Post on 11-Jan-2017
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
!Atmospheric Correction of Ocean Color
RS Observations
Menghua Wang
NOAA/NESDIS/STARE/RA3, Room 102, 5200 Auth Rd.Camp Springs, MD 20746, USA
IOCCG Summer Lecture Series, Villefranche-sur-Mer, France, July 2-14, 2012
!"#$%&'()*(+($,-./!"#$%&'"()*"+%#,--.#,"/%#%"(*)01%*.)2+"0.++.)&+3",4543"6,%7.863"9:;!63"%&/"<!!=63
,#>43".&"+.#2"/%#%"(*)0"6,%?@66"A(*)0"1%*.)2+"B!+C"%&/
+)0,")#$,*"/%#%D%+,+4"6)0,"+-./,+"%*,"(*)0"E)F%*/
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Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
1. Introduction! Brief history! Basic concept of ocean color measurements! Why need atmospheric correction
2. Radiometry and optical properties! Basic radiometric quantities! Apparent optical properties (AOPs)! Inherent optical properties (IOPs)
3. Optical properties of the atmosphere! Molecular absorption and scattering! Aerosol properties and models
— Non- and weakly absorbing aerosols— Strongly absorbing aerosols (dust, smoke, etc.)
4. Radiative Transfer! Radiative Transfer Equation (RTE)! Successive-order-of-scattering method! Single-scattering approximation
Lecture Outlines (1)
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
5. Atmospheric Correction! Define reflectance and examine the various terms! Sea surface effects! Atmospheric diffuse transmittance! Normalized water-leaving radiance! Single-scattering approximation! Aerosol multiple-scattering effects! Open ocean cases: using NIR bands for atmospheric correction! Coastal and inland waters
— Brief overviews of various approaches— The SWIR-based atmospheric correction
! Examples from MODIS-Aqua measurements
6. Addressing the strongly-absorbing aerosol issue! The issue of the strongly-absorbing aerosols! Some approaches for dealing with absorbing aerosols! Examples of atmospheric correction for dust aerosols using MODIS-Aqua
and CALIPSO data
7. Requirements for future ocean color satellite sensors
8. Summary
Lecture Outlines (2)
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
IOCCG Report #10 at http://www.ioccg.org/reports_ioccg.html“Atmospheric Correction for Remotely-Sensed Ocean ColourProducts”.
Reference citations from my presentation can be found from thereport.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
1. Introduction! Brief history! Basic concept of ocean color measurements! Why need atmospheric correction
Introduction
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
" Color photographs of the oceans were obtained from spacecraft (Apollo, etc.,1960’s).
" Clarke et al. (1970) showed the systematic measurements of radiance spectra ofsea (ocean color) from aircraft, demonstrated the possibility of detecting thechlorophyll concentration within the ocean upper layers. They also showedatmospheric effects on the measured signals.
" Tyler & Smith (1970) performed field measurements of upward & downwardirradiance spectra in different water bodies. Thereafter, many similar in situ wateroptical measurements.
" Interpretation of in situ reflectance measurements was given in the frame ofradiative transfer by Gordon et al. (1975) and also in terms of optically-significantwater substances by Morel and Prieur (1977) and Smith and Baker (1978).
" Gordon (1978; 1980) developed a single-scattering atmospheric correctionalgorithm for processing the NASA CZCS ocean color data, demonstrating thefeasibility of satellite ocean color remote sensing.
" Advanced atmospheric correction algorithm (Gordon and Wang, 1994) has beendeveloped for various more sophisticated ocean color satellite sensors, e.g.,SeaWiFS, OCTS, MODIS, MERIS, etc., following the successful CZCS proof ofconcept mission.
" In recent years, atmospheric correction effort has been on dealing with morecomplex water properties in coastal and inland waters, as well as strongly-absorbing aerosols.
Brief History
IOCCG Report-10
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Satellite ocean color remote sensing is possible because
" Ocean color (spectral radiance/reflectance) data--water-leaving radiance/reflectance spectra--can be related to waterproperties, e.g., chlorophyll-a concentration. In other words,there exist various relationships between water opticalproperty and water biological / biogeochemical et al.properties.
" It is possible to carry out atmospheric correction for derivingaccurate water radiance/reflectance spectra data from satellitemeasurements.
Satellite Ocean Color Measurements
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction Chesapeake BayLake Taihu
Ocean Color Spectra
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Satellite-Measured Reflectance (Radiance)
!t "( ) = !r "( )Rayleigh!
