Geographic distribution of air temperature near the earth's surface. Earth's surface temperature. Air temperature distribution on Earth. What factors determine the temperature distribution

1. What is the thickness of the atmosphere and what gases form it?

The thickness is conventionally 1000 km. Gases: nitrogen, oxygen, argon, carbon dioxide, neon, helium, methane, krypton, hydrogen, xenon.

2. What layers does the atmosphere consist of?

The Earth's atmosphere consists of four layers: troposphere, stratosphere, mesosphere, ionosphere (thermosphere).

3. How are the average monthly and average annual temperatures of the Earth determined?

The average monthly temperature is the arithmetic average of the temperatures of each day, and the average annual temperature is the arithmetic average of the average monthly temperature.

4. What conditions are necessary for the formation of atmospheric precipitation? Can cold air contain a lot of moisture? What air is called saturated with water vapor?

The main condition for the formation of atmospheric precipitation is the cooling of warm air, leading to condensation of the vapor contained in it. The moisture content of the air depends on atmospheric pressure... Cold air, when descending, cannot contain much moisture; when lowering, it compresses and heats up, thereby moving away from the saturation state, becoming drier. Therefore, in areas of increased pressure over the tropics and at the poles, little precipitation falls. Air saturated with water vapor is air in which the vapor content is higher than 75%.

5. What is atmospheric pressure? How does it affect the weather in your area?

Atmospheric pressure - the pressure of the atmosphere on all objects in it and the Earth's surface. It affects the fact that we are in a zone with low pressure and because of this there is precipitation in the Urals.

6. What effect does wind direction have on the weather in your area, and air masses?

The direction of the wind and air masses have a significant impact on the weather in our area, since they are constantly in motion and transfer heat and cold, moisture and dryness from one latitude to another, from oceans to continents and from continents to oceans. The nature of the weather is determined by the descending and ascending air movements.

7. Determine: a) which isotherms cross the 80 z meridian. etc .; b) what are the annual temperatures in the tropical, temperate, polar zones of illumination?

a) Isotherms of –10 ° С, 0 ° С, + 10 ° С, + 20 ° С cross the 80 ° meridian. b) In the tropical zone of illumination, the annual temperature is + 20 ° С, in temperate zones the annual illumination temperature is from + 20 ° С to –10 ° С, in the polar zones of illumination the annual temperature is below –10 ° С.

8. What pattern is confirmed by the card data?

The amount of heat received by the Earth decreases from the equator.

9. On the climatic maps, determine: a) which isotherms of annual temperatures cross the 40th meridian. etc .; b) the average annual temperature in southern Africa; c) the annual precipitation in the Sahara, in the Moscow region, in the Amazon basin.

Isotherms of –10 ° С, 0 ° С, + 10 ° С, + 20 ° С cross the 40th meridian. etc .; b) the average annual temperature in southern Africa is + 20 ° C; c) the annual precipitation in the Sahara is 76 mm, in the Moscow region - 650 mm, in the Amazon River basin - up to 3000 mm.

10. By climate map Australia define: average temperatures in January and July; annual precipitation in the west and east of the mainland; prevailing winds.

The average January temperature in Australia ranges from +20 C to +27 C; average temperature in July +14 C - +18 C; in the west 250 mm, in the east 2,000 mm; westerly winds prevail.

Questions and tasks

1. What is the main reason for the temperature distribution on the Earth's surface?

The closer to the equator, the greater the angle of incidence sun rays, which means that the earth's surface heats up more, which contributes to an increase in the temperature of the surface layer of the atmosphere.

2. What can be learned from climate maps?

Temperature distribution, annual precipitation, prevailing winds.

3. Why is there a lot of precipitation near the equator, and little in tropical regions?

The main reason is the movement of air, which depends on the belts of atmospheric pressure and the rotation of the Earth around its axis. In areas of increased pressure over the tropics and at the poles, little precipitation falls. A lot of precipitation falls in areas where there is low atmospheric pressure.

