10.045×10 3 J/(kg*K) (in the temperature range from 0-100°C), C v 8.3710*10 3 J/(kg*K) (0-1500°C). The solubility of air in water at 0°C is 0.036%, at 25°C - 0.22%.

Composition of the atmosphere

History of the formation of the atmosphere

Early history

At present, science cannot trace all the stages of the formation of the Earth with 100% accuracy. According to the most common theory, the Earth's atmosphere has been in four different compositions over time. Initially, it consisted of light gases (hydrogen and helium) captured from interplanetary space. This so-called primary atmosphere. At the next stage, active volcanic activity led to the saturation of the atmosphere with gases other than hydrogen (hydrocarbons, ammonia, water vapor). This is how secondary atmosphere. This atmosphere was restorative. Further, the process of formation of the atmosphere was determined by the following factors:

• constant leakage of hydrogen into interplanetary space;
• chemical reactions occurring in the atmosphere under the influence of ultraviolet radiation, lightning discharges and some other factors.

Gradually, these factors led to the formation tertiary atmosphere, characterized by a much lower content of hydrogen and a much higher content of nitrogen and carbon dioxide (formed as a result of chemical reactions from ammonia and hydrocarbons).

The emergence of life and oxygen

With the advent of living organisms on Earth as a result of photosynthesis, accompanied by the release of oxygen and the absorption of carbon dioxide, the composition of the atmosphere began to change. However, there are data (an analysis of the isotopic composition of atmospheric oxygen and that released during photosynthesis) that testify in favor of the geological origin of atmospheric oxygen.

Initially, oxygen was spent on the oxidation of reduced compounds - hydrocarbons, the ferrous form of iron contained in the oceans, etc. At the end of this stage, the oxygen content in the atmosphere began to grow.

In the 1990s, experiments were carried out to create a closed ecological system (“Biosphere 2”), during which it was not possible to create a stable system with a single air composition. The influence of microorganisms led to a decrease in the level of oxygen and an increase in the amount of carbon dioxide.

Nitrogen

The formation of a large amount of N 2 is due to the oxidation of the primary ammonia-hydrogen atmosphere by molecular O 2, which began to come from the surface of the planet as a result of photosynthesis, as expected, about 3 billion years ago (according to another version, atmospheric oxygen is of geological origin). Nitrogen is oxidized to NO in the upper atmosphere, used in industry and bound by nitrogen-fixing bacteria, while N 2 is released into the atmosphere as a result of the denitrification of nitrates and other nitrogen-containing compounds.

Nitrogen N 2 is an inert gas and reacts only under specific conditions (for example, during a lightning discharge). It can be oxidized and converted into a biological form by cyanobacteria, some bacteria (for example, nodule bacteria that form rhizobial symbiosis with legumes).

Oxidation of molecular nitrogen by electric discharges is used in the industrial production of nitrogen fertilizers, and it also led to the formation of unique saltpeter deposits in the Chilean Atacama Desert.

noble gases

Fuel combustion is the main source of pollutant gases (CO , NO, SO 2). Sulfur dioxide is oxidized by air O 2 to SO 3 in the upper atmosphere, which interacts with H 2 O and NH 3 vapors, and the resulting H 2 SO 4 and (NH 4) 2 SO 4 return to the Earth's surface along with precipitation. The use of internal combustion engines leads to significant air pollution with nitrogen oxides, hydrocarbons and Pb compounds.

Aerosol pollution of the atmosphere is due to both natural causes (volcanic eruptions, dust storms, sea ​​water and pollen particles of plants, etc.), and economic activity human (mining ores and building materials, fuel combustion, cement production, etc.). Intensive large-scale removal of particulate matter into the atmosphere is one of the possible causes planetary climate change.

The structure of the atmosphere and the characteristics of individual shells

The physical state of the atmosphere is determined by weather and climate. The main parameters of the atmosphere: air density, pressure, temperature and composition. As altitude increases, air density and atmospheric pressure decrease. The temperature also changes with the change in altitude. Vertical structure atmosphere is characterized by different temperature and electrical properties, different air conditions. Depending on the temperature in the atmosphere, the following main layers are distinguished: troposphere, stratosphere, mesosphere, thermosphere, exosphere (scattering sphere). The transitional regions of the atmosphere between adjacent shells are called the tropopause, stratopause, etc., respectively.

