OSA's Digital Library

Optics Express

Optics Express

  • Editor: C. Martijn de Sterke
  • Vol. 15, Iss. 8 — Apr. 16, 2007
  • pp: 5227–5236

Optics InfoBase > Optics Express > Volume 15 > Issue 8 > Page 5227

« Show journal navigation

Simultaneous determination of aerosol optical thickness and exponent of Junge power law from satellite measurements of two near-infrared bands over the ocean

Qingshan Xu, Heli Wei, Ruizhong Rao, and Huanling Hu  »View Author Affiliations


Optics Express, Vol. 15, Issue 8, pp. 5227-5236 (2007)
http://dx.doi.org/10.1364/OE.15.005227


View Full Text Article

Acrobat PDF (845 KB)


Advanced Search

Browse Journals / Lookup Meetings

Browse by Journal and Year


   


Lookup Conference Papers

Close Browse Journals / Lookup Meetings

Article Tools

Share
Citations

Abstract

An iterative algorithm is presented in this study for simultaneous determination of both the aerosol optical thickness and the exponent of the Junge power law from the total reflectance data of two satellite-based, near-infrared bands over the ocean. The atmospheric aerosol model is assumed as the Junge power-law size distribution in retrieval of the data. Numerical simulations show that relative errors in retrieval of the aerosol optical thickness and the exponent of the Junge power law are less than 5% when the actual atmospheric aerosol follows the Junge power-law size distribution. For other aerosol size distributions, relative errors of the aerosol optical thickness are less than approximately 10%. The proposed method is applied to a case study of the data of two near-infrared channels of the Sea-Viewing Wide Field-of-View Sensor (SeaWiFS) over the East China Sea area. The results show that reasonable spatial distribution of the exponent of the Junge law and the aerosol optical thickness may be obtained on a pixel-by-pixel basis through use of the proposed retrieval algorithm.

© 2007 Optical Society of America

1. Introduction

At the top of the atmosphere, the total outgoing radiance at wavelength λ in the visible and near-infrared regions contains coupling information of both radiance and reflectance between the atmosphere and the ground. If only satellite-derived data are relied on, it is difficult to simultaneously retrieve the two unknown parameters: the atmospheric parameter and the ground optical parameter. It is known that only accumulation and coarse model particles may be detected by using the method of optical remote sensing. With the assumption of spherical aerosol particles, the unknown aerosol optical parameters are size distribution, complex refractive index, and optical thickness. It is necessary for retrieval of aerosol concentration or atmospheric correction of satellite data to assume an aerosol model [1–3

C. R. N. Rao, E. P. McClain, and L. L. Stowe, “Remote sensing of aerosols over the oceans using AVHRR data theory, practice, and applications,” Int. J. Remote Sens. 10, 743–749 (1989). [CrossRef]

], or to select several components externally mixing to form an aerosol-type model by using the optimum inversion method [4

D. Tanre, Y. J. Kaufman, M. Herman, and S. Mattoo, “Remote sensing of aerosol properties over oceans using the MODIS/EOS spectral radiances,” J. Geophys. Res. 102, 16971–16988 (1997). [CrossRef]

]. Such a pre-assumption, which is not based on local practical measurements, will result inevitably in some errors in retrieval of aerosol concentration and atmospheric correction of satellite data.

The Junge power-law model is a simple and popular aerosol model that is usually used to fit a realistic atmospheric aerosol size distribution for most cases. Zhao and Nakajima [5

F. S. Zhao and T. Nakajima, “Simultaneous determination of water-leaving reflectance and aerosol optical thickness from coastal zone color scanner measurements,” Appl. Opt. 36, 6949–6956 (1997). [CrossRef]

] and Zhao et al. [6

F. Zhao, Y. Li, C. Dong, and N. Lu, “An algorithm for determination of aerosol optical thickness from AVHRR imagery over oceans,” Meteorol. Atmos. Phys. 80, 73–88 (2002). [CrossRef]

] suggested that a realistic atmospheric aerosol can be approximated as the Junge power-law size distribution for satellite remote sensing in their algorithm. Zhao and Nakajima [5

F. S. Zhao and T. Nakajima, “Simultaneous determination of water-leaving reflectance and aerosol optical thickness from coastal zone color scanner measurements,” Appl. Opt. 36, 6949–6956 (1997). [CrossRef]

] noted that errors in the retrieved aerosol optical thickness are less than 10% with simulated test data by use of the Simplex Method [7

S. S. Rao, Optimization Theory and Applications (Wiley Eastern, Ltd., New Delhi, 1978).

] in the iterative procedure. They made numerical experiments based on wavelength relationships among water-leaving radiances and employed Junge power-law size distribution models with the same complex refractive index for atmospheric correction. Zhao et al. [6

F. Zhao, Y. Li, C. Dong, and N. Lu, “An algorithm for determination of aerosol optical thickness from AVHRR imagery over oceans,” Meteorol. Atmos. Phys. 80, 73–88 (2002). [CrossRef]

] developed an iterative algorithm for the simultaneous determination of aerosol optical thickness and the exponent of the Junge power law over ocean areas from the upwelling radiances measured in Advanced Very High Resolution Radiometer (AVHRR) visible and near-infrared channels with 1.50-j0.01 of the complex refractive indexes of the aerosols. In the iterative step, the new aerosol size distribution parameters are selected by using the Powell method [7

S. S. Rao, Optimization Theory and Applications (Wiley Eastern, Ltd., New Delhi, 1978).

].

