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This study explores performance requirements for the retrieval of the atmospheric aerosol optical depth (AOD) by airborne optical remote sensing instruments. Independent of any retrieval techniques, the calculated AOD retrieval requirements are compared with the expected performance parameters of the upcoming hyperspectral sensor APEX at the reference wavelength of 550nm. The AOD accuracy requirements are defined to be capable of resolving transmittance differences of 0.01 to 0.04 according to the demands of atmospheric corrections for remote sensing applications. For the purposes of this analysis, the signal at the sensor level is simulated by radiation transfer equations. The resulting radiances are translated into the AOD retrieval sensitivity
(Δτλaer) and compared to the available measuring sensitivity of the sensor
(NEΔLλsensor). This is done for multiple signal-to-noise ratios (SNR) and surface reflectance values. It is shown that an SNR of 100 is adequate for AOD retrieval at 550nm under typical remote sensing conditions and a surface reflectance of 10% or less. Such dark surfaces require the lowest SNR values and therefore offer the best sensitivity for measuring AOD. Brighter surfaces with up to 30% reflectance require an SNR of around 300. It is shown that AOD retrieval for targets above 50% surface reflectance is more problematic with the current sensor performance as it may require an SNR larger than 1000. In general, feasibility is proven for the analyzed cases under simulated conditions.
It is known that atmospheric aerosols influence the Earth climate system. Various efforts are being made to investigate the global distribution and concentration of these aerosols and to quantify their forcing on the radiation budget. Numerous data from passive optical Earth observation satellites are used to map aerosol properties on a global scale. Not only atmospheric scientists, but also the remote sensing community relies on aerosol information. Earth observation data in particular have to be corrected for the atmospheric influence in order to provide accurate physical measuring quantities.
During the last two decades, several aerosol retrieval techniques have been developed for satellite instruments. An overview is given by [1] and recent inter-comparisons are provided for the retrieval over land by [2] and over sea by [3], [4] and [5]. In general, relatively large discrepancies between different satellite instruments were found, especially on the scale of single pixels [2]. Even long-term studies over the ocean reveal differences between well established satellite instruments of up to 0.1 aerosol optical depth (AOD or
τλaer) and 0.45 Ångstrøm exponent [4].
State-of-the-art hyperspectral airborne imagers may be able to outperform the limitations of most current satellite instruments. For example, the typical ground sampling distance (GSD) of spaceborne instruments retrieving AOD routinely is in the range of 1km to 30km. The resulting uncertainty of the surface reflectance is an important contribution to the inaccuracy of the retrieved AOD over land. On the other hand, the GSD of airborne instruments is in the range of meters. One can therefore assume better performances in AOD retrieval over land because the unmixing of the surface and the atmospheric signal is expected to be less difficult. The increased likelihood of observing a uniform surface within one pixel leads to smaller uncertainties in the assumptions about the surface reflectance. This is a major source of error in most satellite-based AOD retrievals. In addition, the use of a hyperspectral sensor allows the avoidance of atmosphere gaseous absorption bands and the use of the complete spectrum from near-UV to SWIR if desired. Furthermore, the spectral and the spatial domain can be binned (adding bands or pixels together) to achieve the desired signal-to-noise ratio (SNR). The Airborne Prism EXperiment (APEX) [6] is chosen for this paper as an example for such an airborne hyperspectral instrument.
This study assesses the feasibility of aerosol retrieval with APEX in terms of the SNR and independent of any particular AOD retrieval technique, which was previously proposed by [7] and [8]. A model which translates atmospheric conditions and surface reflectance into radiance values at-sensor is essential for the establishment of feasibility. It needs also to address the multiple scattering of light while being as simple as possible to avoid excessive computational time or alternatively the use of precalculated lookup tables. This study analyses the SNR requirements and limitations of aerosol retrieval with a focus on the influence of the surface reflectance.
All calculations are carried out at the commonly used aerosol reference wavelength of 550nm to make the results comparable to other studies. Preliminary analysis at other wavelengths within the visible spectrum did not reveal qualitative differences to the findings at 550nm and are therefore not shown in this paper. The figures are plotted for
0<τ550nmaer<1 on the x-axis because the minimum expected visibility for an airborne remote sensing campaign will be about 5km(τ550nmaer≈1). Flights usually will be carried out at visibilities of more than 10km(τ550nmaer≈0.6).
