Atlantic Current and is characterized by relatively high winter temperatures (from -16 0 C to -20 0 C) and significant annual precipitation (300 mm). The rest of the territory of this belt has a continental arctic climate. Dry cold arctic air masses dominate here, due to which the entire water area of ​​the Arctic Ocean, without coastal waters, is bound by dense powerful ice throughout the year. The Arctic belt is a supplier of cold air masses to the continent. In all seasons of the year, their movement is directed to the south.

subarctic belt. It stretches in a narrow strip along the entire continent and includes the island of Iceland, part of Scandinavia, located north of the Arctic Circle and, somewhat expanding in the east, goes to the Bering Strait. The subarctic zone is located between the summer and winter positions of the Arctic front and is characterized by the influence of moderate air masses in summer and cold Arctic air masses in summer. winter period. It also has a maritime and continental climate. The first includes Iceland and the islands adjacent to the west of the Scandinavian Peninsula. This type of climate is characterized by relatively mild (-5 0 С - 10 0 С) winters, cool (no more than +10 0 С) summers and from 300 to 700 mm of precipitation in all seasons in the form of rain and snow.

Temperate zone. The southern boundary of this belt is determined by the summer position of the front of temperate latitudes and runs from south coast Bay of Biscay through the middle of the Black and Caspian Seas to the north of the Korean Peninsula and the middle part of the island of Honshu.

Air masses of temperate latitudes dominate in this zone throughout the year. On the territory of Western Europe, in the temperate zone, two subregions are distinguished - northern and southern. The northern subregion includes Fennoscandia and the north of the island of Great Britain (Scotland). The climate here is temperate with cool summers. In the southern subregion the climate is temperate with warm summers. In the northern subregion, two climatic regions are distinguished: an area with a maritime (Norwegian) climate type and an area with a continental (Swedish) climate type. The first region includes Western Scandinavia and Scotland. The climate of this area is characterized by an abundance of precipitation throughout the year, short cool summers. It is dominated by constantly cloudy, damp, windy weather. Climate Swedish - continental formed in continental Scandinavia (Sweden, Finland), characterized by cold, long winters with stable snow cover, short cool summers. The summer maximum is clearly expressed in the annual distribution of precipitation. Against the background of the continental climate, the climate of the fjelds (flat peaks of the Scandinavian mountains) stands out - humid, cold with an average temperature summer months less than +10 o C.

In the southern subregion of the temperate zone of Europe, the following climatic regions are distinguished: an area with a maritime climate, which includes Atlantic Europe, an area with a climate transitional from maritime to continental climate of Eastern Europe and area of ​​continental climate. Against the background of the transitional climate, the climate of the Hercynian middle mountains and the climate of the highlands (Alpine) stand out.

The maritime climate is characterized by mild cold winters (average temperatures winter months positive), moderately warm summer, small annual temperature range, abundance of precipitation, frequent strong winds. Ireland, England, France without the south, the west of the German-Polish Plain, the west of Jutland have this type of climate. The transitional climate from maritime to continental is characterized by negative average temperatures of two to three winter months, short but stable snow cover, relatively hot and humid summers, and clearly defined transitional (spring, autumn) seasons. This type of climate is represented in the east of the German-Polish lowland. The continental climate of the Danube plains is characterized by rather high summer temperatures (+22 0 C, +24 0 C) with little precipitation. In winter, cold continental air masses from the east and north often invade here, causing sharp cooling.

The climate of the mid-altitude mountains is characterized by high humidity relative to the surrounding plains. The slopes of the western exposure receive more precipitation than the opposite - eastern ones. Temperatures are lower in the mountains, and the snow stays for three to five months.