Troposphere

Stratosphere

Most of the short-wavelength part of ultraviolet radiation (180-200 nm) is retained in the stratosphere and the energy of short waves is transformed. Under the influence of these rays, magnetic fields change, molecules break up, ionization occurs, new formation of gases and other chemical compounds. These processes can be observed in the form of northern lights, lightning, and other glows.

In the stratosphere and higher layers under the influence solar radiation gas molecules dissociate - into atoms (above 80 km CO 2 and H 2 dissociate, above 150 km - O 2, above 300 km - H 2). At an altitude of 100-400 km, ionization of gases also occurs in the ionosphere; at an altitude of 320 km, the concentration of charged particles (O + 2, O - 2, N + 2) is ~ 1/300 of the concentration of neutral particles. In the upper layers of the atmosphere there are free radicals - OH, HO 2, etc.

There is almost no water vapor in the stratosphere.

Mesosphere

Up to a height of 100 km, the atmosphere is a homogeneous, well-mixed mixture of gases. In higher layers, the distribution of gases in height depends on their molecular weights, the concentration of heavier gases decreases faster with distance from the Earth's surface. Due to the decrease in gas density, the temperature drops from 0°С in the stratosphere to −110°С in the mesosphere. However kinetic energy individual particles at altitudes of 200-250 km corresponds to a temperature of ~1500°C. Above 200 km, significant fluctuations in temperature and gas density are observed in time and space.

At an altitude of about 2000-3000 km, the exosphere gradually passes into the so-called near space vacuum, which is filled with highly rarefied particles of interplanetary gas, mainly hydrogen atoms. But this gas is only part of the interplanetary matter. The other part is composed of dust-like particles of cometary and meteoric origin. In addition to these extremely rarefied particles, electromagnetic and corpuscular radiation of solar and galactic origin penetrates into this space.

The troposphere accounts for about 80% of the mass of the atmosphere, the stratosphere for about 20%; the mass of the mesosphere is no more than 0.3%, the thermosphere is less than 0.05% of the total mass of the atmosphere. Based on the electrical properties in the atmosphere, the neutrosphere and ionosphere are distinguished. It is currently believed that the atmosphere extends to an altitude of 2000-3000 km.

Depending on the composition of the gas in the atmosphere, they emit homosphere And heterosphere. heterosphere- this is an area where gravity affects the separation of gases, since their mixing at such a height is negligible. Hence follows the variable composition of the heterosphere. Below it lies a well-mixed, homogeneous part of the atmosphere called the homosphere. The boundary between these layers is called turbopause, it lies at an altitude of about 120 km.

Atmospheric properties

Already at an altitude of 5 km above sea level, an untrained person develops oxygen starvation and, without adaptation, a person's performance is significantly reduced. This is where the physiological zone of the atmosphere ends. Human breathing becomes impossible at an altitude of 15 km, although up to about 115 km the atmosphere contains oxygen.

The atmosphere provides us with the oxygen we need to breathe. However, due to the drop in the total pressure of the atmosphere as you rise to a height, the partial pressure of oxygen also decreases accordingly.

The human lungs constantly contain about 3 liters of alveolar air. The partial pressure of oxygen in the alveolar air at normal atmospheric pressure is 110 mm Hg. Art., pressure of carbon dioxide - 40 mm Hg. Art., and water vapor −47 mm Hg. Art. With increasing altitude, the oxygen pressure drops, and the total pressure of water vapor and carbon dioxide in the lungs remains almost constant - about 87 mm Hg. Art. The flow of oxygen into the lungs will completely stop when the pressure of the surrounding air becomes equal to this value.

At an altitude of about 19-20 km, the atmospheric pressure drops to 47 mm Hg. Art. Therefore, at this height, water and interstitial fluid begin to boil in the human body. Outside the pressurized cabin at these altitudes, death occurs almost instantly. Thus, from the point of view of human physiology, "space" begins already at an altitude of 15-19 km.

Dense layers of air - the troposphere and stratosphere - protect us from the damaging effects of radiation. With sufficient rarefaction of air, at altitudes of more than 36 km, ionizing radiation has an intense effect on the body - primary cosmic rays; at altitudes of more than 40 km, the ultraviolet part of the solar spectrum, which is dangerous for humans, operates.

Troposphere

Its upper limit is at an altitude of 8-10 km in polar, 10-12 km in temperate and 16-18 km in tropical latitudes; lower in winter than in summer. The lower, main layer of the atmosphere contains more than 80% of the total mass atmospheric air and about 90% of all water vapor in the atmosphere. In the troposphere, turbulence and convection are highly developed, clouds appear, cyclones and anticyclones develop. Temperature decreases with altitude with an average vertical gradient of 0.65°/100 m

tropopause

The transitional layer from the troposphere to the stratosphere, the layer of the atmosphere in which the decrease in temperature with height stops.

