Albedo - wikipedia Albedo For other uses, see Albedo ( disambiguation ). Percentage of diffusely reflected sunlight in relation to various surface conditions Albedo ( / ælˈbiːdoʊ / ) is a measure for reflectance or optical brightness ( Latin albedo, `` whiteness '' ) of a surface. It is dimensionless and measured on a scale from zero ( corresponding to a black body that absorbs all incident radiation ) to one ( corresponding to a white body that reflects all incident radiation ). Surface albedo is defined as the ratio of irradiance reflected to the irradiance received by a surface. The proportion reflected is not only determined by properties of the surface itself, but also by the spectral and angular distribution of solar radiation reaching the Earth 's surface. These factors vary with atmospheric composition, geographic location and time ( see Position of the Sun ). While bi-hemispherical reflectance is calculated for a single angle of incidence ( i.e., for a given position of the sun ), albedo is the directional integration of reflectance over all solar angles in a given period. The temporal resolution may range from seconds ( as obtained from flux measurements ) to daily, monthly or annual averages. Unless given for a specific wavelength ( spectral albedo ), albedo refers to the entire spectrum of solar radiation. Due to measurement constraints, it is often given for the spectrum in which most solar energy reaches the surface ( approximately between 0.3 and 3 μm ). This spectrum includes visible light ( 0.39 - 0.7 μm ), which explains why surfaces with a low albedo appear dark ( e.g., trees absorb most radiation ), whereas surfaces with a high albedo appear bright ( e.g., snow reflects most radiation ). Albedo is an important concept in climatology, astronomy, and environmental management ( e.g., as part of the Leadership in Energy and Environmental Design ( LEED ) program for sustainable rating of buildings ). The average albedo of the Earth at the top of the atmosphere, its planetary albedo, is 30 to 35 % because of cloud cover, but widely varies locally across the surface because of different geological and environmental features. The term albedo was introduced into optics by Johann Heinrich Lambert in his 1760 work Photometria. Contents 1 Terrestrial albedo 1.1 White - sky and black - sky albedo 2 Astronomical albedo 3 Examples of terrestrial albedo effects 3.1 Illumination 3.2 Insolation effects 3.3 Climate and weather 3.4 Albedo -- temperature feedback 3.5 Snow 3.6 Small - scale effects 3.7 Solar photovoltaic effects 3.8 Trees 3.9 Water 3.10 Clouds 3.11 Aerosol effects 3.12 Black carbon 3.13 Human activities 4 Other types of albedo 5 See also 6 References 7 External links Terrestrial albedo Sample albedos Surface Typical albedo Fresh asphalt 0.04 Open ocean 0.06 Worn asphalt 0.12 Conifer forest ( Summer ) 0.08, 0.09 to 0.15 Deciduous trees 0.15 to 0.18 Bare soil 0.17 Green grass 0.25 Desert sand 0.40 New concrete 0.55 Ocean ice 0.5 -- 0.7 Fresh snow 0.80 -- 0.90 Any albedo in visible light falls within a range of about 0.9 for fresh snow to about 0.04 for charcoal, one of the darkest substances. Deeply shadowed cavities can achieve an effective albedo approaching the zero of a black body. When seen from a distance, the ocean surface has a low albedo, as do most forests, whereas desert areas have some of the highest albedos among landforms. Most land areas are in an albedo range of 0.1 to 0.4. The average albedo of Earth is about 0.3. This is far higher than for the ocean primarily because of the contribution of clouds. 2003 -- 2004 mean annual clear - sky and total - sky albedo Earth 's surface albedo is regularly estimated via Earth observation satellite sensors such as NASA 's MODIS instruments on board the Terra and Aqua satellites, and the CERES instrument on the Suomi NPP and JPSS. As the amount of reflected radiation is only measured for a single direction by satellite, not all directions, a mathematical model is used to translate a sample set of satellite reflectance measurements into estimates of directional - hemispherical reflectance and bi-hemispherical reflectance ( e.g., ). These calculations are based on the bidirectional reflectance distribution function ( BRDF ), which describes how the reflectance of a given surface depends on the