**1. Introduction**

Bare soil albedo has been widely used in climate models and remote sensing estimates of surface energy balance as one key component of the surface albedo by determining the amount of solar radiation reflected and absorbed at the Earth's surface [1,2]. Bare soil albedo has also been widely used in ecological research as a controlling factor in algorithms for deriving leaf area index (LAI) and fraction of Photosynthesis Active Radiation (fPAR) from satellite observations, which requires fine resolution data for satellite applications, e.g., [3,4]. A limited number of prescribed bare soil albedo values are assigned based on global soil color maps [5–7]. However, soil reflectivity varies both temporally and spatially. Besides soil color, bare soil albedo is also a function of moisture content [8,9], organic

matter [10], texture/roughness [11], and other surface characteristics. Oversimplified soil albedo parameterization has been reported to introduce uncertainties both in climate modeling [12,13] and satellite LAI/fPAR products [14–17]. Significant differences in soil albedo were found in comparisons of land surface models and satellite products [12], which lead to substantially different estimations of surface energy balance and hydrologic budget partitioning [18].

Efforts have been made towards generating global or regional soil albedo datasets that are independent of coarse resolution soil color maps. Zhou et al. [19] analyzed the Moderate Resolution Imaging Spectroradiometer (MODIS) 1 km albedo products over desert areas using principle component analysis and found the extracted spatial pattern could improve the soil albedo parameterization in climate models. In a recent study, a method has been proposed to estimate soil albedo by removing impacts of solar zenith angle and soil moisture empirically from MODIS albedo products [20]. In their method, coarse resolution (~15–100 km) soil moisture data from the North American and Global Land Data Assimilation System (LDAS) were used.

To develop a bare soil albedo dataset over densely vegetated area and without the support of reanalysis data, a method has been developed based on an empirical relationship between broadband albedos and the Normalized Difference Vegetation Index (NDVI) [21]. In their method, broadband albedo of bare soil over densely vegetated area was predicted through extrapolation of linear logarithmic relationship between albedo and NDVI. It was proposed that bare soil albedos were estimated at NDVI = 0.09 globally, based on the empirical relationship. However, we found that this empirical relationship could generate larger values for visible albedo than near infrared albedo due to lack of training data for extrapolation purposes. In addition, previous studies have proved that NDVI may not be a good quantitative indicator of surfaces with sparse vegetation coverage because of mutual shadow effects on surface anisotropy [22,23].

Pisek and Chen [16] proposed a method using multi-angular satellite observations to map background spectral reflectance in forested pixels and found significant variations between coniferous and deciduous forests, particularly in the near infrared wavelengths.

In some recent studies, MODIS LAI and fPAR products were introduced to calculate vegetation fraction used in a linear regression to estimate soil albedo and the difference of vegetation and soil albedos based on the assumption that these two variables were invariant within a certain period [24,25]. This was later improved by using a Kalman filter to generate dynamic albedo on a daily basis [26]. However, MODIS LAI/fPAR products were derived assuming a prescribed bare soil albedo based on a soil type map, and these products were believed to have lower reliability during the vegetation growing season [14,15].

Existing bare soil albedo datasets are subject to several limitations. First, most suffer from uncertainties in ancillary input products used in the albedo retrieval algorithm due to, for example residual cloud contamination, inaccurate soil maps, or scale differences between model inputs and the retrieval scale. Second, most of the existing global bare soil albedo datasets are only available at a spatial resolution coarser than 5 km, which cannot satisfy the increasing demand for high resolution soil parameterizations, especially in agricultural and ecological applications, e.g., [27]. Third, validation of these datasets has been generally limited to inter-comparison against model-simulated results.

In addition to mapping the broadband albedo for bare soil, there is also a need to generate spatially dynamic background spectral reflectance/albedo to improve the LAI/fPAR estimates from remote sensing data [16]. Thus, it is important to develop an approach that can generate both spectral and broadband albedos at a fine spatial resolution (e.g., 30–500 m) to satisfy the needs of climate modeling and ecosystem monitoring purposes. Significant impacts of soil moisture content on soil reflectivity have been reported based on laboratory measurements [28,29], ground measurements [8,9,30], and satellite products [31–33]. However, few studies have demonstrated the relationship over a large spatial domain, which is critical for land surface energy balance and hydrological modeling purposes.