+ !A "( )Aerosols"#$
+ t "( )t0 "( )Transmittance" #% $%
!w "( )#$ %&N
Ocean" #% $%
Satellite-Measured Ocean Contribution" #%%% $%%%
! "( ) = # L "( ) µ0 F0 "( )
!path "( ) = !r "( ) + !A "( )!a "( )+!ra "( )!"#
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Normalized water-leaving radiance:
Lw !( )"# $%N, nLw !( ) mWcm-2
µm-1 str-1
Normalized water-leaving reflectance:
!w "( )#$ %&N, !wN "( ) unitless
Remote sensing reflectance:
Rrs !( ) = "wN !( ) /# str-1
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Ocean Color Remote Sensing
Sensor-Measured
Blue ocean
“Green” ocean
From H. Gordon
Atmospheric Correction (removing >90% sensor-measured signals)
Calibration (0.5% error in TOA >>>> 5% in surface)
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Ocean Contributions:
Case-1 Waters
10-2
10-1
100
101
400 450 500 550 600 650 700
C = 0.03 mg/m 3
C = 0.10 mg/m 3
C = 0.30 mg/m 3
C = 1.00 mg/m 3
[ !w ("
)]N (
%)
Wavelength (nm)
Case-1 Water: Gordon et al. (1988)
(a)
10-2
10-1
100
101
400 500 600 700 800 900
Sediment WatersYellow-Substance
[!w("
)] N
(%
)
Wavelength (nm)
Examples of Case-2 Water
(b)
Ocean Contributions:
Case-2 Waters
IOCCG Report-10
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Satellite Sensor Measured TOA Reflectance Spectra
10-2
10-1
400 500 600 700 800 900
Case 1, C = 0.1 mg/m 3
Case 2, Sediment DominatedCase 2, Yellow Substance
Wavelength (nm)
TO
A R
efle
cta
nce
!t("
)
(a)
M80 model, #a(865) = 0.1
$0 = 60o, $ = 45o, %& = 90o
IOCCG Report-10
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
The TOA Ocean Contributions
0
10
20
30
40
50
400 500 600 700 800 900
Case 1, C = 0.1 mg/m 3
Case-2, Sediment DominatedCase-2, Yellow Substance
Wavelength (nm)
% o
f T
OA
t!
w( "
)
M80 model, #a(865) = 0.1
$0 = 60o, $ = 45o, %& = 90o
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Ocean TOA Radiance Contributions for Case-1 Waters
10-2
10-1
0
1
400 500 600 700 800 900
Case-1, C = 0.1 mg/m 3
Rayleigh, Black Ocean
Wavelength (nm)
M80 model, !a(865) = 0.1
Ratio "r(#)/"
t(#)
Ratio "path
(#)/"t(#)
"r(#)
"t(#)
$0 = 60o, $ = 45o, %& = 90o
(b)
TO
A R
efle
cta
nce
"t(#
)
Reflectance
RatioIOCCG Report-10
15
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
For a typical Case-1 (open ocean) water:Satellite-Measured water-leaving reflectancecontributions at the TOA are 6.4%, 9.8%, 12.1%,10.8%, 5.5%, and 1.3% at wavelengths of 412, 443,490, 510, 555, and 670 nm.
IOCCG Report-10
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Ocean TOA Radiance Contributions for
Sediment-type Case-2 Waters
10-2
10-1
0
1
400 500 600 700 800 900
Case-2, Sediment
Rayleigh, Black Ocean
Wavelength (nm)
M80 model, !a(865) = 0.1
Ratio "r(#)/"
t(#)
Ratio "path
(#)/"t(#)
"r(#)
"t(#)
$0 = 60o, $ = 45o, %& = 90o
(c)
Re
flecta
nce
Ra
tio V
alu
e
IOCCG Report-10 17
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
For a typical sediment-dominated water:Satellite-Measured water-leaving reflectancecontributions at the TOA are 5.8%, 11.2%, 26.3%,30.6%, 39.0%, 16.4%, 3.7%, and 2.4% at wavelengthsof 412, 443, 490, 510, 555, 670, 765, and 865 nm.
IOCCG Report-10
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
10-2
10-1
0
1
400 500 600 700 800 900
Case-2, Yellow Subs.Rayleigh, Black Ocean
Wavelength (nm)
M80 model, !a(865) = 0.1
Ratio "r(#)/"
t(#)
Ratio "path
(#)/"t(#)
"r(#)
"t(#)
$0 = 60o, $ = 45o, %& = 90o
(d)
TO
A R
efle
cta
nce
"t(#
)R
efle
cta
nce
Ra
tio V
alu
e
Signals are
very small
IOCCG Report-1019
Ocean TOA Radiance Contributions for
Yellow Substance-type Case-2 Waters
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
For a yellow-substance-dominated water:Satellite-Measured water-leaving reflectancecontributions at the TOA are 0.2%, 0.4%, 1.2%, 1.7%,3.6%, 5.3%, 1.2%, and 1.0% at wavelengths of 412,443, 490, 510, 555, 670, 765, and 865 nm.