4. Name constant winds and explain their education. What criteria can be used to group the winds?

The trade winds blow in equatorial belt, since low pressure prevails there, and near the thirties latitudes - high, then at the surface of the Earth winds blow from high-pressure belts to the equator. Westerly winds blow from tropical belts high pressure towards the poles, since 65 s. and y. sh. low pressure prevails. However, due to the rotation of the Earth, they gradually deviate to the east and create an air flow from west to east.

5. What is air mass?

Air mass is a large volume of tropospheric air with homogeneous properties.

6. What is the role of air currents in the distribution of heat and moisture on the Earth's surface?

Constant winds carry air masses from one territory on the Earth's surface to another. The weather, and ultimately the climate of this area, depends on what air mass enters a particular area. Each air mass has its own individual properties: humidity, temperature, transparency, density.

7. What professions are people involved in studying the atmosphere and the processes occurring within it?

Meteorologists, forecasters, climatologists, ecologists.

The air temperature is also influenced by the terrain. The air temperature decreases with altitude (by 0.6 ºC for every 100 m), therefore, mountainous and lowland territories located along the same latitude have unequal average air temperatures. In the mountains, it is significantly lower (see fig. 2).

Rice. 2. Decrease in temperature with height

Summer is coldest on The far north... On some islands in the Arctic Ocean, the average temperatures of the warmest month are 0ºC.

The highest air temperature in July (+ 45ºC), with an average + 24ºC (as at the equator), was recorded at Caspian lowland, in the area of ​​the famous salt lakes Elton and Baskunchak. This territory is located in the south of our country, and in summer it is characterized by a high angle of incidence of sunlight. Low air humidity and cloudless skies increase the proportion of direct radiation. Cool winds from the Atlantic do not reach the territory, but sultry and dry winds from Central Asia often blow, bringing continental tropical air masses. At this time, the most high temperatures air (see fig. 3).

Rice. 3. Factors shaping the climate of the Caspian lowland

The distribution of January temperatures is decisively influenced by atmospheric circulation, i.e., the movement of air masses. Warm in winter time the air of the Atlantic does not allow the European part of the country to cool down. January isotherms in most of the territory of Russia have not sublatitudinal, but submeridional strike: the closer to the Atlantic Ocean, the warmer. In Rostov-on-Don the average January temperatures are -4… -8ºC, in Moscow -8… -12ºC; in Omsk and Yekaterinburg -16… -20º C; in Irkutsk -24… -32º C; in Yakutsk below -40ºC (see fig. 4).

Rice. 4. Average January temperatures in Russia ()

The lowest temperatures are typical for the north-east of Siberia. This territory is remote from the Atlantic Ocean, it is separated from the Pacific Ocean by mountains. In addition, the penetration of Pacific air is hindered by the dominance of high atmospheric pressure here in winter. The settlements of Verkhoyansk and Oymyakon are considered the "poles of cold" in the Northern Hemisphere (see fig. 5).

Rice. 5. Verkhoyansk and Oymyakon - cold poles of the northern hemisphere

V late XIX v. (1892) the lowest air temperature was recorded in Verkhoyansk: -69ºC. No observations were made in Oymyakon that year. However, in other years it was noted that on the coldest nights the air temperature in Oymyakon is about 2ºC lower than in Verkhoyansk. Based on this, it was considered that the absolute minimum temperature is typical for Oymyakon and amounts to 71ºC. Only icy Antarctica competes with northeastern Siberia. At the Vostok station, the absolute minimum air temperature on Earth was recorded - -89.2 ºC (July 21, 1983) (see fig. 6).

Rice. 6. Station "Vostok"

Abnormally low air temperatures in this area are due to the cumulative impact of all climate-forming factors. The territory is located in the Arctic Circle and receives little solar heat in winter. The clear sky due to high atmospheric pressure contributes to additional cooling. Both points are located in intermontane basins, where cold air stagnates. Spatial and temporal coincidence of all conditions led to the formation of the "pole of cold" in the northern hemisphere (see fig. 7).