The concept of a "soil line", a linear relationship between red and near infrared (NIR) reflectances typically observed over bare soils, has been widely used to discriminate vegetation from soil using spectral information [34–39]. The soil line has been commonly used to develop the vegetation indices, such as the simple ratio (SR), NDVI, Enhanced Vegetation Index (EVI), and Soil-Adjusted Vegetation Index (SAVI), to identify dense vegetation. However, this concept had mostly been applied to extracting information about the vegetation canopy rather than the understory and soil.

The purpose of this study is to build a 500 m bare soil albedo dataset over the contiguous United States (CONUS) on a pixel-basis from multi-year MODIS data based on the soil line feature and to explore the relationship between bare soil albedo and other surface properties such as soil moisture, soil type, and vegetation type. A description of the data and methodology is given in Section 2. Comparison results against Landsat data are presented in Section 3 and are followed by the evaluation of soil albedo with regards to soil moisture content, soil type, and land cover type.

### **2. Materials and Methods**

#### *2.1. MODIS Albedo Anisotropy Products*

The MODIS albedo and bidirectional reflectance distribution function (BRDF) products (MCD43A) [40] are available at a 500 m resolution globally using a 16-day temporal acquisition window. Of the available albedo anisotropy products, this study primarily used three datasets: Spectral/broadband albedos, nadir view corrected surface spectral reflectance, and quality control (QC) flags (overall accuracy and snow flag). Two types of albedos were included in the MODIS products: Black-sky albedo (BSA), also called directional-hemispherical albedo, and white-sky albedo (WSA), also called bi-hemispherical albedo. Datasets covering CONUS were chosen for the 13-year period from 2000 to 2012. Information of the datasets used in this study is summarized in Table 1.

To assist in the removal of possible vegetation, water, snow, and residual cloud shadow contaminated albedo values, the NDVI and normalized difference water index (NDWI) [41] were used, calculated from nadir BRDF-adjusted reflectances (NBAR) for the spectral bands (Equations (1) and (2)).

$$NDVI = \frac{\rho\_{b2} - \rho\_{b1}}{\rho\_{b2} + \rho\_{b1}},\tag{1}$$

$$NDWI = \frac{\rho\_{b2} - \rho\_{b5}}{\rho\_{b2} + \rho\_{b5}},\tag{2}$$

where *ρb*1, *ρb*2, and *ρb*5 are the spectral reflectances for MODIS band 1 (620–670 nm), band 2 (841–876 nm), and band 5 (1230–1250 nm), respectively.


**Table 1.** Information of the datasets used in this study.

## *2.2. Soil Type Map*

Current climate and ecological modeling applications generally use maps of soil type to assign albedo values to certain locations [42] because soil type is believed to be the dominant factor controlling soil reflectivity. The Natural Resources Conservation Service (NRCS) in the U.S. Department of Agriculture (USDA) provides a general soil taxonomy map for the CONUS (Figure 1). In the soil taxonomy map, a dominant soil type is given for each pixel at 2 arcmin resolution (~4 km) from the 12 soil types, including: Alfisols, Andisols, Aridisols, Entisols, Gelisols, Histosols, Inceptisols, Mollisols, Oxisols, Spodosols, Ultisols, and Vertisols [43]. This soil type map was used in the soil albedo derivation methodology described in the following sections.

**Figure 1.** Dominant soil type map over the contiguous United States (CONUS) extracted from U.S. Department of Agriculture (USDA) soil survey data.

#### *2.3. Using the Soil Line to Detect Bare Soil*

In the solar shortwave range, bare soil surfaces normally have small reflectivity in shorter wavelength, with reflectance gradually increasing with wavelength [44,45]. In contrast, a vegetation canopy has very strong absorption in the visible spectrum and back scattering in the near infrared spectrum. The soil line is one of the key and stable spectral signatures of soil and has been examined in many experiments [34–36]. The soil line describes the linear feature (the "envelope") of surface reflectivity in multi-band space over a landscape of a given soil type. For example, the soil line is the lower envelope in the red-NIR space and has been commonly used to identify areas with dense vegetation. However, in practice, the red-NIR soil line can exhibit significant variation because both residual vegetation (leaf litter) and soil moisture may affect the NIR reflectivity greatly. This can cause problems for deriving a universal threshold to separate soil from vegetation, especially when sparse vegetation cover is not available for certain surfaces. In contrast, the green-red based soil line is very stable [35,46]. To verify the green-red soil line feature, surface spectra from Advanced Spaceborne Thermal Emission and Reflection Radiometer (ASTER) and US Geological Survey (USGS) spectral libraries [44,45] were collected and used to identify soil line features with different combinations of spectral albedo and vegetation/soil related indices including NDVI, EVI, SR, NDWI, and Visible Atmospherically Resistant Index (VARI). Of all combinations tested, the green-red band combination could detect soil line with the highest R<sup>2</sup> of 0.92, while the others ranged from 0.6 to 0.8.