It is very difficult to do atmospheric correction at theblue bands.
IOCCG Report-10
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
At satellite altitude~90% of sensor-measured signal over ocean
comes from the atmosphere & surface!
Factor of 1:10 from TOA to the surface
• It is crucial to have accurate atmospheric correction andsensor calibrations.
• 0.5% error in atmospheric correction or calibrationcorresponds to possible of ~5% error in the derived oceanwater-leaving radiance.
• We need ~0.1% sensor calibration accuracy.
Atmospheric Correction
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Ocean Color Remote Sensing: Derive theocean water-leaving radiance spectra byaccurately removing the atmospheric andsurface effects.
Ocean properties: e.g., chlorophyll-aconcentration, diffuse attenuation coefficientat 490 nm, can be derived from the oceanwater-leaving radiance spectra.
22
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
References
Austin, R. W. (1974), The remote sensing of spectral radiance from below the ocean surface, in Optical Aspects ofOceanography, edited by N. G. Jerlov and E. S. Nielsen, pp. 317-344, Academic, San Diego, Calif.
Bricaud, A., and A. Morel (1987), Atmospheric correction and interpretation of marine radiances in CZCS imagery: useof a reflectance model, Oceanologica Acta, SP, 33-50.
Clarke, G. K., G. C. Ewing, and C. J. Lorenzen (1970), Spectra of backscattered light from the sea obtained from aircraftas a measure of chlorophyll, Science, 167, 1119-1121.
Gordon, H. R., O. B. Brown, and M. M. Jacobs (1975), Computed relationship between the inherent and apparent opticalproperties of a flat homogeneous ocean, Appl. Opt., 14, 417-427.
Gordon, H. R. (1978), Removal of atmospheric effects from satellite imagery of the oceans, Appl. Opt., 17, 1631-1636.
Gordon, H. R. (1980), A preliminary assessment of the NIMBUS-7 CZCS atmospheric correction algorithm in ahorizontally inhomogeneous atmosphere, in Oceanography from Space, edited by J. F. R. Gower, pp. 281-294,Plenum Press, New York and London.
Gordon, H. R., and D. K. Clark (1981), Clear water radiances for atmospheric correction of coastal zone color scannerimagery, Appl. Opt., 20, 4175-4180.
Gordon, H. R., and A. Morel (1983), Remote assessment of ocean color for interpretation of satellite visible imagery: Areview, 114 pp., Springer-Verlag, New York.
Gordon, H. R., and M. Wang (1994), Retrieval of water-leaving radiance and aerosol optical thickness over the oceanswith SeaWiFS: A preliminary algorithm, Appl. Opt., 33, 443-452.
Morel, A. (1980), In-water and remote measurements of ocean color, Boundary-layer Meteorology, 18, 177-201.
Morel, A., and L. Prieur (1977), Analysis of variations in ocean color, Limnol. Oceanogr., 22, 709-722.
Smith, R. C., and K. S. Baker (1978), The bio-optical state of ocean waters and remote sensing, Limnol. Oceanogr., 23,247-259.
Smith, R. C., and W. H. Wilson (1981), Ship and satellite bio-optical research in the California Bight, in Oceanographyfrom Space, edited by J. F. R. Gower, pp. 281-294, Plenum Press, New York and London.
Tyler, J. E., and R. C. Smith (1970), Measurements of spectral irradiance underwater, 103 pp., Gordon and BreachScience Publishers.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
2. Radiometry and optical properties! Basic radiometric quantities! Apparent optical properties (AOPs)! Inherent optical properties (IOPs)
Radiometry and Optical Properties
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Radiant Power:
P !( ) = Nhc
!/ t = Energy / t N " # of photons
Radiance is Apparent Optical Property (AOP).Ocean color sensors measure Radiance!