Chomko and Gordon [8

R. M. Chomko and R. Gordon, “Atmospheric correction of ocean color imagery: use of the Junge power-law aerosol size distribution with variable refractive index to handle aerosol absorption,” Appl. Opt. 37, 5560–5572 (1998). [CrossRef]

] explored the efficacy of using the Junge power-law size distribution with a variable refractive index. They adopted a nonlinear optimization procedure [9

P. E. Gill and W. Murray, “Quasi-Newton methods for unconstrained optimization,” J. Inst. Math. Appl. 9, 91–108 (1972). [CrossRef]

] for estimating the relevant oceanic and atmospheric optical parameters. Simulated experiments showed that the ocean’s pigment concentration (C) can be retrieved with good accuracy; however, the aerosol optical thickness is retrieved with large errors. They thought that the discrepancy is due to significant differences in the scattering phase functions for bimodal, lognormal, and power-law distributions. The exponent of the Junge power law was determined by comparing the measured values of two near-infrared channels without the wavelength factor in their expressions, which is a possible error source for the retrieval of aerosol optical thickness. Even if the wavelength factor is included, relying on an analytical formula only, our numerical experiments may show that the relative errors in the estimation of size parameter ν are in the 20-40% range and the maximum relative error of the aerosol optical thickness is close to 50%. To improve the accuracy of retrieval, a new iterative algorithm is presented in this study for retrieval of size parameter ν and the aerosol optical thickness. Simulations show that the retrieval accuracy of size parameter ν and the aerosol optical thickness is improved satisfactorily by using the iterative algorithm.

First, a formula is derived in this study for retrieval of the exponent of the Junge power law, and some results are given by using simulated test data. Second, an iterative algorithm is presented and the feasibility of the algorithm is investigated with numerical simulations. Finally, the iterative algorithm is applied to local SeaWiFS imagery.

2. Retrieval scheme and simulated performance

2.1 The equation derived and the numerical simulations

It is assumed in the following retrieval scheme that the signal received by the satellite comes only from atmospheric scattering radiance and that the contributions of ground reflectance can be ignored. It is well-recognized that the assumption can be satisfied for the signals received by satellite at near-infrared bands for open ocean conditions. This generation of ocean-color sensors has two near-infrared channels: the SeaWiFS and the Moderate-Resolution Imaging Spectroradiometer (MODIS).

Ignoring the surface sun glitter and whitecaps in clear water, at the top of the atmosphere the total reflectance at a near-infrared wavelength λ in the single-scattering case can be written as [2

H. R. Gordon and M. Wang, “Retrieval of water-leaving radiance and aerosol optical thickness over the oceans with SeaWiFS: a preliminary algorithm,” Appl. Opt. 33, 443–452 (1994). [CrossRef] [PubMed]

,10

M. Wang and H. R. Gordon, “Retrieval of the columnar aerosol phase function and single-scattering albedo from sky radiance over the ocean: simulations,” Appl. Opt. 32, 4598–4609 (1993). [CrossRef] [PubMed]

]

ρp ( θ0, ϕ0,θ,ϕ)= ρm ( θ0, ϕ0,θ,ϕ) + ωa τa (λ) Pa ( θ0, ϕ0,θ,ϕ) 4cos θ0cosθ,
(1)

where ρm (θ0 ,ϕ0 ,θ,ϕ) is the reflectance by atmospheric molecules (Rayleigh scattering), parameters ωa , τa , and Pa (θ0 ,ϕ0 ,θ,ϕ) are the aerosol single-scattering albedo, aerosol optical thickness, and scattering phase function, respectively. Angles θ0 and ϕ0 are the solar zenith and azimuth angles, respectively. Likewise, θ and ϕ are the viewing zenith and azimuth angles.

