Generalized Split-Window Algorithm for Estimate of Land Surface Temperature from Chinese Geostationary FengYun Meteorological Satellite (FY-2C) Data

Abstract

On the basis of the radiative transfer theory, this paper addressed the estimate of Land Surface Temperature (LST) from the Chinese first operational geostationary meteorological satellite-FengYun-2C (FY-2C) data in two thermal infrared channels (IR1, 10.3-11.3 μm and IR2, 11.5-12.5 μm), using the Generalized Split-Window (GSW) algorithm proposed by Wan and Dozier (1996). The coefficients in the GSW algorithm corresponding to a series of overlapping ranging of the mean emissivity, the atmospheric Water Vapor Content (WVC), and the LST were derived using a statistical regression method from the numerical values simulated with an accurate atmospheric radiative transfer model MODTRAN 4 over a wide range of atmospheric and surface conditions. The simulation analysis showed that the LST could be estimated by the GSW algorithm with the Root Mean Square Error (RMSE) less than 1 K for the sub-ranges with the Viewing Zenith Angle (VZA) less than 30° or for the sub-rangs with VZA less than 60° and the atmospheric WVC less than 3.5 g/cm² provided that the Land Surface Emissivities (LSEs) are known. In order to determine the range for the optimum coefficients of the GSW algorithm, the LSEs could be derived from the data in MODIS channels 31 and 32 provided by MODIS/Terra LST product MOD11B1, or be estimated either according to the land surface classification or using the method proposed by Jiang et al. (2006); and the WVC could be obtained from MODIS total precipitable water product MOD05, or be retrieved using Li et al.' method (2003). The sensitivity and error analyses in term of the uncertainty of the LSE and WVC as well as the instrumental noise were performed. In addition, in order to compare the different formulations of the split-window algorithms, several recently proposed split-window algorithms were used to estimate the LST with the same simulated FY-2C data. The result of the intercomparsion showed that most of the algorithms give comparable results.

1. Introduction

Land Surface Temperature (LST) is not only a good indicator of both the energy equilibrium of the Earth's surface and greenhouse effects, but also one of the key variables controlling fundamental biospheric and geospheric interactions between the Earth's surface and its atmosphere. It can play either a direct role such as when estimating longwave fluxes, or indirectly as when estimating latent and sensible heat fluxes [1, 2]. Moreover, many other applications, such as evaportranspiration modeling [3, 4], estimating soil moisture [5], and climatic, hydrological, ecological and biogeochemical studying [6, 7] and so on, rely on the knowledge of LST. Consequently, it is crucial to have access to reliable estimates of surface temperature over large spatial and temporal scales. It is practically impossible to obtain such information from ground based measurements, whereas the satellite observations in the Thermal Infra-Red (TIR) appears to be very attractive since it can give access to global and temporal estimates of LST.

However, the retrieval of the LST from satellite data is a very difficult task because, besides the radiometric calibration and the cloud screening procedures, three types of corrections have to be made. They are emissivity corrections, atmospheric corrections and topography corrections [8]. Up to now, many algorithms for estimating the LST from satellite observations have been proposed. They may be roughly grouped into three categories: the single channel algorithm [9, 10], the split window algorithm [11, 12] and the triple window algorithm [13].

The single channel method is a simple inversion of the radiative transfer equation providing that the Land Surface Emissivities (LSEs) and the atmospheric profiles are known in advance. The triple window method combines two thermal window channels and one middle infrared channel to estimate the LST for nighttime satellite observations. The split window method is used to retrieve the LST based on the differential water vapor absorption in two adjacent infrared channels. This method was firstly proposed by McMillin (1975) [11] to estimate sea surface temperature from satellite measurements. Since then, a variety of split window algorithms have been developed and modified to retrieve LST, and, currently, most of them have been successfully applied to the LST retrieval from the data observed by the AVHRR, MODIS, and Spinning Enhanced Visible and Infrared Imager (SEVIRI) instruments [8, 14-22].

The FengYun-2C (FY-2C), a geostationary meteorological satellite developed by Shanghai Academy of Space Flight Technology (SAST, also known as 8^th Space Academy) and China Academy of Space Technology (CAST, also know as 5^th Space Academy) and operated by China Meteorological Administration (CMA), was launched on 19 October 2004 and is becoming fully operational in 2006. The FY-2C is the Chinese first operational meteorological satellite, which is also the fourth satellite of the FY series and is located above the Equator at longitude 105° E, and some 35,800 km away. The objective of the mission is to monitor the temperature and the clouds above China and neighboring areas and also to provide meteorological information for the Asia-Pacific region. The upgraded Stretched-Visible and Infrared Spin-Scan Radiometer (S-VISSR) is one of the major payloads onboard the FY-2C. This optical imaging radiometer consists of one visible channel and four infrared channels. The characteristics of the instrument are shown in

Table 1. Specifications of S-VISSR channels: spectral range and spatial resolutions.

