Editing Troposphere (section)

==Structure==
===Composition===
The Earth's planetary atmosphere contains, besides other gases, water vapour and carbon dioxide, which produce carbonic acid in [[rain water]], which therefore has an approximate natural pH of 5.0 to 5.5 (slightly acidic).   (Water other than atmospheric water vapour fallen as fresh rain, such as fresh/sweet/potable/river water, will usually be affected by the physical environment and may not be in this pH range.) Atmospheric water vapour holds suspended gasses in it (not by mass), 78.08% [[nitrogen]] as N<sub>2</sub>, 20.95% [[oxygen]] as O<sub>2</sub>, 0.93% [[argon]], trace gases, and variable amounts of condensing water (from [[saturated water vapor]]). Any carbon dioxide released into the atmosphere from a pressurised source combines with the carbonic acid water vapour and momentarily reduces the atmospheric pH by negligible amounts. Respiration from animals releases out of equilibrium carbonic acid and low levels of other ions. Combustion of hydrocarbons which is not a chemical reaction releases to atmosphere carbonic acid water as; saturates, condensates, vapour or gas (invisible steam). Combustion can releases particulates (carbon/soot and ash) as well as molecules forming nitrites and sulphites which will reduce the atmospheric pH of the water slightly or harmfully in highly industrialised areas where this is classed as air pollution and can create the phenomena of acid rain, a pH lower than the natural pH5.56. The negative effects of the by-products of combustion released into the atmospheric vapour can be removed by the use of scrubber towers and other physical means, the captured pollutants can be processed into a valuable by-product. The sources of atmospheric water vapor are the bodies of water (oceans, seas, lakes, rivers, swamps), and vegetation on the [[planetary surface]], which humidify the troposphere through the processes of [[evaporation]] and [[transpiration]] respectively, and which influences the occurrence of weather phenomena; the greatest proportion of water vapor is in the atmosphere nearest the surface of the Earth. The temperature of the troposphere decreases at high [[altitude]] by way of the [[Inversion (meteorology)|inversion layer]]s that occur in the [[tropopause]], which is the atmospheric boundary that demarcates the troposphere from the [[stratosphere]]. At higher altitudes, the low air-temperature consequently decreases the [[saturation vapor pressure]], the amount of atmospheric water vapor in the upper troposphere.

===Pressure===
The maximum air pressure (weight of the atmosphere) is at [[sea level]] and decreases at high altitude because the atmosphere is in [[hydrostatic equilibrium]], wherein the air pressure is equal to the weight of the air above a given point on the planetary surface. The relation between decreased air pressure and high altitude can be equated to the density of a fluid, by way of the following [[Fluid statics|hydrostatic]] equation:

:<math> \frac{dP}{dz} = -\rho g_n = - \frac {mPg_n}{RT}</math>

where:

:*''g<sub>n</sub>'' is the [[standard gravity]]
:*''ρ'' is the [[density]]

:*''z'' is the [[altitude]]
:*''P'' is the [[pressure]]
:*''R'' is the [[gas constant]]
:*''T'' is the [[thermodynamic temperature|thermodynamic (absolute) temperature]]
:*''m'' is the [[molar mass]]<ref name="LL">Landau and Lifshitz, ''Fluid Mechanics'', Pergamon, 1979</ref>

===Temperature===
The planetary surface of the Earth heats the troposphere by means of [[latent heat]], [[outgoing long-wave radiation|thermal radiation]], and [[sensible heat]].
The gas layers of the troposphere are less dense at the geographic poles and denser at the equator, where the average height of the tropical troposphere is 13&nbsp;km, approximately 7.0&nbsp;km greater than the 6.0&nbsp;km average height of the polar troposphere at the geographic poles; therefore, surplus heating and vertical expansion of the troposphere occur in the tropical latitudes. At the middle latitudes, tropospheric temperatures decrease from an average temperature of {{convert|15|°C|°F|abbr=on}} at sea level to approximately {{convert|-55|°C|°F|abbr=on}} at the [[tropopause]]. At the [[equator]], the tropospheric temperatures decrease from an average temperature of {{convert|20|°C|°F|abbr=on}} at sea level to approximately {{convert|-70|to|-75|C|F}} at the tropopause. At the [[geographical pole]]s, the [[Arctic]] and the [[Antarctica|Antarctic]] regions, the tropospheric temperature decreases from an average temperature of {{convert|0|°C|°F|abbr=on}} at sea level to approximately {{convert|-45|°C|°F|abbr=on}} at the tropopause.<ref name="ZonalFlowDef">{{cite book|first=Paul E. |last=Lydolph|year=1985|title=The Climate of the Earth|publisher=Rowman and Littlefield Publishers Inc.|page=12}}</ref>