view angle of the observer and the solar angle. Thereby, the BRDF allows to translate observations of reflectance into albedo. Earth 's average surface temperature due to its albedo and the greenhouse effect is currently about 15 ° C. If Earth were frozen entirely ( and hence be more reflective ), the average temperature of the planet would drop below − 40 ° C. If only the continental land masses became covered by glaciers, the mean temperature of the planet would drop to about 0 ° C. In contrast, if the entire Earth was covered by water -- a so - called aquaplanet -- the average temperature on the planet would rise to almost 27 ° C. White - sky and black - sky albedo For land surfaces, it has been shown that the albedo at a particular solar zenith angle θ can be approximated by the proportionate sum of two terms : the directional - hemispherical reflectance at that solar zenith angle, α  ̄ ( θ i ) ( displaystyle ( ( \bar ( alpha ) ) ( \theta _ ( i ) ) ) ), and the bi-hemispherical reflectance, α  ̄  ̄ ( displaystyle ( \bar ( \bar ( alpha ) ) ) ), with D − 1 ( displaystyle ( D - 1 ) ) being the proportion of direct radiation from a given solar angle, and D ( displaystyle ( D ) ) being the proportion of diffuse illumination. Hence, the actual albedo α ( displaystyle ( alpha ) ) ( also called blue - sky albedo ) can then be given as : α = ( 1 − D ) α  ̄ ( θ i ) + D α  ̄  ̄. ( displaystyle ( alpha ) = ( 1 - D ) ( \bar ( alpha ) ) ( \theta _ ( i ) ) + D ( \bar ( \bar ( alpha ) ) ). ) Directional - hemispherical reflectance is sometimes referred to as black - sky albedo and bi-hemispherical reflectance as white - sky albedo. These terms are important because they allow the albedo to be calculated for any given illumination conditions from a knowledge of the intrinsic properties of the surface. Astronomical albedo The albedos of planets, satellites and minor planets such as asteroids can be used to infer much about their properties. The study of albedos, their dependence on wavelength, lighting angle ( `` phase angle '' ), and variation in time comprises a major part of the astronomical field of photometry. For small and far objects that can not be resolved by telescopes, much of what we know comes from the study of their albedos. For example, the absolute albedo can indicate the surface ice content of outer Solar System objects, the variation of albedo with phase angle gives information about regolith properties, whereas unusually high radar albedo is indicative of high metal content in asteroids. Enceladus, a moon of Saturn, has one of the highest known albedos of any body in the Solar System, with 99 % of EM radiation reflected. Another notable high - albedo body is Eris, with an albedo of 0.96. Many small objects in the outer Solar System and asteroid belt have low albedos down to about 0.05. A typical comet nucleus has an albedo of 0.04. Such a dark surface is thought to be indicative of a primitive and heavily space weathered surface containing some organic compounds. The overall albedo of the Moon is measured to be around 0.136, but it is strongly directional and non-Lambertian, displaying also a strong opposition effect. Although such reflectance properties are different from those of any terrestrial terrains, they are typical of the regolith surfaces of airless Solar System bodies. Two common albedos that are used in astronomy are the ( V - band ) geometric albedo ( measuring brightness when illumination comes from directly behind the observer ) and the Bond albedo ( measuring total proportion of electromagnetic energy reflected ). Their values can differ significantly, which is a common source of confusion. In detailed studies, the directional reflectance properties of astronomical bodies are often expressed in terms of the five Hapke parameters which semi-empirically describe the variation of albedo with phase angle, including a characterization of the opposition effect of regolith surfaces. The correlation between astronomical ( geometric ) albedo, absolute magnitude and diameter is : A = ( 1329 × 10 − H / 5 D ) 2 ( displaystyle A = left ( ( \frac ( 1329 \times 10 ^ ( - H / 5 ) ) ( D ) ) \right ) ^ ( 2 ) ), where A ( displaystyle A ) is the astronomical albedo, D ( displaystyle D ) is the diameter in kilometers, and H ( displaystyle H ) is the absolute