Validation of Solar Backscatter Radiances Using Antarctic Ice Glen Jaross and Jeremy Warner Science...
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![Page 1: Validation of Solar Backscatter Radiances Using Antarctic Ice Glen Jaross and Jeremy Warner Science Systems and Applications, Inc. Lanham, Maryland, USA.](https://reader036.fdocuments.net/reader036/viewer/2022082213/56649cd85503460f949a0877/html5/thumbnails/1.jpg)
Validation of Solar Backscatter Radiances Using Antarctic Ice
Glen Jaross and Jeremy Warner
Science Systems and Applications, Inc.
Lanham, Maryland, USA
Outline
• Justification for using ice surfaces
• The technique, including necessary external information
• Error budget – where do we focus attention?
• Results for OMI, TOMS, MODIS, and SCIAMACHY
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What products benefit most from scene-based calibration ?
Cloud Fractions (λ-independent radiance errors)– Cloud studies
– Energy balance and UV irradiance
– Cloud height: errors are directly proportional to cloud fraction (low cloud amounts)
– Gas vertical column amounts: Air Mass Factor errors directly related to cloud fraction. ( 3% - 5% column NO2 error per 5% cloud error; low cloud amounts)
Aerosol Properties (λ-independent and λ-dependent radiance errors)– 0.015 error in single-scatter albedo per 1% radiance error
– Optical Depth error 0.06-0.12 per 1%/100 nm λ-dependent radiance errors
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Where is scene-based calibration less effective ?
Spectral fitting algorithms (e.g. DOAS)– Insensitive to low-order-in-λ calibration errors
– Conversion from slant to vertical column still sensitive
Gas abundances (slant column)– Need knowledge of abundance to calculate expected radiances, but gas
abundance depends upon calibration
Limb scattering and Occultation– Normalizing radiances at a reference height nearly eliminates sensitivity to
underlying scene reflectance
– Most instruments do not have a nadir view
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TOMS Earth Probe
360 nm Reflectivity (1996)
Antarctica is a good radiance calibration target
• High Reflectance
> direct / diffuse TOA radiance ratio greatest
> radiances least affected by clouds and aerosols
• Low Aerosol Loading
• Uniform Reflectance Over a Large Area
• Highly Repeatable (stable) Reflectance
R (Lambertian) > 0.95
90 % 100 %
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TOMS Earth Probe
360 nm Reflectivity (1996)
Areas with Slope<0.005 radians
Data Selection Region
Region selected for
• low surface slope
• high reflectivity
• uniformity
90 % 100 %
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cloud = 5
at 440 mb
Are clouds an issue ?
Modeled nadir-scene
357 mn
775 nm
albedo ratio
GOME (Jan. 2000) nadir-scene
357 mn
775 nm
albedo ratio
Either the cloud
model is wrong,
or …
Clouds are statisticallyunimportant
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Time Dependence of radiometric calibration
Seasonal Cycle:
• Neglecting terrain height variations
• Surface reflectance non-uniformity
TOMS Nimbus 7 380 nm
TOMS Earth Probe 360 nm
OMI (Aura) 360 nm
Greenland
Antarctica
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1996 1997
1996 1997
Comparison between sensors
GOME / TOMS-EP Radiance Ratio
Very early GOME calibration
Comparisons need not be over the same time period
360 nm
331 / 360 nm
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Validation of Absolute Radiometry
1. Develop a 2 steradian directional reflectance (BRDF) model for the Antarctic surface; independent of wavelength.
2. Combine BRDF with surface measurements of total hemispheric reflectance measurements; wavelength-dependent
3. Create a look-up table of sun-normalized Top-of-the-Atmosphere (TOA) radiances for all satellite observing conditions using a radiative transfer model
4. Process sensor sun-normalized radiance data from a region of Antarctica chosen for uniformity and low surface slope
5. Compute ratio between each measurement and table entries; average results
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Warren et al. Reflectance anisotropy derived from
1986-1992 data
Spectral Albedo Measuremnts at South
Pole, 1986
= 600 nm
Sol. ZA = 80
BRDF probably the same:
300-800 nm
Surface properties based upon reflectance measurements by Warren et al.