Stratosphere

The layer of the atmosphere located at an altitude of 11 to 50 km. A slight change in temperature in the 11-25 km layer (the lower layer of the stratosphere) and its increase in the 25-40 km layer from -56.5 to 0.8 °C (the upper stratosphere layer or inversion region) are typical. Having reached a value of about 273 K (almost 0 °C) at an altitude of about 40 km, the temperature remains constant up to an altitude of about 55 km. This region of constant temperature is called the stratopause and is the boundary between the stratosphere and the mesosphere.

Stratopause

The boundary layer of the atmosphere between the stratosphere and the mesosphere. There is a maximum in the vertical temperature distribution (about 0 °C).

Mesosphere

The mesosphere begins at an altitude of 50 km and extends up to 80-90 km. The temperature decreases with height with an average vertical gradient of (0.25-0.3)°/100 m. The main energy process is radiant heat transfer. Complex photochemical processes involving free radicals, vibrationally excited molecules, etc., cause atmospheric luminescence.

Mesopause

Transitional layer between mesosphere and thermosphere. There is a minimum in the vertical temperature distribution (about -90 °C).

Karman Line

Altitude above sea level, which is conventionally accepted as the boundary between the Earth's atmosphere and space. The Karmana line is located at an altitude of 100 km above sea level.

Earth's atmosphere boundary

Thermosphere

The upper limit is about 800 km. The temperature rises to altitudes of 200-300 km, where it reaches values ​​of the order of 1500 K, after which it remains almost constant until high altitudes. Under the influence of ultraviolet and x-ray solar radiation and cosmic radiation, air is ionized (“polar lights”) - the main regions of the ionosphere lie inside the thermosphere. At altitudes above 300 km, atomic oxygen predominates. The upper limit of the thermosphere is largely determined by the current activity of the Sun. During periods of low activity, there is a noticeable decrease in the size of this layer.

Thermopause

The region of the atmosphere above the thermosphere. In this region, the absorption of solar radiation is insignificant and the temperature does not actually change with height.

Exosphere (scattering sphere)

Atmospheric layers up to a height of 120 km

Exosphere - scattering zone, the outer part of the thermosphere, located above 700 km. The gas in the exosphere is very rarefied, and hence its particles leak into interplanetary space (dissipation).

Up to a height of 100 km, the atmosphere is a homogeneous, well-mixed mixture of gases. In higher layers, the distribution of gases in height depends on their molecular masses, the concentration of heavier gases decreases faster with distance from the Earth's surface. Due to the decrease in gas density, the temperature drops from 0 °C in the stratosphere to −110 °C in the mesosphere. However, the kinetic energy of individual particles at altitudes of 200–250 km corresponds to a temperature of ~150 °C. Above 200 km, significant fluctuations in temperature and gas density are observed in time and space.

At an altitude of about 2000-3500 km, the exosphere gradually passes into the so-called near space vacuum, which is filled with highly rarefied particles of interplanetary gas, mainly hydrogen atoms. But this gas is only part of the interplanetary matter. The other part is composed of dust-like particles of cometary and meteoric origin. In addition to extremely rarefied dust-like particles, electromagnetic and corpuscular radiation of solar and galactic origin penetrates into this space.

The troposphere accounts for about 80% of the mass of the atmosphere, the stratosphere accounts for about 20%; the mass of the mesosphere is no more than 0.3%, the thermosphere is less than 0.05% of the total mass of the atmosphere. Based on the electrical properties in the atmosphere, the neutrosphere and ionosphere are distinguished. It is currently believed that the atmosphere extends to an altitude of 2000-3000 km.

Depending on the composition of the gas in the atmosphere, homosphere and heterosphere are distinguished. The heterosphere is an area where gravity has an effect on the separation of gases, since their mixing at such a height is negligible. Hence follows the variable composition of the heterosphere. Below it lies a well-mixed, homogeneous part of the atmosphere, called the homosphere. The boundary between these layers is called the turbopause and lies at an altitude of about 120 km.

The composition of the atmosphere. The air shell of our planet - atmosphere protects the earth's surface from the harmful effects on living organisms of ultraviolet radiation from the Sun. It also protects the Earth from cosmic particles - dust and meteorites.

