ライフサイエンスコーパス: albedo

1 properties (masses, radii, temperatures and albedos).

2 5 g/L in the juice and 5.24 +/- 0.12 mg/g in albedo.

3 melting, plays a crucial role in decreasing albedo.

4 trations, aerosol emissions, or land surface albedo.

5 and key drivers are changes in snow and ice albedo.

6 cts of seabird-influenced particles on cloud albedo.

7 tem properties, including canopy density and albedo.

8 ed conditions and corresponding variation in albedo.

9 prisingly does not correlate well with model albedo.

10 are possible with no change in water use or albedo.

11 nuclei and possibly influences ice and snow albedo.

12 s by effective density and single-scattering albedo.

13 creases in transpiration, but also to higher albedo.

14 e an important contribution to the planetary albedo.

15 and water ice sublimation rates for a given albedo.

16 positively correlated with shortwave surface albedo.

17 dem bifacial solar cells with back-reflected albedo.

18 cloud droplet number concentration and cloud albedo.

19 olar radiation exposure on litter is surface albedo.

20 oughness-changes that can dramatically alter albedo.

21 d asteroids near the Sun typically have high albedos.

22 natively, improvements in water use (13%) or albedo (34%) can likewise be made with no loss of produc

23 All four moons have high albedos (~50 to 90%) suggestive of a water-ice surface c

24 ce ranges from 0.8 to 1.6 per 0.01 change in albedo, a range of more than 40%.

25 itous across the Arctic and the reduction in albedo accelerates snow melt and increases the time and

26 icating that up to 75% of the variability in albedo across the southwestern GrIS may be attributable

27 The reduction in radiative forcing from albedo alone is equivalent to a carbon emissions reducti

28 Increasing postfire albedo along a south-north climatic gradient was offset

29 el, indicating that the observed interannual albedo alterations strongly influence the martian enviro

30 glacier and sea ice expansion, increased NH albedo, AMOC weakening, more NH cooling, and a consequen

31 The single scattering albedo and aerosol forcing efficiency showed that primar

32 s, longer average lifetime, and higher cloud albedo and cloud fraction compared with unpolluted traje

33 altering surface physical properties (e.g., albedo and emissivity) and land-atmosphere energy exchan

34 feedbacks including changes in land surface albedo and enhanced evapotranspiration.

35 a positive feedback through changes in ocean albedo and evaporation.

36 y the net cooling associated with changes in albedo and evapotranspiration.

37 al surfaces leading to a decrease in surface albedo and eventually higher melting rates.

38 . shrub expansion, resulting in reduction in albedo and greater C fixation in aboveground vegetation

39 Smaller changes in surface albedo and humidity feedbacks also contribute to the ove

40 se losses are accelerating, reducing Earth's albedo and increasing heat absorption.

41 unit that is about a factor of four lower in albedo and is found mostly in the bottoms of cup-like cr

42 cooling is triggered by increases in surface albedo and is reinforced by a land albedo-sea ice feedba

43 cument the Arctic-wide decrease in planetary albedo and its amplifying effect on the warming.

44 climate system via its influence on surface albedo and may offer a simple approach for monitoring fo

45 rosols are hypothesized to enhance planetary albedo and offset some of the warming due to the buildup

46 The single scattering albedo and scattering and absorption cross sections are

47 ls a striking relationship between planetary albedo and sea ice cover, quantities inferred from two i

48 st United States was already decreasing snow albedo and shortening the duration of snow cover by seve

49 However, it is possible that increasing crop albedo and soil carbon sequestration might contribute to

50 increasing aerosol concentration changes the albedo and suppresses precipitation formation not only t

51 responsible for a poleward shift of runoff, albedo and surface temperature records over the Greenlan

52 c implications for our understanding of snow albedo and the processing of atmospheric BC aerosol in s

53 istent with confirmed mid-latitude RSL; (ii) albedo and thermal inertia values are comparable to thos

54 Observed relationships between albedo and tree cover differ substantially between snow-

55 and coupled climate model representations of albedo and tree cover for the boreal and Arctic region.

