The troposphere is the lowest portion of
Earth's atmosphere. It contains approximately 75% of the atmosphere's mass and almost all of its water vaporand aerosols.
The average depth of the troposphere is about 11 km (7 miles) in the middle latitudes. It is deeper in the tropical regions (up to 20 km (12 miles)) and shallower near the poles (about 7 km (4 miles) in summer, indistinct in winter). The lowest part of the troposphere, where
frictionwith the Earth's surface influences air flow, is the planetary boundary layer. This layer is typically a few hundred meters to 2 km (1.2 miles) deep depending on the landformand time of day. The border between the troposphere and stratosphere, called the tropopause, is a temperature inversion.Danielson, Levin, and Abrams, "Meteorology", McGraw Hill, 2003]
The word troposphere derives from the Greek "tropos" for "turning" or "mixing," reflecting the fact that turbulent mixing plays an important role in the troposphere's structure and behavior. Most of the phenomena we associate with day-to-day
weatheroccur in the troposphere.
Pressure and temperature structure
The chemical composition of the troposphere is essentially uniform, with the notable exception of
water vapor. The source of water vapor is at the surface through the processes of evaporationand transpiration. Furthermore the temperature of the troposphere decreases with height, and saturation vapor pressuredecreases strongly with temperature, so the amount of water vapor that can exist in the atmosphere decreases strongly with height. Thus the proportion of water vapor is normally greatest near the surface and decreases with height.
The pressure of the atmosphere is maximum at
sea leveland decreases with higher altitude. This is because the atmosphere is very nearly in hydrostatic equilibrium, so that the pressure is equal to the weight of air above a given point. The change in pressure with height therefore can be equated to the density with this hydrostatic equation:Landau and Lifshitz, "Fluid Mechanics", Pergamon, 1979]
:*"gn" stands for the
standard gravity:*"ρ" stands for density:*"z" stands for height:*"p" stands for pressure:*"R" stands for the gas constant:*"T" stands for temperature in kelvins:*"m" stands for the molar mass
Since temperature in principle also depends on altitude, one needs a second equation to determine the pressure as a function of height, as discussed in the next section.
temperatureof the troposphere generally decreases as altitude increases. The rate at which the temperature decreases, , is called the lapse rate. The reason for this decrease is as follows. When a parcel of air rises, it expands, because the pressure is lower at higher altitudes. As the air parcel expands, it pushes on the air around it, doing work; but generally it does not gain heatin exchange from its environment, because its thermal conductivityis low (such a process is called adiabatic). Since the parcel does work and gains no heat, it loses energy, and so its temperature decreases. (The reverse, of course, will be true for a sinking parcel of air.)
Since the heat exchanged dQ is related to the
entropychange dS by dQ=T dS, the equation governing the temperature as a function of height for a thoroughly mixed atmosphere is :where "S" is the entropy. The rate at which temperature decreases with height under such conditions is called the adiabatic lapse rate.
For "dry" air, which is approximately an
ideal gas, we can proceed further. The adiabatic equation for an ideal gas is Landau and Lifshitz, "Statistical Physics Part 1", Pergamon, 1980] :where is the heat capacity ratio(=7/5, for air). Combining with the equation for the pressure, one arrives at the dry adiabatic lapse rate, [Kittel and Kroemer, "Thermal Physics", Freeman, 1980; chapter 6, problem 11] :If the air contains water vapor, then cooling of the air can cause the water to condense, and the behavior is no longer that of an ideal gas. If the air is at the saturated vapor pressure, then the rate at which temperature drops with height is called the saturated adiabatic lapse rate. More generally, the actual rate at which the temperature drops with altitude is called the environmental lapse rate. In the troposphere, the average environmental lapse rate is a drop of about 6.5 °C for every 1 km (1000 meters) increase in height.
The environmental lapse rate (the actual rate at which temperature drops with height, ) is not usually equal to the adiabatic lapse rate (or correspondingly, ). If the upper air is warmer than predicted by the adiabatic lapse rate (), then when a parcel of air rises and expands, it will arrive at the new height at a lower temperature than its surroundings. In this case, the air parcel is denser than its surroundings, so it sinks back to its original height, and the air is stable against being lifted. If, on the contrary, the upper air is cooler than predicted by the adiabatic lapse rate, then when the air parcel rises to its new height it will have a higher temperature and a lower density than its surroundings, and will continue to accelerate upward.
Temperatures decrease at middle latitudes from an average of 15°C at sea level to about -55°C at the beginning of the
tropopause. At the poles, the troposphere is thinner and the temperature only decreases to -45°C, while at the equatorthe temperature at the top of the troposphere can reach -75°C.Fact|date=August 2007
The tropopause is the boundary region between the troposphere and the stratosphere.
Measuring the temperature change with height through the troposphere and the stratosphere identifies the location of the tropopause. In the troposphere, temperature decreases with altitude. In the stratosphere, however, the temperature remains constant for a while and then increases with altitude. The region of the atmosphere where the lapse rate changes from positive (in the troposphere) to negative (in the stratosphere), is defined as the tropopause. Thus, the tropopause is an
inversion layer, and there is little mixing between the two layers of the atmosphere.
Table of Global Climate System Components
* [http://www.met-office.gov.uk/education/secondary/teachers/atmosphere.html#main The vertical structure of the atmosphere]
* [http://csep10.phys.utk.edu/astr161/lect/earth/atmosphere.html Composition of the Atmosphere] , from the University of Tennessee Physics dept.
* [http://jan.ucc.nau.edu/~doetqp-p/courses/env440/env440_2/lectures/lec32/lec32.htm Chemical Reactions in the Atmosphere]
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См. также в других словарях:
troposphère — [ trɔpɔsfɛr ] n. f. • av. 1913; de tropo et (atmo)sphère ♦ Sc. Partie de l atmosphère comprise entre le sol et la stratosphère. Adj. TROPOSPHÉRIQUE . ● troposphère nom féminin Zone la plus basse de l atmosphère des planètes telluriques, qui s… … Encyclopédie Universelle
Troposphere — Troposphère Ne doit pas être confondu avec Troposphère (fusées). Schéma des couches de l atmosphère (à l echelle). La stratosphère ( 50 km) ne compte que pour environ … Wikipédia en Français
troposphere — 1914, from Fr. troposphère, lit. sphere of change, coined by French meteorologist Philippe Teisserenc de Bort (1855 1913) from Gk. tropos a turn, change (see TROPE (Cf. trope)) + sphaira sphere (see SPHERE (Cf. sphere)) … Etymology dictionary
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troposphere — ► NOUN ▪ the lowest region of the atmosphere, extending from the earth s surface to a height of about 6 10 km (the lower boundary of the stratosphere). DERIVATIVES tropospheric adjective. ORIGIN from Greek tropos turning … English terms dictionary
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