Comparison of seasonal and spatial variations of albedos from Moderate‐Resolution Imaging Spectroradiometer (MODIS) and Common Land Model

Zhou, Lei; Dickinson, Robert E.; Tian, Yuhong; Zeng, Xubin; Dai, Yongjiu; Yang, Zong‐Liang; Schaaf, Crystal B.; Gao, Feng; Jin, Yufang; Strahler, Alan H.; Myneni, Ranga B.; Yu, Hongbin; Wu, Wanru; Shaikh, Muhammad

doi:10.1029/2002jd003326

Cited by 124 publications

(115 citation statements)

References 35 publications

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“…In general, the snow cover is vertically inhomogeneous, and sometimes it is optically thin (Voisin et al, 2012). The stratified structure of snow cover will lead to the discrepancies between computed spectral albedo from semi-infinite snow cover and measured albedo (Aoki et al, 2000;Grenfell, 1994;Kuipers Munneke et al, 2008;Zhou et al, 2003). In this study, we usually collected snow samples from the top 5-10 cm.…”

Section: Reflectance Measurements and Albedo Simulationsmentioning

confidence: 99%

Black carbon and mineral dust in snow cover on the Tibetan Plateau

et al. 2018

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Abstract. Snow cover plays a key role for sustaining ecology and society in mountainous regions. Light-absorbing particulates (including black carbon, organic carbon, and mineral dust) deposited on snow can reduce surface albedo and contribute to the near-worldwide melting of snow and ice. This study focused on understanding the role of black carbon and other water-insoluble light-absorbing particulates in the snow cover of the Tibetan Plateau (TP). The results found that the black carbon, organic carbon, and dust concentrations in snow cover generally ranged from 202 to 17 468 ng g −1 , 491 to 13 880 ng g −1 , and 22 to 846 µg g −1 , respectively, with higher concentrations in the central to northern areas of the TP. Back trajectory analysis suggested that the northern TP was influenced mainly by air masses from Central Asia with some Eurasian influence, and air masses in the central and Himalayan region originated mainly from Central and South Asia. The relative biomassburning-sourced black carbon contributions decreased from ∼ 50 % in the southern TP to ∼ 30 % in the northern TP. The relative contribution of black carbon and dust to snow albedo reduction reached approximately 37 and 15 %, respectively. The effect of black carbon and dust reduced the snow cover duration by 3.1 ± 0.1 to 4.4 ± 0.2 days. Meanwhile, the black carbon and dust had important implications for snowmelt water loss over the TP. The findings indicate that the impacts of black carbon and mineral dust need to be properly accounted for in future regional climate projections, particularly in the high-altitude cryosphere.

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Section: Reflectance Measurements and Albedo Simulationsmentioning

confidence: 99%

Black carbon and mineral dust in snow cover on the Tibetan Plateau

et al. 2018

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“…This has allowed for the careful evaluation of albedo in various LSMs (e.g. Wei et al, 2001;Oleson et al, 2003;Zhou et al, 2003;Wang et al, 2004) and the development of vegetation and soil albedo parameterisations (e.g. Liang et al, 2005;Yang et al, 2008).…”

Section: Published By Copernicus Publications On Behalf Of the Europementioning

confidence: 99%

Implementation of a soil albedo scheme in the CABLEv1.4b land surface model and evaluation against MODIS estimates over Australia