magnitude. Examples of terrestrial albedo effects Illumination Although the albedo -- temperature effect is best known in colder, whiter regions on Earth, the maximum albedo is actually found in the tropics where year - round illumination is greater. The maximum is additionally in the northern hemisphere, varying between three and twelve degrees north. The minima are found in the subtropical regions of the northern and southern hemispheres, beyond which albedo increases without respect to illumination. Insolation effects The intensity of albedo temperature effects depend on the amount of albedo and the level of local insolation ( solar irradiance ) ; high albedo areas in the arctic and antarctic regions are cold due to low insolation, where areas such as the Sahara Desert, which also have a relatively high albedo, will be hotter due to high insolation. Tropical and sub-tropical rainforest areas have low albedo, and are much hotter than their temperate forest counterparts, which have lower insolation. Because insolation plays such a big role in the heating and cooling effects of albedo, high insolation areas like the tropics will tend to show a more pronounced fluctuation in local temperature when local albedo changes. Arctic regions notably release more heat back into space than what they absorb, effectively cooling the Earth. This has been a concern since arctic ice and snow has been melting at higher rates due to higher temperatures, creating regions in the arctic that are notably darker ( being water or ground which is darker color ) and reflects less heat back into space. This feedback loop results in a reduced albedo effect. Climate and weather Albedo affects climate by determining how much radiation a planet absorbs. The uneven heating of Earth from albedo variations between land, ice, or ocean surfaces can drive weather. Albedo -- temperature feedback When an area 's albedo changes due to snowfall, a snow -- temperature feedback results. A layer of snowfall increases local albedo, reflecting away sunlight, leading to local cooling. In principle, if no outside temperature change affects this area ( e.g., a warm air mass ), the raised albedo and lower temperature would maintain the current snow and invite further snowfall, deepening the snow -- temperature feedback. However, because local weather is dynamic due to the change of seasons, eventually warm air masses and a more direct angle of sunlight ( higher insolation ) cause melting. When the melted area reveals surfaces with lower albedo, such as grass or soil, the effect is reversed : the darkening surface lowers albedo, increasing local temperatures, which induces more melting and thus reducing the albedo further, resulting in still more heating. Snow Snow albedo is highly variable, ranging from as high as 0.9 for freshly fallen snow, to about 0.4 for melting snow, and as low as 0.2 for dirty snow. Over Antarctica they average a little more than 0.8. If a marginally snow - covered area warms, snow tends to melt, lowering the albedo, and hence leading to more snowmelt because more radiation is being absorbed by the snowpack ( the ice -- albedo positive feedback ). Cryoconite, powdery windblown dust containing soot, sometimes reduces albedo on glaciers and ice sheets. Hence, small errors in albedo can lead to large errors in energy estimates, which is why it is important to measure the albedo of snow - covered areas through remote sensing techniques rather than applying a single value over broad regions. Small - scale effects Albedo works on a smaller scale, too. In sunlight, dark clothes absorb more heat and light - coloured clothes reflect it better, thus allowing some control over body temperature by exploiting the albedo effect of the colour of external clothing. Solar photovoltaic effects Albedo can affect the electrical energy output of solar photovoltaic devices. For example, the effects of a spectrally responsive albedo are illustrated by the differences between the spectrally weighted albedo of solar photovoltaic technology based on hydrogenated amorphous silicon ( a-Si : H ) and crystalline silicon ( c - Si ) - based compared to traditional spectral - integrated albedo predictions. Research showed impacts of over 10 %. More recently, the analysis was extended to the effects of spectral