Thermal balance of atmosphere and surface. Earth's heat balance Earth's heat balance of the atmosphere
The difference between absorbed solar radiation and effective radiation is the radiation balance, or residual radiation of the earth's surface (B). The radiation balance, averaged over the entire surface of the Earth, can be written as the formula B = Q * (1 - A) - E eff or B = Q - R k - E eff. Figure 24 shows the approximate percentage of different types of radiation involved in the radiation and heat balance. It is obvious that the surface of the Earth absorbs 47% of all the radiation that has arrived on the planet, and the effective radiation is 18%. Thus, the radiation balance, averaged over the surface of the entire Earth, is positive and amounts to 29%.
Rice. 24. Scheme of radiation and heat balances of the earth's surface (according to K. Ya. Kondratiev)
The distribution of the radiation balance over the earth's surface is highly complex. Knowledge of the patterns of this distribution is extremely important, since under the influence of residual radiation the temperature regime of the underlying surface and the troposphere and the Earth's climate as a whole are formed. Analysis of maps of the radiation balance of the earth's surface for the year (Fig. 25) leads to the following conclusions.
The annual sum of the radiation balance of the Earth's surface is almost everywhere positive, with the exception of the ice plateaus of Antarctica and Greenland. Its annual values zonally and regularly decrease from the equator to the poles in accordance with the main factor - total radiation. Moreover, the difference in the values of the radiation balance between the equator and the poles is more significant than the difference in the values of the total radiation. Therefore, the zonality of the radiation balance is very pronounced.
The next regularity of the radiation balance is its increase during the transition from land to the ocean with discontinuities and mixing of isolines along the coast. This feature is better expressed in the equatorial-tropical latitudes and gradually smoothes out to the polar ones. The greater radiation balance over the oceans is explained by the lower water albedo, especially in the equatorial-tropical latitudes, and the reduced effective radiation due to the lower temperature of the Ocean surface and the significant moisture content of the air and cloudiness. Due to the increased values of the radiation balance and the large area of the Ocean on the planet (71%), it is he who plays the leading role in the thermal regime of the Earth.And the difference in the radiation balance of the oceans and continents determines their constant and deep mutual influence on each other at all latitudes.
Rice. 25. Radiation balance of the earth's surface for the year [MJ / (m 2 X year)] (according to S. P. Khromov and M. A. Petrosyants)
Seasonal changes in the radiation balance in the equatorial-tropical latitudes are small (Fig. 26, 27). This results in small fluctuations in temperature throughout the year. Therefore, the seasons of the year are determined there not by the course of temperatures, but by the annual rainfall regime. In extratropical latitudes, there are qualitative changes in the radiation balance from positive to negative values during the year. In summer, over vast expanses of temperate and partly high latitudes, the values of the radiation balance are significant (for example, in June on land near the Arctic Circle they are the same as in tropical deserts) and its fluctuations in latitudes are relatively small. This is reflected in the temperature regime and, accordingly, in the weakening of the interlatitudinal circulation during this period. In winter, over large expanses, the radiation balance is negative: the line of zero radiation balance of the coldest month passes over the land approximately along 40 ° latitude, over the oceans - along 45 °. Different thermobaric conditions in winter lead to the activation of atmospheric processes in temperate and subtropical latitude zones. The negative radiation balance in winter in temperate and polar latitudes is partly compensated by the influx of heat with air and water masses from the equatorial-tropical latitudes. In contrast to low latitudes in temperate and high latitudes, the seasons of the year are determined primarily by thermal conditions that depend on the radiation balance.
Rice. 26. Radiation balance of the earth's surface for June [in 10 2 MJ / (m 2 x M es.) |
In the mountains of all latitudes, the distribution of the radiation balance is complicated by the influence of height, duration of snow cover, insolation exposure of slopes, cloudiness, etc. In general, despite the increased values of total radiation in the mountains, the radiation balance is lower there due to the albedo of snow and ice, an increase in the proportion of effective radiation and other factors.
The Earth's atmosphere has its own radiation balance. The arrival of radiation into the atmosphere is due to the absorption of both short-wave solar radiation and long-wave terrestrial radiation. Radiation is consumed by the atmosphere with counter radiation, which is completely compensated by terrestrial radiation, and due to outgoing radiation. According to experts, the radiation balance of the atmosphere is negative (-29%).