Channel no.	Channel name	Spectral range (μm)	Spatial resolution (km)
1	IR1	10.3-11.3	5
2	IR2	11.5-12.5	5
3	IR3	6.3-7.6	5
4	IR4	3.5-4.0	5
5	VIS	0.55-0.90	1.25

. It can acquire one full disc image covering the Earth surface from 60° N to 60° S in latitude and from 45° E to 165° E in longitude per hour and 30 min per acquisition for flood season.

The work presented in this paper aims to retrieve LST from the FY-2C satellite data in two thermal infrared channels (IR1, 10.3-11.3 μm and IR2, 11.5-12.5 μm), using the Generalized Split-Window (GSW) algorithm proposed by Wan and Dozier (1996) [21]. Section 2 describes the theory associated with the LST retrieval using the GSW algorithm and presents the algorithm development for FY-2C data. Section 3 gives the results and the numerical values of the coefficients in the GSW algorithm. The sensitivity and error analyses in term of the uncertainty of the LSE and Water Vapor Content (WVC) in the atmosphere as well as the instrumental noise are also presented in this section. In addition, in order to compare the different formulations of the split-window algorithms, this section gives the intercomparsion of the LSTs estimated by several split-window algorithms. Section 4 gives an example of retrieving LST from FY-2C satellite data. The Conclusion is drawn in Section 5.

2. Theory

2.1. Radiative transfer for split-window algorithm

On the basis of the radiative transfer theory, for a cloud-free atmosphere under thermodynamic equilibrium, the channel radiance B_i(T_i) measured at the Top Of the Atmosphere (TOA) in a Thermal Infra-Red (TIR) channel of the sensor onboard the satellite, is given with a good approximation as [23]

$$B_i\left(T_i\right)={\mathit{\varepsilon }}_i{B}_i\left(T_s\right){\mathit{\text{τ}}}_i+R_{\mathit{\text{atm}}\_i}^{\uparrow }+\left(1-{\mathit{\varepsilon }}_i\right)R_{\mathit{\text{atm}}\_i}^{\downarrow }{\mathit{\text{τ}}}_i$$

(1)

where T_i is the channel brightness temperature observed in channel i at the TOA, B_i is the Planck function, B_i(T_s) is the radiance measured if the surface is a black body with surface temperature T_s, ε_i is the channel emissivity in channel i, τ_i is the total atmospheric transmittance along the target to sensor path in channel i, $R_{\mathit{\text{atm}}\_i}^{\uparrow }$ is the thermal path atmospheric upwelling radiance in channel i, and $R_{\mathit{\text{atm}}\_i}^{\downarrow }$ is the channel downwelling atmospheric radiance from the whole hemisphere in channel i. The first term on the right hand side of Eq. (1) represents the surface emission that is attenuated by the atmosphere. The second term represents the upwelling atmosphere emission toward the sensor and the third term represents the downwelling atmosphere emission that is reflected by the surface and reaches the sensor.

Inverting Eq. (1), one can get

$$T_s=B^{-1}[\frac{B_i\left(T_i\right)-R_{\mathit{\text{atm}}\_i}^{\uparrow }-\left(1-{\mathit{\varepsilon }}_i\right)R_{\mathit{\text{atm}}\_i}^{\downarrow }{\mathit{\text{τ}}}_i}{{\mathit{\varepsilon }}_i{\mathit{\text{τ}}}_i}]$$

(2)

in which B⁻¹ is the inverse of the Planck function. Once the channel emissivity ε_i is known, there are two ways to estimate the LST from satellite data. One is to use Eq. (2) with atmospheric radiative transfer model such as MODTRAN 4 [24] or 4A/OP [25], if the atmospheric profile is available from either conventional radiosoundings or satellite soundings. The other is to employ the split-window algorithm developed on the basis of the differential water vapor absorption in two adjacent infrared channels (McMilin, 1975) [11] if the atmospheric profile is not available.

As S-VISSR sensor onboard FY-2C has two adjacent thermal infrared channels (IR1 and IR2), the GSW algorithm proposed by Wan and Dozier [21] is adopted to estimate the LST from FY-2C satellite data. According to GSW algorithm, the LST can be expressed as

$$T_s=a_0+(a_1+a_2\frac{1-\mathit{\varepsilon }}{\mathit{\varepsilon }}+a_3\frac{\mathrm{\Delta }\mathit{\varepsilon }}{{\mathit{\varepsilon }}^2})\frac{T_i+T_j}{2}+(a_4+a_5\frac{1-\mathit{\varepsilon }}{\mathit{\varepsilon }}+a_6\frac{\mathrm{\Delta }\mathit{\varepsilon }}{{\mathit{\varepsilon }}^2})\frac{T_i-T_j}{2}$$

(3)

with ε = (ε_i + ε_j)/2 and Δε = ε_i − ε_j.

where T_i and T_j are the TOA brightness temperatures measured in channels i (11.0 μm) and j (12.0 μm), respectively; ε_i and ε_j are, respectively, the land surface emissivities in channels i and j; ε is the averaged emissivity; Δε is the emissivity difference between the two adjacent channels; and a₀ − a₆ are unknown coefficients which will be derived in the following from simulated FY-2C data..