BRDF derived from parameterization of measured
reflectance anisotropy
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New Reflectance Measurements by Warren et al.
Funded by U.S. National Science Foundation and CNES
• will support radiometric validation for SPOT4 (Laboratoire de Glaciologie et Géophysique de l’Environnement)
• data not yet published
Measurements at Dome C, 2003-2005
• Spectral BRDF of surface 0.35 – 2.5 m
• Solar Zenith Angles 52 - 87
• Measure spectral transmission of sunlight into snow
• Measurements used for inputs to models for effect of clouds on TOA radiances
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Error Budget
Surface BRDF model represents single largest error source
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Surface BRDF model vs. Solar Zenith Angle
SolZA=40
SolZA=60
SolZA=50
SolZA=85
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BRDF is most important at longer wavelengths
Simulated Nadir-scene albedos
Solar Zenith Angle = 75
Column Ozone = 325 DU
BRDF plays bigger role as
diffuse / direct ratio decreases
Lambertian
Non-Lambertian
Non-Lambertian / Lambertian Radiance Ratio
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OMI Results
OMI L1b Data:
7 Dec – 4 Jan, 2004
• Perfect model would yield flat SolZA dependence
• Perfect calibration would yield values = 1 at all wavelengths
Plot suggests probable radiative transfer errors
– surface BRDF model
– treatment of atmosphere
We believe that results obtained below SolZA = 70 fall within our 2.2% uncertainty estimate
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OMI Full spectral range ice radiance results
Flat spectral result gives us confidence that
result is resonable
62 < SolZA < 68
83 < SolZA < 86
Spectral dependence is not realistic –
consistent with BRDF error
Apparent error increases at long as predicted
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Shadowing Errors
Large scale structures (snow dunes) not captured by ground characterizations
From Radarsat-1
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Simple linear shadow model for testing errors
Tune barrier height and separation to yield flattest SolZA dependence in data
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Shadow study using MODIS / Aqua
Comparison to RTM, without correction
Comparison to RTM, with shadow correction
Consistent with ~2% uncertainty estimate
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RTM handles ozone poorly at
< 330 nm
Comparison between MODIS, OMI, TOMS and model radiances
OMI / Aura
MODIS / AquaTOMS / EP
O2O2
Absorption
RTM does not include Ring
Effect or O2-O2 abs.
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Preliminary SCIAMACHY Results
SCIAMACHY Level 1b ( v5.04 )
18 – 24 Dec., 2004
Provided by R. van Hees, SRON
}
Ozone Absorption
ignored
Comparison with RTM over Sahara (from G. Tilstra,
KNMI)
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Summary
Model calculations of TOA radiances over Antarctica are good to approximately 2% at low solar zenith angles (i.e. near Dec. 21)
Radiometric characteristics of nadir-viewing sensors can be validated from ~330 nm to ~750 nm
Wavelength-to-wavelength radiometry is better than 2%, but not useful for absorption spectroscopy
We derive the following sensor calibration errors (preliminary)
OMI / Aura: -2.5% (330 < < 500 nm)
MODIS / Aqua : -0.5% ( < 500 nm)
TOMS / Earth Probe : 0% (331 nm), -1% (360 nm)
Future Work :
Evaluate more sensors. SCIAMACHY, GOME 2 ?
Refine BRDF for improved performance at high SolZA and SatZA
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Spares
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X-track dependence is mostly Lambertian near SolZA = 50
Results near 50 are least affected by BRDF errors
BRDF surface slices at 67
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Same time and geographic
location
OMI radiances compared directly to MODIS / Aqua band 3
MODIS has broad bandwidth
(459 < < 479 nm) which includes O2-
O2 absorption
OMI
MODIS
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Developed a 2 steradian BRDF model
Existing parameterization from
Warren et al.J. Geophys. Res., 103, 1998
s 50 o 67 all
Extrapolate function for use at s > 50
Invoke reciprocity ( s > 67 o< 67 )
Fill remaining “hole” ( s < 67 o< 67 )– assume s
2 dependence for all o < 67
– derive (s=0) at each o < 67 from a quadratic
parameterization of observed scattering phase fn. (Warren, et al., ibid)
s- 67 + 67
(
s=
0)
o