Stratosphere is essential for human being
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Answer:
h
yes without it life is not possible
1 Introduction
The stratosphere is the layer of highly stratified air that extends for roughly 40 km above the tropopause and contains approximately 20% of the mass of the atmosphere. The climatology, seasonal evolution, and variability of the stratospheric circulation are strongly governed by the combined influences of solar and infrared radiation, ozone chemistry, and transport and momentum transport by Rossby and gravity waves that propagate upward from the troposphere below. While it contains a smaller fraction of atmospheric mass than the troposphere, the stratosphere is far from being a passive bystander to tropospheric influences. It exhibits a diverse range of variability on a spectrum of timescales with, in many cases, a well-established influence on the tropospheric circulation below. As a result, knowledge of the state of the stratosphere has the potential to enhance the predictability of the troposphere on sub-seasonal to seasonal (S2S) timescales and beyond.
This chapter reviews our knowledge of the coupling between the stratosphere and troposphere in the tropics (Section 2) and the extratropics (Section 3) to provide a clear understanding of where and when coupling is important. In Section 4, we review the progress to date in trying to harness stratosphere-troposphere coupling to enhance predictability on the S2S timescale, a key focus of the World Climate Research Programme/Stratosphere-Troposphere Processes And Their Role in Climate (WCRP/SPARC) Stratospheric Network for the Assessment of Predictability (SNAP) project. Finally, in Section 5, we examine a number of open questions and provide some perspective on where and how improved understanding and simulation of stratosphere-troposphere coupling are most likely to lead to improved skill. Throughout the chapter, it is important to emphasize that one of the significant difficulties in assessing and understanding stratosphere-troposphere coupling (in common with other low-frequency phenomena, such as Deser et al., 2017) is the relatively short observational record that exists for the stratosphere.
Fig. 1 highlights the major phenomena relevant to coupling between the stratosphere and troposphere, including the Quasi-Biennial Oscillation (QBO), solar variability, ozone, and the role of tropospheric planetary-scale waves.
Fig. 1
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Fig. 1. Schematic showing phenomena of known relevance to stratosphere-troposphere coupling. Contours show the zonal mean zonal wind schematically (red-filled contours indicate mean westerly winds and blue-filled indicate easterly winds). Left panel shows Southern Hemisphere (SH) winter and spring and right panel shows Northern Hemisphere (NH) winter and spring. Red- and blue-unfilled contours indicate zonal mean, zonal wind anomalies associated with the QBO.
Meteorology, Dynamic (Stratosphere)☆
Erdal Yiğit, Rolando R. Garcia, in Reference Module in Earth Systems and Environmental Sciences, 2018
Abstract
The stratosphere is the layer of Earth's atmosphere immediately above the troposphere; it extends from a lower boundary (the tropopause) whose altitude varies between about 8 and 16 km to an upper boundary (the stratopause) near 50 km. The stratosphere is characterized by increasing temperature with altitude, which is due primarily to the absorption of solar ultraviolet radiation by ozone. The meteorology of the stratosphere is governed mainly by the seasonal variation of heating due to absorption of solar radiation, and by the upward propagation of internal atmospheric waves originating in the troposphere. Transient processes such as sudden stratospheric warmings, and atmospheric waves can impact the middle and upper atmosphere and thus are a central subject of whole atmosphere coupling.
STRATOSPHERE/TROPOSPHERE EXCHANGE & STRUCTURE | Local Processes
J.F. Lamarque, P. Hess, in Encyclopedia of Atmospheric Sciences (Second Edition), 2015
The Subtropics
Stratosphere–troposphere exchange in this region occurs between the upper and mid-equatorial troposphere and the lowermost stratosphere. The subtropical tropopause drops rapidly near 30° from tropical heights to the level of the extratropical tropopause (approximately from 100 hPa to 300 hPa) (Figure 1). Trajectories from analyzed winds suggest very little STE occurs across this portion of the tropopause during the winter months but that considerable S