# Review of Land Surface Albedo: Variance Characteristics, Climate Effect and Management Strategy
## 4 Climate Feedback and Management Strategy for Surface Albedo
### Monitoring Short-to-Long-Term Albedo Change and Climate Effects
#### 4.1.1 Relationships between Surface Albedo Variance and Climate Feedback
Surface melt and subsequent snow air depletion can ultimately lead to the disintegration of ice shelves and accelerate sea-level rise, and foehn winds enhance melting near the grounding line, leading to the disintegration of the most northerly ice shelves in the Antarctic Peninsula [172]. The melting of relatively thin Arctic sea ice pack was monitored in the summer [31], and reportedly, Arctic sea ice has shrunk substantially over recent decades [32]. Impurity (e.g., black carbon)-induced snow albedo reduction has greatly enhanced glacier melting on the Tibetan Plateau by approximately 15% during 2001-2018 [117], and forest fire-generated aerosols have also reduced glacier albedo by 4-81% in a 20-year record (2000 to 2019) of MODIS, leading to an increase in air temperature [132]. Continental-scale snow albedo anomalies in the meteorological activitiesof wintertime Arctic oscillation were observed [173]. A small increase in precipitation in interior Antarctica can increase snow albedo by 0.4% on average during the 21 st century based on simulations, which has shown an inhibition of positive SAF induced by global warming [174]. Substantial Antarctic sea ice losses from 2016-2018 reduced its negative climate feedback by an increase trend of +0.26 \(\pm\) 0.15 W/m\({}^{2}\)[175]. In addition, surface albedo changes when natural disasters occur. Climate warming and drying intensify the fire dynamics of forests (e.g., boreal forests), which leads to a shift in vegetation composition [176]. Nevertheless, studies on desert dust and biomass burning aerosols can exhibit dramatic shifts in radiative forcing at the TOA from cooling to warming at surface albedos of below 0.5 to above 0.75 [72]. During the 2003 European heat wave, a significant total negative shortwave radiative forcing (\(-\)10 W/m\({}^{2}\)) was observed, especially over cropland areas, while a small effect (\(-\)1 W/m\({}^{2}\)) was observed at the subcontinental scale [109]. Altered albedo dominates the radiative forcing changes in a subtropical forest following an extreme snow event [177]. Based on the analysis of a historical dataset of mountain pine beetle outbreaks in North America over a 60-year period, albedo increased, and change in annual albedo (0.06 \(\pm\) 0.006 W/m\({}^{2}\)) and negative radiative forcing (\(-\)0.8 \(\pm\) 0.1 W/m\({}^{2}\)) first reached its peak after 14-20 years and then recovered to preoutbreak levels within 30-40 years [178]. The desert shows sharp reductions in albedo to less than 0.2 when the surface is flooded [179]. Surface albedo can also be used for the interpretation of natural geographic processes and phenomena. For example, surface albedo data can aid in more accurately extracting the zenith light intensity of atmospheric emissions at night (i.e., auroral), which are always contaminated by backscattered light from the ground or clouds below the emission layer for satellite observations [180]. In addition, surface albedo impacts artificial night sky brightness at the zenith along with land types and seasons [181].