2.2. Algorithm development for FY-2C

So far, as there is no available database of in situ LST measurements in coincidence with the FY-2C overpasses, the only possible way to obtain the coefficients in Eq. (3) is to use numerical simulation for establishing the database used in the statistical regression. To this end, the atmospheric radiative transfer model MODTRAN 4 was used to simulate the TOA radiance with the appropriate thermal infrared channel response function of the S-VISSR onboard FY-2C.

Keeping in mind that a practical LST algorithm should accommodate atmospheric variations wide enough to cover all possible real situations, two radiosonde observation databases were taken into account in our simulation. One is the latest version of the Thermodynamic Initial Guess Retrieval (TIGR) database TIGR2002, which was constructed by the Laboratoire de Meteorologie Dynamique (LMD) and represents a worldwide set of atmospheric situations (2311 radisoundings) from polar to tropical atmosphere with varying water vapor amounts ranging from 0.1 to 8 g/cm² ( http://ara.lmd.polytechnique.fr/htdocs-public/products/TIGR/TIGR.html). The other is the six standard atmospheric profiles (tropical, mid-latitude summer, mid-latitude winter, sub-arctic summer, sub-arctic winter, and US76) stored in the MODTRAN 4. For LST retrieval, we only consider atmospheric variation in clear-sky conditions. Consequently, the profiles with relative humidity at one of levels greater than 90% in TIGR2002 were discarded as this seldom happens under clear-sky conditions. Therefore, 1413 representative atmospheric situations were extracted from TIGR2002. Figure 1 shows a plot of the atmospheric Water Vapor Content (WVC) as function of the atmospheric temperature T₀ in the first boundary layer of these selected atmospheres. As shown in this figure, the T₀ varies from 231 K to 315 K and the atmospheric WVC changes from 0.06 g/cm² to 6.44 g/cm².

Taking into account the angular dependence of the TOA radiance, six different Viewing Zenith Angles (VZAs) (0°, 33.56°, 44.42°, 51.32°, 56.25°, 60°) varying from 0° to 60° were used in MODTRAN simulations. With the VZAs and the radiosoundings mentioned above as MODTRAN input, we can obtain the channel atmospheric parameters (τ_i, $R_{\mathit{\text{atm}}\_i}^{\uparrow }$, $R_{\mathit{\text{atm}}\_i}^{\downarrow }$) with spectral integration of the channel response function for each VZA and each atmospheric profile.

In addition, in order to make the simulation more representatives, the reasonable variations of LST are varied in a wide range according to the atmospheric temperature T₀ in the first boundary layer of the atmospheric profiles used. That is, LST varies from T₀ − 5 K to T₀ + 15 K in steps of 5 K for T₀ ≥ 290 K, and from T₀ − 5 K to T₀ + 5 K in steps of 5 K for T₀ < 290 K. Moreover, considering the most land covers, the averaged emissivity ε varying from 0.90 to 1.0 with a step of 0.02 and the emissivity difference Δε from -0.025 to 0.015 with a step of 0.005, were used in our simulation [21].

Then for a given LST, in combination with the atmospheric parameters (τ_i, $R_{\mathit{\text{atm}}\_i}^{\uparrow }$, $R_{\mathit{\text{atm}}\_i}^{\downarrow }$), LST (T_s) and LSE (ε_i), the channel brightness temperature T_i at the TOA can be determined according to Eq. (1) with the inverse of Planck's law. At this stage, the T_s is directly related to the TOA measured brightness temperatures T_i and T_j. The coefficients a₀ − a₆ in Eq. (3) can be obtained through statistical regression method. In total, for the TIGR2002 database and the six standard MODTRAN 4 atmospheres, 261738 different situations were obtained for each VZA.

3. Results and Analysis

3.1. GSW algorithm coefficients

In order to determine the coefficients a₀ − a₆ in Eq. (3), Wan and Dozier (1996) [21] divided the averaged emissivity, atmospheric WVC and atmospheric surface temperature (T₀) into several tractable sub-ranges for improving the fitting accuracy. Taking into account the fact that the S-VISSR sensor onboard FY-2C has no atmospheric sounding channels, the atmospheric surface temperature is not simultaneously available, and thus it will be substituted in this work for the determination of the coefficients in Eq. (3) by the approximate Land Surface Temperature (LST).