Rice. 7. Factors shaping the climate of the north-east of Siberia

The distribution of precipitation is mainly influenced by circulation processes and relief. Most of the moisture in the territory of Russia is brought by cyclones Atlantic Ocean... Due to westerly winds and the absence of mountain barriers, they penetrate far to the east. The wet "breath" of the Atlantic is felt up to the Yenisei. From west to east, the amount of precipitation gradually decreases. In St. Petersburg and the Moscow region, the annual precipitation is more than 650 mm; in Samara - no more than 500 mm; in Yakutsk - about 350 mm; and in Verkhoyansk - 128 mm (less than in Baghdad, surrounded by deserts).

Rice. 8. Annual precipitation ()

The largest amount of precipitation is typical for the windward slopes of the mountains. This applies to the western slopes of the Urals, Altai and especially the Greater Caucasus. Much less moisture is brought from the Pacific Ocean. Deep penetration of the Pacific air masses is impeded by the western transport, which prevails in temperate latitudes, and, in addition, by the nature of the relief.

Air masses from the Arctic Ocean can penetrate far to the south. But this is cold, which means dry air. In addition, when moving south, the northern air masses warm up, and their relative humidity becomes even lower - in summer, the penetration of air from the Arctic Ocean to the south causes droughts.

Along with the amount of precipitation is equally important climatic feature is their mode, that is, the distribution over the seasons of the year. In most of the territory of our country, precipitation is unevenly distributed: most of it falls on the warm season, that is, in the summer. The summer maximum precipitation is more distinctly expressed in the Asian part of the country. This is due to the low amount of precipitation in winter due to the dominance of the area of ​​high atmospheric pressure here. (see fig. 9).

Rice. 9. Precipitation of the warm period ()

Summer maximum precipitation is most pronounced in Primorye (Vladivostok); the amount of summer precipitation here is approximately equal to the amount of precipitation for the rest of the seasons.

The eastern coast of Kamchatka and the western slopes are characterized by a relatively uniform distribution of moisture over the seasons. Caucasus mountains... In any of the seasons, at least 200 mm of moisture falls here. These are not only the wettest, but also the snowiest areas of the country.

The place with the maximum annual precipitation is the windward slopes of the Achishkho ridge near Sochi (western slope of the Greater Caucasus), where the annual precipitation is 3240 mm. Moist air is brought in by the Black Sea cyclones. Meeting mountain slopes on its way, the air rises and cools, which contributes to precipitation. These processes are taking place all year round regardless of the seasons, which leads to a relatively uniform distribution of atmospheric moisture throughout the year.

Rice. 10. Achishkho ridge ()

The driest places in Russia are the intermontane basins of Altai (Chuy steppe) and Sayan (Ubsunur basin). The annual amount of precipitation here barely exceeds 100 mm. Moist air does not reach the interior of the mountains. Moreover, sinking along the slopes into the hollows, the air heats up and dries up even more. (see fig. 11 and fig. 12).

Rice. 11. Chuya steppe ()

Rice. 12. Ubsunur Basin ()

Note that places with both minimum and maximum precipitation are located in the mountains. At the same time, the maximum amount of precipitation falls on the windward slopes of mountain systems, and the minimum - in intermontane basins.

Is 300 mm of precipitation a lot or a little? This question cannot be answered unequivocally. This amount of precipitation is typical, for example, for both the northern and southern parts of the West Siberian Plain. At the same time, in the north, the territory is clearly waterlogged, as evidenced by the strong swampiness; and in the south, dry steppes are common - a manifestation of moisture deficit. Thus, with the same amount of precipitation, the moisture conditions turn out to be fundamentally different.

In order to assess whether the climate in a given place is dry or humid, it is necessary to take into account not only the annual precipitation, but also the evaporation.

Evaporation- the amount of moisture that could evaporate under the given temperature conditions. Like precipitation, evaporation is measured in millimeters.

At the same time, the amount of evaporation does not depend on the amount of precipitation. It is determined by the amount of heat that a given territory receives. The higher the air temperature, the more moisture can evaporate.

Lines connecting points with the same volatility on the map are latitudinal. Evaporation can be greater than, equal to, or less than precipitation (see fig. 13).