Definition of Radiance L:
L !( ) ="
2P !( )
cos# "$"A
Apparent Optical Properties
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Absorption coefficient a:
a !( ) ="P !( )
P !( )"l
Scattering coefficient b:
Inherent Optical Properties (IOPs) (1)
b !( ) ="P !( )
P !( )"l
Extinction coefficient c:
c !( ) ="P !( )
P !( )"l= a !( ) + b !( )
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Volume Scattering Function:
! "( ) =#2
P $( )
P $( )#%#l
Scattering phase function P:
Inherent Optical Properties (IOPs) (2)
P !( ) =" !( )
b
! "( )4#$ d% =
&P '( )
P '( )&l( b '( )
Definition of Scattering Angle
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
The single scattering albedo is a dimensionlessparameter which represents the percentage of photonsbeing scattered in the single scattering case:
!0 "( ) =b "( )
c "( )
Single-Scattering Albedo
Optical Thickness (e.g., aerosol optical thickness (AOT),Rayleigh optical thickness, cloud optical thickness, etc.)
! "( ) = c #z ,"( )0
Z
$ d #z
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
3. Optical properties of the atmosphere! Molecular absorption and scattering! Aerosol properties and models
— Non- and weakly absorbing aerosols— Strongly absorbing aerosols (dust, smoke, etc.)
Optical Properties of the Atmosphere
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Molecular (Rayleigh) Scattering
" The scattering of air molecules is purely electric dipole incharacter.
" The scattering phase function is symmetry, i.e., equalamounts of radiance are scattered into the forward andbackward directions.
" The amount of scattered radiance varies nearly as theinverse fourth power of wavelength (blue sky).
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Molecular (Rayleigh) Scattering
Rayleigh Phase Function: Pr !( ) "1+ cos2!
The Rayleigh optical thickness is (Hansen & Travis, 1974):
! r ",P0( ) = 0.008569"#4 1+ 0.0113"#2+ 0.00013"#4( )
P0 is the standard atmospheric pressure of 1013.25 hPa, andfor a pressure P,
! r ",P( ) = ! r ",P0( )P
P0
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Atmospheric Pressure
Variation
Usually, it is within~±3%
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Haze C Aerosol Model
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Shettle and Fenn (1979)Aerosol Models
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Aerosol Optical Property
The complex refractive index of aerosol particles is:m = mr - i mi,
mr is the real refractive index, e.g., ~1.33 for water in the visible,and mi the index related to particle absorption.
" Aerosol particles can be characterized with particle sizedistribution and particle refractive index.
" Given the size distribution, refractive index of the individualparticles, and assuming that the particles are spherical,aerosol optical properties can be computed using the Mietheory. These properties are:• The scattering phase function P(!)
• The single scattering albedo "0
• The extinction coefficient c
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Aerosol Phase Function
Aerosol Optical Thickness
Shettle and Fenn (1979)Aerosol Models
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
! a "( )
! a "0( )=
"0
"#$%
&'() " ,"0( )
) ","0( ) = ln! a "( )! a "0( )
#
$%&
'(ln
"0
"#$%
&'(
The Ångström Exponent # (particle size)
Small aerosol particle size has large # value, while largeparticle has small # value.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
g =1
2cos!P !( )
0
"
# sin!d! =1
2µ P µ( )
$1
1
# dµ
The Asymmetry Parameter g (phase function)
The value of g ranges between -1 for entirely backscatteredlight to +1 for entirely forward-scattered light. Generally, g = 0indicates scattering direction evenly distributed betweenforward and backward directions, e.g., isotropic scattering.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Shettle and Fenn (1979) aerosol models used (12 models):Oceanic with relative humidity (RH) of 99%Maritime with RH of 50%, 70%, 90%, and 99%Coastal with RH of 50%, 70%, 90%, and 99%Tropospheric with RH of 50%, 90%, and 99%
Other models from AERONET measurements (Ahmad et al., 2010)
Aerosol Models
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Characteristics of the Aerosol Models
Aerosol Model Single Scattering Albedo a(865)
Asymmetry Parameter g
Ångström Exponent (510, 865)
Oceanic! 1.0 0.724-0.840 -0.087~ -0.016
Maritime! 0.982-0.999 0.690-0.824 0.09-0.50
Coastal!! 0.976-0.998 0.682-0.814 0.23-0.76
Tropospheric! 0.930-0.993 0.603-0.769 1.19-1.53
Urban! 0.603-0.942 0.634-0.778 0.85-1.14
Dust!!! 0.836-0.994 0.662-0.763 0.29-0.36
! Shettle and Fenn (1979) aerosol models. !!Gordon and Wang (1994) !!! Shettle (1984) and Moulin et al. (2001).
Strongly-absorbing aerosols
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
4. Radiative Transfer! Radiative Transfer Equation (RTE)! Successive-order-of-scattering method! Single-scattering approximation
Radiative Transfer
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
The RTE is simply an accounting for the changes in radiancealong a path.