The atmosphere consists of a mechanical mixture of gases: 78% of its volume is nitrogen, 21% is oxygen, and less than 1% is helium, argon, krypton and other inert gases. The amount of oxygen and nitrogen in the air is practically unchanged, because nitrogen almost does not enter into combinations with other substances, and oxygen, which, although very active and is spent on respiration, oxidation and combustion, is constantly replenished by plants.

Up to a height of about 100 km, the percentage of these gases remains practically unchanged. This is due to the fact that the air is constantly mixed.

In addition to these gases, the atmosphere contains about 0.03% carbon dioxide, which is usually concentrated near earth's surface and is distributed unevenly: in cities, industrial centers and areas of volcanic activity, its number increases.

There is always a certain amount of impurities in the atmosphere - water vapor and dust. The content of water vapor depends on the temperature of the air: the higher the temperature, the more vapor the air holds. Due to the presence of vaporous water in the air, atmospheric phenomena such as rainbows, refraction of sunlight, etc. are possible.

Dust enters the atmosphere during volcanic eruptions, sand and dust storms, with incomplete combustion of fuel at thermal power plants, etc.

The structure of the atmosphere. The density of the atmosphere changes with height: it is highest at the Earth's surface, and decreases as it rises. So, at an altitude of 5.5 km, the density of the atmosphere is 2 times, and at an altitude of 11 km - 4 times less than in the surface layer.

Depending on the density, composition and properties of gases, the atmosphere is divided into five concentric layers (Fig. 34).

Rice. 34. Vertical section of the atmosphere (atmospheric stratification)

1. The bottom layer is called troposphere. Its upper boundary runs at an altitude of 8-10 km at the poles and 16-18 km at the equator. The troposphere contains up to 80% of the total mass of the atmosphere and almost all of the water vapor.

The air temperature in the troposphere decreases with height by 0.6 °C every 100 m and at its upper boundary it is -45-55 °C.

The air in the troposphere is constantly mixed, moving in different directions. Only here fogs, rains, snowfalls, thunderstorms, storms and other weather phenomena are observed.

2. Above is located stratosphere, which extends to a height of 50-55 km. Air density and pressure in the stratosphere are negligible. The rarefied air consists of the same gases as in the troposphere, but it contains more ozone. The highest concentration of ozone is observed at an altitude of 15-30 km. The temperature in the stratosphere rises with height and reaches 0 °C or more at its upper boundary. This is due to the fact that ozone absorbs the short-wavelength part of solar energy, as a result of which the air heats up.

3. Above the stratosphere lies mesosphere, extending to a height of 80 km. In it, the temperature drops again and reaches -90 ° C. The air density there is 200 times less than at the surface of the Earth.

4. Above the mesosphere is thermosphere(from 80 to 800 km). The temperature in this layer rises: at an altitude of 150 km to 220 °C; at an altitude of 600 km to 1500 °C. The atmospheric gases (nitrogen and oxygen) are in an ionized state. Under the action of short-wave solar radiation, individual electrons are detached from the shells of atoms. As a result, in this layer - ionosphere layers of charged particles appear. Their densest layer is at an altitude of 300-400 km. Due to the low density, the sun's rays do not scatter there, so the sky is black, stars and planets shine brightly on it.

In the ionosphere there are polar lights, powerful electric currents that cause disturbances in the Earth's magnetic field.

5. Above 800 km, the outer shell is located - exosphere. The speed of movement of individual particles in the exosphere approaches the critical one - 11.2 mm/s, so individual particles can overcome the Earth's gravity and escape into the world space.

The value of the atmosphere. The role of the atmosphere in the life of our planet is exceptionally great. Without it, the Earth would be dead. The atmosphere protects the Earth's surface from intense heating and cooling. Its influence can be likened to the role of glass in greenhouses: to let in the sun's rays and prevent heat from escaping.

The atmosphere protects living organisms from the shortwave and corpuscular radiation of the Sun. The atmosphere is the environment where weather phenomena occur, with which all human activity is associated. The study of this shell is carried out at meteorological stations. Day and night, in any weather, meteorologists monitor the state of the lower atmosphere. Four times a day, and at many stations every hour they measure temperature, pressure, air humidity, note cloudiness, wind direction and speed, precipitation, electrical and sound phenomena in the atmosphere. Meteorological stations are located everywhere: in Antarctica and in tropical rainforests, on high mountains and in the vast expanses of the tundra. Observations are also being made on the oceans from specially built ships.

