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1  properties (masses, radii, temperatures and albedos).
2  are possible with no change in water use or albedo.
3  nuclei and possibly influences ice and snow albedo.
4 s by effective density and single-scattering albedo.
5 creases in transpiration, but also to higher albedo.
6 e an important contribution to the planetary albedo.
7  and water ice sublimation rates for a given albedo.
8 positively correlated with shortwave surface albedo.
9 oughness-changes that can dramatically alter albedo.
10 and sea ice, and postfire changes in surface albedo.
11 al growth temperature as well as mutation of albedo.
12 equired to discern climate trends in Earth's albedo.
13 ese deposition styles that determine the cap albedo.
14 etermine independently both the size and the albedo.
15  melting, plays a crucial role in decreasing albedo.
16 trations, aerosol emissions, or land surface albedo.
17  and key drivers are changes in snow and ice albedo.
18 cts of seabird-influenced particles on cloud albedo.
19 tem properties, including canopy density and albedo.
20 ed conditions and corresponding variation in albedo.
21 prisingly does not correlate well with model albedo.
22 d asteroids near the Sun typically have high albedos.
23 mates for the effect of soot on snow and ice albedos (1.5% in the Arctic and 3% in Northern Hemispher
24 natively, improvements in water use (13%) or albedo (34%) can likewise be made with no loss of produc
25                     All four moons have high albedos (~50 to 90%) suggestive of a water-ice surface c
26 itous across the Arctic and the reduction in albedo accelerates snow melt and increases the time and
27      The reduction in radiative forcing from albedo alone is equivalent to a carbon emissions reducti
28 el, indicating that the observed interannual albedo alterations strongly influence the martian enviro
29  glacier and sea ice expansion, increased NH albedo, AMOC weakening, more NH cooling, and a consequen
30                        The single scattering albedo and aerosol forcing efficiency showed that primar
31 ortant positive reinforcements including ice-albedo and cloud-radiation feedbacks.
32 ard of this boundary is distinguished by its albedo and color contrasts, elevated temperatures, extre
33 a positive feedback through changes in ocean albedo and evaporation.
34 y the net cooling associated with changes in albedo and evapotranspiration.
35 al surfaces leading to a decrease in surface albedo and eventually higher melting rates.
36 . shrub expansion, resulting in reduction in albedo and greater C fixation in aboveground vegetation
37                   Smaller changes in surface albedo and humidity feedbacks also contribute to the ove
38 se losses are accelerating, reducing Earth's albedo and increasing heat absorption.
39 unit that is about a factor of four lower in albedo and is found mostly in the bottoms of cup-like cr
40 cooling is triggered by increases in surface albedo and is reinforced by a land albedo-sea ice feedba
41 cument the Arctic-wide decrease in planetary albedo and its amplifying effect on the warming.
42  climate system via its influence on surface albedo and may offer a simple approach for monitoring fo
43 xistence of a particular combination of mean albedo and optimum individual growth temperature which m
44 ous, in part because of its low density, low albedo and relatively featureless visible reflectance sp
45                        The single scattering albedo and scattering and absorption cross sections are
46 ls a striking relationship between planetary albedo and sea ice cover, quantities inferred from two i
47 st United States was already decreasing snow albedo and shortening the duration of snow cover by seve
48 However, it is possible that increasing crop albedo and soil carbon sequestration might contribute to
49 increasing aerosol concentration changes the albedo and suppresses precipitation formation not only t
50  responsible for a poleward shift of runoff, albedo and surface temperature records over the Greenlan
51  which enhance volcanic effects on planetary albedo and the global carbon cycle, and trigger northern
52 c implications for our understanding of snow albedo and the processing of atmospheric BC aerosol in s
53               Observed relationships between albedo and tree cover differ substantially between snow-
54 and coupled climate model representations of albedo and tree cover for the boreal and Arctic region.
55 e then used to determine the PD and PI cloud albedos and, thus, the effect of anthropogenic aerosols
56 ge of morphology, composition (inferred from albedo), and age (as seen in occurrences of different du
57 d facilitate sea ice formation, increase the albedo, and isolate the high heat capacity of the ocean
58 al sulfur cycling(2) and affects the Earth's albedo, and potentially climate, via sulfate aerosol and
59 oud albedo, cloud coverage, and snow and ice albedo, and the optical consequences of aerosol mixing)
60  thinning through feedbacks altering surface albedo, and to potentially seed recently deglaciated ter
61  conversion of forests to wetlands increases albedo: and bulk surface conductance for water vapour an
62 ture changes unrelated to changes in surface albedo are an important contributor to the overall cooli
63                      As models with non-zero albedo are cooler, this essentially eliminates uniform b
64    Decadal variations of the martian surface albedo are generally attributed to removal and depositio
65 actures, laminated outcrop rocks with higher albedo are observed.