The climate of the Alps is characterized by high humidity, the presence of climatic zones, low temperatures on the tops of mountains and, as a result, the presence of snow and mountain glaciers. On the territory of the rest of Eurasia, the climate is temperate continental (Russian Plain), continental (Western, Central, Eastern Siberia, Central Asia, Central Asia itself) and monsoonal, which covers northeast China, the Korean Peninsula, Hokkaido Island and the northern half of the island of Honshu . In winter, cold and dry continental air dominates here, which comes from the Central Asian baric center. In summer, it is replaced by warm and humid air, which brings here the Pacific monsoon. The maximum precipitation occurs in the summer - from 60 to 70% per annum. Central Asia proper has a continental climate, on the territory of which the center of high pressure and the Central Asian anticyclone are located. Winters are cold and dry, and summers are dry and hot.

subtropical belt also crosses Eurasia from the Atlantic to the Pacific. The whole south of Western Europe is located in this belt, the Western Asian highlands up to 30 0 s. sh., north of the Arabian Peninsula, Tibet and the Yangtze basin. It is characterized by a change in the types of air masses: tropical dry and hot prevail in summer, in summer - wet air temperate latitudes. The Mediterranean climate stands out in this zone, the main features of which are dry and hot summers, mild wet autumns and winters. It is divided into marine and continental. The western windward sections of the peninsulas of the Perinean, Apennine, Balkan have a maritime climate, the rest of the European Mediterranean has a continental climate.

In Asia, within the subtropical climate zone, several types of climate are also distinguished. In the west (the western and southern coasts of Asia Minor and the mountainous west of the Levant) the climate is Mediterranean with hot and dry summers and warm and humid winters. Winter temperatures range from +10 0 С to +12 0 С in the south, from 2 0 С to 3 0 С in the north. Annual precipitation amounts are 500-600 mm on the plains and up to 3000 mm on the windward slopes of the mountains. The continental climate of this belt is characterized by low annual precipitation (from 400 mm in the Anatolian Highlands to 200-100 mm in the Armenian and Iranian Highlands), the maximum of which occurs in autumn and winter, hot and dry summers. This type of climate is characteristic of all the Near Asian highlands up to 30 0 s. sh., Northern Arabia up to 30 0 s. sh. without the west of the Levant. Throughout the year, the continental air of temperate latitudes dominates over the Near Asian highlands. In winter, there is a strong cooling of the surface of these highlands. In summer, this air warms up and acquires the properties of continental tropical. The annual temperature amplitudes are large (up to 90 0).

The territory of Tibet stands out in the high-mountain subregion of the subtropical belt, which is characterized by cold winters with little snow and rather cool and dry (in most of the territory of Tibet) summer. Only in eastern regions Tibet increases the amount of precipitation brought by the Pacific monsoon. Their maximum here is in the summer. In general, the relative humidity of the air in Tibet is very low. The air is dry and cold throughout the year.

In the east, in the Yangtze basin, the climate is monsoonal and humid. In summer, precipitation is brought by the Pacific monsoon, and in winter it rains due to frontal processes. Up to 75% of the annual precipitation occurs in the summer. On the windward slopes falls up to 2000 mm, on the plains - from 700 to 900 mm.

Tropical trade wind climate belt. This belt contains the southern half of Arabia, the south of the Iranian Highlands and the Thar Desert. Continental tropical air prevails here throughout the year. In winter it is dry and warm weather and dry and hot in summer. The daily temperature ranges are large. Precipitation in most areas falls below 100 mm. Only in the mountains of Yemen from 400 mm to 1000 mm. This is a zone of negligible moisture.

Subequatorial belt or otherwise the climate of the equatorial monsoons. On its territory are the Hindustan Peninsula without the Thar Desert, the island of Ceylon without the southwest, the Indochina Peninsula, South China, the Philippine Islands without the south, Mindanao, the islands of the southeast of the Malay Archipelago. In winter, continental dry air is brought here with the trade wind of the northern hemisphere. In summer - humid equatorial air and Indian Ocean monsoon. Winter and spring are dry. The dry season lasts until May-June. Summer and autumn are wet. The hottest time of the year is spring, when the Indus Plain heats up more than the regions of the equator. In April and May, temperatures reach 40 0 ​​C and even up to 52 0 C. On the windward slopes of the Assam Mountains in Cherrakunji, an average of 12666 mm of precipitation falls annually, and on the leeward slope of the same mountains - 1700 mm. But there are areas of this belt that receive only 81 mm per year (the upper reaches of the Indus River).

equatorial belt. Most of the Malay Archipelago (without the eastern half of Java, the Lesser Sunda Islands), the Malay Peninsula, the southwest of Ceylon, and the south of the Philippine Islands are located in this belt. Equatorial air dominates here throughout the year. This belt is characterized by uniform moisture throughout the year with two maxima, heavy precipitation - from 1500 mm to 4000 mm or more (in the mountains), convective rains, and insignificant annual temperature amplitudes (2 0 С - 3 0 С). The average temperatures of the warmest month are 27 0 C - 28 0 C, and the coldest - 25 0 C - 26 0 C. Precipitation prevails over evaporation. Humidification is excessive.