Rice. 13. Evaporation and volatility ()

The ratio of annual precipitation to evaporation is called humidification coefficient:

K = O / I

K - moisture coefficient

О - annual rainfall

And - volatility

If K> 1 - excessive moisture (tundra, taiga, forests).

If K = 1, moisture is sufficient (forest-steppe and steppe).

If K< 1 - увлажнение недостаточное (полупустыня).

If K< < - увлажнение скудное (пустыня).

The moisture coefficient is the main characteristic of the moisture supply of the territory. It largely determines the features of such natural components as surface water, soil and vegetation cover, and fauna.

Bibliography

1. Geography of Russia. Nature. Population. 1 h. 8 class / V.P. Dronov, I.I. Barinova, V. Ya Rom, A.A. Lobzhanidze.
2. V.B. Pyatunin, E.A. Customs. Geography of Russia. Nature. Population. 8th grade.
3. Atlas. Geography of Russia. Population and economy. - M .: Bustard, 2012.
4. V.P. Dronov, L.E.Savelyeva. UMK (educational-methodical kit) "SPHERES". Textbook “Russia: nature, population, economy. 8th grade". Atlas.

1. No. 3. Distribution of heat and moisture in the territory of Russia. ()
2. Climate-forming factors and atmospheric circulation ()
3. monthly climatic data for Russian cities ()
4. The temperature in Russia is growing 2.5 times faster than in the rest of the world ()
5. New records of negative temperatures were recorded in many regions of Russia ()
6. Temperature maps with region selection ()
7. Precipitation maps with region selection ()

Homework

1. What patterns of heat and moisture exist on the territory of our country?
2. How is the moisture coefficient determined and why is this indicator so important?
3. Using the atlas maps, fill in the table:

Indicators / Item	Kaliningrad		Yekaterinburg
Average temperatures in July
Average January temperatures
Evaporation
Humidification factor

Heat turnover, one of the climate-forming processes, describes the processes of receiving, transferring, transferring and losing heat in the earth-atmosphere system. The peculiarities of heat circulation processes determine the temperature regime of the area. The thermal regime of the atmosphere is primarily due to the heat exchange between the atmospheric air and environment... In this case, the environment is understood to mean outer space, neighboring masses and especially the earth's surface. Crucial to thermal conditions atmosphere has heat exchange with the earth's surface by molecular and turbulent heat conduction.

The distribution of air temperature over the globe depends on general conditions inflow of solar radiation at latitudes ( influence of latitude), from the distribution of land and sea, which absorb radiation in different ways and heat up in different ways ( underlying surface influence), and from air currents carrying air from one area to another ( atmospheric circulation effect).

As follows from Fig. 1.9, the least deviations from latitudinal circles on the map of average annual temperatures for sea level. In winter, the continents are colder than the oceans, in summer they are warmer; therefore, in average annual values, the opposite deviations of the isotherms from the zonal distribution are partially mutually compensated. On the map of the average annual temperature on both sides of the equator - in the tropics there is a wide zone where the average annual temperatures are above + 25 ° C. Inside the zone, heat islands are outlined by closed isotherms above North Africa, India and Mexico, where the average annual temperature is above +28 ° C. There are no heat islands over South America, South Africa and Australia. However, over these continents, the isotherms sag to the south, forming "tongues of heat" in which high temperatures spread further towards high latitudes than over the oceans. Thus, the tropics of the continents are warmer than the tropics of the oceans (we are talking about the average annual air temperature above them).

Rice. 1.9. Distribution of the average annual air temperature at sea level (ºС) (Khromov S.P., Petrosyants M.A., 2006)

In extratropical latitudes, the isotherms deviate less from the latitudinal circles, especially in the Southern Hemisphere, where the underlying surface in the middle latitudes is an almost continuous ocean. In the Northern Hemisphere, at middle and high latitudes, more or less noticeable deviations of isotherms to the south over the continents of Asia and North America are observed. This means that, on average, the continents in these latitudes are somewhat colder than the oceans. The warmest places on the Earth in average annual distribution are observed on the coasts of the southern part of the Red Sea. In Massawa (Eritrea, 15.6 ° N, 39.4 ° E), the average annual temperature at sea level is +30 ° C, and in Hodeidah (Yemen, 14.6 ° N, 42.8 ° E). ) 32.5 ° C. The coldest region is East Antarctica, where in the center of the plateau average annual temperatures are of the order of -50¸-55 ° C (Klimatologiya, 1989).

