4.6 The Climate Impact of Aerosols on the Lightning Flash Rate: Is It Detectable from Long-Term Measurements?

Wednesday, 9 January 2019: 9:45 AM
North 225AB (Phoenix Convention Center - West and North Buildings)
Zhanqing Li, Univ. of Maryland, College Park, College Park, MD; and Q. Wang and J. Guo

The effect of aerosols on lightning has been noted in many case studies, but much less is known about the long-term impact, relative importance of dynamics-thermodynamics versus aerosol, and any difference by different types of aerosols. Attempts are made to tackle with all these factors whose distinct roles are discovered by analyzing 11-year datasets of lightning, aerosol loading and composition, and dynamic-thermodynamic data from satellite and model reanalysis. Variations in the lightning rate are analyzed with respect to changes in dynamic-thermodynamic variables and indices such as the convective available potential energy (CAPE), vertical wind shear, etc. In general, lightning has strong diurnal and seasonal variations, peaking in an afternoon and summer. The lightning flash rate is much higher in moist central Africa than in dry northern Africa presumably because of the combined influences of surface heating, CAPE, relative humidity, and aerosol type. In both regions, the lightning flash rate changes with AOD in a boomerang shape: first increasing with AOD, tailing off around AOD = 0.3, and then behaving differently, i.e., decreasing for dust and flattening for smoke aerosols. The deviation is arguably caused by the tangled influences of different thermodynamics (in particular humidity and CAPE) and aerosol type between the two regions. In northern Africa, the two branches of opposite trends seem to echo the different dominant influences of the aerosol microphysical effect and the aerosol radiative effect that are more pronounced under low and high aerosol loading conditions, respectively. Under low AOD conditions, the aerosol microphysical effect more likely invigorates deep convection. This may gradually yield to the suppression effect as AOD increases, leading to more and smaller cloud droplets that are highly susceptible to evaporation under the dry conditions of northern Africa. For smoke aerosols in moist central Africa, the aerosol invigoration effect can be sustained across the entire range of AOD by the high humidity and CAPE. This, plus a potential heating effect of the smoke layer, jointly offset the suppression of convection due to the radiative cooling at the surface by smoke aerosols. Various analyses were done that tend to support this hypothesis.
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