For different values of the numerical experiments, in order to improve the accuracy of the retrieval LST, for each VZA as done in [21], the averaged emissivity was divided into two groups: one varies from 0.90 to 0.96 and the other ranges from 0.94 to 1.0. The WVC was divided into six sub-ranges with an overlap of 0.5 g/cm²: [0, 1.5], [1.0, 2.5], [2.0, 3.5], [3.0, 4.5], [4.0, 5.5], and [5.0, 6.5] g/cm². The LST, T_s, was divided into five sub-ranges with an overlap of 5 K: T_s ≤ 280 K, 275 ≤ T_s ≤ 295 K, 290 ≤ T_s ≤ 310 K, 305 ≤ T_s ≤ 325 K, T_s ≥ 320 K. Then, the coefficients a₀ − a₆ in Eq. (3) can be obtained through statistical regressions method for each VZA and each sub-range.

As an example, Figure 2 displays the coefficients of the GSW algorithm as functions of the secant VZA for the sub-range with WVC from 1.0 g/cm² to 2.5 g/cm², and LST varying from 290 K to 310 K for the two emissivity groups. As shown in this figure, the coefficients a₀ − a₆ for other VZAs can be linearly interpolated in function of the secant VZA. Similar results are obtained for the other subranges.

3.2. Estimation of LST

Figure 3 shows, respectively, the histogram of the difference between the actual T_s and the T_s estimated using GSW algorithm with the coefficients corresponding to the sub-range WVC ∈ [1.0, 2.5], and T_s ∈ [290K, 310K] for two different emissivity groups and VZA=0°. The Root Mean Square Errors (RMSEs) between the actual and estimated T_s is 0.37 K for the emissivity group ε ∈ [0.94, 1.0], and 0.48 K for the other emissivity group ε ∈ [0.90, 0.96]. Similar results were obtained for the other VZAs.

In addition, Figure 4 gives the RMSEs between the actual and estimated T_s as functions of the secant VZA for the two emissivity groups with different sub-ranges. Taking into account that, in reality, the lower LST is usually accompanied with much less WVC, as shown in figure 1, Therefore, for the LST less than 280 K, the maximum WVC is 2.5 g/cm², while for the LST between 275 K and 295 K, the maximum WVC is 5.5 g/cm².

From figure 4, one can see that the RMSEs increase with the increase of the VZA. The RMSEs are less than 1 K for all sub-ranges with the VZA less than 30°, or for all sub-ranges with the VZA less than 60° and the WVC less than 3.5 g/cm². The RMSEs increase dramatically with the increase of the VZA when the WVC larger than 3.0 g/cm², with the maximum RMSE of 2.7 K for the sub-range ε ∈ [0.94, 1.0], WVC ∈ [5.0, 6.5], and T_s ∈ [305K, 325K], for VZA=60°.

It should be pointed out here that, in practice, the LST is estimated in two steps for actual satellite data. Firstly, approximate LSTs are estimated using Eq. (3) with the coefficients derived for the whole range of LST providing that the sub-ranges of emissivity and WVC are known, and then more accurate LSTs are estimated once again using Eq. (3), but with the coefficients a₀ − a₆ corresponding to the sub-range of LST which is determined according to the approximate LST obtained in the first step. Figure 4 also shows the RMSEs between the actual T_s and the T_s estimated with the coefficients obtained for the whole range of LST.

Keeping in mind that the GSW algorithm also requires LSE and WVC as model input, the following section will present the determination of these two parameters.

3.3. Determination of the LSEs

The LSEs in channels IR1 and IR2 of S-VISSR can be estimated from the LSEs in channels 31 (11 μm) and 32 (12 μm) of MODIS provided by the MODIS LST product MOD11B1 at 5 km resolution. To determine the emissivity relationship between S-VISSR channels and MODIS 31 and 32 channels, two spectral databases, one from the University of California Santa Barbara (UCSB) ( http://www.icess.ucsb.edu/modis/EMIS/html/em.html) and the other from the Johns Hopkins University (JHU) ( http://speclib.jpl.nasa.gov/), are used. The emissivities in the two split-window channels of MODIS (ε₃₁ and ε₃₂) and S-VISSR (ε_IR1 and ε_IR2) were calculated by the integrals of the spectral emissivity with the channel response functions over the spectral range of the channels. The channel response functions of the two split-window channels for MODIS and FY-2C are displayed respectively in figure 5.

