1. An important constraint on tropical cloud-climate feedback Dennis L. Hartmann and Kristin Larson Geophysical Res. Lett., 2002

2. The emission temperature of tropical anvil clouds doesn’t depend on SST, thus it will remain constant during climate change. Positive feedback Main result: This is relevant for climate change, because LW radiative effects of tropical convection are dominated by convective anvil clouds.

4. In the tropics: the heat balance is between convective heating and radiative cooling The most active convection is constrained to the altitude where radiative cooling is efficient Observations show a peak of probability of optically thick cloud tops (i.e. anvils) at 200 hPa and that clear- sky cooling rate decreases rapidly above 200 hPa The radiative cooling is balanced by adiabatic heating (subsidence). The rapid decrease in clear-sky cooling is accompanied by a strong convergence of mass at 200 hPa, which is balanced by a strong divergence of mass from the convective regions

5. Hypothesis: Even if SST increases, the emission temperature of anvil clouds remains the same.

6. The temperature at which tropical convection detrains and convective anvil tops occur is constrained by the Clausius-Clapeyron relationship. This is because anvil tops occurs where cooling rate declines rapidly, and this happens when water vapor emission becomes inefficient. Low water vapor emissivity is due to low saturation vapor pressure, which is related principally to the air temperature through C-C, rather than to pressure. Physical explanation:

7. Test of hypothesis with model: 3D Radiative-Convective model in which they specify SST and solve for equilibrium climate of the troposphere as a function of SST Convective (non-convective) regions of the models are defined to be those with ice visible optical depths > (<)0.1

9. Results (I): Clear-sky cooling decreases rapidly with height way before tropopause. As T drops < 200 K, emission from water vapor becomes inefficient. As SST goes up, the pressure at which rapid cooling occurs goes down (height goes up). This is because the troposphere warms up more than surface, so that the pressure (height) where T drops < 200 K gets lower (higher).

10. T@ cooling rate drops off T@ const 200 hPa T@ high clouds anvils T@ max/min vertical vel.

11. Results (II): The T where cooling rate drops is about const. compared to the T at fixed p = 200 hPa.

12. Ideas for CRG -> Fall 2012: 1.ENSO (mechanisms, teleconnections, prediction, asymmetry, climate change…) 2.IPCC/Anthropogenic climate change 3.Aerosols radiative impacts on climate 4.TCs and climate variability 5.Models uncertainty 6.Decadal variability/predictability 7.Stochastic climate models/Noise 8.ITCZs, single or not 9.Teleconnections 10.Stratocumulus clouds 11.Subtropical highs (already done?) 12.Simple climate models