The mesopause is the point of minimum temperature at the boundary between the mesosphere and the thermosphere atmospheric regions. Due to the lack of solar heating and very strong radiative cooling from carbon dioxide, the mesosphere is the coldest region on Earth with temperatures as low as -100 °C (-148 °F or 173 K).[1] The altitude of the mesopause for many years was assumed to be at around 85 km (53 mi), but observations to higher altitudes and modeling studies in the last 10 years have shown that in fact there are two mesopauses - one at about 85 km and a stronger one at about 100 km (62 mi), with a layer of slightly warmer air between them.[2]
Another feature is that the summer mesopause is cooler than the winter (sometimes referred to as the mesopause anomaly). It is due to a summer-to-winter circulation giving rise to upwelling at the summer pole and downwelling at the winter pole. Air rising will expand and cool resulting in a cold summer mesopause and conversely downwelling air results in compression and associated increase in temperature at the winter mesopause. In the mesosphere the summer-to-winter circulation is due to gravity wave dissipation, which deposits momentum against the mean east–west flow, resulting in a small north–south circulation.[3]
In recent years the mesopause has also been the focus of studies on global climate change associated with increases in CO2. Unlike the troposphere, where greenhouse gases result in the atmosphere heating up, increased CO2 in the mesosphere acts to cool the atmosphere due to increased radiative emission. This results in a measurable effect - the mesopause should become cooler with increased CO2. Observations do show a decrease of temperature of the mesopause, though the magnitude of this decrease varies and is subject to further study.[4] Modeling studies of this phenomenon have also been carried out.[5][6][7]
See also
editReferences
edit- ^ International Union of Pure and Applied Chemistry. "mesosphere". Compendium of Chemical Terminology Internet edition
- ^ Xu, Jiyao; Liu, H.-L.; Yuan, W.; Smith, A.K.; Roble, R. G.; Mertens, C.J.; Russell, J.M.; Mlynczak, M.G. (2007). "Mesopause structure from Thermosphere, Ionosphere, Mesosphere, Energetics, and Dynamics (TIMED)/Sounding of the Atmosphere Using Broadband Emission Radiometry (SABER)". Journal of Geophysical Research. 112 (D9). Bibcode:2007JGRD..112.9102X. doi:10.1029/2006jd007711. S2CID 54715803.
- ^ The Physics of Atmospheres, John Theodore Houghton, section and references therein of The general circulation of the middle atmosphere
- ^ Beig, G.; Keckhut, P.; Lowe, R.P.; et al. (2003). "Review of mesospheric temperature trends (2003)". Rev. Geophys. 41 (4): 1015. Bibcode:2003RvGeo..41.1015B. doi:10.1029/2002rg000121.
- ^ Roble, R.G.; Dickinson, R.E. (1989). "How will changes in carbon-dioxide and methane modify the mean structure of the mesosphere and thermosphere?". Geophys. Res. Lett. 16 (12): 1441–1444. Bibcode:1989GeoRL..16.1441R. doi:10.1029/gl016i012p01441.
- ^ Akmaev, R.A.; Fomichev, V.I.; Zhu, X. (2006). "Impact of middle-atmospheric composition changes on greenhouse cooling in the upper atmosphere". J. Atmos. Sol.-Terr. Phys. 68 (17): 1879–1889. Bibcode:2006JASTP..68.1879A. doi:10.1016/j.jastp.2006.03.008.
- ^ Cnossen, Ingrid; Harris, Matthew J.; Arnold, Neil F.; Yiğit, Erdal (2009). "Modelled effect of changes in the CO2 concentration on the middle and upper atmosphere: Sensitivity to gravity wave parameterization". Journal of Atmospheric and Solar-Terrestrial Physics. Long-Term Changes and Solar Impacts in the Atmosphere-Ionosphere System. 71 (13): 1484–1496. Bibcode:2009JASTP..71.1484C. doi:10.1016/j.jastp.2008.09.014. ISSN 1364-6826.