For the Junge power-law size distribution, the wavelength dependence of an aerosol optical thickness between 0.4 and 1.1μm is described in the Angstrom formula [11

A. Angström, “Techniques of determining the turbidity of the atmosphere,” Tellus 13, 214–223 (1961). [CrossRef]

], which is written as

τa (λ)= βλ −α,
(2)

where α is the Angstrom coefficient and β is the turbidity factor. Combining Eqs. (1) and (2), the following expression can be obtained:

ln ρ p1 ( θ0, ϕ0,θ,ϕ)− ρ m1 ( θ0, ϕ0,θ,ϕ) ρ p2 ( θ0, ϕ0,θ,ϕ)− ρ m2 ( θ0, ϕ0,θ,ϕ)=ln ω a1P a1 ( θ0, ϕ0,θ,ϕ) ω a2 P a2 ( θ0, ϕ0,θ,ϕ) −αIn λ1 λ2,
(3)

where the subscripts 1 and 2 denote two near-infrared wavelengths. The Angstrom coefficient α describes the relative spectral course of the extinction coefficient σe in

σe=β′ λ −α,
(4)

where β’ is the aerosol extinction coefficient at wavelength 1μm . The formula is valid if the particle size distribution obeys the Junge power-law model. From Eq. (4), the ratio of the single scattering albedo in the two near-infrared bands is given by

ω a1 ω a2= σ s1 σ s2 ( λ1 λ2)α,
(5)

where σs is the scattering coefficient. The phase function is expressed as

Pa (φ)= 4πβs (φ) σs,
(6)

where φ is the scattering angle and βs (φ) is the scattering function. The ratio of the phase function values in two near-infrared bands is given by

P a1 (φ) P a2 (φ)= σ s2 β s1 (φ) σ s1 β s2 (φ).
(7)

For the Junge power-law size distribution, the aerosol scattering function may be written as [12

K. Bullrich, “Scattered radiation in the atmosphere and the natural aerosol,” Adv. Geophys. 10, 99–260 (1964). [CrossRef]

]

βs (φ)= 0.4343C ( λ 2π) −α∙ 12 η(φ),
(8)

where C is a constant and η(φ) is a dimensionless function that is used to describe the aerosol scattering direction. 03B7;(φ) is related to the scattering angle, complex refractive index, and size parameter, which may be written as

η (φ)= ∫ x1 x2 ( i1+ i2) x − ( ν+1)dx,
(9)

where x is the size parameter and i is the intensity distribution function. η(φ) is insensitive to wavelength if the scattering angle is more than 4° [12

K. Bullrich, “Scattered radiation in the atmosphere and the natural aerosol,” Adv. Geophys. 10, 99–260 (1964). [CrossRef]

]. The scattering angle is always larger than 4° for the downward observations by satellite sensors. Thus, according to Eqs. (5), (7), and (8), we obtain

ω a1 P a1 (φ) ω a2 P a2 (φ)= η1 (φ) η2 (φ) ≈ 1.
(10)

So, Eq. (3) can be modified by

α= −ln ρ p1 ( θ0, ϕ0,θ,ϕ)− ρ m1 ( θ0, ϕ0,θ,ϕ) ρ p2 ( θ0, ϕ0,θ,ϕ)− ρ m2 ( θ0, ϕ0,θ,ϕ) ln λ1 λ2.
(11)

According to the Mie scattering theory, the relationship between the exponent of the Junge power-law ν and the Angstrom coefficient α is

ν= α+ 2.
(12)

Deschamps et al. [13

P. Y. Deschamps, M. Herman, and D. Tanre, “Modeling of the atmospheric effects and its application to the remote sensing of ocean color,” Appl. Opt. 22, 3751–3758 (1983). [CrossRef] [PubMed]

] approximated the contribution of the aerosol on the right-hand side of Eq. (1) as the aerosol optical thickness, and further approximated it as λ -α, i.e.,

{ ωa τa (λ) Pa ( θ0, ϕ0,θ,ϕ) 4cos θ0 cosθ≈ τa (λ). τa (λ) ≈ λ −α
(13)

Based on the simplification in Eq. (13), Eq. (11) could also be obtained. However, the aerosol optical thickness must be small enough to keep the approximation of Eq. (13) reasonable.

Because there was only one near-infrared band for the satellite at that time, further numerical simulation was not done in Ref. [13

P. Y. Deschamps, M. Herman, and D. Tanre, “Modeling of the atmospheric effects and its application to the remote sensing of ocean color,” Appl. Opt. 22, 3751–3758 (1983). [CrossRef] [PubMed]

]. The following simulation results indicate that the errors are large in retrieval of the exponent of Junge power-law v from Eq. (11) only.

A test dataset is simulated by computing ρp (θ0 ,ϕ0 ,θ,ϕ) for 2.5, 3.0, 3.5, 4.0, 4.5, and 5.0 of ν with τa (550)=0.3 at a band of 550nm, and the complex refractive index m=1.45+0.0035i. The size range of the particle radius in the calculations is taken as 0.04-10μm. The two near-infrared bands are 0.765 and 0.865μm with a bandwidth of 40nm. Note that the simulated data were given for sensor viewing angles of 15°, 30°, 45°, 60°, and azimuth of 200°, with solar zenith of 30° and azimuth of 180°.