====Altitude====
[[File:Sky outside plane.jpg|thumb|upright=1.5|A picture of Earth's atmosphere as viewed from an [[airplane]], traveling over the [[Arctic]].]]
The temperature of the troposphere decreases with increased altitude, and the rate of decrease in air temperature is measured with the Environmental Lapse Rate (<math>-dT/dz</math>) which is the numeric difference between the temperature of the [[planetary surface]] and the temperature of the tropopause divided by the altitude. Functionally, the ELR equation assumes that the planetary atmosphere is static, that there is no mixing of the layers of air, either by [[Atmospheric convection|vertical atmospheric convection]] or winds that could create turbulence.

The difference in temperature derives from the planetary surface absorbing most of the energy from the sun, which then radiates outwards and heats the troposphere (the first layer of the atmosphere of Earth) while the radiation of surface heat to the upper atmosphere results in the cooling of that layer of the atmosphere. The ELR equation also assumes that the atmosphere is static, but heated air becomes buoyant, expands, and rises. The dry [[adiabatic]] lapse rate (DALR) accounts for the effect of the expansion of dry air as it rises in the atmosphere, and the wet adiabatic lapse rate (WALR) includes the effect of the condensation-rate of water vapor upon the environmental lapse rate.

{| class="wikitable" style="border-spacing: 5px; margin:auto;"
|+ '''Environmental Lapse Rate (ELR)'''
|-
! scope="col" style="width:150px;"| Altitude Region
! scope="col" style="width:100px;"| Lapse rate
! scope="col" style="width:100px;"| Lapse Rate
|-
! scope="col" style="width:150px;"| (m)
! scope="col" style="width:100px;"| (°C / km)
! scope="col" style="width:100px;"| (°F / 1000 ft)
|- align="center";
| &nbsp;&nbsp; &nbsp; 0.0 &nbsp; – 11,000 ||  &nbsp; 6.50 || &nbsp; 3.57
|- align="center";
| 11,000 – 20,000 ||  &nbsp; 0.0&nbsp; || &nbsp; 0.0&nbsp; &nbsp;
|- align="center";
| 20,000 – 32,000 || −1.0 ||  −0.55 
|- align="center";
| 32,000 – 47,000 || −2.8 || −1.54
|- align="center";
| 47,000 – 51,000 || &nbsp; 0.0 &nbsp; || &nbsp; 0.0 &nbsp; &nbsp;
|- align="center";
| 51,000 – 71,000 || &nbsp; 2.80 ||  &nbsp; 1.54 
|- align="center";
| 71,000 – 85,000 || &nbsp; 2.00 || &nbsp; 1.09
|-
|}

====Compression and expansion====
A [[air parcel|parcel of air]] rises and expands because of the lower atmospheric pressure at high altitudes. The expansion of the air parcel pushes outwards against the surrounding air, and transfers [[energy]] (as [[Work (thermodynamics)|work]]) from the parcel of air to the atmosphere. Transferring energy to a parcel of air by way of [[heat]] is a slow and inefficient exchange of energy with the environment, which is an [[adiabatic process]] (no energy transfer by way of heat). As the rising parcel of air loses energy while it acts upon the surrounding atmosphere, no heat energy is transferred from the atmosphere to the air parcel to compensate for the heat loss. The parcel of air loses energy as it reaches greater altitude, which is manifested as a decrease in the temperature of the air mass. Analogously, the reverse process occurs within a cold parcel of air that is being compressed and is sinking to the planetary surface.<ref name="DLA"/>

The compression and the expansion of an air parcel are reversible phenomena in which energy is not transferred into or out of the air parcel; atmospheric compression and expansion are measured as an [[isentropic|isentropic process]] (<math>dS = 0</math>) wherein there occurs no change in entropy as the air parcel rises or falls within the atmosphere. Because the heat exchanged (<math>dQ = 0</math>) is related to the change in [[entropy]] (<math>dS</math> by <math>dQ = T dS</math>) the equation governing the air temperature as a function of altitude for a mixed atmosphere is: <math> \frac{\, dS\,}{dz} = 0 </math> where {{mvar|S}} is the entropy. The isentropic equation states that atmospheric entropy does not change with altitude; the adiabatic lapse rate measures the rate at which temperature decreases with altitude under such conditions.