Sensor Characteristics of APEX
APEX is a dispersive push-broom imaging spectrometer, which is expected to provide unique hyper-spectral data to geophysical and biochemical studies on land, water and atmospheric processes. APEX will contribute to the Earth observation community by simulating, calibrating and validating future space- and airborne optical sensors. The expected performance of APEX along with a novel spectral, radiometric and geometric calibration methodology provide an opportunity to overcome limitations of currently available remote sensing instruments. This potential is especially important in addressing the requirements for the remote sensing of aerosols.
APEX features more than 500 spectral bands from 385nm to 2500nm with a sampling interval of 0.4nm to 10nm in the full spectral mode. The standard spectral mode comprises more than 300 bands, where bands are binned together to increase the SNR. The typical gain in SNR is in the order of 40% per domain (spectral or spatial). This corresponds to a factor of 1.4^{2} ≈ 2 for the binning in both domains.
The GSD is governed by 0.028° instantaneous field of view and 1000 pixels across track. It varies from 2.5m to 8m depending on the flight altitude.
Table 1 provides the preflight APEX-specific sensor performance for minimum, average and maximum radiance levels at 550nm(L550nmsensor). They correspond to surface reflectances
(ρ550nmsfc) of 0%, 30% and 100%.
ρ550nmsfc=0.3 represents a relatively bright surface reflectance, which can be expected during remote sensing campaigns over land. The minimum and maximum surface reflectance was chosen to account for the extreme values following [9]. The sensor performance is expressed by the noise equivalent spectral radiance difference
(NEΔL550nmsensor). The relation between
L550nmsensor and
NEΔL550nmsensor is given by:
NEΔLλsensor=LλsensorSNRλ,where SNR_{λ} is the band-specific signal-to-noise ratio or sensor efficiency. It consists of the instrument and photon noise. The latter is mainly a function of the spectral radiance level
Lλsensor.
The actual sensor performance values are going to be measured in mid 2008 during the first full calibration of APEX. This instrument is currently in assembly and its maiden flight is scheduled later in 2008.
Radiance Simulation
Some basic radiation transfer equations are needed to simulate the attenuation of the light traveling from the top of the atmosphere down to a surface pixel and upward to the airborne sensor. The upwelling spectral radiance into an instrument (at-sensor-radiance
Lλsensor) is a function of successive orders of radiation interactions within the coupled surface-atmosphere system. In theory, it can be decoupled into a contribution from the atmosphere (path-radiance
Lλatm) and from the underlying surface
(Lλsfc).
Lλatm can be split into the direct
(Lλatm,drc) and the diffuse
(Lλatm,dfs) reflected spectral radiance from the scattering atmospheric layer:
Lλsensor=Lλatm+Lλsfc=Lλatm,drc+Lλatm,dfs+Lλsfc
Path-Radiance
If we assume a homogeneous scattering layer and the single scattering approximation (SSA), the atmospheric spectral path-radiance can be derived from the well known Radiation Transfer Equation by [10] as follows:
Lλ,SSAatm=E0λμ0π︸I[1−e−τλ(1μ0+1μ)]︸IIω0Pλ(Θ)4(μ+μ0),︸IIIwhere the incoming spectral radiance (I) is reflected by the scattering atmosphere (II) and scattered directly (single scattering) into the sensor's viewing geometry (III). E_{0}_{λ}μ_{0} is the solar spectral irradiance, scaled by the cosine of the solar zenith angle. μ describes the sensor viewing geometry, where μ = cos(0°) = 1 is valid for a nadir viewing instrument, such as APEX. The atmospheric single scattering albedo ω_{0} is the ratio of the scattering to the extinction coefficient. The atmospheric phase function P_{λ} (Θ) takes care of the amount of light, which is diverted into the sensor viewing direction. For aerosol remote sensing, the atmospheric optical depth can be decomposed into its molecular and particle (aerosol) extinction part, such that
τλ=τλmlc+τλaer.
The multiple scattering of light at molecules and aerosols is an important contribution to
Lλsensor for λ < 800nm. It leads to increasing errors for smaller λ due to the SSA in Equation 3. Unfortunately, multiple scattering is difficult to express in form of a simple equation. But its influence can be taken into account by introducing a correction factor f(τ_{λ}) [11]:
f(τλ)=LλatmLλ,SSAatm.It represents the ratio of the exact radiance calculation by a multiple scattering radiation transfer code (i.e. [12] or [11]) to the SSA radiance calculation. f(τ_{λ}) can be interpreted in Figure 1(a) by taking the ratio between the MODTRAN4 [13] curve and the SSA curve from Equation 3. One finds that the multiple scattering intensifies
Lλsensor by a factor of 1.5 at
τ550nmaer=0.2 and by a factor of 2.0 at
τ550nmaer=0.85.