66  vapor, lapse rate, clouds, and snow/sea ice albedo are usually considered.
67 al diversity, pigmentation and, consequently albedo, are ubiquitous across the Arctic and the reducti
68  forcings associated with changes in surface albedo as a result of forestation in temperate and borea
69 served effects of no-till farming on surface albedo, as well as possible reductions in soil evaporati
70 eroids eventually break up, we find that low-albedo asteroids are more likely to be destroyed farther
71 edo near-Earth objects and suggests that low-albedo asteroids break up more easily as a result of the
72 Although both bright and dark (high- and low-albedo) asteroids eventually break up, we find that low-
73                                  The extreme albedo asymmetry of Saturn's moon Iapetus, which is abou
74 ow 370 nm and as a drop in single-scattering albedo at 450 nm.
75 ght-absorbing: the average single scattering albedo at 532 nm was 0.36 for the BDS and 0.47 for the T
76 recycling mechanism, rather than the classic albedo-based mechanism.
77 rom Northern Hemisphere forest fires reduced albedo below a critical threshold in the dry snow region
78    The asteroid's surface is dark (estimated albedo between 0.035 and 0.050) and similar in color to
79 ect climate-vegetation feedbacks via surface albedo, Bowen ratio, and carbon cycling.
80  balances changes in surface temperature and albedo, but during summer, fall, and winter, cloud forci
81  estimated that the overall decrease in snow albedo by red pigmented snow algal blooms over the cours
82                The modeled single-scattering albedo can likewise vary from 0.97 to 0.85 at 310 nm (UV
83 the positive forcing induced by decreases in albedo can offset the negative forcing that is expected
84 o identify and quantify enhancement of cloud albedo caused by anthropogenic aerosols in satellite obs
85 ud droplet concentration, optical depth, and albedo caused by anthropogenic aerosols is thought to co
86 efit of biochar systems by 13-22% due to the albedo change as compared to an analysis which disregard
87  to 1.5 times larger than the forcing due to albedo change from the forest.
88                                 Land surface albedo change is considered to be the dominant mechanism
89  simulate the impact of the observed surface albedo change on monthly and annual surface air temperat
90  The identified asymmetric impact of surface albedo change on summer temperature opens new avenues fo
91 h the spatiotemporal pattern of land surface albedo change.
92          Our results suggest that documented albedo changes affect recent climate change and large-sc
93            It is unknown, however, how these albedo changes affect wind circulation, dust transport a
94 cing a positive feedback system in which the albedo changes strengthen the winds that generate the ch
95 ion properties for calculations of BC's snow albedo climate forcing.
96 its RF (including the effects of BC on cloud albedo, cloud coverage, and snow and ice albedo, and the
97 ce displays diverse landforms, terrain ages, albedos, colors, and composition gradients.
98               Ice-albedo feedback due to the albedo contrast between water and ice is a major factor
99 or to the Caloris basin displaying color and albedo contrasts have comparable crater densities and th
100 , showing that terrestrial changes in summer albedo contribute substantially to recent high-latitude
101                Averaged over the globe, this albedo decrease corresponds to a forcing that is 25% as
102  contrast between snow-covered and snow-free albedo (Deltaalpha), which influences predictions of fut
103 nsible for the abrupt change seems to be the albedo discontinuity at the snow-ice edge.
104 lbedo, thus compensating for the increase in albedo due to the dust aerosols themselves.
105 cterize the impacts of boreal forest loss on albedo, eco-physiological and aerodynamic surface proper
106 edo-induced cooling, but during hot days the albedo effect is the dominating factor.
107 ther biophysical processes may overwhelm the albedo effect to generate warming instead.
108 compared to an analysis which disregards the albedo effect.
109 latitude of 30 degrees, owing to the runaway albedo effect.
110                    We argue that such a 'bio-albedo' effect has to be considered in climate models.
111 ce sheet runoff is primarily associated with albedo effects due to deposition of ash sourced from hig
112    Our results indicate that fine-scale snow albedo effects influence the response of both hot and co
113 lobal impacts on land use, water, nutrients, albedo, energy and cost.
114  lower impact on land, water use, nutrients, albedo, energy requirement and cost, so have fewer disad
115 ation, which include changes in land surface albedo, evapotranspiration, and cloud cover also affect
116 specially when snow is lying, and decreasing albedo exerts a positive radiative forcing on climate.
