Satellite remote sensing of aerosols & clouds: An introduction

Transcription

1 Satellite remote sensing of aerosols & clouds: An introduction Jun Wang & Kelly Chance April 27, 2006

2 Outline Principals in retrieval of aerosols Principals in retrieval of water clouds Principals in retrieval of ice clouds Outstanding issues

3 Scattering regime The scattering of solar and terrestrial radiation by atmospheric aerosols and clouds is mostly in the Mie scattering regime.

4 1 channel retrieval algorithm Ω Ω Ω + = + = d P I B J d T J T I I s s s ) ( ) ( 4 ) ( ) (1 ) (,0) ( ) (,0) ( ), ( (0) 0 τ π ϖ τ ϖ τ τ τ τ τ τ λ λ τ In visible spectrum: Surface properties Aerosol properties Refractive index, Size, Shape, etc No Emission ) ( 4 (0) Ω + = = P R R F I R Define sfc sat µµ ϖτ µ π Under single scattering assumption and if surface reflectance is low: Key factors for the retrieval of AOT : ω, P(θ), and R sfc

5 Satellite retrieval of AOT in visible spectrum single scattering, low R sfc (<0.1) Key factors : ω, P(θ), and R sfc R sat = R sfc + ωτp(θ) 4µµ 0 Refractive index, Size, Shape, etc Sun Satellite τ Earth Surface Dust Optical Thickness Liu, Wang & Christopher, Int. J. Rem. Sen.,2003 simulated R sat (%)

6 2 channel retrieval algorithm Wavelength dependence can be used as an indicator to the aerosol size Eck et al., JGR, 1999 Urban aerosols in Washing DC Dust aerosols in Mongolia

7 Small vs. big size mode fraction d 2 2 dv 1 log = 10 r log10 rvn = C n exp log10 r n 1 2 log10σ n Angstrom exponent can provide information for small/big size

8 R sat = R sfc + Challenges: surface reflectance ωτp(θ) 4µµ 0 Only valid when Rsfc is small. Reflectance over ocean is low and relatively homogenous. Larger uncertainties over land. For small particles: Kaufman and Fraser, 1985

9 Smoke signal is not in NIR 0.46um 2.13um King et al., BAMS, um

10 Aerosol Effects on Reflected Solar Radiation over Land Biomass burning Cuiabá, Brazil (August 25, 1995) 10 km 20 km R = 0.66 µm G = 0.55 µm B = 0.47 µm θ0 = 36 R = 1.65 µm G = 1.2 µm B = 2.1 µm

11 Using NIR reflectance to derive VIS A g (0.47 µm) = 0.5 A g (0.66 µm) = 0.25A g (2.1 µm)

12 How aerosol optical properties are calculated? Remer et al., 2005 The selection of aerosol optical model primarily is primarily based on geographical locations.

13 MODIS AOT MODIS AOT. (a) fine mode AOT (b) coarse mode AOT, September 2000

14 Challenges: Aerosol optical property

15 MISR Imaging SpectroRadiometer MISR

16 Avoiding sunglint glint Sunglint over water invalidates the assumption of a dark surface, and multiple cameras provide the flexibility to avoid this smoke specular reflection of solar beam cloud ξ glint nadir 70º backward Southern Mexico 2 May 2002 MISR aerosol retrievals require glitter avoidance of at least 40º

17 Enhancing sensitivity to thin aerosols Thin haze over land is difficult to detect in the nadir view due to the brightness of the land surface The longer atmospheric path length enhances the haze path radiance nadir 70º Appalachians, 6 March 2000 nadir 70º 558-nm aerosol optical depth

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19 Radiance and Polarization Measurements from POLDER Western Europe March 10, 1997 R = µm G = µm B = µm Radiance Polarization Notice the land

20 POLDER April 1997 Aerosol Optical Thickness No Data Aerosol Optical Thickness (0.865 µm)

21 Ångström Exponent POLDER April 1997 No Retrieval No Data Angstrom Exponent

22 Remote sensing of water clouds

23 Determination of the Optical Thickness and Effective Particle Radius of Clouds Solar reflectance technique: Principles: The reflection function of a nonabsorbing band is primarily a function of optical depth. The reflection function of a near-ir absorbing band is primarily a function of effective radius. NAKAJIMA & King, 1990

24 Why choose the specific near IR and VIS channels? These channels (0.75, 1.64, 2.16 µm) are selected because they are outside the water vapor and oxygen absorption bands. A* the spherical albedo of a semi-infinite atmosphere, and m, n and I constants. All five asymptotic constants that appear in this expression [A*, m, n, 1 and k/( 1 - g)] are strongly dependent on the single scattering albedo ω 0, with a somewhat weaker dependence on g. These constants can be well represented by a function of a similarity parameter s, defined by (Nakajima & King, 1990)

25 Calculation of liquid water path Why is aerosol indirect effect important?

26 Retrieval

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28 Retrieval of Ice cloud Complicated: Shape Cloud retrieval algorithm for MODIS:

29 Other challenge issues Cloud phase Cloud morphology Ice crystals