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using the aerosols as passive tracers of the atmospheric dynamic processes. The sun photometer data are used to provide the aerosol optical thickness (AOT) values at selected wavelengths and thus, to derive the Ångström exponent (AE) values. The synergy of Cimel and lidar measurements also acts to minimize the uncertainties of the assumptions made, especially when inverting the lidar signal using Klett’s technique ( Klett 1985 ). In Brazil, a continent-sized country, there are only two operating
using the aerosols as passive tracers of the atmospheric dynamic processes. The sun photometer data are used to provide the aerosol optical thickness (AOT) values at selected wavelengths and thus, to derive the Ångström exponent (AE) values. The synergy of Cimel and lidar measurements also acts to minimize the uncertainties of the assumptions made, especially when inverting the lidar signal using Klett’s technique ( Klett 1985 ). In Brazil, a continent-sized country, there are only two operating
function is estimated to be equal to 1 between 350 and 500 m ( Matthias et al. 2004b ). An AERONET sun/sky radiometer is used to retrieve columnar aerosol volume size distributions, real and imaginary refractive indices ( n and k ), single-scattering albedo (SSA) values, and aerosol optical thicknesses (AOTs). The automatic, robotically operated sun-tracking sky radiometer, with a 1.2° field of view and two detectors, measures the direct sun radiance at eight spectral channels: 340, 380, 440, 500
function is estimated to be equal to 1 between 350 and 500 m ( Matthias et al. 2004b ). An AERONET sun/sky radiometer is used to retrieve columnar aerosol volume size distributions, real and imaginary refractive indices ( n and k ), single-scattering albedo (SSA) values, and aerosol optical thicknesses (AOTs). The automatic, robotically operated sun-tracking sky radiometer, with a 1.2° field of view and two detectors, measures the direct sun radiance at eight spectral channels: 340, 380, 440, 500
(the transition layer between PBL and the free troposphere) are not well understood and thus are not well parameterized in atmospheric models. Observations of fluxes covering the entire PBL and the entrainment zone are rare. With respect to aerosols, vertical transport is even more complicated because the ascent of particles is often combined with water uptake because of a relative humidity increase with height in the PBL. The particle mass concentration and optical and microphysical properties
(the transition layer between PBL and the free troposphere) are not well understood and thus are not well parameterized in atmospheric models. Observations of fluxes covering the entire PBL and the entrainment zone are rare. With respect to aerosols, vertical transport is even more complicated because the ascent of particles is often combined with water uptake because of a relative humidity increase with height in the PBL. The particle mass concentration and optical and microphysical properties
. Rev. , 132 , 2954 – 2976 . 10.1175/MWR2839.1 Turner, D. , Ferrare R. , Brasseur L. H. , Feltz W. , and Tooman T. , 2002 : Automated retrievals of water vapor and aerosol profiles from an operational Raman lidar. J. Atmos. Oceanic Technol. , 19 , 37 – 50 . 10.1175/1520-0426(2002)019<0037:AROWVA>2.0.CO;2 Wandinger, U. , 2005 : Raman lidar. Lidar: Range-Resolved Optical Remote Sensing of the Atmosphere, C. Weitkamp, Ed., Springer, 241–271 . Whiteman, D. , 2003 : Examination
. Rev. , 132 , 2954 – 2976 . 10.1175/MWR2839.1 Turner, D. , Ferrare R. , Brasseur L. H. , Feltz W. , and Tooman T. , 2002 : Automated retrievals of water vapor and aerosol profiles from an operational Raman lidar. J. Atmos. Oceanic Technol. , 19 , 37 – 50 . 10.1175/1520-0426(2002)019<0037:AROWVA>2.0.CO;2 Wandinger, U. , 2005 : Raman lidar. Lidar: Range-Resolved Optical Remote Sensing of the Atmosphere, C. Weitkamp, Ed., Springer, 241–271 . Whiteman, D. , 2003 : Examination
