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Thetropopause is the atmospheric boundary that demarcates thetroposphere from thestratosphere, which are the lowest two of the five layers of theatmosphere of Earth. The tropopause is a thermodynamic gradient-stratification layer that marks the end of thetroposphere, and is approximately 17 kilometres (11 mi) above theequatorial regions, and approximately 9 kilometres (5.6 mi) above thepolar regions.
Rising from the planetary surface of the Earth, the tropopause is the atmospheric level where the air ceases to become cool with increased altitude and becomes dry, devoid of water vapor. The tropopause is the boundary that demarcates thetroposphere below from thestratosphere above, and is part of the atmosphere where there occurs an abrupt change in theenvironmental lapse rate (ELR) of temperature, from a positive rate (of decrease) in the troposphere to a negative rate in the stratosphere. The tropopause is defined as the lowest level at which the lapse rate decreases to 2°C/km or less, provided that the average lapse-rate, between that level and all other higher levels within 2.0 km does not exceed 2°C/km.[1] The tropopause is afirst-order discontinuity surface, in which temperature as a function of height varies continuously through the atmosphere, while thetemperature gradient has a discontinuity.[2]
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The troposphere is the lowest layer of the Earth's atmosphere; it starts at theplanetary boundary layer, and is the layer in which mostweather phenomena occur. The troposphere contains the boundary layer, and ranges in height from an average of 9 km (5.6 mi; 30,000 ft) at the poles, to 17 km (11 mi; 56,000 ft) at theEquator.[3][4] In the absence ofinversions and not consideringmoisture, thetemperature lapse rate for this layer is 6.5 °C per kilometer, on average, according to theU.S. Standard Atmosphere.[5] A measurement of the tropospheric and the stratospheric lapse rates helps identify the location of the tropopause, since temperature increases with height in the stratosphere, and hence the lapse rate becomes negative.
Since the tropopause responds to the average temperature of the entire layer that lies underneath it, it is at its maximum levels over the Equator, and reaches minimum heights over the poles. There are variations of starting height, which aScience Advances study found to correspond with the thermal structure both above and below where tropopause was recognized. These variations were determined to have a positive correlation to tropospheric temperature anomalies and a negative correlation to stratospheric temperature anomalies.[6] On account of this, the coolest layer in the atmosphere lies at about 17 km over the equator. Due to the variation in starting height, the tropopause extremes are referred to as the equatorial tropopause and the polar tropopause.
Given that the lapse rate is not a conservative quantity when the tropopause is considered for stratosphere-troposphere exchanges studies, there exists an alternative definition nameddynamic tropopause.[7] It is formed with the aid ofpotential vorticity, which is defined as the product of theisentropicdensity, i.e. the density that is measurable by usingpotential temperature as the vertical coordinate, and theabsolute vorticity, given that this quantity attains quite different values for the troposphere and the stratosphere.[8] Instead of using the vertical temperature gradient as the defining variable, the dynamic tropopause surface is expressed inpotential vorticity units (PVU, 1 PVU = 10-6 K m2 kg-1 s-1[9]). Given that the absolute vorticity is positive in the Northern Hemisphere and negative in theSouthern Hemisphere, the threshold value should be considered as positive north of the Equator and negative south of it.[10] Theoretically, to define a global tropopause in this way, the two surfaces arising from the positive and negative thresholds need to be matched near the equator using another type of surface such as a constantpotential temperature surface. Nevertheless, the dynamic tropopause is useless at equatorial latitudes because the isentropes are almost vertical.[9] For the extratropical tropopause in theNorthern Hemisphere the WMO established a value of 1.6 PVU,[9]: 152 but greater values ranging between 2 and 3.5 PVU have been traditionally used.[11]
It is also possible to define the tropopause in terms of chemical composition.[12] For example, the lower stratosphere has much higherozone concentrations than the upper troposphere, but much lowerwater vapor concentrations, so an appropriate boundary can be defined.
In 1949Alan West Brewer proposed that tropospheric air passes through the tropopause into the stratosphere near the equator, then travels through the stratosphere to temperate and polar regions, where it sinks into the troposphere.[13]This is now known asBrewer-Dobson circulation.Because gases primarily enter the stratosphere by passing through the tropopause in the tropics where the tropopause is coldest, water vapor is condensed out of the air that is entering the stratosphere. This ″tropical tropopause layercold trap″ theory has become widely accepted.[14]This cold trap limits stratospheric water vapor to 3 to 4 parts per million.[15]Researchers atHarvard have suggested that the effects ofGlobal Warming on air circulation patterns will weaken the tropical tropopause layer cold trap.[16]
Water vapor that is able to make it through the cold trap eventually rises to the top of the stratosphere, where it undergoesphotodissociation intooxygen andhydrogen orhydroxide ions and hydrogen.[17][18]This hydrogen is then able toescape the atmosphere.Thus, in some sense, the tropical tropopause layer cold trap is what prevents Earth from losing its water to space.James Kasting has predicted thatin 1 to 2 billion years, as theSun increases in luminosity, the temperature of the Earth will rise enough that the cold trap will no longer be effective, and so the Earth will dry out.[19]
The tropopause is not a fixed boundary. Vigorousthunderstorms, for example, particularly those of tropical origin, willovershootinto the lower stratosphere and undergo a brief (hour-order or less) low-frequency verticaloscillation.[20] Such oscillation results in a low-frequency atmosphericgravity wave capable of affecting both atmospheric and oceanic currents in the region.[citation needed]
Most commercial aircraft are flown in the lower stratosphere, just above the tropopause, during thecruise phase of their flights; in this region, the clouds and significant weather perturbations characteristic of the troposphere are usually absent.[21]
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