In this study, thirteen years of MODIS albedo/BRDF data (2000–2012) were used to identify bare soil albedo characteristics over the CONUS using the following procedure. First, the soil line was generated for each of the 12 major soil types in the NRCS classification using MODIS data in 2005. To reduce uncertainties and minimize effects of vegetation and snow, only high quality snow-free albedo values (based on the QC flag in MODIS albedo product) collected between November and March were used in the soil line generation. MODIS NDVI and NDWI products were used to further exclude possible vegetation, snow/ice, water, and residual cloud/shadow pixels. Once the soil line was detected, the second step was to calculate statistics describing the distance of the bare soil albedo from the soil line for each pixel over the whole period 2000–2012. Considering the accuracy of the estimated soil line and the uncertainty in MODIS data products, the soil albedos were considered as candidates if their distance to the soil line was smaller than 20% of the magnitude of their albedo

values. Our sensitivity test showed that the 20% threshold did not introduce any significant difference in the soil albedo climatology results, and, at the same time, it significantly increased the number of samples that were used in the calculation. The bare soil albedos (both spectral and broadband) were generated at a 16-day interval. The third step was to calculate the mean and standard deviation (SDEV) of the 16-day bare soil albedos over the entire thirteen years for each location. Figure 2 illustrates the procedure used to generate the multiyear mean bare soil albedos from the MODIS datasets. In the final bare soil albedo map, the soil albedo represents the average state of the soil condition, regardless of the differences in moisture content and organic matter. The SDEV maps contain information regarding impacts of variation in soil moisture, organic matter, and residual vegetation on the apparent soil reflectivity.

**Figure 2.** Flowchart for mapping bare soil albedo from multiyear Moderate Resolution Imaging Spectroradiometer (MODIS) data based on soil line.

### **3. Results and Discussion**

#### *3.1. Charateristics of Soil Lines Derived from MODIS Albedo*

It has been demonstrated that the visible spectral space is useful in estimating vegetation fraction and indicating crop development stages tested at multiple crop sites with various soil backgrounds [35,46]. Based on field data, the green-red soil line feature has been proven to be a robust method for separating bare soil and vegetated surface conditions [35]. However, this feature has not ye<sup>t</sup> been well documented using long-term satellite data. Figure 3 shows the soil line feature in green-red space from MODIS albedo samples over different land cover types based on MODIS land cover product during 2000–2012 using red and green bands.

In both crop and forest MODIS-derived samples, there was an obvious linear-line feature with relatively high green and red reflectance values in the spectral space (black line shown in Figure 3), which was in accordance with in-situ observations [46]. Based on the observations, this line was occupied mostly by samples in winter when vegetation had not sprouted. Such samples tend to be

bare soil samples with low NDVI and positive NDWI. The variations in surface reflectivity at this stage were likely due to changes of soil moisture [28].

There are several reasons why data obtained in winter are preferable for deriving the soil line, as demonstrated in Figure 3. First, the effect of vegetation is minimized during the fall and winter dormant months. As vegetation grows such as in spring, surface albedos for green and red bands rapidly decrease due to the strong absorption by chlorophyll pigment in leaves, while the red band has a larger decrease rate because chlorophyll absorbance coefficient is much higher in red than in green [47]. Samples were moving downwards in spring when vegetation began to grow and ended up by a short "vegetation line" with red reflectance almost invariant occupied mostly by samples in summer when vegetation density was quite high. During the fall at the onset of vegetation senescence, green and red reflectance increased due to less absorption by the degraded chlorophyll pigments. As such, the samples at this stage were moving upwards from "vegetation line" back to "soil line" (red points in Figure 3). Thus, we can see from Figure 3 that albedos in winter are on the soil line and those in summer are on the vegetation line. For spring and fall, the albedo values lie between these extremes due to partial (sub-pixel) vegetation cover.

**Figure 3.** MODIS white-sky albedo (or diffuse reflectance) for the red and green bands over crop and forest samples in MODIS tile h11v04 during 2000–2012. The left panel shows the albedo values for one pixel for the time period; the right panel shows albedo values for the pixels in the 5-by-5 surrounding spatial window with the same land cover type to that in the left panel.