In general, the radiation balance of the Earth's surface and atmosphere is 0, i.e., the Earth is in a state of radiative equilibrium. However, the excess of radiation on the Earth's surface and the lack of it in the atmosphere make one ask the question: why, with an excess of radiation, the Earth's surface does not incinerate, and the atmosphere, with its deficiency, does not freeze to a temperature absolute zero? The fact is that between the surface of the Earth and the atmosphere (as well as between the surface and deep layers of the Earth and water) there are non-radiative methods of heat transfer. The first one is molecular thermal conductivity and turbulent heat transfer (H), during which the atmosphere is heated and heat is redistributed in it vertically and horizontally. The deep layers of the earth and water are also heated. The second is active heat exchange, which occurs when water passes from one phase state to another: during evaporation, heat is absorbed, and during condensation and sublimation of water vapor, the latent heat of vaporization (LE) is released.
It is non-radiative methods of heat transfer that balance the radiation balances of the earth's surface and atmosphere, bringing both to zero and preventing overheating of the surface and supercooling of the Earth's atmosphere. The earth's surface loses 24% of radiation as a result of water evaporation (and the atmosphere, respectively, receives the same amount due to subsequent condensation and sublimation of water vapor in the form of clouds and fogs) and 5% of radiation when the atmosphere is heated from the earth's surface. In total, this amounts to the very 29% of radiation that is excessive on the earth's surface and which is lacking in the atmosphere.
Rice. 27. Radiation balance of the earth's surface for December [in 10 2 MJ / (m 2 x M es.)]
Rice. 28. Components of the heat balance of the earth's surface in the daytime (according to S. P. Khromov)
The algebraic sum of all incomes and expenditures of heat on the earth's surface and in the atmosphere is called the heat balance; the radiation balance is thus the most important component of the heat balance. The equation for the heat balance of the earth's surface has the form:
B – LE – P±G = 0,
where B is the radiation balance of the earth's surface, LE is the heat consumption for evaporation (L is the specific heat of evaporation, £ is the mass of evaporated water), P is the turbulent heat exchange between the underlying surface and the atmosphere, G is the heat exchange with the underlying surface (Fig. 28). The loss of surface heat for heating the active layer during the day and summer is almost completely compensated by its flow back from the depths to the surface at night and in winter, therefore, the average long-term annual temperature of the upper layers of soil and water of the World Ocean is considered constant and G for almost any surface can be considered equal to zero. Therefore, in the long-term conclusion, the annual heat balance of the land surface and the World Ocean is spent on evaporation and heat exchange between the underlying surface and the atmosphere.
The distribution of heat balance over the Earth's surface is more complex than that of radiation due to numerous factors affecting it: cloudiness, precipitation, surface heating, etc. At different latitudes, the heat balance values differ from 0 in one direction or another: at high latitudes it negative, and in low - positive. The lack of heat in the northern and southern polar regions is compensated by its transfer from tropical latitudes mainly with the help of ocean currents and air masses, thereby establishing thermal equilibrium between different latitudes of the earth's surface.
The heat balance of the atmosphere is written as follows: –B + LE + P = 0.
It is obvious that the mutually complementary thermal regimes of the Earth's surface and atmosphere balance each other: all solar radiation entering the Earth (100%) is balanced by the loss of Earth's radiation due to reflection (30%) and radiation (70%), therefore, in general, thermal The balance of the Earth, like the radiation one, is equal to 0. The Earth is in radiant and thermal equilibrium, and any violation of it can lead to overheating or cooling of our planet.
The nature of the heat balance and its energy level determine the features and intensity of most of the processes occurring in the geographic envelope, and above all the thermal regime of the troposphere.
The source of heat and light energy for the Earth is solar radiation. Its value depends on the latitude of the place, since the angle of incidence of the sun's rays decreases from the equator to the poles. The smaller the angle of incidence of the sun's rays, the large surface a beam of solar rays of the same cross section is distributed, and therefore there is less energy per unit area.
Due to the fact that during the year the Earth makes 1 revolution around the Sun, moving, maintaining a constant angle of inclination of its axis to the plane of the orbit (ecliptic), seasons of the year appear, characterized by different surface heating conditions.
On March 21 and September 23, the Sun is at its zenith under the equator (equinoxes). On June 22, the Sun is at its zenith over the Northern Tropic, on December 22 - over the Southern. Light zones and thermal zones are distinguished on the earth's surface (according to the average annual isotherm + 20 ° C, the boundary of the warm (hot) zone passes; between the average annual isotherms + 20 ° C and the isotherm + 10 ° C there is a temperate zone; according to the isotherm + 10 ° C - the boundaries cold belt.
