Fascinating analysis. Consistent with my tropical met training. Saturated boundary layer at dawn; weak inversion; AM insolation/heating overturns the boundary layer mixing drier/cooler air from aloft; random CU form; low/medium sun angle reflects off sides of CU casting medium/long shadows; late morning sun angle increases reducing CU shadow footprint; surface heating increases; random CU organize into TCU; max insolation/heating in early afternoon; CB and rainfall mid-late afternoon; surface insolation/heating reduced by CB-induced CS footprint; surface also cooled by rainfall and subsidence/downdraft of cooler drier air aloft. Rinse, repeat.
Guest Post by Willis Eschenbach
I discussed the role of tropical albedo in regulating the temperature in two previous posts entitled Albedic Meanderings and An Inherently Stable System. This post builds on that foundation. I said in the latter post that I would discuss the diurnal changes in tropical cloud albedo. For this I use a marvelous dataset called the TAO dataset. It is measurements from a number of moored buoys in the tropical Pacific.
Sadly, despite the billions spent on “global warming”, the TAO buoys don’t have funds for maintenance. As a result, the records from some have ceased entirely. But I digress … the great thing about the TAO buoy records is that they are either hourly, or every ten minutes, or even every two minutes in some cases…
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