Second, soil albedo varies with soil moisture. During drier seasons (fall and winter) soil albedo tends to have a higher value, while during wetter seasons (spring and summer), it decreases as soil moisture increases. As soil moisture is usually small in winter (excluding the snow albedo), a small increase/decrease in moisture can cause large decrease/increase in albedo. Thus, a large range of soil albedo would produce robust soil line estimation.

Therefore, the soil line features were estimated by fitting the albedo values obtained in winter after excluding the data with large NDVI (>0.3) and/or negative NDWI to reduce the impacts of dense vegetation, clouds, and snow/ice.

The scatter plots in the left panel in Figure 3 are based on data at a single 500 m pixel; the plots in the right panel include data from the 5-by-5 surrounding pixels with the same land cover type. Because soil albedo varies both seasonally and inter-annually as the averaging area increases, including more surrounding pixels of the same land cover type as shown in the right panel, the slope of the soil line does not change much, but the R<sup>2</sup> increases. This procedure was tested over other locations with different land cover types, yielding results similar to those presented in Figure 3.

Soil line characteristics estimated from MODIS data from 2005 are listed in Table 2. The variability in these soil lines indicates that a global unified soil line may not be good enough to extract bare soil albedo. Most of the soil line estimations have an R<sup>2</sup> greater than 0.9 except for Alfisols, which demonstrates that the soil type information can support soil line estimations and other soil properties (e.g., soil moisture, organic matter, and surface texture/roughness) may have a secondary impact to the soil line [34].


**Table 2.** Parameters of soil lines estimated for the major soil types over the CONUS

\*Statisticsarebased on 95%confidencelevel.

Following the procedure described in Figure 2, bare soil albedo over the CONUS was first generated on a 16-day interval including black-sky (direct) and white-sky (diffuse) albedos for the seven spectral bands and three broadbands, and then aggregated temporally to generate the climatological mean and SDEV for each of the bands. Statistics for broadband white-sky albedos are presented in Figure 4. Based on visual comparison, a general agreemen<sup>t</sup> can be reached in terms of magnitude and spatial pattern between the bare soil shortwave albedo map generated in this study and the data aggregated from MODIS data during 2001–2010 in a recent study [26]. The shortwave albedo for soil is lower in the East and Northwest CONUS (around 0.15~0.18) where dense vegetation is located with a wetter climate and higher in the central and Southwest CONUS from 0.20 to more than 0.40 where much of the land is covered with crops, grass, and bare soil with a drier climate. A more detailed spatial pattern in the soil albedo over the CONUS is provided in this study.

**Figure 4.** *Cont.*

**Figure 4.** Bare soil albedo over the CONUS: Total shortwave (0.3–5.0 μm) mean value (**a**) and standard deviation (SDEV) (**b**); visible (0.3–0.7 μm) mean value (**c**) and SDEV (**d**); and near infrared (NIR) (0.7–5.0 μm) mean value (**e**) and SDEV (**f**).

#### *3.2. Validation of MODIS Bare Soil Albedo*

As bare soil albedo ground measurements are not widely available, validation of the bare soil albedo extracted from MODIS data at 500 m resolution is difficult. In previous studies, bare soil albedo was either directly compared with model inputs or indirectly validated against MODIS albedo products using pure vegetation albedo and vegetation fraction as inputs to calculate soil/vegetation mosaic albedos. In this study, we proposed an approach using finer resolution satellite data to help verify the 500 m MODIS-based bare soil albedo estimations.

Landsat data are available from the USGS at 16-day intervals and at a spatial resolution of 30 m. Though it is usually difficult to find pure bare soil pixels at the MODIS resolution, they are considerably easier to identify at the Landsat resolution. The finer resolution offers a unique capability to observe the bare soil directly, which is otherwise mixed with vegetation at MODIS resolution. In this study, it was assumed that if the Landsat pixels that belong to a MODIS pixel with a 500m-by-500m nominal spatial coverage can be identified as bare soil, the averaged soil albedo value of the Landsat pixels will represent the bare soil albedo for the MODIS pixel. The Landsat shortwave broadband albedo was estimated following the procedure described by He et al. [48] for the atmospheric correction and narrow-to-broadband conversion. Clouds in Landsat data were screened using the Landsat Ecosystem Disturbance Adaptive Processing System (LEDAPS) tool [49].