The climatic features of the mainland are determined by its huge size, large extent from south to north (from the equator to the Arctic latitudes), from west to east, as well as the structure of the surface - the presence of high mountain systems in the south and east, the wide distribution of basin relief.

Due to its great length from north to south, Eurasia is located in all climatic zones of the Northern Hemisphere: from the Arctic to the equatorial. The temperate zone occupies the largest areas, because it is in temperate latitudes that the mainland is more elongated from west to east.

In the arctic and subarctic belts, western regions with a maritime climate are distinguished: small temperature amplitudes due to relatively warm winter and cool summers. In the east of the belts, the climate is continental with very cold (down to -40 ... -45 ° C) winters.

Within the temperate zone, climatic conditions are very diverse. The climate of the west coast is maritime, it is formed during the year under the influence of air masses with Atlantic Ocean. Summers are cool, winters are relatively warm even in northern latitudes, for example, on the coast of the Scandinavian Peninsula. Precipitation falls throughout the year. During the passage of cyclones, the weather changes rapidly, in summer there may be cold snaps, in winter thaws.

Some features of the maritime type of climate persist further to the east, almost throughout Europe: weather instability, relatively wet winters. However, with distance from the ocean, the difference between summer and winter temperatures increases: winter becomes noticeably colder. There is more precipitation in summer than in winter. This is an area of ​​transition from maritime to continental climate. Often this type of climate is called temperate continental. Transitional conditions are typical for Central and Eastern Europe.

Beyond the Urals, in Siberia, and Central Asia, winters are very cold and dry; summers are hot and moderately humid. This area has a sharply continental climate.

On the east coast of the mainland, the climate is monsoonal with relatively warm, humid summers and cold, dry winters.

In the subtropical zone on the plains, temperatures are positive throughout the year. There are three climatic regions. In the west - the Mediterranean, where dry tropical air reigns in summer (heat and cloudless), and in winter - sea air of temperate latitudes (precipitation falls).

In the regions of the Asian highlands, the climate is subtropical continental with relatively cold (in places with temperatures below 0 ° C) winters and hot, very dry summers. The total amount of precipitation is small, they fall in the winter-spring period.

In the east of the subtropical zone there is an area of ​​monsoon climate with a typical precipitation regime (summer maximum).

The climatic features of the tropical zone are peculiar. On the Arabian Peninsula, in Mesopotamia, in the south of the Iranian Highlands and in the basin of the lower Indus, continental tropical air masses dominate during the year, very dry and hot. Summers are very hot (average July temperatures are +30°...+35°С), winters are warm (average January temperatures are +18°...+24°С). The amount of precipitation on the plains does not exceed 200 mm, and in some places - below 50 mm per year.

To the east, the tropical belt becomes wedge-shaped. At 10-20°C. sh. it is replaced by a subequatorial belt with a monsoon climate prevailing on the peninsulas of Hindustan, Indochina, in most of the Indo-Gangetic lowland and in the very south of China.

To the south is the equatorial belt. It occupies the Malay Peninsula and the islands of the Malay Archipelago. The climate is the same as in the Amazonian lowlands and in the basin of the Congo River.

In the climate Eurasia shows features associated with the huge size of its territory. The position of the main part of the mainland between the equator and the Arctic Circle, the massiveness of the eastern and central parts, the dissection of the western and southern margins, the influence of ocean basins, and the complex structure of the surface create an exceptional variety of climatic conditions in Eurasia.