bias due to the specular reflectivity of 22 commonly occurring surface materials ( both human - made and natural ) and analyzes the albedo effects on the performance of seven photovoltaic materials covering three common photovoltaic system topologies : industrial ( solar farms ), commercial flat rooftops and residential pitched - roof applications. Trees Because forests generally have a low albedo, ( the majority of the ultraviolet and visible spectrum is absorbed through photosynthesis ), some scientists have suggested that greater heat absorption by trees could offset some of the carbon benefits of afforestation ( or offset the negative climate impacts of deforestation ). In the case of evergreen forests with seasonal snow cover albedo reduction may be great enough for deforestation to cause a net cooling effect. Trees also impact climate in extremely complicated ways through evapotranspiration. The water vapor causes cooling on the land surface, causes heating where it condenses, acts a strong greenhouse gas, and can increase albedo when it condenses into clouds Scientists generally treat evapotranspiration as a net cooling impact, and the net climate impact of albedo and evapotranspiration changes from deforestation depends greatly on local climate In seasonally snow - covered zones, winter albedos of treeless areas are 10 % to 50 % higher than nearby forested areas because snow does not cover the trees as readily. Deciduous trees have an albedo value of about 0.15 to 0.18 whereas coniferous trees have a value of about 0.09 to 0.15. Studies by the Hadley Centre have investigated the relative ( generally warming ) effect of albedo change and ( cooling ) effect of carbon sequestration on planting forests. They found that new forests in tropical and midlatitude areas tended to cool ; new forests in high latitudes ( e.g., Siberia ) were neutral or perhaps warming. Water Water reflects light very differently from typical terrestrial materials. The reflectivity of a water surface is calculated using the Fresnel equations ( see graph ). Reflectivity of smooth water at 20 ° C ( refractive index = 1.333 ) At the scale of the wavelength of light even wavy water is always smooth so the light is reflected in a locally specular manner ( not diffusely ). The glint of light off water is a commonplace effect of this. At small angles of incident light, waviness results in reduced reflectivity because of the steepness of the reflectivity - vs. - incident - angle curve and a locally increased average incident angle. Although the reflectivity of water is very low at low and medium angles of incident light, it becomes very high at high angles of incident light such as those that occur on the illuminated side of Earth near the terminator ( early morning, late afternoon, and near the poles ). However, as mentioned above, waviness causes an appreciable reduction. Because light specularly reflected from water does not usually reach the viewer, water is usually considered to have a very low albedo in spite of its high reflectivity at high angles of incident light. Note that white caps on waves look white ( and have high albedo ) because the water is foamed up, so there are many superimposed bubble surfaces which reflect, adding up their reflectivities. Fresh ' black ' ice exhibits Fresnel reflection. Clouds Cloud albedo has substantial influence over atmospheric temperatures. Different types of clouds exhibit different reflectivity, theoretically ranging in albedo from a minimum of near 0 to a maximum approaching 0.8. `` On any given day, about half of Earth is covered by clouds, which reflect more sunlight than land and water. Clouds keep Earth cool by reflecting sunlight, but they can also serve as blankets to trap warmth. '' Albedo and climate in some areas are affected by artificial clouds, such as those created by the contrails of heavy commercial airliner traffic. A study following the burning of the Kuwaiti oil fields during Iraqi occupation showed that temperatures under the burning oil fires were as much as 10 ° C colder than temperatures several miles away under clear skies. Aerosol effects Aerosols ( very fine particles / droplets in the atmosphere ) have both direct and indirect effects on Earth 's radiative balance. The direct ( albedo ) effect is generally to cool