Abstract:A method is presented for determining the optical absorption coefficient, or the imaginary refractive index, of particulate material that has been collected from aerosols or hydrosols by means of filtration. The method, based on the Kubelka-Munk theory of diffuse reflectance, is nondestructive and requires no other knowledge of the sample than the amount present, the specific gravity, and an estimate of the real index of refraction. The theoretical development of the method is discussed along with an analysis … Show more
“…The bulk absorption coefcient (¾ a ) and the mass-speci c absorption (B a ) for the ANL, PSC, and UPRA samples are presented in Table 5. The absorption coef cient was calculated from the relation k D (¸=4¼ )¾ a (Gosse et al 1997;Lindberg et al 1994), and the mass-speci c absorption was calculated by assuming black carbon to be the major absorbing component of the aerosol, with a density of 1,200 kg/m 3 (Horvath 1993). The mass-speci c absorption coef cients ranged from 5.7 to 16 m 2 /g.…”
To adequately assess the effects of atmospheric aerosols on climate, their optical constants (scattering and absorption coef cients) must be known. The absorption and scattering coef cients of the aerosols are derived from the real and imaginary parts of the complex refractive index and are dependent on their size and chemical composition. Because aerosol properties vary signi cantly with location, it is dif cult to assign values for the absorption and scattering of solar radiation by aerosols in models of global climate change. This study reports a new method of collecting size-fractionated atmospheric aerosol samples for the purpose of directly measuring their transmission and re ectance spectra followed by the determination of the complex refractive index across the entire atmospherically relevant spectral range. The samples were collected with a modi ed Sierra high-volume cascade impactor with the usual lter collection surfaces replaced with Te on sheets machined to hold quartz (ultraviolet [UV]/visible transparent) and/or silver chloride (infrared transparent) sample collection plates. Re ectance and transmission spectra can be obtained on the aerosol samples directly as a function of wavelength, from 280 nm to 2.5 m, with an integrating sphere coupled to an UV/visible or a Fourier transform infrared (FTIR) spectrophotometer. The effective real and imaginary components of the refractive index of the bulk sample material can then be approximated, as a function of wavelength, from the sample spectra. Preliminary results are presented for carbon soot samples generated in the laboratory and for standard diesel soot samples in the UV/visible spectral range. These are compared to results obtained for size-fractionated atmospheric aerosol samples collected near Pasco, WA, West Mesa, AZ, and Argonne, IL.
“…The bulk absorption coefcient (¾ a ) and the mass-speci c absorption (B a ) for the ANL, PSC, and UPRA samples are presented in Table 5. The absorption coef cient was calculated from the relation k D (¸=4¼ )¾ a (Gosse et al 1997;Lindberg et al 1994), and the mass-speci c absorption was calculated by assuming black carbon to be the major absorbing component of the aerosol, with a density of 1,200 kg/m 3 (Horvath 1993). The mass-speci c absorption coef cients ranged from 5.7 to 16 m 2 /g.…”
To adequately assess the effects of atmospheric aerosols on climate, their optical constants (scattering and absorption coef cients) must be known. The absorption and scattering coef cients of the aerosols are derived from the real and imaginary parts of the complex refractive index and are dependent on their size and chemical composition. Because aerosol properties vary signi cantly with location, it is dif cult to assign values for the absorption and scattering of solar radiation by aerosols in models of global climate change. This study reports a new method of collecting size-fractionated atmospheric aerosol samples for the purpose of directly measuring their transmission and re ectance spectra followed by the determination of the complex refractive index across the entire atmospherically relevant spectral range. The samples were collected with a modi ed Sierra high-volume cascade impactor with the usual lter collection surfaces replaced with Te on sheets machined to hold quartz (ultraviolet [UV]/visible transparent) and/or silver chloride (infrared transparent) sample collection plates. Re ectance and transmission spectra can be obtained on the aerosol samples directly as a function of wavelength, from 280 nm to 2.5 m, with an integrating sphere coupled to an UV/visible or a Fourier transform infrared (FTIR) spectrophotometer. The effective real and imaginary components of the refractive index of the bulk sample material can then be approximated, as a function of wavelength, from the sample spectra. Preliminary results are presented for carbon soot samples generated in the laboratory and for standard diesel soot samples in the UV/visible spectral range. These are compared to results obtained for size-fractionated atmospheric aerosol samples collected near Pasco, WA, West Mesa, AZ, and Argonne, IL.
“…H anel (1987,1994) applied radiative transfer schemes to deal with the radiative transfer problem for a plane layer that both scatters and absorbs radiation. Lindberg, Douglass, & Garvey (1994) employed a variation of the Kubelka-Munk theory of di use re ectance and considered a single layer consisting of an aerosol-powder mixture.…”
“…(24) to relate estimates of the median diameters of various distribution functions in order to overcome the limitations of Eq. (38), is doubtful.…”
Section: Geometric Mean Diametersmentioning
confidence: 99%
“…In the German (DIN) notation, however, the mean diameter r k x , is expressed only in terms of the median and the geometrical standard deviation of its density function ) (x q r , see Eq. (38). Using an equation similar to Eq.…”
Section: Geometric Mean Diametersmentioning
confidence: 99%
“…Values of the real component of refractive indices have been published for many bulk materials [37]. The imaginary refractive component (i.e., the absorption part) is more difficult to find in the literature [38,39]. Mie theory, which describes scattering of light by homogeneous spheres of arbitrary size, is the most rigorous scattering model available, and is used in many commercial instruments.…”
Section: A3 An Overview Of Particle Size Distribution Measurement Mementioning
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