Annual total radiation in Eurasia, it varies within the following limits (Fig. 5): on the Arctic islands it is 2520 MJ / m 2 (60 kcal / cm 2), in the western part of Europe - from 2940 to 5880 (from 70 to 140), in the south and south -East of Asia - 5000-7570 (120-180), and in Arabia reaches the maximum value on Earth - 8400-9240 (200-220).

Rice. 5. Total solar radiation per year

The annual radiation balance varies within Eurasia from 420 to 3360 MJ/m 2 (10-80 kcal/cm 2). In January, to the north of the line Brittany - the north of the Adriatic - the center of the Black Sea - the south of the Caspian - the north of the Korean Peninsula - the north of the Japanese Islands, the radiation balance is negative (Fig. 6).

Rice. 6. Radiation balance for the year

Main atmospheric process for most of Eurasia - west-east transport and associated cyclonic activity. With the western transfer to the mainland throughout the year, air enters from the Atlantic Ocean and spreads to its eastern outskirts. As it moves east, the Atlantic air transforms, giving off moisture, cooling in winter and warming up in summer. Due to the large horizontal dissection of the western part of Eurasia and the absence of sharp orographic obstacles, the process of transformation of air masses over Europe is relatively slow, and therefore climatic conditions change gradually. Only beyond the Urals, within Asia, is the predominance of continental air masses observed throughout the year. Sharp contrasts in heating and in pressure conditions between the mainland and the Pacific Ocean, intensified by the peculiarities of the orography of Central and East Asia, determine the monsoon circulation typical of the east of Eurasia, which is most pronounced here in comparison with all other regions of the Earth. The circulation over the southern parts of Eurasia also has a monsoon character, only here it manifests itself in the interaction between the mainland and the Indian Ocean.

Consider how meteorological conditions change in Eurasia by season.

in winter the contrasts in heating and pressure distribution over the mainland, on the one hand, and the Atlantic and Pacific oceans, on the other, are especially pronounced. The January isobar maps over Eurasia and neighboring oceanic basins clearly show the following baric regions ( rice. 7).

Rice. 7. Air pressure and winds in January

In the northern part of the Atlantic Ocean there is a closed area of ​​low pressure(North Atlantic, or Icelandic, low), due to the influence of the warm North Atlantic Current and the frequent passage of deep cyclonic depressions moving from the coast North America to the East. Due to the influence of the warm current and the deep penetration of sea basins into the interior of the continent, the reduced pressure also extends to the southern part of the Arctic Ocean and the western coast of Europe.

The boundaries of the greatest distribution of floating ice (in March, April - for the northern hemisphere, in September for southern hemisphere) Areas for which the values ​​of the radiation balance have not been determined: mountainous areas continental ice lakes and seas areas with sea

To the south, 30° N, there is high pressure area(North Atlantic, or Azores, maximum), which is part of the subtropical high pressure zone of the northern hemisphere. The interaction of these baric regions is of particular importance for the formation of meteorological conditions in Europe. The air flowing along the northern and eastern periphery of the North Atlantic High is drawn into the region reduced pressure over the North Atlantic and the western margin of Europe, creating in temperate latitudes a system of cyclonic winds of the western and southwestern direction, blowing from the relatively warm ocean to the mainland and bringing a lot of moisture. In the polar latitudes, winds with an easterly component prevail at this time. The main routes of movement of cyclonic depressions in winter pass through Iceland, the Scandinavian Peninsula and the Barents Sea. Over the waters of the Mediterranean Sea, which accumulate a large amount of heat, local cyclogenesis develops in winter. Most often, cyclones form over the Ligurian Sea and the Gulf of Lion, over the southern part of the Tyrrhenian Sea and the island of Cyprus. From here they head east and northeast, penetrating in some years up to the Indus Valley.

Passage of cyclones in Europe it is accompanied by cloudy weather with rain or sleet, typical of the Western European winter. Often the sea air of temperate latitudes is replaced by arctic air, causing a sharp decrease in temperature and a decrease in precipitation. Arctic air spreads to the south, but relatively rarely penetrates into the southern part of Europe, as it is delayed by sublatitudinally located mountain ranges. The farther to the east, the more frequent and longer the arctic air intrusions.