First, attenuation produces a loss:
L + !L =P + !P
!A!"=
P 1# c!l( )
!A!"
The Radiative Transfer Equation (RTE)
dL !̂( )dl
= "c L !̂( )
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Second, scattering produces a gain:
dL !̂( )dl
= " ˆ#! $ !̂( )#%& L ˆ#!( )d% ˆ#!( )
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
The RTE:
dL !̂( )dl
= "cL !̂( ) + # ˆ$! % !̂( )$&' L ˆ$!( )d& ˆ$!( )
For the atmosphere-ocean system:
cos!dL z,!,"( )
dz= #c z( )L z,!,"( )
+ $ z, %! , %" &!,"( )%'( L z, %! , %"( )d %'
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
The RTE:
Can be written as:
cos!dL z,! ,"( )
dz= #c z( )L z,! ,"( ) + $ z, %! , %" & ! ,"( )
%'
( L z, %! , %"( )d %'
cos!dL z,! ,"( )
c z( )dz= #L z,! ,"( ) + $
0z( ) P z, %! , %" & ! ,"( )
%'
( L z, %! , %"( )d %'
cos!dL " ,! ,#( )
d"= $L " ,! ,#( ) + %
0"( ) P " , &! , &# ' ! ,#( )
&(
) L " , &! , &#( )d &(
where " = c &z( )0
Z
) d &z is the optical thickness
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
See section from Wang (1991).
Successive-order-of-scattering method
Wang, M. (1991), “Atmospheric Correction of the Second Generation of Ocean ColorSensors,” Ph.D. Dissertation, 135 pp., University of Miami, Coral Gables, Florida, USA.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
See section from Wang (1991).
Single-Scattering Approximation
!as "( ) =#0 "( )$ "( )
4 cos% cos%0
P &' ,"( ) + r %( ) + r %0( )( )P &+,"( )() *+
,#0 "( )$ "( )P &' ,"( )
Fresnel reflectivity of the surface
Wang, M. (1991), “Atmospheric Correction of the Second Generation of Ocean ColorSensors,” Ph.D. Dissertation, 135 pp., University of Miami, Coral Gables, Florida, USA.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Aerosol reflectance (radiance)
!"a #( )$ a #( )Pa %&,#( )
AOT can be routinely measured, butNOT Phase Function
For non- and weakly absorbingaerosols, aerosol reflectance: !" a #( )Pa $
%,#( )
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Aerosol Single-Scattering Epsilon
! ","0( ) =#
as"( )
#as
"0( )
=$
a"( )%
a"( ) P
a&
',"( ) + r (( ) + r (0( )( )P
a&
+,"( )[ ]
$a"0( )% a
"0( ) Pa&
',"0( ) + r (( ) + r (0( )( )P
a&
+,"0( )[ ]
Spectral variation of aerosol reflectance
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Characteristics of the Aerosol Models
Aerosol Model Single Scattering Albedo a(865)
Asymmetry Parameter g
Ångström Exponent (510, 865)
Oceanic! 1.0 0.724-0.840 -0.087~ -0.016
Maritime! 0.982-0.999 0.690-0.824 0.09-0.50
Coastal!! 0.976-0.998 0.682-0.814 0.23-0.76
Tropospheric! 0.930-0.993 0.603-0.769 1.19-1.53
Urban! 0.603-0.942 0.634-0.778 0.85-1.14
Dust!!! 0.836-0.994 0.662-0.763 0.29-0.36
! Shettle and Fenn (1979) aerosol models. !!Gordon and Wang (1994) !!! Shettle (1984) and Moulin et al. (2001).
Strongly-absorbing aerosols Non- and weakly-absorbing aerosols
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Aerosol Single-Scattering Epsilon (!0 = 865 nm)
0.6
0.7
0.8
0.9
1
2
300 420 540 660 780 900
O99M50M70M90M99C50C70C90C99T50T90T99! (
", "
0)
Wavelength (nm)
"0 = 865 nm, #
0 = 60
o, # = 45
o, $% = 90
o
(a)
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Epsilon and Aerosol Reflectance
! ","0( ) =#
as"( )
#as
"0( )$ exp c "0 % "( ){ }
"(!, !0) can be computed from two bands (e.g., NIR bands) #as(!).Thus, #as(!) values in other wavelengths (e.g., visible bands) canbe estimated:
!as "( ) = # ","0( ) $ !as "0( )
A simple atmospheric correction (aerosol correction) scheme(Wang and Gordon, 1994)--Single-scattering approximation.
Menghua Wang, IOCCG Lecture Series--Atmospheric Correction
Questions?
Radiance $ ?