The atmospheric spectral radiance corrected for the multiple scattered light is therefore given by:
Lλatm=E0λμ0π[1−e−τλ(1μ0+1μ)]ω0Pλ(Θ)4(μ+μ0)f(τλ).
Surface Contribution
Since
Lλsfc is often the dominating contribution to
Lλsensor, one must account for the underlying surface. The ratio of incoming and outgoing spectral irradiance at the surface level yields the homogeneous Lambertian surface reflectance:
Eλ↓sfc/Eλ↑sfc=ρλsfc. Since
Eλ↑sfc=πLλsfc and therefore
Eλ↓sfc/πρλsfc=Lλsfc we find:
Lλsfc=E0λμ0πρλsfcTλ↕1−sλρλsfc.
s_{λ} is the spherical albedo and describes the portion of the light scattered back to the surface as a result of isotropic illumination of the atmosphere by the surface. It is therefore also a function of T_{λ} and τ_{λ}.
Tλ↕ denotes the total spectral transmittance, comprising of the down- and upward direct
(Tλdrc,sca) and diffuse
(Tλdfs,sca) scattering transmittance and the absorption transmittance
(Tλabs):
Tλ↕=(Tλ↓drc,sca+Tλ↓dfs,sca)Tλ↓abs(Tλ↑drc,sca+Tλ↑dfs,sca)Tλ↑abs.[14] offers a parameterization by polynomial series with a satisfying accuracy to describe
Tλdfs,sca and s_{λ}. Additionally, a non-uniform surface could be considered by adjusting
ρλsfc in the denominator of Equation 6 to incorporate an environment reflectance according to [15] and [16] or [17].
At-Sensor-Radiance
In the case of an airborne remote sensor, the atmospheric extinction has to be adjusted to the reduced atmospheric path length between the surface and the sensor. An approximating method would be to use the air pressure ratio (p*) between the sensor and the surface level to scale the upward optical depth due to molecular scattering:
p*⋅τλ↑mlc, which is equal to
(τλ↑mlc)p*. The extinction by aerosols above the sensor (ie. background volcanic particles in the stratosphere) is neglected here. For this study, p* is set to 0.5, which corresponds to a sensor height of about 5500 meters above sea level using the international standard atmosphere.
Finally, the complete spectral radiance at the sensor level is given by adding Equations 5 and 6:
Lλsensor=E0λμ0π[[1−e−τλ(1μ0+1μ)]ω0Pλ(Θ)4(μ+μ0)f(τλ)+ρλsfcTλ↕1−sλρλsfc].
Verification with MODTRAN4
Equation 8 was compared against results from the widely accepted radiation transfer model MOD-TRAN4 [13] including the multiple stream algorithm DISORT [12] to account for the multiple scattering. The 1976 U.S. Standard Model Atmosphere was used to describe the vertical profile of gas mixing ratios. The aerosol optical properties within the planetary boundary layer were taken into account in MODTRAN4 by a rural type of aerosol with a mixing ratio of 0.7 small water-soluble and 0.3 large dust-like particles. A tropospheric type with small water soluble particles was used for the free troposphere. Equation 8 was fed by the Average Continental model from [18], which adds a few particles of soot (0.06 mixing ratio) to the troposphere type. The results and conclusions of this paper were derived by means of Equation 8 and they are therefore not affected by differences in the aerosol models. Further parameters used with Equation 8 and with MODTRAN4 for the verification are given in Table 2.
Figure 1 presents the simulation of
Lλsensor as a function of
τλaer. The black lines are the results from Equation 8 over different
ρλsfc while the colored lines with circles referring to the MODTRAN4 reference calculations. Figure 1(a) shows the intermediate step with the SSA (dashed lines) over a black surface
(ρ550nmsfc=0), which is given by Equation 3. The influence of the multiple scattering is clearly visible as the offset between the dashed and the solid line. This offset is represented in the multiple scattering correction factor f(τ_{λ}) used in Equation 5.