Size distribution parameters for ν are calculated in terms of Eq. (11). The relative errors of ν are listed in Table 1. The τa (550) are calculated iteratively according to the iterative Eq. (16) in the next paragraphs by inputting the ν to the 6S code [14

E. F. Vermote, D. Tanre, J. L. Deuze, M. Herman, and J. J. Morcrette, The Second Simulation of the Satellite Signal in the Solar Spectrum (6S) User Guide (Laboratoire d’Optique Atmosphérique, France, 1997).

] for radiative transfer calculation while ignoring the absorption of atmospheric molecules for the ocean’s surface of clear waters. The relative errors in retrievals of aerosol optical thicknesses τa (550) are listed in Table 2.

Table 1.  Relative errors (%) of the size distribution parameters ν.
ν 2.53.03.54.04.55.0
θν 15°36.734530927.926.727.8
30°33.233.731.027.726.728.0
45°40334930126.826.027.3
60°26.226324823.924626.7
Table 2.  Relative errors (%) of the aerosol optical thickness τa (550).
ν 2.53.03.54.04.55.0
θν 15°-46.7-19.915.034.537.933.0
30°-18.6-1.922.334.934.228.1
45°-35.5-12.922.334.934.228.1
60°-47.6-39.7-13.15.110.99.3

Tables 1 and 2 show that the relative errors of ν are within 20–40% and the maximum relative error of τa (550) is close to 50%. It is found that computational errors cannot be tolerated in computing the size distribution parameters of ν and τa (550). To see the influence of multiple scattering, we have also carried out simulations with τa (550)=0.1 and 0.05, which are clear atmospheres over the ocean. Unfortunately, the relative errors of ν are still within 20-35% in the case of small aerosol optical thickness, which indicates that multiscattering is not an important factor for the above errors. Simulations suggest that such large errors may not result only from the ignorance of multiple scattering according to Eq. (11). So, it is understood that large errors of τa (550) can be ascribed to the inaccurate ν.

2.2 The new iterative algorithm and the numerical simulations

In order to improve the retrieval accuracy of ν and τa (550), based on the process derived in the above equation, an expression is created:

[ ρ p1 ( θ0, ϕ0,θ,ϕ) − ρ m1 ( θ0, ϕ0,θ,ϕ)] [ ρ p2c ( θ0, ϕ0,θ,ϕ) − ρ m2 ( θ0, ϕ0,θ,ϕ)] [ ρ p2 ( θ0, ϕ0,θ,ϕ) − ρ m2 ( θ0, ϕ0,θ,ϕ)] [ ρ p1c ( θ0, ϕ0,θ,ϕ) − ρ m1 ( θ0, ϕ0,θ,ϕ)],

= ω a1 τ a1 ( λ1) P a1 ( θ0, ϕ0,θ,ϕ) ω a2c τ a2c ( λ2) P a2c ( θ0, ϕ0,θ,ϕ) ω a2 τ a2 ( λ2) P a2 ( θ0, ϕ0,θ,ϕ) ω a1c τ a1c ( λ1) P a1c ( θ0, ϕ0,θ,ϕ)
(14)

where values with a superscript c are calculated from the 6S mode in the two near-infrared bands. We denote the left side of Eq. (14) as Y. Combining Eqs. (2) and (10), Eq. (14) then becomes

α= lnY ( ln λ2 − ln λ1) + αn,
(15)

where αn cf is the input value for the 6S mode at the nth iteration. Using the α calculated from Eq. (15), new τa (550) can be obtained with a near-infrared wavelength by using the iterative calculation [15

Q. Xu, H. W., and F. Zhao, “Retrieval of reflectance along coastal zone with SeaWiFS,” J. Remote Sens. (in Chinese) 6, 352–356 (2002).

]

τa (550)= ρp ( θ0, ϕ0,θ,ϕ)− ρm( θ0, ϕ0,θ,ϕ) ρpc ( θ0, ϕ0,θ,ϕ)− ρm ( θ0, ϕ0,θ,ϕ) τan (550)
(16)

where τn a (550) is the input aerosol optical thickness for the 6S mode. This procedure is followed according to Eq. (16) until the convergence criterion of

∣ ( ρp ( θ0, ϕ0,θ,ϕ) − ρpc ( θ0, ϕ0,θ,ϕ)) ρp ( θ0, ϕ0,θ,ϕ)∣ <ε
(17)

is satisfied. The α and new τa (550) are selected as the next input values for the 6S mode, and the two procedures according to Eqs. (15) and (16) are repeated, until the convergence criterion of

∑ i=12∣ ( ρpi ( θ0, ϕ0,θ,ϕ) − ρpic ( θ0, ϕ0,θ,ϕ)) ρpi ( θ0, ϕ0,θ,ϕ)∣ <δ
(18)

is satisfied. The oα and the τa (550) in the last step are determined as the actual required values.