56 by narrowing the inter-model spreads of ice-albedo and water vapor feedbacks, and better understandi

57 e then used to determine the PD and PI cloud albedos and, thus, the effect of anthropogenic aerosols

58 ll lead to decreases in mean annual postfire albedo, and hence a decreasing strength of the negative

59 al sulfur cycling(2) and affects the Earth's albedo, and potentially climate, via sulfate aerosol and

60 article (INP), BC could affect the lifetime, albedo, and radiative properties of clouds containing bo

61 oud albedo, cloud coverage, and snow and ice albedo, and the optical consequences of aerosol mixing)

62 thinning through feedbacks altering surface albedo, and to potentially seed recently deglaciated ter

63 conversion of forests to wetlands increases albedo: and bulk surface conductance for water vapour an

64 ture changes unrelated to changes in surface albedo are an important contributor to the overall cooli

65 As models with non-zero albedo are cooler, this essentially eliminates uniform b

66 Decadal variations of the martian surface albedo are generally attributed to removal and depositio

67 rategies aimed at increasing green cover and albedo are more efficient in dry regions, whereas the ch

68 The intensity of the OH feature and low albedo are similar to thermally and/or shock-metamorphos

69 vapor, lapse rate, clouds, and snow/sea ice albedo are usually considered.

70 al diversity, pigmentation and, consequently albedo, are ubiquitous across the Arctic and the reducti

71 served effects of no-till farming on surface albedo, as well as possible reductions in soil evaporati

72 eroids eventually break up, we find that low-albedo asteroids are more likely to be destroyed farther

73 edo near-Earth objects and suggests that low-albedo asteroids break up more easily as a result of the

74 Although both bright and dark (high- and low-albedo) asteroids eventually break up, we find that low-

75 The extreme albedo asymmetry of Saturn's moon Iapetus, which is abou

76 ow 370 nm and as a drop in single-scattering albedo at 450 nm.

77 ght-absorbing: the average single scattering albedo at 532 nm was 0.36 for the BDS and 0.47 for the T

78 forming a Snowball Earth because of reduced albedo at low latitudes.

79 Bennu is a low-albedo B-type asteroid(2) that has been linked to organi

80 recycling mechanism, rather than the classic albedo-based mechanism.

81 these relationships and predicting postfire albedo becomes increasingly important as the climate cha

82 rom Northern Hemisphere forest fires reduced albedo below a critical threshold in the dry snow region

83 ect climate-vegetation feedbacks via surface albedo, Bowen ratio, and carbon cycling.

84 estimated that the overall decrease in snow albedo by red pigmented snow algal blooms over the cours

85 The modeled single-scattering albedo can likewise vary from 0.97 to 0.85 at 310 nm (UV

86 limate (influencing atmospheric circulation, albedo, carbon storage, etc.) and ecology (harboring the

87 efit of biochar systems by 13-22% due to the albedo change as compared to an analysis which disregard

88 to 1.5 times larger than the forcing due to albedo change from the forest.

89 ) over an analysis period of 50 years for an albedo change in a pavement surface.

90 Land surface albedo change is considered to be the dominant mechanism

91 simulate the impact of the observed surface albedo change on monthly and annual surface air temperat

92 The identified asymmetric impact of surface albedo change on summer temperature opens new avenues fo

93 Analysis of a hypothetical albedo change to all darker pavements in the US would pr

94 h the spatiotemporal pattern of land surface albedo change.

95 Our results suggest that documented albedo changes affect recent climate change and large-sc

96 It is unknown, however, how these albedo changes affect wind circulation, dust transport a

97 cing a positive feedback system in which the albedo changes strengthen the winds that generate the ch

98 ion properties for calculations of BC's snow albedo climate forcing.

99 its RF (including the effects of BC on cloud albedo, cloud coverage, and snow and ice albedo, and the

100 ce displays diverse landforms, terrain ages, albedos, colors, and composition gradients.

101 and are attributed to reductions in snowpack albedo combined with enhanced post-depositional melting.