The temperature decreases from the equator to the poles in accordance with the distribution of the radiation balance earth surface.

The isotherms on the maps do not completely coincide with the latitudinal circles, as well as the isolines of the radiation balance, i.e. are not zoned. They deviate especially strongly from zoning in the Northern Hemisphere, where the influence of the dismemberment of the earth's surface on land and sea is clearly visible. In addition, disturbances in temperature distribution are associated with the presence of snow or ice cover, mountain ranges, and warm and cold ocean currents.

The distribution of temperature is also influenced by the features of the general circulation of the atmosphere, since the temperature in each given place is determined not only by the conditions of the radiation balance in this place, but also by the advection of air from other regions. For example, in the western part of Eurasia, temperatures are higher in winter and lower in summer than in the eastern part, precisely because with the prevailing western direction of air currents from the west, masses of sea air from the Atlantic Ocean penetrate far into Eurasia.

Temperature is a highly variable characteristic of the atmosphere; it changes over time and space. Changes in temperature over time are associated with the diurnal variation of the radiation balance, but the temperature during the day also changes due to the action of other factors, for example, advection of air masses, which causes non-periodic changes in air temperature.

There are certain and significant differences in the heating of the surface layers of soil and water, affecting diurnal variation temperature, as well as the seasonal run. So, the water surface heats up relatively little, but a thick layer of water warms up. The surface of the soil heats up very strongly, but the heat is poorly transferred to the depths. As a result, the ocean gives off a lot of heat at night, while the soil surface is very quickly cooled.

These differences are also reflected in the seasonal variation of the surface temperature. However, seasonal temperature changes are mainly caused by the changing seasons, which is especially evident in the temperate and polar zones. At the same time, during the cold season, the water constantly gives up the accumulated heat (while the soil does not store so much heat), therefore, in the cold season, over the ocean, as well as over areas subject to it direct influence, warmer than over land that is not affected by sea air.

Examining the maps of the long-term average distribution of air temperature at sea level for individual calendar months and for the whole year, we find in this distribution a number of patterns that indicate the influence of geographic factors. This is primarily the influence of latitude. The temperature generally decreases from the equator to the poles in accordance with the distribution of the radiation balance of the earth's surface. This decrease is especially significant in each hemisphere in winter, because near the equator the temperature changes little in the annual cycle, while in high latitudes in winter it is much lower than in summer.

However, the isotherms on the maps do not completely coincide with the latitudinal circles, as well as the isolines of the radiation balance (Figure 6.8). They deviate especially strongly from zoning in the northern hemisphere. This clearly shows the influence of the division of the earth's surface into land and sea. In addition, disturbances in the temperature distribution are associated with the presence of snow or ice cover, mountain ranges, and ocean currents. Finally, the temperature distribution is also influenced by the peculiarities of atmospheric circulation. After all, the temperature in each given place is determined not only by the conditions of the radiation balance in this place, but also by the transfer of air from other regions. For example, the lowest temperatures in Eurasia are found not in the center of the continent, but are strongly shifted to its eastern part... In the western part of Eurasia, temperatures are higher in winter and lower in summer than in the eastern part, precisely because, with the prevailing western direction of air currents from the west, masses of sea air from the Atlantic Ocean penetrate far into Eurasia.

The deviations from latitudinal circles are the smallest on the map of average annual temperatures for sea level. In winter, the continents are colder than the oceans, and in summer they are warmer; therefore, in average annual values, the opposite deviations of the isotherms from the zonal distribution are partially mutually compensated. On the average annual map, we find on both sides of the equator in the tropics a wide zone where the average annual temperatures are above 25 ° C. Inside this zone, heat islands are outlined over North Africa and, less significant in size, over India and Mexico, where the average annual temperature is above 28 ° C. There are no such warm islands over South America, South Africa and Australia; however, over these continents, the isotherms sag to the south, forming "tongues of heat": high temperatures spread here farther towards high latitudes than over the oceans. Thus, in the tropics, on average, the continents are warmer than the oceans (we are talking about the air temperature above them).