the planet ; the indirect effect ( the particles act as cloud condensation nuclei and thereby change cloud properties ) is less certain. As per the effects are : Aerosol direct effect. Aerosols directly scatter and absorb radiation. The scattering of radiation causes atmospheric cooling, whereas absorption can cause atmospheric warming. Aerosol indirect effect. Aerosols modify the properties of clouds through a subset of the aerosol population called cloud condensation nuclei. Increased nuclei concentrations lead to increased cloud droplet number concentrations, which in turn leads to increased cloud albedo, increased light scattering and radiative cooling ( first indirect effect ), but also leads to reduced precipitation efficiency and increased lifetime of the cloud ( second indirect effect ). Black carbon Another albedo - related effect on the climate is from black carbon particles. The size of this effect is difficult to quantify : the Intergovernmental Panel on Climate Change estimates that the global mean radiative forcing for black carbon aerosols from fossil fuels is + 0.2 W m, with a range + 0.1 to + 0.4 W m. Black carbon is a bigger cause of the melting of the polar ice cap in the Arctic than carbon dioxide due to its effect on the albedo. Human activities Human activities ( e.g., deforestation, farming, and urbanization ) change the albedo of various areas around the globe. However, quantification of this effect on the global scale is difficult. Other types of albedo Single - scattering albedo is used to define scattering of electromagnetic waves on small particles. It depends on properties of the material ( refractive index ) ; the size of the particle or particles ; and the wavelength of the incoming radiation. See also Cool roof Daisyworld Emissivity Global dimming Irradiance Kirchhoff 's law of thermal radiation Opposition surge Polar see - saw Solar radiation management References Jump up ^ Coakley, J.A. ( 2003 ). Reflectance and albedo, surface. Encyclopedia of the Atmosphere, JR Holton and JA Curry ( eds. ) ( PDF ). Academic Press. pp. 1914 -- 1923. Jump up ^ Henderson - Sellers, A. ; Wilson, M.F. ( 1983 ). `` Albedo observations of the Earth 's surface for climate research ''. Philosophical Transactions of the Royal Society of London A. 309 ( 1508, The Study of the Ocean and the Land Surfacefrom Satellites ) : pp. 285 -- 294. Bibcode : 1983RSPTA. 309... 285H. JSTOR 37357. doi : 10.1098 / rsta. 1983.0042. CS1 maint : Extra text ( link ) Jump up ^ Environmental Encyclopedia, 3rd ed., Thompson Gale, 2003, ISBN 0 - 7876 - 5486 - 8 ^ Jump up to : Pon, Brian ( 30 June 1999 ). `` Pavement Albedo ''. Heat Island Group. Archived from the original on 29 August 2007. Retrieved 27 August 2007. Jump up ^ `` Thermodynamics Thermodynamics : Albedo National Snow and Ice Data Center ''. nsidc.org. Retrieved 2016 - 08 - 14. Jump up ^ Alan K. Betts ; John H. Ball ( 1997 ). `` Albedo over the boreal forest ''. Journal of Geophysical Research. 102 ( D24 ) : 28,901 -- 28,910. Bibcode : 1997JGR... 10228901B. doi : 10.1029 / 96JD03876. Archived from the original on 30 September 2007. Retrieved 27 August 2007. ^ Jump up to : `` The Climate System ''. Manchester Metropolitan University. Archived from the original on 1 March 2003. Retrieved 11 November 2007. ^ Jump up to : Tom Markvart ; Luis CastaŁżer ( 2003 ). Practical Handbook of Photovoltaics : Fundamentals and Applications. Elsevier. ISBN 1 - 85617 - 390 - 9. Jump up ^ Tetzlaff, G. ( 1983 ). Albedo of the Sahara. Cologne University Satellite Measurement of Radiation Budget Parameters. pp. 60 -- 63. Jump up ^ `` Albedo -- from Eric Weisstein 's World of Physics ''. Scienceworld.wolfram.com. Retrieved 19 August 2011. Jump up ^ Goode, P.R. ; et al. ( 2001 ). `` Earthshine Observations of the Earth 's Reflectance ''. Geophysical Research Letters. 28 ( 9 ) : 1671 -- 1674. Bibcode : 2001GeoRL... 