et al. 2014

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Abstract. Land surface albedo, the fraction of incoming solar radiation reflected by the land surface, is a key component of the Earth system. This study evaluates snow-free surface albedo simulations by the Community Atmosphere Biosphere Land Exchange (CABLEv1.4b) model with the Moderate Resolution Imaging Spectroradiometer (MODIS) and the Satellite Pour L'Observation de la Terre (SPOT) albedo. We compare results from offline simulations over the Australian continent. The control simulation has prescribed background snow-free and vegetation-free soil albedo derived from MODIS whilst the experiments use a simple parameterisation based on soil moisture and colour, originally from the Biosphere Atmosphere Transfer Scheme (BATS), and adopted in the Common Land Model (CLM). The control simulation, with prescribed soil albedo, shows that CABLE simulates overall albedo over Australia reasonably well, with differences compared to MODIS and SPOT albedos within ±0.1. Application of the original BATS scheme, which uses an eight-class soil classification, resulted in large differences of up to −0.25 for the near-infrared (NIR) albedo over large parts of the desert regions of central Australia. The use of a recalibrated 20-class soil colour classification from the CLM, which includes a higher range for saturated and VIS (visible) and NIR soil albedos, reduced the underestimation of the NIR albedo. However, this soil colour mapping is tuned to CLM soil moisture, a quantity which is not necessarily transferrable between land surface models. We therefore recalibrated the soil color map using CABLE's climatological soil moisture, which further reduced the underestimation of the NIR albedo to within ±0.15 over most of the continent as compared to MODIS and SPOT albedos. Small areas of larger differences of up to −0.25 remained within the central arid parts of the continent during summer; however, the spatial extent of these large differences is substantially reduced as compared to the simulation using the default eight-class uncalibrated soil colour map. It is now possible to use CABLE coupled to atmospheric models to investigate soil-moisture-albedo feedbacks, an important enhancement of the model.

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“…Several studies have addressed the deficiencies in the parameterisation of land surface albedo in the Community Land Model 2.0 by comparing the model-computed albedo against MODIS observations (Oleson et al, 2003;Zhou et al, 2003;Wang et al, 2004). These studies report better agreement of simulated albedo to observations during summer (Oleson et al, 2003), overestimation of simulated albedo over snow-covered regions by as much as 20% and underestimation of the albedo in the desert regions of the Sahara and the Arabian Peninsula (Oleson et al, 2003;Zhou et al, 2003).…”

Section: The Clm-modis Experimentsmentioning

confidence: 94%

“…These studies report better agreement of simulated albedo to observations during summer (Oleson et al, 2003), overestimation of simulated albedo over snow-covered regions by as much as 20% and underestimation of the albedo in the desert regions of the Sahara and the Arabian Peninsula (Oleson et al, 2003;Zhou et al, 2003). These studies suggested CLM needs to be improved to have a better representation of albedo, leaf area index (LAI), snow cover etc.…”

Section: The Clm-modis Experimentsmentioning

confidence: 98%

Comparison of satellite‐derived TOA shortwave clear‐sky fluxes to estimates from GCM simulations constrained by satellite observations of land surface characteristics

Anantharaj

Nair

Lawrence

et al. 2010

Intl Journal of Climatology

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Clear-sky, upwelling shortwave flux at the top of the atmosphere S ↑ TOA , simulated using the atmospheric and land model components of the Community Climate System Model 3 (CCSM3), is compared to corresponding observational estimates from the Clouds and Earth's Radiant Energy System (CERES) sensor. Improvements resulting from the use of land surface albedo derived from Moderate Resolution Imaging Spectroradiometer (MODIS) to constrain the simulations are also examined. Compared to CERES observations, CCSM3 overestimates global, annual averaged S ↑ TOA over both land and oceans. However, regionally, CCSM3 overestimates S ↑ TOA over some land and ocean areas while underestimating it over other sites. CCSM3 underestimates S ↑ TOA over the Saharan and Arabian Deserts and substantial differences exist between CERES observations and CCSM3 over agricultural areas. Over selected sites, after using groundbased observations to remove systematic biases that exist in CCSM computation of S ↑ TOA , it is found that use of MODIS albedo improves the simulation of S ↑ TOA . Inability of coarse resolution CCSM3 simulation to resolve spatial heterogeneity of snowfall over high altitude sites such as the Tibetan Plateau causes overestimation of S ↑ TOA in these areas. Discrepancies also exist in the simulation of S ↑ TOA over ocean areas as CCSM3 does not account for the effect of wind speed on ocean surface albedo. This study shows that the radiative energy budget at the TOA is improved through the use of MODIS albedo in Global Climate Models.

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Comparison of seasonal and spatial variations of albedos from Moderate‐Resolution Imaging Spectroradiometer (MODIS) and Common Land Model

Cited by 124 publications

References 35 publications

Black carbon and mineral dust in snow cover on the Tibetan Plateau

Black carbon and mineral dust in snow cover on the Tibetan Plateau

Implementation of a soil albedo scheme in the CABLEv1.4b land surface model and evaluation against MODIS estimates over Australia

Comparison of satellite‐derived TOA shortwave clear‐sky fluxes to estimates from GCM simulations constrained by satellite observations of land surface characteristics

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