In extratropical latitudes, the isotherms deviate less from the latitudinal circles, especially in the southern hemisphere, where the underlying surface in the middle latitudes is an almost continuous ocean. But in the northern hemisphere, we still find in middle and high latitudes more or less noticeable deviations of the isotherms to the south over the continents of Asia and North America. This means that, on average, the continents in these latitudes are somewhat colder than the oceans.

Figure 6.8. Distribution average annual temperature air at sea level

The features of the temperature distribution in January and July also differ significantly (these months are usually used in climatology as a characteristic of winter and summer). Such maps are shown in Figures 6.9 and 6.10.

In January, winter is in the northern hemisphere. The deviations of the isotherms from the zonal direction are significant. Inside the tropics, the temperature varies little with latitude. But outside the tropics in the northern hemisphere, it rapidly decreases towards the pole. Isotherms are very dense here in comparison with the July map. In addition, we find over the cold continents of the northern hemisphere in extratropical latitudes, pronounced troughs of isotherms in the direction to the south, and over warmer oceans - to the north: tongues of cold and warmth.

Especially significant is the deflection of isotherms to the north over the warm waters of the North Atlantic, over the eastern part of the ocean, where the Atlantic Current branch of the Gulf Stream passes. We see here a striking example of the influence of ocean currents on temperature distribution. The zero isotherm in this region of the North Atlantic penetrates even beyond the Arctic Circle (in winter!). The sharp thickening of isotherms off the coast of Norway speaks of another factor - the influence of coastal mountains, behind which cold air accumulates in the depths of the peninsula.

Figure 6.9. Distribution of mean monthly air temperature at sea level in January

Figure 6.10. Distribution of mean monthly air temperature at sea level in July

This enhances the contrast between temperatures over the Gulf Stream and the Scandinavian Peninsula. In the Pacific coast of North America, a similar influence of the Rocky Mountains can be seen. But the thickening of isotherms on the east coast of Asia is mainly associated with the nature of atmospheric circulation: in January, warm air masses from the Pacific Ocean almost do not reach the Asian mainland, and cold continental air masses quickly warm up over the ocean. Over northeast Asia and over Greenland, we even find closed isotherms that outline a kind of cold island. In the first region, between Lena and Indigirka, the average January temperatures reach -50 ° C, this is the region of the Yakut cold pole. The second pole of cold in the northern hemisphere is Greenland.The average January temperature at the terrain level here drops to -55 ° С, and lowest temperatures in the center of the island they apparently reach the same low values ​​as in Yakutia. In the region of the North Pole, the average temperature in winter is higher than in Yakutia and Greenland, since cyclones relatively often bring air masses here from the Atlantic and Pacific oceans.

In the southern hemisphere, it is summer in January. The distribution of temperature in the tropics of the southern hemisphere over the oceans is extremely uniform. But over the continents in South Africa, South America and especially in Australia there are well-defined heat islands with average temperatures up to 34 ° C in Australia. Maximum temperatures reach 55 ° C in Australia. In South Africa, temperatures at the terrain level are not so high due to the significant altitudes of the terrain above sea level: the absolute maximum temperatures do not exceed 45 ° C.

In the extratropical latitudes of the southern hemisphere, the temperature drops more or less rapidly to about the 50th parallel. Then there is a wide zone with uniform temperatures close to 0 ° C, to the very shores of Antarctica. In the depths of the icy continent, the temperature drops to -35 ° C.

In July, summer is in the northern hemisphere. In July, in the tropics and subtropics of the northern summer hemisphere, heat islands with closed isotherms over North Africa, Arabia, Central Asia and Mexico are well-defined.

The air is colder over the oceans than over the continents, both in the tropics and in extratropical latitudes.