28.1671 G. doi : 10.1029 / 2000GL012580. Jump up ^ `` MODIS BRDF / Albedo Product : Algorithm Theoretical Basis Document, Version 5.0 '' ( PDF ). Archived from the original ( PDF ) on 1 June 2009. Retrieved 2 June 2009. Jump up ^ `` Snowball Earth : Ice thickness on the tropical ocean '' ( PDF ). Retrieved 20 September 2009. Jump up ^ `` Effect of land albedo, CO2, orography, and oceanic heat transport on extreme climates '' ( PDF ). Retrieved 20 September 2009. Jump up ^ `` Global climate and ocean circulation on an aquaplanet ocean - atmosphere general circulation model '' ( PDF ). Archived from the original ( PDF ) on 20 September 2009. Retrieved 20 September 2009. Jump up ^ Roman, M.O. ; C.B. Schaaf ; P. Lewis ; F. Gao ; G.P. Anderson ; J.L. Privette ; A.H. Strahler ; C.E. Woodcock ; M. Barnsley ( 2010 ). `` Assessing the Coupling between Surface Albedo derived from MODIS and the Fraction of Diffuse Skylight over Spatially - Characterized Landscapes ''. Remote Sensing of Environment. 114 ( 4 ) : 738 -- 760. Bibcode : 2010RSEnv. 114... 738R. doi : 10.1016 / j. rse. 2009.11. 014. Jump up ^ Sicardy, B. ; Ortiz, J.L. ; Assafin, M. ; Jehin, E. ; Maury, A. ; Lellouch, E. ; Gil - Hutton, R. ; Braga - Ribas, F. ; et al. ( 2011 ). `` Size, density, albedo and atmosphere limit of dwarf planet Eris from a stellar occultation '' ( PDF ). European Planetary Science Congress Abstracts. 6 : 137. Bibcode : 2011epsc. conf... 137S. Retrieved 14 September 2011. Jump up ^ Wm. Robert Johnston ( 17 September 2008 ). `` TNO / Centaur diameters and albedos ''. Johnston 's Archive. Archived from the original on 22 October 2008. Retrieved 17 October 2008. Jump up ^ Wm. Robert Johnston ( 28 June 2003 ). `` Asteroid albedos : graphs of data ''. Johnston 's Archive. Archived from the original on 17 May 2008. Retrieved 16 June 2008. Jump up ^ Robert Roy Britt ( 29 November 2001 ). `` Comet Borrelly Puzzle : Darkest Object in the Solar System ''. Space.com. Archived from the original on 22 January 2009. Retrieved 1 September 2012. Jump up ^ Matthews, G. ( 2008 ). `` Celestial body irradiance determination from an underfilled satellite radiometer : application to albedo and thermal emission measurements of the Moon using CERES ''. Applied Optics. 47 ( 27 ) : 4981 -- 4993. Bibcode : 2008ApOpt... 47.4981 M. PMID 18806861. doi : 10.1364 / AO. 47.004981. Jump up ^ Medkeff, Jeff ( 2002 ). `` Lunar Albedo ''. Archived from the original on 23 May 2008. Retrieved 5 July 2010. Jump up ^ Dan Bruton. `` Conversion of Absolute Magnitude to Diameter for Minor Planets ''. Department of Physics & Astronomy ( Stephen F. Austin State University ). Archived from the original on 10 December 2008. Retrieved 7 October 2008. ^ Jump up to : Winston, Jay ( 1971 ). `` The Annual Course of Zonal Mean Albedo as Derived From ESSA 3 and 5 Digitized Picture Data ''. Monthly Weather Review. 99 ( 11 ) : 818 -- 827. Bibcode : 1971MWRv... 99... 818W. doi : 10.1175 / 1520 - 0493 ( 1971 ) 099 < 0818 : TACOZM > 2.3.CO ; 2. Jump up ^ `` The thawing Arctic threatens an environmental catastrophe ''. The Economist. Retrieved 2017 - 05 - 08. Jump up ^ Schneider, Stephen Henry ; Mastrandrea, Michael D. ; Root, Terry L. ( 2011 ). Encyclopedia of Climate and Weather : Abs - Ero. Oxford University Press. ISBN 9780199765324. Jump up ^ Hall, D.K. and Martinec, J. ( 1985 ), Remote sensing of ice and snow. Chapman and Hall, New York, 189 pp. Jump up ^ `` Changing Greenland -- Melt Zone '' page 3, of 4, article by Mark Jenkins in National Geographic June 2010, accessed 8 July 2010 Jump up ^ `` Health and Safety : Be Cool ! ( August 1997 ) ''. Ranknfile-ue.org. Retrieved 19 August 2011. Jump up ^ Andrews, Rob W. ; Pearce, Joshua M. ( 2013 ). `` The effect of spectral albedo on amorphous silicon and crystalline silicon solar photovoltaic device performance ''. Solar Energy. 91 : 233 -- 241. Bibcode : 2013SoEn... 91... 233A. doi : 10.1016 / j. solener. 2013.01. 030. Jump up ^ Brennan, M.P. ; Abramase, A.L. ; Andrews, R.W. ; Pearce, J.M. ( 2014 ). `` Effects of spectral albedo on solar photovoltaic devices ''. Solar Energy Materials and Solar Cells. 124 : 111 -- 116. doi : 10.1016 / j. solmat. 2014.01. 046. Jump up ^ Betts, RA ( 2000 ). `` Offset of the potential carbon sink from boreal forestation by decreases in surface albedo ''. Nature. 408 ( 6809 ) : 187 -- 190. Bibcode : 2000Natur. 408... 187B. PMID 11089969. doi : 10.1038 / 35041545. Jump up ^ Boucher ; et al. ( 2004 ). `` Direct human influence of irrigation on atmospheric water vapour and climate ''. Climate Dynamics. 22 ( 6 -- 7 ) : 597 -- 603. Bibcode : 2004ClDy... 22... 597B. doi : 10.1007 / s00382 - 004 - 0402 - 4. Jump up ^ Bonan, GB ( 2008 ). `` Forests and Climate Change : Forcings, Feedbacks, and the Climate Benefits of Forests ''. Science. 