A statistical relationship between MODIS channels and S-VISSR channels was established by a linear regression analysis. As a result, the emissivities in S-VISSR channels IR1 and IR2 are, respectively, related to the emissivities in MODIS channels 31 and 32 by Eq. (4) and (5).

$${\mathit{\varepsilon }}_{IR1}=-0.0611+1.0614{\mathit{\varepsilon }}_{31}$$

(4)

$${\mathit{\varepsilon }}_{IR2}=-0.0210+1.0199{\mathit{\varepsilon }}_{32}$$

(5)

Figure 6 shows the emissivities and linear regression results. Only the emissivities of soil, vegetation, water, and snow/ice in JHU and UCSB databases were included in this work. Some few deviated points in this figure are due to the fact that the spectral ranges of S-VISSR channels IR1 and IR2 are broader than those of MODIS channels 31 and 32 as shown in figure 5. However, as shown in figure 6, the results of the linear regression are good with the RMSEs within 0.002, which indicates that the emissivities in S-VISSR channels IR1 and IR2 can be directly derived from those in MODIS channels 31 and 32, respectively.

Alternatively, the emissivities of the S-VISSR IR1 and IR2 channels can be estimated either with the land surface classification as did by Sun and Pinker (2003) [13] or using the method developed by Jiang et al. (2006) [26] which combined mid-infrared and thermal infrared data of SEVIRI to retrieve LSE.

3.4. Determination of the atmospheric WVC

The MODIS total precipitable water product MOD05 provides the atmospheric column water vapor amounts, which can be used as the model input when the scanning times of the sensors MODIS and S-VISSR are close to each other. However, MODIS provides the instantaneous WVC only four times per day, which can not meet the need for the temporal resolutions (an hour) of S-VISSR onboard FY-2C. Since the atmospheric WVC changes with time, the method developed by Li et al. (2003) [27] can be used to determine the WVC from S-VISSR IR1 and IR2 data.

According to Li et al. (2003) [27], the atmospheric WVC can be derived by the use of the transmittance ratio of split-window channels,

$$\mathit{\text{WVC}}=c_1+c_2\times \frac{{\mathit{\text{τ}}}_j}{{\mathit{\text{τ}}}_i}$$

(6)

$$\begin{array}{cc}\text{with}& \frac{{\mathit{\text{τ}}}_j}{{\mathit{\text{τ}}}_i}=\frac{{\mathit{\varepsilon }}_i}{{\mathit{\varepsilon }}_j}{R}_{\mathit{\text{ji}}}\end{array}$$

(7)

$$\begin{array}{cc}\text{and}& R_{\mathit{\text{ji}}}=\frac{\sum _{k=1}^N(T_{i,k}-{\overline{T}}_i)(T_{j,k}-{\overline{T}}_j)}{\sum _{k=1}^N{(T_{i,k}-{\overline{T}}_i)}^2}\end{array}$$

(8)

where c₁ and c₂ are unknown coefficients, τ_i and τ_j are the atmospheric transmittances in the split-window channels i and j, the subscript k denotes pixel k, and the T̅_i and T̅_j are the TOA mean (or the median) channel brightness temperatures of the N neighboring pixels considered for channels i and j, respectively.

On the basis of the numerical results obtained in Section 2.2, coefficients c₁ and c₂ can be respectively derived as functions of secant VZA as

$$c_1=28.104-14.996/cos\left(\mathit{\text{VZA}}\right)+3.211/{cos}^2\left(\mathit{\text{VZA}}\right)$$

(9)

$$c_2=-28.056+14.954/cos\left(\mathit{\text{VZA}}\right)-3.206/{cos}^2\left(\mathit{\text{VZA}}\right)$$

(10)

Figure 7 shows the curve fits of the coefficients c₁, c₂ as functions of secant VZA. As noted, the fitting results are quit well with both R-squares equal to 0.999. In addition, with the actual WVC and the transmittance ratio of split-window channels IR1 and IR2 obtained in Section 2.2, the RMSE between the actual WVC and the WVC estimated using Eqs. (6), (9) and (10) is 0.17 g/cm², which indicates that the fitting results are good.

3.5. Sensitivity analysis

As Wan and Dozier (1996) [21] indicated that the errors of LST estimated by the GSW algorithm come mainly from the uncertainties of LSEs, atmospheric properties and the instrument noises. These three uncertainties of error are taken into account in this investigation.

3.5.1 Sensitivity analysis to instrumental noises (NEAT)

In order to see how significant the effect of the instrumental NEAT on the retrieval of LST, a Gaussian random distribution error of 0.1 K, 0.2 K and 0.5 K are, respectively added to the TOA brightness temperatures T_i and T_j in Eq. (3). Then we estimate the LST using GSW algorithm with the noised TOA brightness temperatures. As an example, compared the actual LST with the estimated LST for the sub-range: ε ∈ [0.94, 1.0], WVC ∈ [1.0, 2.5], and T_s ∈[290K, 310K], the RMSE is 0.38 K for NEΔT=0.1 K, 0.43 K for NEΔT=0.2 K, and 0.67 K for NEΔT=0.5 K. Compared the RMSE of 0.37 K for no instrumental noise, the accuracy of retrieval LST can be affected by 3% for NEΔT=0.1 K, by 16% for NEΔT=0.2 K, and by 81% for NEΔT=0.5 K.