From the 30s. 20th century observations began in the free atmosphere. They began to launch radiosondes, which rise to a height of 25-35 km, and with the help of radio equipment transmit to Earth information about temperature, pressure, air humidity and wind speed. Nowadays, meteorological rockets and satellites are also widely used. The latter have television installations that transmit images of the earth's surface and clouds.

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5. Air shell of the earth§ 31. Heating of the atmosphere

The atmosphere has distinct layers of air. Air layers differ in temperature, difference in gases and their density and pressure. It should be noted that the layers of the stratosphere and troposphere protect the Earth from solar radiation. In the higher layers, a living organism can receive a lethal dose of the ultraviolet solar spectrum. To quickly jump to the desired layer of the atmosphere, click on the corresponding layer:

Troposphere and tropopause

Troposphere - temperature, pressure, altitude

The upper limit is kept at around 8 - 10 km approximately. In temperate latitudes 16 - 18 km, and in polar 10 - 12 km. Troposphere It is the lower main layer of the atmosphere. This layer contains more than 80% of the total mass of atmospheric air and close to 90% of the total water vapor. It is in the troposphere that convection and turbulence arise, clouds form, cyclones occur. Temperature decreases with height. Gradient: 0.65°/100 m. The heated earth and water heat up the enclosing air. The heated air rises, cools and forms clouds. The temperature in the upper boundaries of the layer can reach -50/70 °C.

It is in this layer that changes in climatic weather conditions occur. The lower limit of the troposphere is called surface since it has a lot of volatile microorganisms and dust. Wind speed increases with height in this layer.

tropopause

This is the transitional layer of the troposphere to the stratosphere. Here, the dependence of the decrease in temperature with an increase in altitude ceases. The tropopause is the minimum height where the vertical temperature gradient drops to 0.2°C/100 m. The height of the tropopause depends on strong climatic events such as cyclones. The height of the tropopause decreases above cyclones and increases above anticyclones.

Stratosphere and Stratopause

The height of the stratosphere layer is approximately from 11 to 50 km. There is a slight change in temperature at an altitude of 11-25 km. At an altitude of 25–40 km, inversion temperature, from 56.5 rises to 0.8°C. From 40 km to 55 km the temperature stays at around 0°C. This area is called - stratopause.

In the Stratosphere, the effect of solar radiation on gas molecules is observed, they dissociate into atoms. There is almost no water vapor in this layer. Modern supersonic commercial aircraft fly at altitudes up to 20 km due to stable flight conditions. High-altitude weather balloons rise to a height of 40 km. There are steady air currents here, their speed reaches 300 km/h. Also in this layer is concentrated ozone, a layer that absorbs ultraviolet rays.

Mesosphere and Mesopause - composition, reactions, temperature

The mesosphere layer begins at about 50 km and ends at around 80-90 km. Temperatures decrease with elevation by about 0.25-0.3°C/100 m. Radiant heat exchange is the main energy effect here. Complex photochemical processes involving free radicals (has 1 or 2 unpaired electrons) since they implement glow atmosphere.

Almost all meteors burn up in the mesosphere. Scientists have named this area Ignorosphere. This zone is difficult to explore, as aerodynamic aviation here is very poor due to the air density, which is 1000 times less than on Earth. And for launching artificial satellites, the density is still very high. Research is carried out with the help of meteorological rockets, but this is a perversion. Mesopause transitional layer between mesosphere and thermosphere. Has a minimum temperature of -90°C.

Karman Line

Pocket line called the boundary between the Earth's atmosphere and outer space. According to the International Aviation Federation (FAI), the height of this border is 100 km. This definition was given in honor of the American scientist Theodor von Karman. He determined that at about this height the density of the atmosphere is so low that aerodynamic aviation becomes impossible here, since the speed of the aircraft must be greater first space velocity. At such a height, the concept of a sound barrier loses its meaning. Here to manage aircraft possible only due to reactive forces.

Thermosphere and Thermopause

The upper boundary of this layer is about 800 km. The temperature rises up to about 300 km, where it reaches about 1500 K. Above, the temperature remains unchanged. In this layer there is Polar Lights- occurs as a result of the effect of solar radiation on the air. This process is also called the ionization of atmospheric oxygen.

Due to the low rarefaction of the air, flights above the Karman line are possible only along ballistic trajectories. All manned orbital flights (except flights to the Moon) take place in this layer of the atmosphere.

Exosphere - Density, Temperature, Height

The height of the exosphere is above 700 km. Here the gas is very rarefied, and the process takes place dissipation— leakage of particles into interplanetary space. The speed of such particles can reach 11.2 km/sec. The growth of solar activity leads to the expansion of the thickness of this layer.