When driving western air flow over the continent is its cooling and drying. In the interior of Asia, in connection with the cooling of the surface layers of the atmosphere, an area of ​​increased pressure is created, above which a hollow is formed in the upper troposphere. Transformed air coming from the west is drawn into this hollow, cools and settles, replenishing the high pressure area in the surface layers. The influence of the relief of the inner parts of Asia also has an effect: high mountain structures rising south of the maximum formation region prevent the spread of cold air masses and contribute to their concentration in a relatively limited space. As a result of the interaction of all these processes, the largest high-pressure area on Earth, the Asian quasi-stationary maximum, is created over the interior of Eurasia in winter.

Along the northern and eastern periphery of this maximum, cold and dry continental air flows towards the Pacific Ocean, which is warmer at this time. The resulting northerly and northwesterly winds are known as the winter monsoon.

Asian High can form a spur, which sometimes extends as far as Western Europe, causing severe cooling there.

Southern Asia in winter it is under the influence of the trade wind circulation. The Arabian Peninsula, together with the neighboring Sahara, is influenced by the eastern periphery of the North Atlantic High and the dry northern winds associated with it. Over Hindustan and Indochina, on the island of Sri Lanka, the Philippines and in the north of the Sunda Islands, the northeast trade wind dominates, flowing from the North Pacific maximum towards the equatorial trough, shifted to the south at this time. In the countries of South and Southeast Asia, it is called the winter monsoon.

Despite the negative radiation balance north of 39-40° N, in areas, adjacent to the Atlantic Ocean, the average January temperature is much higher than 0 ° C, since in winter the Atlantic air is a relatively warm air mass. The January isotherms extend submeridionally over most of the temperate zone of Eurasia and take a sublatitudinal direction only to the east of the Yenisei (Fig. 8).

Rice. eight. average temperature air in Eurasia at the level earth's surface(January)

off the west coast In the Scandinavian Peninsula, the zero isotherm of January rises up to 70° N, fixing the highest positive anomaly of mid-latitude winter temperatures (over 20°). The farther to the east, the lower the average winter temperature becomes. Already in the eastern part of foreign Europe, it acquires a negative value.

Atlantic air brings a large amount of moisture to land, which falls in the west of Europe in the form of rain or sleet. Especially a lot of precipitation occurs on the mountain slopes of the western exposure. Winter cyclonic precipitation is also characteristic of the Mediterranean coast and the western regions of Asia. Their number sharply decreases from west to east due to the weakening of frontal activity in the inner parts of the continent.

In most of overseas Asia in winter precipitation missing. In the interior, this is due to the anticyclonic state of the atmosphere and strong supercooling of the surface. On the eastern edge of the mainland, the reason for the lack of precipitation is the continental monsoon, which carries dry cold air towards the ocean. In this regard, Central and East Asia is characterized by low winter temperatures with a pronounced negative anomaly, which is felt up to the tropic, where temperatures can drop to 0 °C. In the north, the average January temperature is -20, -25 °С.

In the southern peninsulas and islands of Asia, where trade winds operate in winter, dry weather also prevails. Precipitation occurs only in those areas where the trade winds or northern winds bring enough moisture (windward slopes of the Philippine Islands, the southeastern tip of Hindustan and the islands of Sri Lanka). On the Sunda Islands, located on the equator and south of it, convective rain falls. The January temperature in the entire southern part of Asia is high: 16 ... 20 ° C, on the islands of the Malay Archipelago it reaches 25 ° C in places.

Summer meteorological conditions in Eurasia and its neighboring oceans are changing significantly. The Asian maximum disappears, and a low pressure is established over the warmed continent with a closed center in the Indus River basin and on the shores of the Persian Gulf (South Asian minimum). It is the northern margin of the equatorial trough, which in Eurasia extends farthest from the equator (up to 22-28° N). The pressure rises towards the oceans. The Iceland Low is weakening and the North Pacific Low is disappearing. An area of ​​high pressure persists over the polar basin. The North Atlantic and North Pacific highs intensify and widen to the north. In the Indian Ocean, south of the tropic, the South Indian High grows in the winter season of the southern hemisphere. This distribution of pressure in the surface layers of the atmosphere creates conditions for the transfer of air masses to Eurasia from the surrounding oceans ( rice. 9).