Another numerical simulation is carried out by the proposed iterative algorithm with the same preset parameters as above for the mid-latitude winter of the atmospheric model in which multiscattering and molecule absorption are considered. The errors of retrieved values of ν and τa (550) are listed in Tables 3 and 4, respectively. It can be seen from Tables 3 and 4 that the relative errors of the retrieved ν and τa (550) are less than 5%, which indicates that excellent retrievals of both ν and τa (550) can be obtained for the Junge power-law model in the iterative algorithm.

Table 3.  Relative errors (%) of ν in the iterative algorithm.
ν 2.53.03.54.04.55.0
θν 15°0.50.20.60.60.50.4
30°-2.23.21.40.91.20.7
45°1.00.60.70.90.70.3
60°-1.01.50.70.70.60.8
Table 4.  Relative errors (%) of τa (550) in the iterative algorithm.
ν 2.53.03.54.04.55.0
θν 15°0.70.31.20.90.4.10
30°-2.23.81.70.90.60.1
45°1.00.91.21.20.60.1
60°-0.41.00.50.40.2-0.2

2.3 Applications to other aerosol size distributions

Atmospheric aerosol has large spatial-temporal variations. It is possible that actual atmospheric aerosol may not obey Junge power-law size distribution. The iterative algorithm is derived from the Junge power-law aerosol model. It is a key point, obviously, in its application whether the iterative scheme is still valid for another aerosol model. Many in-situ observations have shown that lognormal distributions are more appropriate to describe realistic aerosol size distribution [16

E. M. Patterson and D. A. Gillette, “Commonalities in measured size distributions for aerosol having a soil-derived component,” J. Geophys. Res. 82, 2074–2082 (1997). [CrossRef]

,17

Y. Kim, H. Sievering, and J. F. Boatmann, “Airborne measurement of atmospheric aerosol particles in the lower troposphere over the central United States,” J. Geophys. Res. 93, 12631–12644 (1988). [CrossRef]

]. Generally, any aerosol size distribution may be described by the combination of three lognormal distribution functions. As in size distribution, lognormal distributions are applied to each component i:

dNi (r)dr= Ni 2πr logσiln10exp [ 12 ( logr− logr modN,i log σi)2],
(19)

where r modN,i is the mode radius, σi measures the width of distribution, and Ni is the total particle number density of the component i in particles per cubic centimeter. The microphysical characteristics of the four components for the standard 6S aerosol types [18

E. F. Vermote, D. Tanre, J. L. Deuze, M. Herman, and J. J. Morcrette, “Second simulation of the satellite signal in the solar spectrum: an overview,” IEEE Trans. Geosci. Remote Sens. 35, 675–686 (1997). [CrossRef]

] are listed in Table 5. From the four basic components, the three aerosol types (maritime, continental, and urban models) are selected by mixing them with the following volume percentages in Table 6. The values of the brackets in Table 6 are the percentage density of particles. The complex refractive index of aerosol is assumed to be uniform as 1.45+0.0035i at the two near-infrared bands (0.765 and 0.865μm).

Table 5.  Microphysical characteristics of the four components for the standard 6S aerosol type.
ComponentDust-LikeWater SolubleOceanicSoot
r modN,i(μm)0.5000.00500.300.0118
σi 2.9902.9902.512.00
Table 6.  Volume percentages of the four basic components for the standard 6S aerosol model.
Dust-LikeWater SolubleOceanicSoot
Maritime 5 (99.9579)95 (4.208E-2) 
Continental70 (2.26490E-2)29 (93.8299) 1 (6.16087)
Urban17 (1.65125E-05)61 (59.2607) 22 (40.7492)

The retrieved values and errors of both ν and τa (550) can be obtained by using the proposed iterative algorithm with the microphysical characteristics in Table 5 and the volume percentages of the two basic components with maritime in Table 6, which are tabulated in Table 7. The true τa (550) is 0.3. The sun-viewing geometries are uniform in the above tables. For the four cases of sun-viewing geometry, the difference of size distribution of parameter ν is little. These values of ν can be evaluated as equivalent exponents of the Junge power law for lognormal distributions. It can be found in Table 7 that the retrieved values of τa (550) are in relative error by <5%.

Table 7.  Values of ν and τa (550) and their errors retrieved by the iterative algorithm with the aerosol type of the lognormal distribution (maritime).
θ;ν ν τa (550)Relative error (%) of τa (550)
15°4.210.2883.9
30°4.240.2941.9
45°4.230.2893.8
60°4.280.2893.6

Assuming that the three components of the lognormal distribution are externally mixed to form aerosol types with the volume percentages of the three basic components with the continental model in Table 6, the examples of performance of the iterative algorithm provide that ν is around 4.7 and the relative error of the τa (550) is around 7%, which is shown in Table 8.