• gas envelope does not fly away into space due to gravity. Air is made up of particles that have their own mass. From the law of gravitation, it can be concluded that every object with mass is attracted to the Earth.
• Buys-Ballot's law states that if you are in the Northern Hemisphere and stand with your back to the wind, then there will be a high pressure zone on the right, and low pressure on the left. In the Southern Hemisphere, it will be the other way around.

The Earth's atmosphere is an air shell.

The presence of a special ball above the earth's surface was proved by the ancient Greeks, who called the atmosphere a steam or gas ball.

This is one of the geospheres of the planet, without which the existence of all life would not be possible.

Where is the atmosphere

The atmosphere surrounds the planets with a dense air layer, starting from the earth's surface. It comes into contact with the hydrosphere, covers the lithosphere, going far into outer space.

What is the atmosphere made of?

The air layer of the Earth consists mainly of air, the total mass of which reaches 5.3 * 1018 kilograms. Of these, the diseased part is dry air, and much less water vapor.

Over the sea, the density of the atmosphere is 1.2 kilograms per cubic meter. The temperature in the atmosphere can reach -140.7 degrees, air dissolves in water at zero temperature.

The atmosphere consists of several layers:

• Troposphere;
• tropopause;
• Stratosphere and stratopause;
• Mesosphere and mesopause;
• A special line above sea level, which is called the Karman line;
• Thermosphere and thermopause;
• Dispersion zone or exosphere.

Each layer has its own characteristics, they are interconnected and ensure the functioning of the air shell of the planet.

The boundaries of the atmosphere

The lowest edge of the atmosphere runs through the hydrosphere and the upper layers of the lithosphere. The upper boundary begins in the exosphere, which is located 700 kilometers from the surface of the planet and will reach 1.3 thousand kilometers.

According to some reports, the atmosphere reaches 10 thousand kilometers. Scientists agreed that the upper boundary of the air layer should be the Karman line, since aeronautics is no longer possible here.

Thanks to constant research in this area, scientists have found that the atmosphere is in contact with the ionosphere at an altitude of 118 kilometers.

Chemical composition

This layer of the Earth consists of gases and gas impurities, which include combustion residues, sea salt, ice, water, dust. The composition and mass of gases that can be found in the atmosphere almost never change, only the concentration of water and carbon dioxide changes.

The composition of water can vary from 0.2 percent to 2.5 percent depending on latitude. Additional elements are chlorine, nitrogen, sulfur, ammonia, carbon, ozone, hydrocarbons, hydrochloric acid, hydrogen fluoride, hydrogen bromide, hydrogen iodide.

A separate part is occupied by mercury, iodine, bromine, nitric oxide. In addition, liquid and solid particles, which are called aerosol, are found in the troposphere. One of the rarest gases on the planet, radon, is found in the atmosphere.

In terms of chemical composition, nitrogen occupies more than 78% of the atmosphere, oxygen - almost 21%, carbon dioxide - 0.03%, argon - almost 1%, the total amount of matter is less than 0.01%. Such a composition of the air was formed when the planet only arose and began to develop.

With the advent of man, who gradually switched to production, the chemical composition changed. In particular, the amount of carbon dioxide is constantly increasing.

Atmosphere functions

The gases in the air layer perform a variety of functions. First, they absorb rays and radiant energy. Secondly, they influence the formation of temperature in the atmosphere and on the Earth. Thirdly, it provides life and its course on Earth.

In addition, this layer provides thermoregulation, which determines the weather and climate, the mode of heat distribution and atmospheric pressure. The troposphere helps regulate flows air masses, determine the movement of water, the processes of heat exchange.

The atmosphere constantly interacts with the lithosphere, hydrosphere, providing geological processes. The most important function is that there is protection from dust of meteorite origin, from the influence of space and the sun.

Data

• Oxygen provides on earth decomposition organic matter solid rock, which is very important for emissions, decomposition of rocks, oxidation of organisms.
• Carbon dioxide contributes to the fact that photosynthesis occurs, and also contributes to the transmission of short waves of solar radiation, the absorption of thermal long waves. If this does not happen, then the so-called greenhouse effect is observed.
• One of the main problems associated with the atmosphere is pollution, which occurs due to the work of enterprises and vehicle emissions. Therefore, in many countries a special environmental control, and at the international level, special mechanisms are being undertaken to control emissions and the greenhouse effect.