The sun's rays pass through the transparent atmosphere without heating it, they reach the earth's surface, heat it, and the air is heated from it due to long-wave radiation. The degree of heating of the surface, and hence the air, depends primarily on the latitude of the area, as well as on 1) height above sea level (as it rises, the air temperature decreases by an average of 0.6ºС per 100 m; 2) features of the underlying surface which can be different in color and have different albedo - the reflective ability of rocks. Also, different surfaces have different heat capacity and heat transfer. Water, due to its high heat capacity, heats up slowly and slowly, while land is vice versa. 3) from the coasts to the depths of the continents, the amount of water vapor in the air decreases, and the more transparent the atmosphere, the less sunlight is scattered in it by water drops, and more sunlight reaches the Earth's surface.
The totality of solar matter and energy entering the earth is called solar radiation. It is divided into direct and scattered. direct radiation- a set of direct sunlight penetrating the atmosphere with a cloudless sky. scattered radiation- part of the radiation scattered in the atmosphere, while the rays go in all directions. P + P = Total radiation. Part of the total radiation reflected from the Earth's surface is called reflected radiation. Part of the total radiation absorbed by the Earth's surface is absorbed radiation. Thermal energy moving from the heated atmosphere to the surface of the Earth, towards the flow of heat from the Earth is called the counter radiation of the atmosphere.
Annual amount of total solar radiation in kcal/cm 2 year (according to T.V. Vlasova).
Effective Radiation- a value expressing the actual transfer of heat from the Earth's surface to the atmosphere. The difference between the radiation of the Earth and the counter radiation of the atmosphere determines the heating of the surface. Radiation balance directly depends on effective radiation - the result of the interaction of two processes of arrival and consumption of solar radiation. The amount of balance is largely affected by cloudiness. Where it is significant at night, it intercepts the long-wave radiation of the Earth, preventing it from escaping into space.
The temperature of the underlying surface and surface layers of air and the heat balance directly depend on the influx of solar radiation.
The heat balance determines the temperature, its magnitude and change on the surface that is directly heated by the sun's rays. When heated, this surface transfers heat (in the long-wave range) both to the underlying layers and to the atmosphere. The surface itself is called the active surface.
The main components of the heat balance of the atmosphere and the surface of the Earth as a whole
|
Indicator |
Value in % |
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Energy coming to the Earth's surface from the Sun |
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Radiation reflected by the atmosphere into interplanetary space, including 1) reflected by clouds 2) dissipates |
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Radiation absorbed by the atmosphere, including: 1) absorbed by clouds 2) absorbed by ozone 3) absorbed by water vapor |
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Radiation reaching the underlying surface (direct + diffuse) |
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From it: 1) is reflected by the underlying surface outside the atmosphere 2) is absorbed by the underlying surface. |
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From it: 1) effective radiation 2) turbulent heat exchange with the atmosphere 3) heat consumption for evaporation |
In the diurnal course of surface temperature, dry and devoid of vegetation, on a clear day, the maximum occurs after 14:00, and the minimum occurs around the time of sunrise. Cloudiness, humidity and surface vegetation can disrupt the daily course of temperature.
Daytime maxima of land surface temperature can be +80 o C or more. Daily fluctuations reach 40 o. The values of extreme values and temperature amplitudes depend on the latitude of the place, season, cloudiness, thermal properties of the surface, its color, roughness, nature of the vegetation cover, slope orientation (exposure).
When heated, the surface transfers heat to the soil. Time is spent on the transfer of heat from layer to layer, and the moments of the onset of maximum and minimum temperature values during the day are delayed by every 10 cm by about 3 hours. The deeper the layer, the less heat it receives and the weaker the temperature fluctuations in it. At an average depth of about 1 m, the daily fluctuations in soil temperature "fade out". The layer in which they stop is called the layer of constant daily temperature.
At a depth of 5-10 m in tropical latitudes and 25 m in high latitudes, there is a layer of constant annual temperature, where the temperature is close to the average annual air temperature above the surface.
Water heats up more slowly and releases heat more slowly. In addition, the sun's rays can penetrate to great depths, directly heating the deeper layers. The transfer of heat to depth is not so much due to molecular thermal conductivity, but to a greater extent due to the mixing of waters in a turbulent way or currents. When the surface layers of water cool, thermal convection occurs, which is also accompanied by mixing.