Table 8.  Values of ν and τa (550) and their errors retrieved by the iterative algorithm with the aerosol type of the lognormal distribution (continental).
θ;ν ν τa (550)Relative error (%) of τa (550)
15°4.780.2787.4
30°4.730.2796.9
45°4.770.2796.9
60°4.700.2835.5

In the same way, we have applied the iterative algorithm for the urban aerosol type. The results are shown in Table 9.

Table 9.  Values of ν and τa (550) and their errors retrieved by the iterative algorithm with the aerosol type of the
θ;ν ν τa (550)Relative error (%) of τa (550)
15°4.950.2845.3
30°4.880.2855.1
45°4.940.2864.8
60°4.880.2874.3

It can be seen from Tables 7–9 that the equivalent exponents of the Junge power law are about 4.2, 4.7, and 5.0, with the complex refractive index of 1.45+0.0035i for the maritime, continental, and urban aerosol models, respectively. The difference among the values of retrieved size distribution parameter ν is small with various sun-viewing geometries for the same aerosol model. The relative errors in retrieved values of τa (550) should be <10%. It can be summarized that it is responsible to approximate the actual atmospheric aerosol as the Junge power-law size distribution in the course of retrieval of aerosol concentrations in this iterative algorithm.

The new algorithm is a physical iterative method, which is different from others and has better accuracy in simultaneous determination of aerosol optical thickness and the Junge power-law size distribution parameter that is relied on in satellite-derived data only.

3. Example of application to SeaWiFS data

By using the iterative algorithm, the values of ν and τa (550) were retrieved from SeaWiFS measurements on January 1, 2001, over the Taiwan Strait region with an aerosol complex refractive index of 1.45+0.0035i [4

D. Tanre, Y. J. Kaufman, M. Herman, and S. Mattoo, “Remote sensing of aerosol properties over oceans using the MODIS/EOS spectral radiances,” J. Geophys. Res. 102, 16971–16988 (1997). [CrossRef]

]. The spatial varieties of ν and τa (550) are shown in Figs. 1 and 2. The black color represents clouds or land, or Case 2 waters in Figs. 1 and 2, which is distinguished from Case 1 waters in terms of the criterion of α > 4 or α≤ 0 during the iterative retrieval process. It can be seen from Fig. 1 that the values of ν can be divided into three groups: 3.0-3.7 near the cloud region; 4.5-5.0 on the coast region, which is close to the one in the continental or urban aerosol models discussed above; and 3.7-4.5 on most open oceans in the Taiwan Strait. In the red areas in Fig. 1, the values of ν between 5.25 and 6.0 are likely to be the influence of the uncertain aerosol model. Although the retrieved equivalent Junge index in the red areas is a little bit large in those cases, the corresponding optical depth that is retrieved is still reasonable (see Fig. 2). It can be seen from Fig. 2 that most of τa (550) values vary within the range of 0.20 to 0.28. Though νis also in the 4.5-5.0 range on the east side of Taiwan, the τa (550) is less than 0.15, which indicates clean air in that region. On the east side of Taiwan and most regions in the center of the Taiwan Strait, the aerosols possibly might obey the Junge power-law size distribution.

Fig. 1. Spatial distribution of ν retrieved from local SeaWiFS data on January 1, 2001.
Fig. 2. Spatial distribution of τa (550) retrieved from local SeaWiFS data on January 1, 2001.

4. Conclusion

By using the Junge power-law size distribution to approximate the actual atmospheric aerosol model, the proposed iterative algorithm avoids the uncertainty of the aerosol model in the retrieval of aerosol concentrations from satellite measurements. The exponent of the Junge power law can be retrieved for each pixel over an entire image, which also avoids the ordinary assumption of uniform aerosol size distribution over an entire image or just a part of an image. The iterative method has performed radiative transfer simulations of the retrieval process. The simulated experiment indicates that the relative error of the retrieved ν and τa (550) is less than 5% if the actual atmospheric aerosol follows the Junge power-law size distribution. If actual atmospheric aerosol is the lognormal distribution, the equivalent exponent of the Junge power law can be obtained by the iterative method, and the relative error of retrieved τa (550) is approximately <10%. The method has been also applied to SeaWiFS local data. It has been demonstrated that the values of retrieved ν and τa (550) are reasonable, and that ν has a large spatial variation over a local-area image. It can be concluded that the assumption of uniform aerosol size distribution parameters over an entire image or a segmented image undoubtedly will lead to retrieval errors of aerosol concentrations.

A fixed aerosol complex-refractive index is assumed for the Junge power-law model in the current algorithm. The assumption would produce additional errors, more or less. The influence of an aerosol complex-refractive index in the retrieval of aerosol concentration is worthy of further investigation.