117        The spot is associated with a surface albedo feature identified in images taken by the Cassini
118          The images reveal intricate surface albedo features that suggest aeolian, tectonic and fluvi
119 ld (or "tipping point") beyond which the ice-albedo feedback causes the ice cover to melt away in an
120                                          Ice-albedo feedback due to the albedo contrast between water
121 odels for current climate due to an enhanced albedo feedback during the last deglaciation.
122 ydrological cycles and the key role of cloud albedo feedback for climates over tropical continents.
123                                     The snow-albedo feedback is controlled largely by the contrast be
124 nses expected through the classic vegetation-albedo feedback mechanism.
125 ed progressively in response to positive ice-albedo feedback mechanisms.
126 classical destabilising influence of the ice-albedo feedback on summertime sea ice, we find that duri
127 , and in turn triggered the positive sea-ice albedo feedback process and accelerated the sea ice melt
128                We show that although the ice-albedo feedback promotes the existence of multiple ice-c
129 e a relationship between tree cover and snow-albedo feedback that may be used to accurately constrain
130  suggest that the "plankton-DMS-clouds-earth albedo feedback" hypothesis is less strong a long-term t
131 s of continental ice-volume changes (the ice-albedo feedback) during the late Pleistocene, because eq
132 er) climate, exhibit a stronger (weaker) ice-albedo feedback, and experience greater (weaker) warming
133 r the abruptness of deglaciation include ice albedo feedback, deep-ocean out-gassing during post-glac
134                          Through the sea ice-albedo feedback, models produce a high-latitude surface
135 thickness, and consequent changes in the ice-albedo feedback, represent one of the largest uncertaint
136  Northern Hemisphere and by terrestrial snow-albedo feedback.
137 ly susceptible to destabilization by the ice-albedo feedback.
138 tral-spring insolation combined with sea-ice albedo feedbacks appear to be the key factors responsibl
139 e used to accurately constrain high latitude albedo feedbacks in coupled climate models under current
140 hus reducing the possibility of Arctic cloud albedo feedbacks mitigating future Arctic warming.
141 ch is remarkable given the importance of ice-albedo feedbacks on the radiative forcing of climate.
142 sis that sea-ice thermodynamics can overcome albedo feedbacks proposed to cause sea-ice tipping point
143 climate sensitivity (excluding long-term ice-albedo feedbacks) for our Pliocene-like future (with CO2
144 atmosphere interactions that, along with ice-albedo feedbacks, amplified obliquity cycles.
145  the high latitudes (> 6 K) by lower surface albedo feedbacks, and increased E(ss) in the Eocene by 1
146 rongly by increasing insolation and sediment/albedo feedbacks.
147 because of robust SW water vapor and surface albedo feedbacks.
148  surface interspersed with high- to moderate-albedo fine-grained deposits occurring in part as drifts
149                                  A dark, low-albedo, flat plain composed of basaltic sand and haemati
150 ction, underestimating the single-scattering albedo for both particle morphologies.
151 solated greenhouse gas, aerosol, and surface albedo forcings.
152 m) images from Meridiani Planum reveal a low-albedo, generally flat, and relatively rock-free surface
153 ng treatments each led to large increases in albedo (>30%).
154 r) because multidecadal increases in surface albedo had a larger impact than fire-emitted greenhouse
155            We find that the Arctic planetary albedo has decreased from 0.52 to 0.48 between 1979 and
156 plified during hot summer days, when surface albedo has more impact on the Earth's radiative balance
157 tellite data provide observations of Earth's albedo, i.e., the fraction of incident solar radiation t
158                       Dark material from low-albedo impactors is diffused over time through the Vesta
159 d the surface temperatures and decreased the albedo in northern Greenland, while inhibiting melting i
160 ffect of vegetation exerts strong control on albedo in northern high latitude ecosystems.
161 sociated with a dramatic increase in surface albedo in the area.
162 deposits are found throughout regions of low albedo in the southern highlands of Mars.
163 lysis of linear density waves; ring particle albedos in select ring regions; and never-before-seen ph
164 e find that the summer cooling from cropland albedo increase is strongly amplified during hot summer
165 ing of 0.25 degrees C associated with a 0.09 albedo increase, and a reduction of 22.8 W m(-2) of net
166 nly coated aggregates, the single scattering albedo increases weakly because of the decreased light a
167 e crop residue cover tends to counteract the albedo-induced cooling, but during hot days the albedo e
168  fail to confirm the 6% relative increase in albedo inferred from observations of earthshine from the
169 lavedo (outer coloured part of the peel) and albedo (inner white part) in response to pathogen infect
170 oured part of the peel) when compared to the albedo (inner white part).
