Atmospheric Chemistry and Physics Discussions
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10.5194/acpd-7-753-2007
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753
783
2007-01-18
The direct effect of aerosols on solar radiation based on satellite observations, reanalysis datasets, and spectral aerosol optical properties from Global Aerosol Data Set (GADS)
N. Hatzianastassiou
nhatzian@cc.uoi.gr
C. Matsoukas
E. Drakakis
P. W. Stackhouse Jr.
P. Koepke
A. Fotiadi
K. G. Pavlakis
I. Vardavas
Laboratory of Meteorology, Department of Physics, University of Ioannina, 45110 Ioannina, Greece
Foundation for Research and Technology-Hellas, Heraklion, Crete, Greece
Department of Environment, University of the Aegean, Mytilene, Greece
Department of Physics, University of Crete, Crete, Greece
Department of Electrical Engineering, Technological Educational Institute of Crete, Heraklion, Greece
Atmospheric Sciences, NASA Langley Research Center, Hampton, Virginia, USA
Meteorological Institute, University of Munich, Munich, Germany
Department of General Applied Science, Technological Educational Institute of Crete, Heraklion, Greece
A global estimate of the seasonal direct radiative effect (DRE) of natural
plus anthropogenic aerosols on solar radiation under all-sky conditions is
obtained by combining satellite measurements and reanalysis data with a
spectral radiative transfer model. The estimates are obtained with detailed
spectral model computations separating the ultraviolet (UV), visible and
near-infrared wavelengths. The global distribution of spectral aerosol
optical properties was taken from the Global Aerosol Data Set (GADS) whereas
data for clouds, water vapour, ozone, carbon dioxide, methane and surface
albedo were taken from various satellite and reanalysis datasets. Using
these aerosol properties and other related variables, we generate
climatological (for the 12-year period 1984–1995) monthly mean aerosol DREs.
The global annual mean DRE on the outgoing SW radiation at the top of
atmosphere (TOA, ΔF<sub>TOA</sub>) is 1.62 Wm<sup>−2</sup> (with a range of –10 to 15 Wm<sup>−2</sup>, positive values corresponding to planetary cooling), the effect on the atmospheric absorption of SW
radiation (ΔF<sub>atmab</sub>) is 1.6 Wm<sup>−2</sup> (values up to 35 Wm<sup>−2</sup>, corresponding to atmospheric warming),
and the effect on the surface downward and absorbed SW radiation
(Δ F<sub>surf</sub>, and ΔF<sub>surfnet</sub>, respectively) is –3.93 and
–3.22 Wm<sup>−2</sup> (values up to –45 and –35 Wm<sup>−2</sup>, respectively, corresponding to surface cooling.)
According to our results, aerosols decrease/increase the planetary albedo by –3 to
13% at the local scale, whereas on planetary scale the result is an
increase of 1.5%. Aerosols can warm locally the atmosphere by up to 0.98 K day<sup>−1</sup>,
whereas they can cool the Earth's surface by up to –2.9 K day<sup>−1</sup>. Both these effects, which can significantly modify atmospheric
dynamics and the hydrological cycle, can produce significant planetary
cooling on a regional scale, although planetary warming can arise over
highly reflecting surfaces. The aerosol DRE at the Earth's surface compared
to TOA can be up to 15 times larger at the local scale. The largest aerosol
DRE takes place in the northern hemisphere both at the surface and the
atmosphere, arising mainly at ultraviolet and visible wavelengths.
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