**Figure 5.** Comparison of 16-day bare soil shortwave albedos derived from MODIS data with estimates from Landsat data.

Potential soil pixels were extracted from the Landsat datasets based on land cover class designated in the National Land Cover Database 2006 (NLCD2006). Only pixels classified as sparse vegetation–including developed, barren, and shrubland–were used [50]. Both NDVI and NDWI were calculated for each Landsat scene to exclude cloud/shadow, water, snow, and vegetation pixels, similar to the MODIS data processing discussed in previous sections. In this study, we used the Landsat scenes (path 042, row 034) centered at 119.0◦W, 37.5◦N for validation, which have a variety of land cover types, including forest, grassland, and cropland. There are four major soil types in this region, including Alfisols, Aridisols, Entisols, and Ultisols. All the available Landsat 5 TM scenes for the period 2005–2007 with nominal cloud coverage less than 30% were used. As the NLCD class and vegetation indices thresholds (NDVI<0.3 same as in Section 3.1) were applied to the Landsat data, it was assumed that the generated Landsat soil albedo can represent the bare soil surfaces with/without vegetation cover in a larger area, e.g., a MODIS pixel. As demonstrated in Figure 5, a general agreemen<sup>t</sup> can be found for bare soil shortwave black-sky albedos derived from MODIS and Landsat data with a bias of 0.003, a root-mean-square-error (RMSE) of 0.036, and an R<sup>2</sup> of 0.316. There are several possible reasons for the differences between these two datasets found in the comparison: Landsat albedo estimations are instantaneous and thus more sensitive to soil moisture changes; Landsat and MODIS surface reflectance may not fit to 1-to-1 line exactly due to the differences in sensor characteristics and data processing; and Landsat pixels may not match MODIS pixels exactly due to the different registration accuracy and adjacency effects in the coarser resolution data.

#### *3.3. Impacts of Soil Moisture Content on Soil Albedo*

The water content in the top layer of soil is believed to have grea<sup>t</sup> impacts on the soil albedo. Previous studies have tried to establish the relationship between soil moisture content and soil reflectivity based on various datasets. Some studies reported that the relationship was linear, while others found an exponential equation provided a better fit (Equation (3)):

$$\mathfrak{a} = A \exp(-B\theta) + \mathbb{C},\tag{3}$$

where *α* is soil albedo and *θ* is soil moisture. *A*, *B*, and *C* are regression coefficients.

Gascoin et al. [9] found that the best fit coefficients (A= 0.31, B =12.7 and C =0.15) with an RMSE of 0.030 using various soil samples from field measurements, and Wang et al. [30] reported a lower value for the B coefficient (B = 3.52, clay soil type). Gascoin et al. [9] also pointed it out that the parameters must be carefully examined before application to other regions.

In this study, a relationship between bare soil albedo and soil moisture was derived using remote sensing data over a large spatial domain. White-sky albedo was used exclusively to minimize the solar zenith impacts on albedo data. In addition, the Advanced Microwave Scanning Radiometer-Earth Observing System (AMSR-E) Level 3 daily soil moisture products were used as estimates of soil moisture in the top ~1 cm of soil averaged over the retrieval footprint [51,52]. The 16-day averaged soil moisture values were generated from the daily AMSR-E products to match the temporal resolution of MODIS albedo during 2002–2011 (due to demise of AMSR-E in 2011) over the CONUS. The MODIS soil albedo data were rescaled to 25 km to match AMSR-E soil moisture products. Comparisons between the soil moisture and broadband white-sky albedos for bare soil in the Southwest U.S. (MODIS tile h08v05) indicate that soil albedo generally decreases with an increase in soil moisture (Figure 6). The rate of decrease for all three broadband albedos are very similar, which suggests that the change of soil moisture is likely the major factor of albedo change and that the soil line approach is resistant to soil moisture changes. Variation in NIR broadband albedo is larger than that in visible and total shortwave albedos, which is likely due to the fact that: (1) NIR albedo is larger than visible, and thus the absolute values are more variant; and (2) soil moisture may cause a larger variation in the longer wavelength part of the NIR spectral domain [34].

