ライフサイエンスコーパス: albedo

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