3.5.2 Sensitivity analysis to LSEs

According to the Eq. (3), the sensitivity of the uncertainties in LSEs is mainly dependent on the terms (1−ε)/ε and Δε/(ε²), which can be written as

$$\mathit{\text{α}}=a_2\frac{T_i+T_j}{2}+a_5\frac{T_i-T_j}{2}$$

(11)

$$\beta =a_3\frac{T_i+T_j}{2}+a_6\frac{T_i-T_j}{2}$$

(12)

Two cases are considered in this investigation. One is the extremely dry atmospheric condition (WVC ∈ [0.0, 1.5]) and the other is the extremely wet atmospheric condition (WVC ∈ [5.0, 6.5]). With the regression coefficients and the T_i and T_j simulated in Section 2.2, using equations (11) and (12) we can obtain the variations of α and β.

Table 2. Statistics of the errors due to the uncertainties in LSEs for the sub-range ε ∈ [0.94, 1.0], T_s ∈[290K, 310K], WVC ∈ [0.0, 1.5] and the sub-range ε ∈ [0.94, 1.0], T_s ∈ [290K, 310K], WVC ∈ [5.0, 6.5], for VZA=0°.

Conditions	ε ∈ [0.94, 1.0], Ts ∈ [290K, 310K], VZA=0°
Water vapor content (g/cm2)	WVC ∈ [0.0, 1.5]		WVC ∈ [5.0, 6.5]
Variable	α	β	α	β
Range of Values (K)	[44.80, 61.23]	[-135.71,-121.05]	[11.57, 34.42]	[-70.13,-19.48]
Mean (K)	52.39	-127.60	23.29	-45.56
Standard deviation (K)	3.10	3.06	4.22	9.32

lists the variations of α and β for the sub-range: ε ∈[0.94, 1.0],T_s ∈[290K, 310K], WVC ∈ [0.0, 1.5] and the sub-range ε ∈ [0.94, 1.0], T_s ∈[290K, 310K], WVC ∈ [5.0, 6.5], for VZA=0°, respectively.

From table 2 one can see that the values of α and β in extremely dry atmospheric condition (WVC ∈ [0.0, 1.5]) are nearly two times as large as those of α and β in extremely wet atmospheric condition, (WVC ∈ [5.0, 6.5]), respectively. This means that the sensitivity of (1−ε)/ε and Δε/(ε²) to LST for wet atmospheric condition is decreased two times as that for dry atmospheric condition.

From Equation (3), the LST error δLST due to the uncertainty in (1−ε)/ε and Δε/(ε²) can be estimated by,

$$\delta \mathit{\text{LST}}=\sqrt{{\mathit{\text{α}}}^2\delta {(\frac{1-\mathit{\varepsilon }}{\mathit{\varepsilon }})}^2+{\beta }^2\delta {(\frac{\mathrm{\Delta }\mathit{\varepsilon }}{{\mathit{\varepsilon }}^2})}^2}$$

(13)

Assuming that the uncertainties of (1−ε)/ε and Δε/(ε²) are around 1%, the LST error is [1.3K, 1.5K] with the mean of 1.4 K for the dry atmosphere and [0.2K, 0.8K] with the mean of 0.5 K for the wet atmosphere.

3.5.3 Sensitivity analysis to the atmospheric WVC

It is well known that the WVC in the atmosphere is not easily determined from satellite data. In order to see how significant the effect of the uncertainty of the WVC on the retrieval of LST in GSW algorithm, the wrong sub-range selection of the WVC is investigated in our work. As mentioned above in Section 3.1, the WVC was divided into six sub-ranges with an overlap of 0.5 g/cm². The overlap WVC could be fallen into two adjacent sub-ranges. That is, it is included by two sub-ranges and corresponded to two pairs of coefficients a₀ − a₆. We aim to analyze the effect of the overlap WVC on the retrieval of LST.

Figure 8 gives an example of the uncertainty of the WVC. From figure 8 one can see that the overlap water vapor content WVC ∈ [1.0, 1.5] falling into two sub-ranges WVC ∈ [0.0, 1.5] and WVC ∈ [1.0, 2.5]. When we estimate the LST with the water vapor content WVC ∈ [1.0, 1.5] using the coefficients corresponding to the sub-range ε ∈ [0.94, 1.0], WVC ∈ [0.0, 1.5], and T_s ∈ [290K, 310K], the RMSE between the actual and the estimated T_s is 0.18 K, while using the coefficients corresponding to the sub-range ε ∈ [0.94, 1.0], WVC ∈ [1.0, 2.5], and T_s ∈ [290K, 310K], the RMSE is 0.43 K.