The accuracy of the spectral radiance simulation is given by qualitatively comparing the results for
L550nm,SSAatm and
L550nmatm with the MODTRAN4 reference calculations in Figure 1(a). The effect of the surface contribution by Equation 6 can be seen in Figure 1(b), where the complet
Lλsensor from Equation 8 is given for different surface reflectances along with the MODTRAN4 results.
At
ρλsfc≊0.5, the model expects to cancel out the change in absorption and the change in scattering due to a changing AOD.
Lλsensor is therefore no longer a function of
τλaer, which makes it impossible to retrieve AOD at a surface reflectance of about 50%. Further investigations showed that this critical
ρλsfc varies with the aerosol scattering properties ω_{0}, P_{λ} (Θ) and with μ_{0}, μ and s_{λ} (not shown).
The atmosphere has a distorting effect on
Lλsensor, which has to be compensated for quantitative remote sensing applications. AOD is a crucial parameter for the atmospheric correction process to derive accurate apparent surface reflectances. We define an accuracy requirement of 1% absolute error in surface reflectance according to [20]. This can be also expressed in terms of transmittance in order to relate it to AOD. A rough estimation of the allowed application specific error (ε) in
T550nm↕drc,sca=e−τ550nm yields 0.01 transmittance values for dark surfaces, such as water bodies
(ρ550nmsfc≈0.05). The relative influence of
Lλatm on
Lλsensor is decreasing for increasing
ρλsfc (Equation 8). For example, at
ρ550nmsfc=0.3 the
L550nmatm accounts for about 25% of
L550nmsensor at
τ550nmaer=0.1 (see Figure 1(b)) and therefore ε yields 0.04 transmittance values.
The required retrieval sensitivity of the total optical depth is calculated by:
Δτλ=ɛ|ddτλTλ↕drc,sca|=|−ɛeτλ|.The exponential dependence of Δτ_{λ} on the total optical depth and therefore also on AOD is obvious. It is found that
Δτλaer≤0.01 is needed for the worst case of a dark surface and low AOD conditions
(τλaer→0). A
Δτλaer≤0.045 is satisfactory for
ρ550nmsfc≈0.3. Equation 9 is also used later in Figures 2 and 3 to define AOD retrieval requirements.
Sensor Sensitivity Requirements
The results from AOD retrieval sensitivity requirements can now be used to define the performance requirements of an optical remote sensing instrument because they are related to the radiometric resolvability (ΔL_{λ}). This is a prerequisite for the successful retrieval of aerosols. For obvious reason, the radiance variation induced due to change in AOD must exceed NE ΔL_{λ} of a sensor [21]:
Δτλaer∝ΔLλaer≥NEΔLλsensor.The sensor-specific sensitivity on AOD
(NEΔτλaer) is given by means of the simulated
Lλsensor from Equation 8 and
NEΔLλsensor from Equations 1 and 10:
NEΔτλaer=1ddτλaerLλsensorNEΔLλsensor.
ResultsSNR Requirements
Figure 2 assesses the SNR requirements depending on surface reflectance and AOD. The retrieval of
τλaer is feasible as long as
NEΔτλaer≤τλaer according to Equation 10. The area where this limit is not fulfilled, because the noise exceeds the signal, is drawn in dark-red in Figures 2 and 3. The dark orange color denotes the area where the desired minimal aerosol retrieval interval
Δτλaer from Equation 9 can not be achieved for the ε = 0.04 requirement. The stricter ε = 0.01 is met within the white area.
Over dark surfaces, where
Lλatm dominates
Lλsensor, AOD retrieval sensitivity is best for small AOD. This is because small
NEΔτλaer can be achieved even for relative low SNR values (Figures 2(a) and 2(b)). An SNR of less than 100 is enough to fulfill the strict atmospheric correction accuracy requirement of ε = 0.01, which is needed for dark targets. Assuming a typical case with a surface of
ρ550nmsfc=0.1 and
τ550nmaer=0.15±0.1, a
NEΔτλaer of at least 0.008 for SNR = 100 can be expected.
Brighter surfaces
(0.1<ρ550nmsfc<0.3) require greater SNR to keep a certain aerosol retrieval sensitivity compared to dark surfaces. This range of surface reflectances is expected to be the typical case for remote sensing over land. To fulfill ε = 0.01, an SNR between 100 and 300 is now required. In terms of atmospheric correction ε can be relaxed to 0.04, where an SNR between 30 and 100 is sufficient (Figures 2(c) and 2(d)). An SNR of 300 allows an aerosol retrieval sensitivity of less than 0.01 with
τ550nmaer≤0.25, which is expected to be the typical condition for most flight campaigns.