Rice. 9. Air pressure and winds in July

In the northwest of Europe, between the area of ​​high pressure in the Arctic and the spur of the North Atlantic High, there is a band of relatively low pressure. Cyclonic activity associated with the Arctic front takes place within its limits. In this regard, western and northwestern winds prevail, which carry relatively cold air from the ocean to the mainland. Over the warmed mainland, it quickly transforms into a continental one. At the same time, the marine Arctic masses are undergoing transformation. This increases not only the temperature, but also the moisture content of the air due to evaporation from the underlying surface. July isotherms in Europe extend sublatitudinally everywhere, with a slight deviation to the south near the coast of the ocean. The average July temperature in the west varies from north to south from 12 to 24 °С, in the east it sometimes reaches 26...28 °С (Fig. 10).

Rice. 10. Average air temperature in Eurasia at ground level (July)

Summer in Europe rains are less plentiful than in winter, as cyclonic activity weakens. AT Southern Europe and Western Asia, where winds blow from the eastern periphery of the North Atlantic High, carrying tropical air, there is almost no precipitation.

Ascending the average July temperature and a decrease in precipitation due to the transformation of the Atlantic air when moving from west to east is felt almost throughout the mainland. It is especially dry and hot in the inner parts of the mainland (Central Asia), protected by mountain rises from moist air currents from the oceans. Dryness and high temperatures (average July up to 32 ° C) are also characteristic of most of the Arabian Peninsula, which is under the influence of the northeast trade wind flowing from the North Atlantic High.

In other conditions are eastern and southern suburbs mainland adjacent to the Pacific and Indian oceans. The temperature and baric contrasts between them and the vast landmass of Eurasia are especially strong in summer. Humid and relatively cold air enters Asia along the western periphery of the Pacific High. As a result of its interaction with continental air masses, heavy rain showers fall. This air current is called the summer monsoon in East Asia.

In the south of Asia(Indostan, Indochina) the role of the summer monsoon is played by the flow of equatorial air, carrying huge masses of moisture from the Indian Ocean. Due to the configuration and size of Eurasia and the expansion of the equatorial trough, the equatorial air in the form of a monsoon of the prevailing southwesterly direction penetrates very far to the north. Where the monsoon flow meets mountain uplifts, precipitation is especially abundant (for example, on the southeastern slopes of the Himalayas, on the southern slope of the Shillong massif, Cherrapunji has a maximum amount of precipitation on the globe- 10719 mm per year, etc.). On equatorial islands, convective intramass precipitation is of great importance (Fig. 11).

Rice. 11. Average annual precipitation in Eurasia, mm

in the Pacific and Indian Oceans Every year from June to November, tropical cyclones, or typhoons, are born, bringing great disasters to the population of the countries of East and South Asia. These are the strongest cyclonic eddies, the speed of which over the open ocean in exceptional cases can reach 100 km/h (usually 30-50 km/h). They are accompanied by downpours, during which 150 mm of precipitation or more can fall. On the coasts, surge waves pose a great threat, which, together with showers, cause catastrophic floods. The Philippines and the Japanese islands are especially affected by typhoons, but sometimes the disaster also captures the outskirts of the continent right up to the south. Far East. In the Indian Ocean, tropical cyclones move north and northwest to the northern coasts of the Bay of Bengal and the Arabian Sea.

According to its size and geographical position, Eurasia with the islands adjacent to it is located in all climatic zones of the northern hemisphere, and within each zone all the climatic regions inherent in it are represented. Thus, we can say that in Eurasia there are all types of climates known on Earth.

northernmost islands Eurasia, and in the east and the strip of the mainland adjacent to the Arctic Ocean, are located within the Arctic belt. Of the foreign territories of Eurasia, the Arctic climate is typical for the Svalbard archipelago and small oceanic islands. Due to the geographical position and the influence of warm currents, the islands have a maritime arctic climate with relatively high winter temperatures (from -16 to -20 ° C) and a significant amount of precipitation (about 300 mm).