Unlike land, the diurnal temperature fluctuations on the surface of the ocean are less. In high latitudes, on average, only 0.1ºС, in temperate - 0.4ºС, in tropical - 0.5ºС. The penetration depth of these oscillations is 15-20 m.
Annual temperature amplitudes on the ocean surface from 1ºС in equatorial latitudes to 10.2ºС in temperate latitudes. Annual temperature fluctuations penetrate to a depth of 200-300 m.
The moments of temperature maxima in water bodies are delayed compared to land. The maximum occurs at about 15-16 hours, the minimum - 2-3 hours after sunrise. The annual maximum temperature on the surface of the ocean in the northern hemisphere occurs in August, the minimum - in February.
In order to correctly assess the degree of heating and cooling of various earth surfaces, calculate evaporation for , determine changes in the moisture content in the soil, develop methods for predicting freezing, and also evaluate the impact of reclamation work on the climatic conditions of the surface air layer, data on the heat balance of the earth's surface are needed.
The earth's surface continuously receives and loses heat as a result of exposure to a variety of flows of short-wave and long-wave radiation. Absorbing to a greater or lesser extent total radiation and counter radiation, the earth's surface heats up and emits long-wave radiation, which means it loses heat. The value characterizing the loss of heat of the earth
surface is the effective radiation. It is equal to the difference between the own radiation of the earth's surface and the counter radiation of the atmosphere. Since the counter radiation of the atmosphere is always somewhat less than that of the earth, this difference is positive. In the daytime, the effective radiation is blocked by the absorbed short-wave radiation. At night, in the absence of short-wave solar radiation, effective radiation lowers the temperature of the earth's surface. In cloudy weather, due to the increase in the counter radiation of the atmosphere, the effective radiation is much less than in clear weather. Less and nightly cooling of the earth's surface. In middle latitudes, the earth's surface loses through effective radiation about half of the amount of heat that they receive from absorbed radiation.
The arrival and consumption of radiant energy is estimated by the value of the radiation balance of the earth's surface. It is equal to the difference between the absorbed and effective radiation, the thermal state of the earth's surface depends on it - its heating or cooling. During the day, it is positive almost all the time, i.e., the heat input exceeds the consumption. At night, the radiation balance is negative and equal to the effective radiation. The annual values of the radiation balance of the earth's surface, with the exception of the highest latitudes, are everywhere positive. This excess heat is spent on heating the atmosphere by turbulent heat conduction, on evaporation, and on heat exchange with deeper layers of soil or water.
If we consider the temperature conditions for a long period (a year or better a number of years), then the earth's surface, the atmosphere separately and the "Earth-atmosphere" system are in a state of thermal equilibrium. Their average temperature varies little from year to year. In accordance with the law of conservation of energy, we can assume that the algebraic sum of heat fluxes coming to the earth's surface and leaving it is equal to zero. This is the equation for the heat balance of the earth's surface. Its meaning is that the radiation balance of the earth's surface is balanced by non-radiative heat transfer. The heat balance equation, as a rule, does not take into account (because of their smallness) such flows as heat transferred by precipitation, energy consumption for photosynthesis, heat gain from biomass oxidation, as well as heat consumption for melting ice or snow, heat gain from freezing water.
The thermal balance of the "Earth-atmosphere" system for a long period is also equal to zero, i.e., the Earth as a planet is in thermal equilibrium: the solar radiation arriving at the upper boundary of the atmosphere is balanced by the radiation leaving the atmosphere from the upper boundary of the atmosphere.
If we take the air coming to the upper boundary as 100%, then 32% of this amount is dissipated in the atmosphere. Of these, 6% goes back into the world space. Consequently, 26% comes to the earth's surface in the form of scattered radiation; 18% of radiation is absorbed by ozone, aerosols and is used to heat the atmosphere; 5% is absorbed by clouds; 21% of radiation escapes into space as a result of reflection from clouds. Thus, the radiation coming to the earth's surface is 50%, of which direct radiation accounts for 24%; 47% is absorbed by the earth's surface, and 3% of the incoming radiation is reflected back into space. As a result, 30% of solar radiation escapes from the upper boundary of the atmosphere into outer space. This value is called the planetary albedo of the Earth. For the Earth-atmosphere system, 30% of reflected and scattered solar radiation, 5% of terrestrial radiation and 65% of atmospheric radiation, i.e., only 100%, go back into space through the upper boundary of the atmosphere.
