Tropical Convection and the Energy Balance at the Top of the Atmosphere

By D. Hartmann, Leslie Moy, Q. Fu. 2001

288 citations recorded by the source corpus.

Subfields: Atmospheric Science, Global and Planetary Change

View Paper: https://www.semanticscholar.org/paper/e58337696ac617f70fbeb3d24a6b113b9d8ab182

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Citations in the corpus

Detection of tropical deep convective clouds from AMSU-B water vapor channels measurements (2005, background): “fraction is about 76% [Hartmann et al., 2001], so the deep convective cloud fraction in the region is about 0.”
Cloud feedback mechanisms and their representation in global climate models (2017, unknown): “The net neutrality of tropical cloud-radiative effects results from a cancelation between positive effects of thin anvil clouds and negative effects of the thicker rainy areas of the cloud.(146) That convective clouds tend to rise in a warmed climate has been discussed above, but it is also possible”
An important constraint on tropical cloud ‐ climate feedback (2002, background): “As the temperature drops below about 200 K, the vapor pressure becomes so low that emission from water vapor is inefficient and radiative relaxation times are very long and mostly dependent on CO2 emission [Hartmann et al., 2001a; Thuburn and Craig, 2002].”
Heat transfer and large scale dynamics in turbulent Rayleigh-Bénard convection (2008, background): “…group, Department of Science and Technology, J. M. Burgers Centre for Fluid Dynamics, and Impact-Institute, University of Twente, 7500 AE Enschede, The Netherlands (Dated: November 5, 2008) The progress in our understanding of several aspects of turbulent Rayleigh-Bénard convection is reviewed.”
On dynamic and thermodynamic components of cloud changes (2004, background): “Most of them represent the 23 tropical large-scale atmospheric circulation is a highly idealized way by considering one box of uniformly ascending motions and one box of uniformly descending motions (e.g. Pierrehumbert 1995, Miller 1997, Larson et al. 1999, Hartmann et al. 2001).”
Computing and Partitioning Cloud Feedbacks Using Cloud Property Histograms. Part I: Cloud Radiative Kernels (2012, methodology): “To quantify the role of changes in histogram-partitioned cloud fraction ( D C ) on the TOA radiative ﬂuxes, we ﬁrst compute the overcast-sky cloud radiative forcing corresponding to each bin of the histogram in a manner similar to that described in Hartmann et al. (2001) and Kubar et al. (2007).”
Insights from a refined decomposition of cloud feedbacks (2016, background): “Second, LW and SW radiative effects of the ensemble of free tropospheric clouds closely cancel [Kiehl, 1994; Hartmann et al., 2001], so changes in their coverage holding their altitude and optical depth fixed should result in a near-zero net amount feedback.”
How Well Do We Understand and Evaluate Climate Change Feedback Processes (2006, background): “Kiehl (1994) argued this is coincidental, while Hartmann et al. (2001) suggest this is a property of the ensemble of cloud types that occurs in association with deep convection in the Tropics.”
Surface Fluxes and Tropical Intraseasonal Variability: a Reassessment (2008, background): “Satellite observations have shown that, in the mean, these clouds produce perturbations in the net radiative energy flux at the top of the atmosphere which are small compared to their largely cancelling shortwave and longwave components (Ramanathan et al. 1989; Harrison et al. 1990; Hartmann et al. ”