## Materials and Methods
### Method  
#### 2.2.1 A Brief Description of SEBS  
The surface energy balance model (SEBS) is a single source model and takes latent heat flux (\(\lambda\)ET) as the residual of the surface energy balance. It is proposed for the estimation of atmospheric turbulent fluxes and evaporative fraction using satellite earth observation data and meteorological information at proper scales [10]. The surface energy balance is normally written as:  
\[\lambda\mathrm{ET}=\mathrm{R_{n}}-\mathrm{G}-\mathrm{H} \tag{1}\]  
where \(\mathrm{R_{n}}\), \(\mathrm{G}\), \(\mathrm{H}\), and \(\lambda\)ET are the net radiation flux, soil surface heat flux, sensible heat flux, and latent heat flux, respectively. The units of these variables are W m\({}^{-2}\). [PERSON] et al. (2001) and [PERSON] (2002) detailed a set of equations for the estimation of the land surface physical parameters and variables, such as albedo, emissivity, vegetation coverage, land surface temperature, etc. [10; 49].  
Sensible heat flux is derived from the similarity theory along with a dynamic roughness height formulation for the heat transfer. In the atmospheric surface layer (ASL), the similarity relationship for the profiles of the mean wind speed (u) and the mean temperature (\(\mathrm{T_{0}}-\mathrm{T_{a}}\)) are usually described as:  
\[\mathrm{u}=\frac{\mathrm{u_{*}}}{\mathrm{k}}\left[\mathrm{ln}\left(\frac{ \mathrm{z}-\mathrm{d_{0}}}{\mathrm{z_{0m}}}\right)-\Psi_{\mathrm{m}}\left( \frac{\mathrm{z}-\mathrm{d_{0}}}{\mathrm{L}}\right)+\Psi_{\mathrm{m}}\left( \frac{\mathrm{z_{0m}}}{\mathrm{L}}\right)\right] \tag{2}\]  
\[\mathrm{T_{0}}-\mathrm{T_{a}}=\frac{\mathrm{H}}{\mathrm{ku_{*}}\mathrm{\sigma C _{p}}}\left[\mathrm{ln}\left(\frac{\mathrm{z}-\mathrm{d_{0}}}{\mathrm{z_{0h}}} \right)-\Psi_{\mathrm{h}}\left(\frac{\mathrm{z}-\mathrm{d_{0}}}{\mathrm{L}} \right)+\Psi_{\mathrm{h}}\left(\frac{\mathrm{z_{0h}}}{\mathrm{L}}\right)\right] \tag{3}\]  
\[\mathrm{L}=\frac{\mathrm{\sigma C_{p}u_{*}^{3}\mathrm{\theta}_{v}}}{\mathrm{ kgH}} \tag{4}\]  
where u is the mean wind speed; u* is the friction velocity (m s\({}^{-1}\)); k is the von [PERSON] constant (0.4); z is the height above the land surface where the meteorological observations were made (m); C\({}_{p}\) is the specific heat of air at constant pressure (J kg\({}^{-1}\) K\({}^{-1}\)); d\({}_{0}\) is the zero plane displacement height (m); and z\({}_{0h}\) and z\({}_{0m}\) are the surface roughness heights for heat and momentum transport (m); \(\Psi_{\mathrm{h}}\) and \(\Psi_{\mathrm{m}}\) are the stability correction functions for heat and momentum transport; g is the acceleration due to gravity (m s\({}^{-2}\)); \(\mathrm{\theta}_{v}\) is the virtual temperature (K); L is the Obukhov length (m); T\({}_{0}\) and T\({}_{a}\) are the temperature of the land surface and air, respectively (K); and \(\mathrm{\theta}\) is the density of air (kg m\({}^{-3}\)). More details about the SEBS model can be found in [PERSON] (2002) [10].  
\begin{table}
\begin{tabular}{c c c} \hline
**Satellite** & **Total Number** & **Day of Year (DOY)** \\ \hline HJ-1B CCD/IRS & 33 & 91, 95, 99, 103, 111, 119, 124, 129, 132, 136, 139, 143, 151, 158, 168, 176, 184,188, 192, 200, 208, 212, 216, 220, 225, 233, 237, 241, 249, 257, 263, 272, 274 \\ \hline HJ-1A CCD & 18 & 105, 117, 121, 134, 138, 149, 190, 202, 206, 211, 215, 223, 235, 255, 256, 260, 275, 276 \\ \hline \end{tabular}
\end{table}
Table 3: Satellite images for this study.