3.6. Intercomparison of different formulations of the split-window algorithms

It is well known that the LST retrieval from satellite observations has been ongoing for several decades. Many different formulations of the split-window algorithms have been proposed. They are somewhat similar in formulation and several of them are directly inspired from Becker and Li's (1990) [12] formulation. In order to perform the intercomparison with the recently proposed split-window algorithms, different formulations were used to estimate the LST with the same simulated FY-2C data in this work. Those formulations are listed in

Table 3. Different formulations of split-window algorithms in literatures, ε is the averaged emissivity in channesl i and j, and Δε is the difference between the two channels emissivities.

Authors	Formulations
Price, 1984 [8]	Ts = a0 + a1Ti + a2(Ti − Tj) + a3(Ti − Tj)(1 − ε) + a4TjΔε
Prata and Platt, 1991 [14]	$T_s=a_0+a_1\frac{T_i}{\mathit{\epsilon }}+a_2\frac{T_j}{\mathit{\epsilon }}$
Vidal, 1991 [15]	$T_s=a_0+a_1{T}_i+a_2(T_i-T_j)+a_3\frac{1-\mathit{\epsilon }}{\mathit{\epsilon }}+a_4\frac{\mathrm{\Delta }\mathit{\epsilon }}{\mathit{\epsilon }}$
Ulivieri et al., 1992 [16]	Ts = a0 + a1Ti + a2(Ti − Tj) + a3(1 − ε) + a4Δε
Sobrino et al., 1993 [17]	Ts = a0 + a1Ti + a2(Ti − Tj) + a3(Ti − Tj)2 + a4(1 − ε) + a5Δε
Sobrino et al., 1994 [18]	$T_s=a_0+a_1{T}_i+a_2(T_i-T_j)+a_3\mathit{\epsilon }+a_4\frac{\mathrm{\Delta }\mathit{\epsilon }}{\mathit{\epsilon }}$
Coll et al., 1997 [19]	Ts = Ti+ a0 + a1(Ti − Tj) + a2(Ti − Tj)2 + a3(1 − ε) + a4Δε

:

In addition, Becker and Li (1995) [20] further modified their split-window algorithm (Becker and Li, 1990) [12] by adding atmospheric water vapor correction as

$$T_s=A_0+P\frac{T_i+T_j}{2}+M\frac{T_i-T_j}{2}$$

(14)

$$\begin{array}{ll}\text{with}\hfill & A_0=a_0+a_{1}w\hfill \\ \hfill & P=a_2+(a_3+a_{4}w\cos \mathit{\theta })(1-\mathit{\varepsilon })-(a_5+a_{6}w)\mathrm{\Delta }\mathit{\varepsilon }\hfill \\ \hfill & M=a_7+a_{8}w+(a_9+a_{10}w)(1-\mathit{\varepsilon })-(a_{11}+a_{12}w)\mathrm{\Delta }\mathit{\varepsilon }\hfill \end{array}$$

where ε = (ε_i + ε_j)/2 and Δε = ε_i − ε_j, w is the total precipitable water amount, and θ is the Viewing Zenith Angle (VZA).

In order to make the intercomparsion more reasonable, the coefficients from the above equations have been recalculated using the same simulated FY-2C data within the same sub-ranges in Section 3.1. As an example,

Table 4. RMSEs between the actual T_s and the T_s estimated using different formulations of the split-window algorithms for the sub-range ε ∈ [0.94, 1.0], WVC ∈ [1.0, 2.5], and T_s ∈[290K, 310K].

RMSE (K)		Authors
	VZA(°)	GSW	Price84	Prata91	Vidal91	Ulivieri92	Sobrino93	Sobrino94	Coll97	BL95
	0	0.37	0.73	1.15	0.38	0.38	0.37	0.38	0.38	0.22
	33.56	0.41	0.74	1.26	0.43	0.42	0.42	0.42	0.43	0.25
	44.42	0.46	0.74	1.35	0.48	0.47	0.47	0.47	0.47	0.28
	51.32	0.52	0.75	1.43	0.53	0.53	0.51	0.53	0.52	0.32
	56.25	0.57	0.77	1.49	0.58	0.58	0.57	0.58	0.57	0.36
	60	0.63	0.80	1.54	0.64	0.64	0.62	0.64	0.62	0.41

depicts the RMSEs between the actual and the estimated T_s versus the secant VZA for the sub-range: ε ∈ [0.94, 1.0], WVC ∈ [1.0, 2.5], and T_s ∈ [290K, 310K]. From this table, one can see that the RMSEs increase with the increase of the VZA for all algorithms. In addition, except for the algorithms proposed by Price (1984) [8], and Prata and Platt (1991) [14], the T_s estimated using the other algorithms are comparable, which indicates that the split-window algorithm can be successfully applied to the LST retrievals from FY-2C data. It should be noted that the RMSE values in Table 4 will be larger, especially for BL95, in considering the sensitivity to WVC errors.