Very bright surfaces
(0.4<ρ550nmsfc<0.6) are found to be most challenging because
L550nmsensor depends weakly on
τ550nmaer. Changes in scattering and absorption of light due to a
Δτλaer may cancel each other out. It can be seen in Figure 1(b), Equation 8 and MODTRAN4 reveal virtually no influence of the aerosol loading on
L550nmsensor in the case of
ρ550nmsfc≈0.5. Due to the derivation of a local minimum in Equation 11,
NEΔτ550nmaer can go to infinity as plotted in Figure 2(e). This critical surface reflectance of about 50% as well as the position (in terms of
τ550nmaer) of
NEΔτ550nmaer→∞ depends on many parameters and can vary between different models. This effect is not analyzed in detail here but shows clearly that aerosol retrieval can be difficult for a certain small range of surface reflectances.
Extremely bright targets, such as snow and clouds, provide adequate sensitivity. Figure 2(f) shows an example for
ρ550nmsfc=0.8, where an SNR of about 100 is sufficient for ε = 0.04, while 300 is needed for the ε = 0.01 requirement. The sensitivity is almost constant over the typical range of
τ550nmaer at this surface reflectance. This is in contrast to the calculations with low surface reflectance
(ρ550nmsfc<0.4), where
NEΔτ550nmaer generally decreases for increasing
τ550nmaer.
Influence of the Surface Reflectance
The influence of the surface reflectance on aerosol retrieval is highlighted by Figure 3. 3(a) reveals clearly that an SNR ≥ 100 is needed to detect aerosols over typical surfaces. Such an SNR allows achieving ε = 0.01 with dark surfaces and ε = 0.04 with
ρ550nmsfc=0.3 and 1.0.
ρ550nmsfc≤0.1 is mostly unproblematic for instruments with SNR greater than 50. A surface reflectance of
ρ550nmsfc≤0.4 or
ρ550nmsfc≥0.8 requires an instrument with an SNR of about 400 to fulfill the strict requirement (Figure 3(b)). It is possible to achieve ε = 0.04 with the same SNR also for
ρ550nmsfc≤0.45 and
ρ550nmsfc≥0.6. Greater SNR enhances the retrieval sensitivity within the white area, where ε < 0.01 is given.
Much higher SNR are required in order to detect aerosols over a surface reflectance of around 50%. Figures 3(c) and 3(d) show that the requirement of ε = 0.04 can be met within a range of
τ550nmaer={0.01−0.25,0.45−0.7,0.85−1.0} with an SNR of 1000. This AOD range becomes smaller for a larger SNR. ε = 0.01 can only be met partially by having an SNR of more than 3000. This can be achieved only by trading off foremost spatial and/or spectral resolution for SNR by binning hyperspectral remote sensing data in these domains.
Feasibility of Aerosol Retrieval with APEX
The crucial question is whether an aerosol retrieval is possible with an airborne hyperspectral sensor optical system, such as APEX. It must be demonstrated that the required signal sensitivity is provided by the instrument. Since APEX has not yet undergone a complete calibration process, one must use preflight SNR requirements for this analysis. These values are given in Table 1 with
NEΔL550nmsensor and the corresponding SNR in Table 3 along with the retrieval requirements.
The feasibility analysis is based upon three scenarios corresponding to the minimal, average and maximal expected spectral radiance levels according to Table 1. Equation 8 was solved for
ρ550nmsfc=0.0, 0.3 and 1.0. to find the modeled
L550nmsensor. The SNR requirements for aerosol retrieval were interpreted from the data, which are shown in Figure 2, where the SNR meets the requirement of ε = 0.01 (Equation 9).
The comparison in Table 3 between the retrieval requirement and the SNR of APEX reveals clearly the feasibility of aerosol retrieval for the analysed cases. However, it might be possible that the SNR does not meet the requirements for aerosol retrieval over the critical surface reflectance around
ρ550nmsfc=0.5 without additional binning.