It is winter in the southern hemisphere in July and there are no closed isotherms over the continents. The influence of cold currents off the western coasts of America and Africa is also felt in July (tongues of cold). But in general, isotherms are especially close to latitudinal circles. In extratropical latitudes, the temperature drops rather quickly towards Antarctica. In the center of East Antarctica, average temperatures are close to -70 ° С. In some cases, temperatures are observed below -80 ° C, the absolute minimum is below -88 ° C (Vostok station). This is the pole of cold not only for the southern hemisphere, but for the entire globe.

The difference between the average monthly temperatures of the warmest and coldest months is called the annual amplitude of air temperature. In climatology, annual temperature amplitudes are considered, calculated from long-term mean monthly temperatures.

The annual amplitude of air temperature primarily increases with geographic latitude. At the equator, the influx of solar radiation varies very little during the year; towards the pole, the differences in the amount of solar radiation between winter and summer increase, and at the same time the annual amplitude of air temperature also increases. Over the ocean, far from the coast, this latitudinal change in the annual amplitude, however, is not large.

The annual temperature amplitudes over land are much greater than over the sea (as well as daily amplitudes). Even over relatively small continental massifs of the southern hemisphere, they exceed 15 ° С, and at a latitude of 60 ° on the Asian mainland, in Yakutia, they reach 60 ° С (Figure 6.11).

Figure 6.11 Distribution of the average annual amplitude of air temperature

But small amplitudes are also observed in many areas over land, even far from the coastline, if air masses often come there from the sea, for example, in Western Europe. On the contrary, increased amplitudes are also observed over the ocean where air masses from the mainland often fall, for example, in the western parts of the oceans of the northern hemisphere. Therefore, the annual temperature range does not simply depend on the nature of the underlying surface or on the proximity of a given place to the coastline. It depends on the frequency of occurrence in a given place of air masses of sea and continental origin, that is, on the conditions of the general circulation of the atmosphere.

Not only seas, but also large lakes reduce the annual amplitude of air temperature and thus soften the climate. In the middle of Lake Baikal, the annual amplitude of air temperature is 30 - 31 ° C, on its shores about 36 ° C, and under the same latitude on the river. Yenisei 42 ° C.

Usually the climate above the sea, characterized by small annual temperature ranges, is called maritime climate , and the climate over land with large annual temperature ranges is continental... The continentality of the climate should always be borne in mind, especially when climatic characteristic terrain. So, Western Europe characterized by a pronounced maritime climate (the influence of the air masses of the Atlantic). And Siberia, on the contrary, has a continental climate. Sometimes, to characterize continentality, they use the so-called. continental indices.

I am used to the climate in which I live, but still I want maximum warmth in summer, and therefore I am going to the south of the country. In winter, admire the beauty of the snowy nature. In fact, the temperature in different regions the country is very different. If in winter it snows almost everywhere, then in summer, if you move from north to south, the weather changes.

What factors determine the temperature distribution

If we take the entire territory of Russia, then even in regions that are located in the same latitudes, the climate can be very different. Here are the main reasons that affect the temperature distribution on the surface:

• relief features;
• proximity or distance from the sea;
• circulation of air masses;
• distance from the equator.

Here are some examples. Ural mountains trap humid air masses, which are directed from the sea, therefore the climate in Siberia is continental. It's hot in here but short summer and also a harsh and long winter.

The sea on one side and the mountains on the other are the main factors that determine subtropical climate in the south of the Krasnodar Territory.

In general, the climate to the Urals is milder than to the east of these mountains.

How the temperature is distributed on the territory of Russia in summer and winter

Russia is characterized by a clear division of the year into different, pronounced seasons, as well as a large temperature difference.

Speaking in general outline, then the temperature is unevenly distributed. Of course, if you move from south to north, the average annual or monthly temperature drops. If in the south it is hot and sunny all summer, then in the north there are only a few warm days.

For example, Siberia has the largest temperature range in the country, because in summer it can be up to +40, and in winter the same, but with a minus sign. In the north, at the beginning of summer, the thermometer may drop below zero, while in the south they are already swimming in the sea with might and main.

Snow falls almost throughout the country in winter, and only in the south the climate is milder. The harshest climate in the north Of the Far East, where the average January temperature is -46 degrees Celsius.