====Humidity====
If the air contains [[water vapor]], then cooling of the air can cause the water to condense, and the air no longer functions as an ideal gas. If the air is at the [[saturation vapor pressure]], then the rate at which temperature decreases with altitude is called the [[Lapse rate#Moist adiabatic lapse rate|saturated adiabatic lapse rate]]. The actual rate at which the temperature decreases with altitude is the [[Lapse rate#Environmental lapse rate|environmental lapse rate]]. In the troposphere, the average environmental lapse rate is a decrease of about 6.5&nbsp;°C for every 1.0&nbsp;km (1,000m) of increased altitude.<ref name="DLA"/>
For dry air, an approximately [[ideal gas]], the adiabatic equation is: <math> p(z) \Bigl[T(z)\Bigr]^{-\frac{\gamma}{\,\gamma\,-\,1\,}} = \text{constant}</math> wherein <math>\gamma</math> is the [[heat capacity ratio]] (<math>\gamma \approx \,</math>{{frac|7|5}}) for air. The combination of the equation for the air pressure yields the [[Lapse rate#Dry adiabatic lapse rate|dry adiabatic lapse rate]]:<math>\frac{\,dT\,}{dz} = - \frac{\; m g \;}{R} \frac{\;\gamma\,-\,1\;}{\gamma} = -9.8^\circ\mathrm{C/km}</math>.<ref>{{cite book |vauthors=Kittel C, Kroemer H |title=Thermal Physics |publisher=Freeman |year=1980 |at=chapter&nbsp;6, problem&nbsp;11}}</ref><ref name="LL1">{{cite book |vauthors=Landau LD, Lifshitz EM |title=Statistical Physics |series=Part&nbsp;1 |publisher=Pergamon |year=1980}}</ref>

====Environment====
The environmental lapse rate (<math>dT/dz</math>), at which temperature decreases with altitude, usually is unequal to the adiabatic lapse rate (<math>dS/dz \ne 0</math>). If the upper air is warmer than predicted by the adiabatic lapse rate (<math>dS/dz > 0</math>), then a rising and expanding parcel of air will arrive at the new altitude at a lower temperature than the surrounding air. In which case, the air parcel is denser than the surrounding air, and so falls back to its original altitude as an air mass that is stable against being lifted. If the upper air is cooler than predicted by the adiabatic lapse rate, then, when the air parcel rises to a new altitude, the air mass will have a higher temperature and a lower density than the surrounding air and will continue to accelerate and rise.<ref name="DLA"/><ref name="LL"/>

===Tropopause===
{{main|Tropopause}}
The tropopause is the atmospheric boundary layer between the troposphere and the [[stratosphere]], and is located by measuring the changes in temperature relative to increased altitude in the troposphere and in the stratosphere. In the troposphere, the temperature of the air decreases at high altitude, however, in the stratosphere the air temperature initially is constant, and then increases with altitude. The increase of air temperature at stratospheric altitudes results from the [[ozone layer]]'s absorption and retention of the ultraviolet (UV) radiation that Earth receives from the Sun.<ref name=ucarOverview>{{cite web |title=The Stratosphere — Overview |url=https://scied.ucar.edu/shortcontent/stratosphere-overview |publisher=University Corporation for Atmospheric Research |access-date=25 July 2018 |language=en |archive-date=29 May 2018 |archive-url=https://web.archive.org/web/20180529220648/https://scied.ucar.edu/shortcontent/stratosphere-overview |url-status=live }}</ref> The coldest layer of the atmosphere, where the temperature lapse rate changes from a positive rate (in the troposphere) to a negative rate (in the stratosphere) locates and identifies the tropopause as an [[Inversion (meteorology)|inversion layer]] in which limited mixing of air layers occurs between the troposphere and the stratosphere.<ref name="DLA"/>