A Model for Transport across the Tropical Tropopause.

By S. Sherwood, Andrew E. Dessler. 2001

206 citations recorded by the source corpus.

Subfields: Atmospheric Science, Global and Planetary Change

View Paper: https://www.semanticscholar.org/paper/f6ae4b56e3ac2ecb93374f980b6a0f425bb65f17

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Citations in the corpus

Kelvin wave variability near the equatorial tropopause observed in GPS radio occultation measurements (2005, background): “[23] The cold temperature anomalies that overly convection near and below the tropopause (� 14–17 km) in Figures 14a and 15 are consistent with cooling due to convective detrainment above the level of neutral buoyancy [ Sherwood and Dessler, 2001; Kuang and Bretherton, 2004].”
The impact of cirrus clouds on tropical troposphere-to-stratosphere transport (2006, unknown): “Moreover, it is thought to be the highest level reached by the deepest convection (e.g., Kelly et al., 1993; Sherwood and Dessler, 2001).”
Unprecedented evidence for deep convection hydrating the tropical stratosphere (2008, background): “[4] The alternative hypothesis, ‘‘convective dehydration’’, postulates that dehydration occurs mainly in very deep, overshooting convection [e.g., Danielsen, 1993; Sherwood and Dessler, 2001].”
A Climatology of the Tropical Tropopause Layer (2002, methodology): “As shown by Sherwood and Dessler (2001) , even a small fraction of convection can have a significant effect on water vapor and ozone in the Fig. 10. Altitude of tropically averaged zero clear sky radiative heating ðQclear ¼ 0Þ estimated using a detailed radiative model (see text) with a monthly mea”
Modeling atmospheric stable water isotopes and the potential for constraining cloud processes and stratosphere‐troposphere water exchange (2005, background): “…include (a) the gradual ascent of water vapor that undergoes freeze-drying at the tropical tropopause, (b) uplift of thin cirrus ice particles and (c) episodic lofting of ice by deep convective overshoot [Holton et al., 1995; Holton and Gettelman, 2001; Sherwood and Dessler, 2001] (among others).”
Tropical troposphere‐to‐stratosphere transport inferred from trajectory calculations (2004, background): “Sherwood and Dessler [2000] termed this layer the ‘‘tropical tropopause layer’’ (TTL) and defined its boundaries to be the level of zero net radiative heating (� 350 K) and the highest level that convection reaches (� 420 K). Air in this layer is considered to slowly ascend through net radiative hea”
Thermal variability of the tropical tropopause region derived from GPS/MET observations (2003, background): “The June–July 1995 and February 1997 time periods also have the highest data quality, so-called ‘prime times’ associated with encryption of the GPS signal [Rocken et al., 1997].”
Detection of tropical deep convective clouds from AMSU-B water vapor channels measurements (2005, methodology): “The tropical tropopause layer (TTL) between about 14–18 km [e.g., Sherwood and Dessler, 2000, 2001; Alcala and Dessler, 2002] is the important transition layer between the convectively dominated tropical troposphere and the radiatively controlled stratosphere [e.g., Highwood and Hoskins, 1998;…”