171   This study demonstrates that aerosol-cloud-albedo interactions can be directly observed by simultan
172      However, measured relative precision in albedo is always superior to that which would be mathema
173 For the first time, the enhancement in cloud albedo is directly measured on a cloud-by-cloud basis an
174 hile the target material efficiency or x-ray albedo is optimized.
175                                 The range of albedos is among the largest observed on Solar System ro
176  population in general is an even mix of low-albedo (less than ten per cent of incident radiation is
177 rm blackbody models, and may also require an albedo lower than any measured for a planet, very strong
178                          Our results support albedo management as a viable means of reducing DeltaT o
179                        Lunar swirls are high-albedo markings on the Moon that occur in both mare and
180                                      The low-albedo material has spectral similarities and compositio
181                    A rise in dryland surface albedo may represent a previously unidentified feedback
182 h as those related to ocean mixing and cloud albedo, may have been responsible for these climate cond
183 relates the contribution of single clouds to albedo measurements and illustrates the significance of
184                           Based on empirical albedo measurements and literature data of arable soils
185 etation-rainfall feedback nor its underlying albedo mechanism has been convincingly demonstrated usin
186 tion-rainfall feedbacks dominated by surface albedo mechanism.
187 of incident radiation is reflected) and high-albedo (more than ten per cent of incident radiation is
188 ubsequent cloud formation cycles and aerosol albedo near cloud edges.
189 , which explains the apparent excess of high-albedo near-Earth objects and suggests that low-albedo a
190 hundreds of megaelectronvolts) is cosmic-ray albedo neutron decay (CRAND).
191 phere interact with neutral atoms to produce albedo neutrons, which, being prone to beta-decay, are a
192 ced aerosol concentrations can augment cloud albedo not only by increasing total droplet cross-sectio
193          We conclude that the deficit of low-albedo objects near the Sun arises from the super-catast
194                       If we assume a uniform albedo of 0.04, which is typical of values found in the
195  mean radius of about 102 metres assuming an albedo of 0.04.
196  very low reflectance of the nucleus (normal albedo of 0.060 +/- 0.003 at 0.55 micrometers), the spec
197                        We also derive a Bond albedo of 0.18(-0.12)(+0.07) and an altitude dependence
198                           In particular, the albedo of a forested landscape is generally lower than t
199 planets' received radiation, assuming a Bond albedo of approximately 0.3.
200 ing through evaporative cooling, but the low albedo of boreal forests is a positive climate forcing.
201 in allergies as well, and that pectin in the albedo of Citrus unshiu may induce anaphylaxis.
202 is case was induced by pectin present in the albedo of Citrus unshiu, but not by the fruit itself.
203  surface temperatures through increasing the albedo of crop plants; and fertilizing the oceans to inc
204 hat no-till management increases the surface albedo of croplands in summer and that the resulting coo
205                             Due to the lower albedo of forests and their masking effect of highly ref
206 sible elliptical shapes, we find a geometric albedo of in the V photometric band, which establishes t
207      Finally, we estimate that the spherical albedo of Kepler-7b over the Kepler passband is in the r
208  reprocessing model with a bolometric (Bond) albedo of less than 0.54 at the 2sigma confidence level,
209 er of D = 900+129-145 km and a red geometric albedo of pR = 0.070+0.030-0.017.
210 ust and black carbon are known to reduce the albedo of snow and enhance melt.
211                            Single scattering albedo of soot particles depends largely on their organi
212 a density in the range of 1 to 2 g cm-3, the albedo of the binary components is between 0.05 and 0.08
213 ter vapor, and clouds in the troposphere and albedo of the Earth's surface.
214 ould potentially shift the single-scattering albedo of the particle from negative to positive radiati
215  for the mechanism seems to be the increased albedo of the umbrella effect.
216     We quantify this by modifying the canopy albedo of vegetation in prescribed cropland areas in a g
217 naphylaxis after eating a Citrus unshiu, the albedo of which is rich in pectin, have been reported.A
218 ary 2005 that reveal that the mean geometric albedos of satellites embedded within the E ring approxi
219 articles, it accounts for the unusually high albedos of the other satellites orbiting within Saturn's
220 usea only after eating fruit, along with the albedo, of Citrus unshiu.