4. Application to actual FY-2C satellite data

The objective of the present work is to estimate the LST from Chinese first operational geostationary meteorological satellite FengYun-2C (FY-2C) data for cloud-free skies. Figure 9 gives an example of the retrieval LST around Beijing in China during FY-2C satellite scanning on May 15, 2006 at 11:00 local time. The model inputs are the TOA brightness temperatures LSTs, VZA, LSEs, and WVC. The TOA brightness temperatures LSTs and VZA are directly extracted from the FY-2C satellite data. The LSEs are derived from the emissivities in MODIS channels 31 and 32 provided by MODIS/Terra LST product MOD11B1, and the WVC are obtained from MODIS total precipitable water product MOD05. Symbols A, B, and C located in red, green and baby blue colored areas in figure 9 represent bare soil, cultivated surface and sea surface, respectively.

In addition,

Table 5. Description of symbols A, B and C in figure 9.

	A (red)	B (green)	C (baby blue)
Longitude (°)	120.06 E	116.15 E	122.75 E
Latitude (°)	43.70 N	33.84 N	38.47 N
VZA (°)	53.44	41.96	49.14
WVC (g/cm2)	0.868	1.465	1.217
εIR1	0.944	0.962	0.986
εIR2	0.946	0.966	0.99
TIR1 (K)	309.42	295.24	281.95
TIR2 (K)	307.32	294.58	282.20
Ts (K)	318.35	299.74	286.47

lists the values of the VZA, WVC, LSE, TOA brightness temperature, and resultant T_s for one representative pixel in each red, green, and baby blue colored areas in figure 9.

It should be pointed out here that the LST estimated from the FY-2C satellite data has not been validated with in situ measurements since there are no in situ measurements available. In addition, due to the extreme difficulty or impossibility to get the LST at ground level representative at 5km*5km, we will try to cross validate LST derived from FY-2C data in the future with the well validated LST product provided by MODIS data.

5. Conclusions

In this paper, we have addressed the retrieval of the Land Surface Temperature (LST) from the Chinese first operational geostationary meteorological satellite FengYun-2C (FY-2C) data in two thermal infrared channels IR1 (10.3-11.3 μm) and IR2 (11.5-12.5 μm), using the Generalized Split-Window (GSW) algorithm proposed by Wan and Dozier (1996) [21].

Taking into account the fact that the S-VISSR sensor onboard FY-2C has no atmospheric sounding channels, the coefficients in the GSW algorithm were derived by dividing the ranges of the mean emissivity, the atmospheric Water Vapor Content (WVC), and the LST into tractable sub-ranges, and were recalculated using a statistical regression method from the numerical values simulated with an accurate atmospheric radiative transfer model MODTRAN 4 over a wide range of the atmospheric and surface conditions. The simulation analysis showed that the LST could be estimated by the GSW algorithm with the Root Mean Square Error (RMSE) less than 1 K for the sub-ranges with the Viewing Zenith Angle (VZA) less than 30° or for the sub-ranges with VZA less than 60° and the atmospheric WVC less than 3.5 g/cm² provided that the Land Surface Emissivities (LSEs) are known.

As the GSW algorithm requires WVC and LSE as model input, the MODIS total precipitable water product MOD05 providing the atmospheric column water vapor amounts, was used to obtain the WVC when the scanning times of the sensors MODIS and S-VISSR are close to each other. As for the other scanning times of S-VISSR, the atmospheric WVC can be determined using the method developed by Li et al. (2003) [27]. As for LSE, the MODIS/Terra LST product MOD11B1 providing the LSEs with 5 km resolution for the thermal infrared channels 31 and 32, was used to derive the LSEs in S-VISSR channels IR1 and IR2, respectively.

In addition, the sensitivity and error analyses in term of the uncertainty of the LSE and WVC as well as the instrumental noise were also performed in this work. The results show that the accuracy of retrieval LST can be affected by 3% for NEAT=0.1 K, by 16% for NEAT=0.2 K, and by 81% for NEAT=0.5 K for the sub-range ε ∈ [0.94, 1.0], WVC ∈ [1.0, 2.5], and T_s ∈ [290K, 310K]; given the uncertainties of (1−ε)/ε and Δε/(ε²) around 1%, the LST error is [1.3K, 1.5K] with the mean of 1.4 K for the dry atmosphere and [0.2K, 0.8K] with the mean of 0.5 K for the wet atmosphere; and the effect of the uncertainty of the WVC on the retrieval LST could be around 0.3 K.

Moreover, in order to compare the different formulations of the split-window algorithm, several split-window algorithms were used to estimate the LST with the same simulated FY-2C data. The result of the intercomparsion showed that most of the algorithms give comparable results, which indicates that the split-window algorithm can be successfully applied to the LST retrievals from FY-2C data.