Summary and Conclusions
A spectral radiance simulation at the sensor level has been presented. It is capable of reproducing MODTRAN4 results under the SSA and within typical airborne remote sensing conditions. The multiple scattered path radiance was taken into account by the DISORT code [12]. This
Lλsensor simulation was used to evaluate the noise equivalent difference aerosol optical thickness
NEΔτλaer as a function of
τλaer for different SNR and surface reflectances at 550nm. The results reveal the sensor performance requirements for a sufficiently accurate AOD retrieval along with a feasibility analysis regarding APEX.
It has been shown that the detection of aerosols is feasible with APEX for low, average and high spectral radiance levels under the evaluated conditions (ie. solar, viewing and sensor configuration). This finding concerns the sensitivity requirements for an optical remote sensing instrument, such as APEX. The resulting feasibility is based on preflight sensor performance values; the final APEX SNR will be available after full scale calibration during the year 2008. Further investigations will be performed to assess the sensitivity and the limitations of the radiation transfer calculation and the aerosol retrieval algorithm itself.
We found that the spectral SNR is vital for aerosol remote sensing and varies strongly with surface reflectance. The latter strongly influences the intensity of
Lλsensor, which drives the SNR. It has been shown that dark surfaces
(ρ550nmsfc<0.1) have the lowest SNR demands for aerosol retrieval. This is crucial for establishing feasibility because the sensor provides a lower SNR over dark surfaces due to the lower spectral radiance. The analysis showed that APEX is expected to provide sufficiently high SNR values even for black surfaces under the given conditions. More critical are relatively bright surfaces
(0.4<ρ550nmsfc<0.6) because
L550nmsensor depends only weakly on
τ550nmaer. Extremely bright surfaces require again a lower SNR, but the unmixing of
Lλatm+Lλsfc is expected to be more difficult because of errors in the estimation of
ρλsfc become dominant. Due to the small GSD of airborne instruments, it is expected that the identification of pure surface materials could be done with an adequate precision compared to satellite platforms. This allows to reduce the uncertainties in allocating a best-guess
ρλsfc to the observed pixels and therefore alleviate the challenge of the unmixing of
Lλatm from
Lλsensor.
The finding of indefinitely high SNR requirements might be an artifact of the approximate simulation of
L550nmsensor (Equation 8) for
ρ550nmsfc=0.5±0.05. It depends strongly upon the aerosol model assumption, in particular the approximation of the phase function and the multiple scattering. Further investigations are needed.
Generally, it was shown that an SNR of 300 or better will provide satisfying aerosol retrieval results for most surface reflectances considered in this analysis. Restricting the ranges to
τ550nmaer<0.25 and
ρ550nmsfc<0.2, which are optimal and representative remote sensing conditions, an SNR of 100 is adequate. This is a promising finding in scope of the development of aerosol retrieval methods because most current instruments fulfill such SNR requirements under typical conditions.
We would like to acknowledge Dr. Alexander Kokhanovsky for sharing his expertise in the field of radiative transfer and multiple light scattering. We would also like to thank Jason Brazile and all involved individuals for their assistance. As well, we acknowledge the detailed and fruitful comments and suggestions of four anonymous reviewers.