Thermal balance ns Earth, the ratio of the income and consumption of energy (radiant and thermal) on the earth's surface, in the atmosphere and in the Earth-atmosphere system. The main source of energy for the vast majority of physical, chemical and biological processes in the atmosphere, hydrosphere and in the upper layers of the lithosphere is solar radiation, therefore, the distribution and ratio of the components of T. b. characterize its transformations in these shells.
T. b. are private formulations of the law of conservation of energy and are compiled for a section of the Earth's surface (T. b. of the earth's surface); for a vertical column passing through the atmosphere (T. b. atmosphere); for the same column passing through the atmosphere and the upper layers of the lithosphere or the hydrosphere (T. b. the Earth-atmosphere system).
Equation T. b. earth surface: R+P+F0+LE= 0 is the algebraic sum of energy flows between an element of the earth's surface and the surrounding space. These streams include radiation balance (or residual radiation) R- the difference between the absorbed short-wave solar radiation and long-wave effective radiation from the earth's surface. The positive or negative value of the radiation balance is compensated by several heat fluxes. Since the temperature of the earth's surface is usually not equal to the temperature of the air, between underlying surface and the atmosphere creates a heat flux R. Similar heat flow F 0 is observed between the earth's surface and deeper layers of the lithosphere or hydrosphere. In this case, the heat flux in the soil is determined by the molecular thermal conductivity, while in water bodies heat exchange, as a rule, has a turbulent character to a greater or lesser extent. heat flow F 0 between the surface of the reservoir and its deeper layers is numerically equal to the change in the heat content of the reservoir over a given time interval and the transfer of heat by currents in the reservoir. Essential value in T. b. the earth's surface usually has a heat loss for evaporation L.E., which is defined as the product of the mass of evaporated water E to the heat of evaporation L. Value LE depends on the moistening of the earth's surface, its temperature, air humidity and the intensity of turbulent heat transfer in the surface layer of air, which determines the rate of transfer of water vapor from the earth's surface to the atmosphere.
Equation T. b. atmosphere looks like: Ra+ L r+P+ Fa= D W.
T. b. atmosphere is made up of its radiation balance R a ; heat input or output L r during phase transformations of water in the atmosphere (r - the amount of precipitation); the arrival or consumption of heat P, due to the turbulent heat exchange of the atmosphere with the earth's surface; heat input or output F a , caused by heat transfer through the vertical walls of the column, which is associated with ordered atmospheric motions and macroturbulence. In addition, in the equation T. b. atmosphere includes a term D W, equal to the change in heat content inside the column.
Equation T. b. systems Earth - atmosphere corresponds to the algebraic sum of the terms of the equations T. b. earth's surface and atmosphere. Components of T. b. Earth's surface and atmosphere for various regions of the globe are determined by meteorological observations (at actinometric stations, at special stations in the sky, and on meteorological satellites of the Earth) or by climatological calculations.
The average latitudinal values of the components of T. b. the earth's surface for the oceans, land and Earth, and T. b. atmospheres are given in tables 1, 2, where the values of the members of T. b. are considered positive if they correspond to the arrival of heat. Since these tables refer to average annual conditions, they do not include terms characterizing changes in the heat content of the atmosphere and the upper layers of the lithosphere, since for these conditions they are close to zero.
For the Earth as a planet, together with the atmosphere, the scheme of T. b. shown in fig. A unit of surface of the outer boundary of the atmosphere receives a flux of solar radiation equal to an average of about 250 kcal/cm 2 per year, of which about 167 kcal/cm 2 per year is absorbed by the Earth (arrow Q s on rice. ). The earth's surface reaches short-wave radiation equal to 126 kcal/cm 2 per year; eighteen kcal/cm 2 per year of this amount is reflected, and 108 kcal/cm 2 per year is absorbed by the earth's surface (arrow Q). The atmosphere absorbs 59 kcal/cm 2 short-wave radiation per year, that is, much less than the earth's surface. The effective long-wave radiation of the Earth's surface is 36 kcal/cm 2 per year (arrow I), therefore, the radiation balance of the earth's surface is 72 kcal/cm 2 per year. The long-wave radiation of the Earth into the world space is equal to 167 kcal/cm 2 per year (arrow I s). Thus, the surface of the Earth receives about 72 kcal/cm 2 per year of radiant energy, which is partially spent on the evaporation of water (circle LE) and is partially returned to the atmosphere through turbulent heat transfer (arrow R).