The relationship between bare soil albedo and soil moisture on a 16-day interval was found to be relatively stable across different seasons and locations over the CONUS (0.18 < A < 0.24; 9.86 < B < 21.33; 0.12 < C < 0.14; 0.031 < RMSE < 0.037). However, as the range of the 16-day averaged soil moisture variation is relatively small (most soil moisture values are between 0.08 and 0.12 g/cm3), the exponential relationship between these two variables cannot be verified without simultaneous instantaneous small soil moisture values (<0.05 g/cm3) and large bare soil albedos (>0.3). Nevertheless, the relationship found in this study is very close to the results presented in Gascoin et al. [9], considering that their soil moisture samples were taken at a ~5 cm depth from the surface.

Soil moisture is among the most important factors that can affect soil reflectivity, which should be considered in bare soil albedo estimations. However, soil moisture varies both spatially and temporally. Thus, it is difficult to remove the impacts of soil moisture in the final 500 m bare soil albedo map without the support of soil moisture products available at a similar resolution.

**Figure 6.** Relationship between bare soil broadband white-sky albedos and soil skin moisture over MODIS tile h08v05 for January 2002–2011. Red line is the best fit curve; its regression coefficients and RMSEs are shown above.

#### *3.4. Relationship of Bare Soil Albedo with Major Soil Types and Land Cover Types*

Traditional methods directly relate soil albedo with soil types, which are currently used by many land surface models to simplify the parameterization of soil albedo besides correcting the illumination angle effects [20].

The climatological bare soil white-sky albedos for different soil types derived for the period 2000–2012 (Table 3) were compared between each other. The Aridisols were found to have the largest soil albedo values because they tend to be the driest among the 12 major soil types—too dry for mesophytic plants to grow. Entisols, many of which are found in steep and rocky settings, have the second largest albedo values. Since the soil reflectivity is very sensitive to moisture changes under dry conditions, albedos of both Aridisols and Entisols have the largest variations. Among three broadband albedos, the near infrared albedos have the highest mean and SDEV values, and the visible albedos have the lowest mean and SDEV values for each soil type.

**Table 3.** Statistics of broadband soil albedo distribution for each of the major soil types.


**Table 4.** *p*-value of two tailed *t*-test on the soil albedos among different soil types.


\*: *p* < 0.05; \*\*: *p* < 0.01; \*\*\*: *p* < 0.001.

Histosols have the lowest reflectivity, probably because of their high organic matter content. Oxisols and Spodosols also have low albedo values. Possible reasons are that the Oxisols are mainly distributed in tropical and subtropical areas where precipitation increases soil moisture, and the Spodosols are acid soils mainly under forest.

The two tailed *t*-test results shown in Table 4 sugges<sup>t</sup> that differences between soil albedo values are statistically significant for most soil types. However, there are several exceptions. Oxisols are quite inseparable from all the other types. It is also difficult to separate the albedos of Gelisols from those of Alfisols and Entisols. Their small sample size (Oxisols have less than 0.004% of the total samples; Gelisols have 0.147% of the total samples) is likely to have resulted in the difficulty in the separation of their soil albedos because a 4 km soil map grid may contain multiple soil types.

Bare soil albedo can also be linked with the type of vegetation above the ground because that the soil moisture–precipitation feedback [53] and vegetation–soil moisture feedback [54] will determine the relationship between vegetation type and magnitude of soil albedo (because of soil moisture). Table 5 lists the climatological values of bare soil albedo for each of the International Geosphere-Biosphere Programme (IGBP) land cover types from MODIS land cover data. In this study, it was found that bare soil albedo decreases as the vegetation density increases from open shrubland to evergreen needle leaf forest.


**Table 5.** Statistics of broadband soil albedo distribution for each of the land cover classes.

ENF: Evergreen needleleaf forest; EBF: Evergreen broadleaf forest; DNF: Deciduous needleleaf forest; DBF: Deciduous broadleaf forest; MIX: Mixed forest; CSH: Closed shrubland; OSH: Open shrublands; WSV: Woody savannas; SAV: Savannas; GRA: Grasslands; WET: Permanent wetlands; CRO: Croplands; URB: Urban and built-up; CRC: Cropland/natural vegetation mosaic; GLA: Snow and ice; BRN: Barren or sparsely vegetated.

Compared with the statistics of albedo–soil types in Tables 2 and 3, bare soil albedos have smaller within-class SDEVs for the albedo–land cover types, except for open shrublands and barren surface. This suggests that land cover type might be a better indicator to quantify the magnitude of bare soil albedo than soil type for the vegetated areas. For sparsely vegetated areas, the soil type map provides spatial variation that is necessary to characterize the relationship between bare soil albedo and soil type.