221 ted, largely because of strong dependence of albedo on cloud liquid water path (LWP), which is inhere
222 a surface temperatures, altitude and surface albedo on local temperatures, which were then calibrated
223 f discernible dependence of optical depth or albedo on modeled sulfate loading, examination of the de
224 arctic sea ice and its effect on the Earth's albedo, ongoing changes in global deep-ocean ventilation
225                                           No albedo or color variations were detected.
226 ures after sunset, uncorrelated with surface albedo or geology.
227 condensation nuclei concentration, and cloud albedo over oceans.
228 se of this historical record, many classical albedo patterns have long been known to shift in appeara
229 anisms are a factor in modifying terrestrial albedo, potentially impacting biosphere feedbacks on pas
230 lassify the surface units according to color/albedo properties, estimate the rates of production of o
231                                     Flavedo, albedo, pulp, seeds, and oil gland content of lemon and
232              The resulting single-scattering albedos ranged from 0.5 to 0.6.
233 ountain environments in Kyrgyzstan, based on albedo reduction and snowmelt models.
234  of surface humidity, an average mean annual albedo reduction of 0.05 has been calculated for applyin
235 ogen concentrations coincide with older, low-albedo regions near the equator, where water ice is unst
236  physical properties such as their sizes and albedos remain unknown.
237 n surface albedo and is reinforced by a land albedo-sea ice feedback.
238 per belt, which may help to explain the high albedos shown by some of these bodies.
239       Scytonemin accumulation decreases soil albedo significantly.
240 nergy budget because of differences in their albedo (solar reflectivity) compared to soils and to nat
241  optical depths (AAOD) and single scattering albedo (SSA) among EC and BrC, using multiwavelength mea
242 d significant absorption with single scatter albedo (SSA) between 0.74 and 0.84.
243 to extinction is known as the single scatter albedo (SSA); thus, the instrument is referred to as the
244 d to calculate the aerosol single scattering albedo (SSA, at 532 nm) for individual truck exhaust plu
245 fficiency, sigma(abs); and single scattering albedo, SSA) from an urban site (Kanpur) in the Indo-Gan
246 ttering versus absorption (single scattering albedo, SSA), along with metrics of the structure of the
247 ate reflectance spectra of the high- and low-albedo surface components.
248 Thermal Emission Spectrometer spectra of low albedo surface materials suggests that a four to one mix
249 l may be challenging, particularly over high albedo surfaces and rigorous instrument calibration is r
250 the volcanic plains in Caloris are higher in albedo than surrounding basin materials and lack spectra
251   Small satellites Hydra and Nix have higher albedos than expected.
252 y glaciating supercooled water, can decrease albedo, thus compensating for the increase in albedo due
253 rbance and predisturbance impacts of dust on albedo to estimate the impact on runoff from the UCRB ac
254 reducing soot emissions, thus restoring snow albedos to pristine high values, would have the double b
255 creasing low cloud formation, which enhances albedo (umbrella effect).
256                    A spatially dominant high-albedo unit having the strong signature of H2O ice contr
257 form, spherical, blackbody emission and zero albedo (unprecedented for planets) is 1,741 K.
258 d on a scale of 200 meters, exhibiting large albedo variations (0.01 to 0.03) and complex geologic re
259 eptember 2007 that reveal distinct color and albedo variations across the surface of this large aster
260 rge-scale weather patterns on Mars, and thus albedo variations are a necessary component of future at
261                                              Albedo variations are restricted to the inner walls of c
262                                        Local albedo variations within and bordering Cassini Regio sug
263  and reradiated because PV plants change the albedo, vegetation, and structure of the terrain.
264           We quantified changes in shortwave albedo via multi-angle, solar-reflectance measurements.
265 asonal RH variations that relate strongly to albedo (via clouds), and that this covariability is mimi
266                   Median cloud-top spherical albedo was enhanced over these episodes, relative to the
267 lication on the carbon cycle and on the soil albedo was integrated into the greenhouse gas (GHG) bala
268 ht materials, often with extremely different albedos, were recently found on Vesta's surface.
269 to agricultural soils can change the surface albedo which could counteract the climate mitigation ben
270 chemical processes, depends strongly on soil albedo, which can be significantly modified by factors s
271  biophysical effects, evapotranspiration and albedo, which in turn are strongly influenced by rainfal
272 the dry season, dramatically increases cloud albedo, which reduces evapotranspiration through its mod
273   Our analyses reveal consistent declines in albedo with increasing tree cover, occurring south of la
274 revious size estimates came from assuming an albedo with the canonical value being 0.04.
275 densation nuclei led to an increase in cloud albedo with the resulting changes in temperature and rad
276 ysical properties of the atmosphere and snow albedo, yet little is known about its emission or deposi

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