320 ( 5882 ) : 1444 -- 1449. Bibcode : 2008Sci... 320.1444 B. PMID 18556546. doi : 10.1126 / science. 1155121. Jump up ^ Betts, Richard A. ( 2000 ). `` Offset of the potential carbon sink from boreal forestation by decreases in surface albedo ''. Nature. 408 ( 6809 ) : 187 -- 190. Bibcode : 2000Natur. 408... 187B. PMID 11089969. doi : 10.1038 / 35041545. Jump up ^ `` Spectral Approach To Calculate Specular reflection Of Light From Wavy Water Surface '' ( PDF ). Vih.freeshell.org. Retrieved 2015 - 03 - 16. Jump up ^ `` Baffled Scientists Say Less Sunlight Reaching Earth ''. LiveScience. 24 January 2006. Retrieved 19 August 2011. Jump up ^ `` Contrails reduce daily temperature range '' ( PDF ). Nature. 418 : 601. 8 August 2002. Bibcode : 2002Natur. 418... 601T. PMID 12167846. doi : 10.1038 / 418601a. Archived from the original ( PDF ) on 3 May 2006. Retrieved 7 July 2015. Jump up ^ Cahalan, Robert F. ( 30 May 1991 ). `` The Kuwait oil fires as seen by Landsat ''. Journal of Geophysical Research : Atmospheres. Adsabs.harvard.edu. 97 : 14565. Bibcode : 1992JGR... 9714565C. doi : 10.1029 / 92JD00799. Jump up ^ `` Climate Change 2001 : The Scientific Basis ''. Grida.no. Archived from the original on 29 June 2011. Retrieved 19 August 2011. Jump up ^ Spracklen, D. V ; Bonn, B. ; Carslaw, K. S ( 2008 ). `` Boreal forests, aerosols and the impacts on clouds and climate '' ( PDF ). Philosophical Transactions of the Royal Society A. 366 ( 1885 ) : 4613 -- 4626. Bibcode : 2008RSPTA. 366.4613 S. PMID 18826917. doi : 10.1098 / rsta. 2008.0201. Jump up ^ `` Climate Change 2001 : The Scientific Basis ''. Grida.no. Archived from the original on 29 June 2011. Retrieved 19 August 2011. Jump up ^ James Hansen & Larissa Nazarenko, Soot Climate Forcing Via Snow and Ice Albedos, 101 Proc. of the Nat'l. Acad. of Sci. 423 ( 13 January 2004 ) ( `` The efficacy of this forcing is '' 2 ( i.e., for a given forcing it is twice as effective as CO in altering global surface air temperature ) `` ) ; compare Zender Testimony, supra note 7, at 4 ( figure 3 ) ; See J. Hansen & L. Nazarenko, supra note 18, at 426. ( '' The efficacy for changes of Arctic sea ice albedo is > 3. In additional runs not shown here, we found that the efficacy of albedo changes in Antarctica is also > 3. `` ) ; See also Flanner, M.G., C.S. Zender, J.T. Randerson, and P.J. Rasch, Present - day climate forcing and response from black carbon in snow, 112 J. GEOPHYS. RES. D11202 ( 2007 ) ( '' The forcing is maximum coincidentally with snowmelt onset, triggering strong snow - albedo feedback in local springtime. Consequently, the `` efficacy '' of black carbon / snow forcing is more than three times greater than forcing by CO. `` ). External links Look up albedo in Wiktionary, the free dictionary. Official Website of Albedo Project Global Albedo Project ( Center for Clouds, Chemistry, and Climate ) Albedo -- Encyclopedia of Earth NASA MODIS BRDF / albedo product site Surface albedo derived from Meteosat observations A discussion of Lunar albedos reflectivity of metals ( chart ) Global warming and climate change Temperatures Brightness temperature Effective temperature Geologic record Hiatus Historical climatology Instrumental record Paleoclimatology Paleotempestology Proxy data Record of the past 1,000 years Satellite measurements Causes Anthropogenic Attribution of recent climate change Aviation Biofuel Black carbon Carbon dioxide Deforestation Earth 's energy budget Earth 's radiation balance Ecocide Fossil fuel Global dimming Global warming potential Greenhouse effect ( Infrared window ) Greenhouse gases ( Halocarbons ) Land use, land - use change and forestry Radiative forcing Tropospheric ozone Urban heat island Natural Albedo Bond events Climate oscillations Climate sensitivity Cloud forcing Cosmic rays Feedbacks Glaciation Global cooling Milankovitch cycles Ocean variability AMO ENSO IOD PDO Orbital forcing Solar variation Volcanism Models Global climate model History History of climate change science Atmospheric thermodynamics Svante Arrhenius James Hansen Charles David Keeling Opinion and climate change Environmental ethics Media coverage of climate change Public opinion on climate change ( Popular culture ) Scientific opinion on climate change Scientists opposing