Tab. 1. - Thermal balance of the earth's surface, kcal/cm 2 year
| Latitude, degrees | Earth average |
||
| R LE R F o | R LE R | R LE R F 0 |
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| 70-60 north latitude 0-10 south latitude Earth as a whole |
Data on the components of T. b. are used in the development of many problems of climatology, land hydrology, and oceanology; they are used to substantiate numerical models of climate theory and to empirically test the results of applying these models. Materials about T. b. play an important role in the study of climate change, they are also used in calculations of evaporation from the surface of river basins, lakes, seas and oceans, in studies of the energy regime sea currents, for the study of snow and ice covers, in plant physiology for the study of transpiration and photosynthesis, in animal physiology for the study of the thermal regime of living organisms. Data about T. b. were also used to study geographic zoning in the works of the Soviet geographer A. A. Grigoriev.
Tab. 2. - The heat balance of the atmosphere, kcal/cm 2 year
| Latitude, degrees | ||||
| 70-60 north latitude 0-10 south latitude Earth as a whole |
Lit.: Atlas of the heat balance of the globe, ed. M. I. Budyko. Moscow, 1963. Budyko M.I., Climate and life, L., 1971; Grigoriev A. A., Patterns of the structure and development of the geographical environment, M., 1966.
The main source of energy for all processes occurring in the biosphere is solar radiation. The atmosphere surrounding the Earth weakly absorbs short-wave radiation from the Sun, which mainly reaches the earth's surface. Some of the solar radiation is absorbed and scattered by the atmosphere. The absorption of incident solar radiation is due to the presence of ozone in the atmosphere, carbon dioxide, water vapor, aerosols.[ ...]
Under the influence of the incident solar flux, as a result of its absorption, the earth's surface heats up and becomes a source of long-wave (LW) radiation directed towards the atmosphere. The atmosphere, on the other hand, is also a source of DW radiation directed towards the Earth (the so-called atmospheric counter-radiation). In this case, mutual heat exchange occurs between the earth's surface and the atmosphere. The difference between the HF radiation absorbed by the earth's surface and the effective radiation is called the radiation balance. The transformation of the energy of HF solar radiation when it is absorbed by the earth's surface and the atmosphere, heat exchange between them constitute the heat balance of the Earth.[ ...]
Main Feature the radiation regime of the atmosphere is the greenhouse effect, which consists in the fact that HF radiation for the most part reaches the earth's surface, causing its heating, and the DW radiation from the Earth is delayed by the atmosphere, while reducing the heat transfer of the Earth into space. The atmosphere is a kind of heat-insulating shell that prevents the Earth from cooling. An increase in the percentage of CO2, H20 vapor, aerosols, etc. will enhance the greenhouse effect, which leads to an increase in the average temperature of the lower atmosphere and climate warming. The main source of thermal radiation of the atmosphere is the earth's surface.[ ...]
The intensity of solar radiation absorbed by the earth's surface and the atmosphere is 237 W/m2, of which 157 W/m2 is absorbed by the earth's surface, and 80 W/m2 by the atmosphere. The heat balance of the Earth in general view shown in fig. 6.15.[ ...]
The radiation balance of the earth's surface is 105 W/m2, and the effective radiation from it is equal to the difference between the absorbed radiation and the radiation balance and is 52 W/m2. The energy of the radiation balance is spent on the turbulent heat exchange of the Earth with the atmosphere, which is 17 W/m2, and on the process of water evaporation, which is 88 W/m2.[ ...]
The scheme of heat transfer of the atmosphere is shown in fig. 6.16. As can be seen from this diagram, the atmosphere receives thermal energy from three sources: from the Sun, in the form of absorbed HF radiation with an intensity of approximately 80 W/m2; heat from condensation of water vapor coming from the earth's surface and equal to 88 W/m2; turbulent heat exchange between the Earth and the atmosphere (17 W/m2).[ ...]
The sum of heat transfer components (185 W/m) is equal to the heat losses of the atmosphere in the form of DW radiation into outer space. An insignificant part of the incident solar radiation, which is significantly less than the given components of the heat balance, is spent on other processes occurring in the atmosphere.[ ...]
The difference in evaporation from the continents and the surfaces of the seas and oceans is compensated by the processes of mass transfer of water vapor through air currents and the flow of rivers flowing into the water areas of the globe.