References and links

1.

C. R. N. Rao, E. P. McClain, and L. L. Stowe, “Remote sensing of aerosols over the oceans using AVHRR data theory, practice, and applications,” Int. J. Remote Sens. 10, 743–749 (1989). [CrossRef]

2.

H. R. Gordon and M. Wang, “Retrieval of water-leaving radiance and aerosol optical thickness over the oceans with SeaWiFS: a preliminary algorithm,” Appl. Opt. 33, 443–452 (1994). [CrossRef] [PubMed]

3.

D. A. Siegal, M. Wang, S. Maritorena, and W. Robinson, “Atmospheric correction of satellite ocean color imagery: the black pixel assumption,” Appl. Opt. 39, 3582–3591 (2000). [CrossRef]

4.

D. Tanre, Y. J. Kaufman, M. Herman, and S. Mattoo, “Remote sensing of aerosol properties over oceans using the MODIS/EOS spectral radiances,” J. Geophys. Res. 102, 16971–16988 (1997). [CrossRef]

5.

F. S. Zhao and T. Nakajima, “Simultaneous determination of water-leaving reflectance and aerosol optical thickness from coastal zone color scanner measurements,” Appl. Opt. 36, 6949–6956 (1997). [CrossRef]

6.

F. Zhao, Y. Li, C. Dong, and N. Lu, “An algorithm for determination of aerosol optical thickness from AVHRR imagery over oceans,” Meteorol. Atmos. Phys. 80, 73–88 (2002). [CrossRef]

7.

S. S. Rao, Optimization Theory and Applications (Wiley Eastern, Ltd., New Delhi, 1978).

8.

R. M. Chomko and R. Gordon, “Atmospheric correction of ocean color imagery: use of the Junge power-law aerosol size distribution with variable refractive index to handle aerosol absorption,” Appl. Opt. 37, 5560–5572 (1998). [CrossRef]

9.

P. E. Gill and W. Murray, “Quasi-Newton methods for unconstrained optimization,” J. Inst. Math. Appl. 9, 91–108 (1972). [CrossRef]

10.

M. Wang and H. R. Gordon, “Retrieval of the columnar aerosol phase function and single-scattering albedo from sky radiance over the ocean: simulations,” Appl. Opt. 32, 4598–4609 (1993). [CrossRef] [PubMed]

11.

A. Angström, “Techniques of determining the turbidity of the atmosphere,” Tellus 13, 214–223 (1961). [CrossRef]

12.

K. Bullrich, “Scattered radiation in the atmosphere and the natural aerosol,” Adv. Geophys. 10, 99–260 (1964). [CrossRef]

13.

P. Y. Deschamps, M. Herman, and D. Tanre, “Modeling of the atmospheric effects and its application to the remote sensing of ocean color,” Appl. Opt. 22, 3751–3758 (1983). [CrossRef] [PubMed]

14.

E. F. Vermote, D. Tanre, J. L. Deuze, M. Herman, and J. J. Morcrette, The Second Simulation of the Satellite Signal in the Solar Spectrum (6S) User Guide (Laboratoire d’Optique Atmosphérique, France, 1997).

15.

Q. Xu, H. W., and F. Zhao, “Retrieval of reflectance along coastal zone with SeaWiFS,” J. Remote Sens. (in Chinese) 6, 352–356 (2002).

16.

E. M. Patterson and D. A. Gillette, “Commonalities in measured size distributions for aerosol having a soil-derived component,” J. Geophys. Res. 82, 2074–2082 (1997). [CrossRef]

17.

Y. Kim, H. Sievering, and J. F. Boatmann, “Airborne measurement of atmospheric aerosol particles in the lower troposphere over the central United States,” J. Geophys. Res. 93, 12631–12644 (1988). [CrossRef]

18.

E. F. Vermote, D. Tanre, J. L. Deuze, M. Herman, and J. J. Morcrette, “Second simulation of the satellite signal in the solar spectrum: an overview,” IEEE Trans. Geosci. Remote Sens. 35, 675–686 (1997). [CrossRef]

OCIS Codes
(010.0010) Atmospheric and oceanic optics : Atmospheric and oceanic optics
(010.1110) Atmospheric and oceanic optics : Aerosols
(120.0280) Instrumentation, measurement, and metrology : Remote sensing and sensors
(280.1100) Remote sensing and sensors : Aerosol detection

ToC Category:
Atmospheric and ocean optics

History
Original Manuscript: September 22, 2006
Revised Manuscript: January 16, 2007
Manuscript Accepted: March 8, 2007
Published: April 13, 2007