In a narrow strip, capturing Iceland and Scandinavia north of the Arctic Circle and expanding somewhat in the east, it crosses Eurasia subarctic belt. It is located between the summer and winter positions of the Arctic front and is characterized by the predominance of westerly circulation in summer and cold eastern Arctic winds in winter. In the west of Europe, especially in Iceland, the subarctic regions are characterized by relatively mild (-5, -10 °С) winters, cool (not more than 10 °С) summers and a large amount of precipitation (300-700 mm) falling in all seasons in the form of rain and snow.

The widest and most massive part of Eurasia lies within temperate climate zone, whose southern boundary, determined by the summer position of the polar front, runs from the southern coast of the Bay of Biscay through the middle of the Black and Caspian Seas to the northern part of the Korean Peninsula and the middle part of the island of Honshu. Despite the dominance of the west-east transfer throughout the year, the temperate zone within Eurasia is characterized by large differences in climatic conditions, which gives reason to consider it by region.

Region oceanic temperate warm climate includes the south of Iceland, the western outskirts of the Scandinavian Peninsula, the British Isles and the extreme west of the mainland - the Jutland Peninsula, the west and north of France. There are reasons to attribute the northwest of the Iberian Peninsula to this region of the temperate zone. Throughout the year, the Atlantic air, brought by the western winds, prevails there, and cyclonic activity is manifested. Winter is characterized by unstable rainy and foggy weather with an average temperature of the coldest month from 1 to 6 ° C, frosts and snowfalls are rare, and there is no stable snow cover. The average summer temperature is 10 ... 18 "C. Precipitation falls throughout the year, with a maximum in winter due to especially intense cyclonic activity. Annual precipitation in almost the entire region is more than 1000 mm, and evaporation does not exceed 800 mm per year. Therefore the Atlantic regions of Europe are characterized by excessive moisture ( rice. 12).

Rice. 12. The difference in precipitation and evaporation for the year

The climate of the rest of the temperate zone of Europe up to Ural mountains can be called transitional, from oceanic to continental. The most important role in climate formation belongs to the transformation of the Atlantic air and the ever-increasing influence of continental air masses that form over the mainland itself. Compared to the previous one, this area is characterized by less precipitation, large amplitudes of temperature fluctuations, and the presence of a frosty period of various durations. Within the area under consideration, more than in the previous one, differences between north and south are expressed. Scandinavia and Finland are characterized by long and severe winters. The Scandinavian mountains enhance the transformation of the Atlantic air and at the same time do not prevent the penetration of cold air masses from the Arctic. Therefore, the temperature in Sweden and Finland can drop to -40 °C, and in exceptional cases even to -50 °C, with an average January temperature of -10, -15 °C. Summer north of the 50th parallel is cool, with maximum precipitation at its beginning. Annual rainfall of 500 to 1000 mm with evaporation less than 600 mm provides excessive moisture throughout the year. The southern part of the region is characterized by less sharp temperature amplitudes, moderately cold winters with an average January temperature only slightly below 0 °C. The duration of snow cover and freeze-up on the rivers is short, it increases from west to east. Summer is warm, with an average July temperature of 12...20 °C. The maximum precipitation occurs in the first half of summer, evaporation increases to 800 mm, and moisture decreases compared to the northern regions.

A significant part of Asia within Russia, the countries of Central Asia, as well as Mongolia and Northwestern China (Gobi and Dzungaria) are located in the region continental climate temperate zone, which is under the influence of inland air masses all year round. Due to the influence of the Asian High, the region is characterized by cold winters with sharp temperature differences from place to place. With an average January temperature from -3 °С in the west of China to -12 °С in the north of Kazakhstan and -25 °С in Mongolia, in calm and cloudless weather, there are drops to -35 ... -50 °С. Due to persistent low winter temperatures and the almost complete absence of snow, permafrost develops in the eastern regions of the region. Almost the entire annual amount of precipitation (about 200 mm) falls in summer in the form of frontal rains. The average July temperature reaches 30 °C in the south of the region. Humidification is insufficient.