the mainstream assessment Climate change denial Global warming conspiracy theory By country & region ( Africa Arctic Argentina Australia Bangladesh Belgium Canada China Europe European Union Finland Grenada Japan Luxembourg New Zealand Norway Russia Scotland South Korea Sweden Tuvalu United Kingdom United States ) Politics Clean Power Plan Climate change denial ( Manufactured controversy ) Intergovernmental Panel on Climate Change ( IPCC ) March for Science People 's Climate March United Nations Framework Convention on Climate Change ( UNFCCC / FCCC ) Global climate regime Potential effects and issues General Abrupt climate change Anoxic event Arctic dipole anomaly Arctic haze Arctic methane release Climate change and agriculture Climate change and ecosystems Climate change and poverty Current sea level rise Drought Economics of global warming Effect on plant biodiversity Effects on health Effects on humans Effects on marine mammals Environmental migrant Extinction risk from global warming Fisheries and climate change Forest dieback Industry and society Iris hypothesis Megadrought Ocean acidification Ozone depletion Physical impacts Polar stratospheric cloud Regime shift Retreat of glaciers since 1850 Runaway climate change Season creep Shutdown of thermohaline circulation By country Australia India Nepal ( South Asia ) United States Mitigation Kyoto Protocol Clean Development Mechanism Joint Implementation Bali Road Map 2009 United Nations Climate Change Conference Governmental European Climate Change Programme G8 Climate Change Roundtable United Kingdom Climate Change Programme Paris Agreement United States withdrawal Regional climate change initiatives in the United States List of climate change initiatives Emissions reduction Carbon credit Carbon - neutral fuel Carbon offset Carbon tax Emissions trading Fossil - fuel phase - out Carbon - free energy Carbon capture and storage Efficient energy use Low - carbon economy Nuclear power Renewable energy Personal Individual action on climate change Simple living Other Carbon dioxide removal Carbon sink Climate change mitigation scenarios Climate engineering Individual and political action on climate change Reducing emissions from deforestation and forest degradation Reforestation Urban reforestation Climate Action Plan Climate action Proposed adaptations Strategies Damming glacial lakes Desalination Drought tolerance Irrigation investment Rainwater storage Sustainable development Weather modification Programmes Avoiding dangerous climate change Land allocation decision support system Glossary of climate change Index of climate change articles Category : Climate change Category : Global warming Portal : Global warming Retrieved from `` https://en.wikipedia.org/w/index.php?title=Albedo&oldid=801070438 '' Categories : Climate forcing Climatology Electromagnetic radiation Land surface effects on climate Radiometry Scattering, absorption and radiative transfer ( optics ) Radiation Hidden categories : CS1 maint : Extra text Use dmy dates from June 2013 All articles with unsourced statements Articles with unsourced statements from November 2013 Pages using div col with small parameter Talk Contents About Wikipedia Afrikaans Alemannisch Aragonés Asturianu Azərbaycanca বাংলা Беларуская Български Bosanski Català Čeština Cymraeg Dansk Deutsch Eesti Ελληνικά Español Esperanto Euskara فارسی Français Gaeilge Galego 한국어 Հայերեն हिन्दी Hrvatski Bahasa Indonesia Italiano עברית ಕನ್ನಡ ქართული Қазақша Kreyòl ayisyen Кыргызча Latina Latviešu Lëtzebuergesch Lietuvių Magyar Македонски മലയാളം Bahasa Melayu Nederlands 日本 語 Нохчийн Norsk Norsk nynorsk Occitan Oʻzbekcha / ўзбекча Plattdüütsch Polski Português Română Русский Scots Shqip Simple English Slovenčina Slovenščina Српски / srpski Srpskohrvatski / српскохрватски Suomi Svenska தமிழ் Татарча / tatarça Türkçe Українська Tiếng Việt 中文 Edit links This page was last edited on 17 September 2017, at 13 : 37. Text is available under the Creative Commons Attribution - ShareAlike License ; additional terms may apply. By using this site, you agree to the Terms of Use and Privacy Policy. Wikipedia ® is a registered trademark of the Wikimedia Foundation, Inc., a non-profit organization. About Wikipedia

Question: which earth’s surfaces have the highest and lowest albedo
Answer: ocean surface