ReferencesKingM.KaufmanY.TanréD.NakajimaT.Remote sensing of tropospheric aerosols from space: Past, present, and futureKokhanovskyA. A.BreonF.-M.CacciariA.CarboniE.DinerD.NicolantonioW. D.GraingerR. G.GreyW. M. F.HöllerR.LeeK.-H.LiZ.NorthP. R. J.SayerA. M.ThomasG. E.von Hoyningen-HueneW.Aerosol remote sensing over land: a comparison of satellite retrievals using different algorithms and instrumentsMyhreG.StordalF.JohnsrudM.IgnatovA.MischenkoM. I.GeogdzhayevI. V.TanréD.DeuzéJ.-L.GoloubP.NakajimaT.HigurashiA.TorresO.HolbenB.Intercomparison of satellite retrieved aerosol optical depth over the oceanMishchenkoM. I.GeogdzhayevI. V.TanréD.DeuzéJ.-L.GoloubP.NakajimaT.HigurashiA.TorresO.HolbenB.Past, present, and future of global aerosol climatologies derived from satellite observations: A perspectiveKahnR. A.GarayM. J.NelsonD. L.YauK. K.BullM. A.GaitleyB. J.MartonchikJ. V.LevyR. C.Satellite-derived aerosol optical depth over dark water from misr and modis: Comparisons with aeronet and implications for climatological studiesNiekeJ.IttenK.DebruynW.The airborne imaging spectrometer apex: from concept to realizationSeidelF.NiekeJ.SchläpferD.HöllerR.Hoyningen-HueneW.IttenK.Aerosol retrieval for apex airborne imaging spectrometer: a preliminary analysisSeidelF.NiekeJ.SchläpferD.IttenK.BowlesJ.Evaluation of near-uv/blue aerosol optical thickness retrieval from airborne hyperspectral imagerySchaepmanM.SchläpferD.MüllerA.Performance requirements for airborne imaging spectrometersChandrasekharS.RozanovV. V.KokhanovskyA. A.The solution of the vector radiative transfer equation using the discrete ordinates technique: Selected applicationsStamnesK.TsayS.-C.WiscombeW.JayaweeraK.Numerically stable algorithm for discrete-ordinate-method radiative transfer in multiple scattering and emitting layered mediaBerkA.BernsteinL.RobertsonD.KokhanovskyA. A.MayerB.RozanovV. V.A parameterization of the diffuse transmittance and reflectance for aerosol remote sensing problemsTanréD.HermanM.DeschampsP. Y.de LeffeA.Atmospheric modeling for space measurements of ground reflectances, including bidirectional propertiesTanréD.HermanM.DeschampsP.Influence of the background contribution upon space measurements of ground reflectanceVermoteE. F.TanréD.DeuzéJ. L.HermanM.MorcretteJ.-J.Second simulation of the satellite signal in the solar spectrum, 6s: An overviewd'AlmeidaG.KoepkeP.ShettleE.BodhaineB. A.WoodN. B.DuttonE. G.SlusserJ. R.On rayleigh optical depth calculationsRichterR.SchläpferD.Geo-atmospheric processing of airborne imaging spectrometry data. Part 2: atmospheric/topographic correctionSchläpferD.SchaepmanM.Modeling the noise equivalent radiance requirements of imaging spectrometers based on scientific applicationsFigures and Tables
Black lines show the radiance simulations, while the MODTRAN4 reference calculations are given by colored lines with circles. (a) Influence of AOD
τ550nmaer on the observed path-radiance
(ρλsfc=0) with the single scattering approximation
(L550nm,SSAatm) from Equation 3 and with multiple scattering
(L550nmatm) from Equation 5. (b) Influence of
τ550nmaer on the observed radiance
(L550nmsensor) including the surface contribution from Equation (8). ρ = ‥% denotes the corresponding surface reflectance
ρλsfc.
Influence of
τ550nmaer on the AOD retrieval sensitivity
NEΔτ550nmaer for different SNR values. AOD retrieval is feasible outside the red area, while the transmittance accuracy requirement complies with 0.01 < ε < 0.04 within the light orange area and with ε < 0.01 within the white area.
Influence of
τ550nmaer on the AOD retrieval sensitivity
NEΔτ550nmaer for different surface reflectances
ρ550nmsfc. AOD retrieval is feasible outside the red area, while the transmittance accuracy requirement complies with 0.01 < ε < 0.04 within the light orange area and with ε < 0.01 within the white area.
Preflight values at 550nm for the spectral radiance resolvability of APEX
(NEΔL550nmsensor) for the corresponding minimum
(ρ550nmsfc=0.0), average
(ρ550nmsfc=0.3) and maximum
(ρ550nmsfc=1.0) spectral radiance level at the sensor
(L550nmsensor). The values are given in units of [W · m^{−2} · sr^{−1} · nm^{−1}] and based on the APEX standard spectral binning pattern.
Minimum
Average
Maximum
L550nmsensor
NEΔL550nmsensor
L550nmsensor
NEΔL550nmsensor
L550nmsensor
NEΔL550nmsensor
0.01631
0.00019
0.09762
0.00030
0.51699
0.00060
Variables used in Equation 8 to plot the figures of this paper.
τλmlc is tabulated in [19].
Variables independent of
τ550nmaer:
μ_{0}
μ
Θ_{μ}_{0},_{μ} [°]
E_{0;550}_{nm}
[W · m^{−2} · nm^{−1}]
τ550nmmlc
0.733
1.00
137
1.90
0.097
Variables depending on
τ550nmaer:
ω_{0}
P_{550}_{nm} (Θ)
s_{550nm}
τ550nmaer=0.05
0.99
0.90
0.10
τ550nmaer=0.5
0.97
0.87
0.20
Feasibility analysis of the aerosol retrieval with APEX by comparing SNR values at 550nm.