Virtual Issues
Vol. 2, Iss. 5 Virtual Journal for Biomedical Optics

Citation
Qingshan Xu, Heli Wei, Ruizhong Rao, and Huanling Hu, "Simultaneous determination of aerosol optical thickness and exponent of Junge power law from satellite measurements of two near-infrared bands over the ocean," Opt. Express 15, 5227-5236 (2007)
http://www.opticsinfobase.org/oe/abstract.cfm?URI=oe-15-8-5227


Sort:  Author  |  Year  |  Journal  |  Reset  

References

  1. C. R. N. Rao, E. P. McClain, and L. L. Stowe, "Remote sensing of aerosols over the oceans using AVHRR data theory, practice, and applications," Int. J. Remote Sens. 10, 743-749 (1989). [CrossRef]
  2. H. R. Gordon and M. Wang, "Retrieval of water-leaving radiance and aerosol optical thickness over the oceans with SeaWiFS: a preliminary algorithm," Appl. Opt. 33, 443-452 (1994). [CrossRef] [PubMed]
  3. D. A. Siegal, M. Wang, S. Maritorena, and W. Robinson, "Atmospheric correction of satellite ocean color imagery: the black pixel assumption," Appl. Opt. 39, 3582-3591 (2000). [CrossRef]
  4. D. Tanre, Y. J. Kaufman, M. Herman, and S. Mattoo, "Remote sensing of aerosol properties over oceans using the MODIS/EOS spectral radiances," J. Geophys. Res. 102, 16971-16988 (1997). [CrossRef]
  5. F. S. Zhao and T. Nakajima, "Simultaneous determination of water-leaving reflectance and aerosol optical thickness from coastal zone color scanner measurements," Appl. Opt. 36, 6949-6956 (1997). [CrossRef]
  6. F. Zhao, Y. Li, C. Dong, and N. Lu, "An algorithm for determination of aerosol optical thickness from AVHRR imagery over oceans," Meteorol. Atmos. Phys. 80, 73-88 (2002). [CrossRef]
  7. S. S. Rao, Optimization Theory and Applications (Wiley Eastern, Ltd., New Delhi, 1978).
  8. R. M. Chomko and R. Gordon, "Atmospheric correction of ocean color imagery: use of the Junge power-law aerosol size distribution with variable refractive index to handle aerosol absorption," Appl. Opt. 37, 5560-5572 (1998). [CrossRef]
  9. P. E. Gill and W. Murray, "Quasi-Newton methods for unconstrained optimization," J. Inst. Math. Appl. 9, 91-108 (1972). [CrossRef]
  10. M. Wang and H. R. Gordon, "Retrieval of the columnar aerosol phase function and single-scattering albedo from sky radiance over the ocean: simulations," Appl. Opt. 32, 4598-4609 (1993). [CrossRef] [PubMed]
  11. A. Angström, "Techniques of determining the turbidity of the atmosphere," Tellus 13, 214-223 (1961). [CrossRef]
  12. K. Bullrich, "Scattered radiation in the atmosphere and the natural aerosol," Adv. Geophys. 10, 99-260 (1964). [CrossRef]
  13. P. Y. Deschamps, M. Herman, and D. Tanre, "Modeling of the atmospheric effects and its application to the remote sensing of ocean color," Appl. Opt. 22, 3751-3758 (1983). [CrossRef] [PubMed]
  14. E. F. Vermote, D. Tanre, J. L. Deuze, M. Herman, and J. J. Morcrette, The Second Simulation of the Satellite Signal in the Solar Spectrum (6S) User Guide (Laboratoire d'Optique Atmosphérique, France, 1997).
  15. Q. Xu, H. W., and F. Zhao, "Retrieval of reflectance along coastal zone with SeaWiFS," J. Remote Sens.(in Chinese) 6, 352-356 (2002).
  16. E. M. Patterson and D. A. Gillette, "Commonalities in measured size distributions for aerosol having a soil-derived component," J. Geophys. Res. 82, 2074-2082 (1997). [CrossRef]
  17. Y. Kim, H. Sievering, and J. F. Boatmann, "Airborne measurement of atmospheric aerosol particles in the lower troposphere over the central United States," J. Geophys. Res. 93, 12631-12644 (1988). [CrossRef]
  18. E. F. Vermote, D. Tanre, J. L. Deuze, M. Herman, and J. J. Morcrette, "Second simulation of the satellite signal in the solar spectrum: an overview," IEEE Trans. Geosci. Remote Sens. 35, 675-686 (1997). [CrossRef]

Cited By

 Alert me when this paper is cited

OSA is able to provide readers links to articles that cite this paper by participating in CrossRef's Cited-By Linking service. CrossRef includes content from more than 3000 publishers and societies. In addition to listing OSA journal articles that cite this paper, citing articles from other participating publishers will also be listed.

Figures

Fig. 1. Fig. 2.
 

« Previous Article  |  Next Article »

OSA is a member of CrossRef.

CrossCheck Deposited