East of the Greater Khingan Range, including Northeast China, northern Korean Peninsula, Hokkaido and northern Honshu, climate monsoonal. This whole area is characterized by sharp differences in temperature, precipitation and moisture according to the seasons of the year. In winter, dry frosty weather prevails with strong winds blowing from the Asian High and raising a lot of dust. Only on the Japanese islands do heavy snows fall, since the continental air, passing over the relatively warm Sea of ​​Japan, is saturated with moisture in the lower layers. In summer, the southeast monsoon blows, bringing humid unstable air from the southern and western periphery of the Pacific anticyclone. Approximately 70% of the annual amount of precipitation is associated with its arrival, falling in the form of showers at intervals of 4-5 days.

Subtropical the climatic zone also crosses Eurasia from the Atlantic to the Pacific. Within its limits, the west-east transfer in summer is replaced by tropical circulation. Of great importance is the system of mountain uplifts of High Asia, which in winter causes the splitting of the western transport stream into two branches - northern and southern. The latter passes south of the Himalayas, causing, according to G. N. Vitvitsky, a shift in comparison with other continents of the southern border of the subtropical belt in the direction of the equator.

The Iberian and Apennine Peninsulas, the south and west of the Balkan Peninsula, the west and south of Asia Minor, the eastern coast of the Mediterranean Sea, the Mediterranean islands, the south of the Crimean Peninsula and the north of Mesopotamia are in a subtropical climate with a dry summer ( Mediterranean). Summer dryness is associated with winds flowing along the eastern periphery of the extended North Atlantic High. The prevailing wind direction is northwest in the Western Mediterranean and northeast in the East. The average temperature in July is from 23 to 28 °C. At almost total absence precipitation volatility is 3-4 times higher than the actual evaporation. In winter, the Azores High shifts to the south and the Mediterranean falls into a system of westerly transport and cyclonic activity, with which 75-80% of the annual precipitation is associated. The average temperature of the coldest month increases from north to south from 4 to 12 °C. In the western part of the region of the Mediterranean climate, Atlantic air is predominant, in the east - continental. Therefore, when moving from west to east, the amount of precipitation decreases and the temperature amplitudes increase.

Inside the mainland, from the Iranian Plateau to the middle Huang He basin, including the Tarim Basin, Beishan, the south of the Gobi and other areas of the Central and Central Asia, climate subtropical continental. This area is characterized by hot summers (25...35 °C) and cool winters with an average temperature above 0 °C, although in some years frosts can reach -20 °C. Precipitation is less than 200 mm per year, the air is very dry, the daily and annual temperature amplitudes are significant. In the rainfall regime, there are differences between west and east. In the west, winter precipitation is associated with the Iranian branch of the polar front and cyclonic activity. The east is dominated by summer precipitation brought by the southeast monsoon.

Special, extracontinental The climate of the highlands is characteristic of the interior regions of Asia (Tibet), which can be attributed to the subtropical zone only by geographical location, and not by actual climatic conditions. Due to the significant absolute heights, temperatures do not rise above 10 ... 15 ° C even in summer, in winter these areas are characterized by the same negative temperatures. The amount of precipitation, even in the most humid areas, does not exceed 500 mm per year, and in some places decreases to 100-150 mm, which causes aridity of the climate.

The climate of the eastern sector of the subtropical zone, as well as the temperate one, monsoonal. It extends to the Yangtze River basin and the southern part of the Japanese Islands. From the monsoon climate of the temperate zone, the subtropical monsoon climate is distinguished by a higher average winter temperature (from 4 to 8 ° C) and large annual precipitation, which exceeds 1000 mm and completely covers the evaporation rate. Winter dryness south of the Yangtze River valley is less pronounced than north of it, since there a front is created between the air flowing along the eastern periphery of the Asian high and the air of the southern branch of the western transport, and therefore rain falls. When the front breaks and the invasion of cold continental air to the south, up to the tropic, the temperature can drop to 0 °C. Noteworthy are the differences in winter conditions in the Mediterranean region and the Yangtze basin. In the first case, due to the direct influence of the Atlantic air, the winter is very warm with an average temperature of the coldest month from 10 to 12 ° C, in the second, the average January temperature is almost twice as low, and significant drops are possible. This is due to the influence of the Asian high, the air of which is carried far to the south. In this regard, the southern border of the subtropical belt in East Asia has shifted almost to the tropic.