102 Ice-albedo feedback due to the albedo contrast between water and ice is a major factor

103 or to the Caloris basin displaying color and albedo contrasts have comparable crater densities and th

104 t appear to contribute equally to the Arctic albedo decline.

105 Averaged over the globe, this albedo decrease corresponds to a forcing that is 25% as

106 h this atmospheric response, SIC and surface albedo decrease with an increase in the surface net shor

107 contrast between snow-covered and snow-free albedo (Deltaalpha), which influences predictions of fut

108 nsible for the abrupt change seems to be the albedo discontinuity at the snow-ice edge.

109 Over longer-term (> 5 years), increases in albedo dominated the surface radiative budget resulting

110 The change in planetary albedo due to aerosol-cloud interactions during the indu

111 lbedo, thus compensating for the increase in albedo due to the dust aerosols themselves.

112 cterize the impacts of boreal forest loss on albedo, eco-physiological and aerodynamic surface proper

113 assessments, location-specific models of the albedo effect for pavements are required.

114 edo-induced cooling, but during hot days the albedo effect is the dominating factor.

115 ther biophysical processes may overwhelm the albedo effect to generate warming instead.

116 latitude of 30 degrees, owing to the runaway albedo effect.

117 compared to an analysis which disregards the albedo effect.

118 We argue that such a 'bio-albedo' effect has to be considered in climate models.

119 ce sheet runoff is primarily associated with albedo effects due to deposition of ash sourced from hig

120 lobal impacts on land use, water, nutrients, albedo, energy and cost.

121 lower impact on land, water use, nutrients, albedo, energy requirement and cost, so have fewer disad

122 ation, which include changes in land surface albedo, evapotranspiration, and cloud cover also affect

123 ld (or "tipping point") beyond which the ice-albedo feedback causes the ice cover to melt away in an

124 Ice-albedo feedback due to the albedo contrast between water

125 odels for current climate due to an enhanced albedo feedback during the last deglaciation.

126 ydrological cycles and the key role of cloud albedo feedback for climates over tropical continents.

127 The snow-albedo feedback is controlled largely by the contrast be

128 nses expected through the classic vegetation-albedo feedback mechanism.

129 ed progressively in response to positive ice-albedo feedback mechanisms.

130 classical destabilising influence of the ice-albedo feedback on summertime sea ice, we find that duri

131 , and in turn triggered the positive sea-ice albedo feedback process and accelerated the sea ice melt

132 We show that although the ice-albedo feedback promotes the existence of multiple ice-c

133 We show that the ice-albedo feedback spread explains uncertainties in polar r

134 e a relationship between tree cover and snow-albedo feedback that may be used to accurately constrain

135 ingly positive in warmer climates, while the albedo feedback weakens as the ice and snow melt.

136 suggest that the "plankton-DMS-clouds-earth albedo feedback" hypothesis is less strong a long-term t

137 s of continental ice-volume changes (the ice-albedo feedback) during the late Pleistocene, because eq

138 er) climate, exhibit a stronger (weaker) ice-albedo feedback, and experience greater (weaker) warming

139 r the abruptness of deglaciation include ice albedo feedback, deep-ocean out-gassing during post-glac

140 Through the sea ice-albedo feedback, models produce a high-latitude surface

141 Northern Hemisphere and by terrestrial snow-albedo feedback.

142 ly susceptible to destabilization by the ice-albedo feedback.

143 his warming can be attributed to the surface albedo feedback.

144 melted surface areas is the key component of albedo feedback.

145 reason for this Arctic Amplification is the albedo feedback.

146 over melted areas significantly reduces the albedo feedback.

147 tral-spring insolation combined with sea-ice albedo feedbacks appear to be the key factors responsibl

148 e used to accurately constrain high latitude albedo feedbacks in coupled climate models under current

149 hus reducing the possibility of Arctic cloud albedo feedbacks mitigating future Arctic warming.

150 ch is remarkable given the importance of ice-albedo feedbacks on the radiative forcing of climate.

151 sis that sea-ice thermodynamics can overcome albedo feedbacks proposed to cause sea-ice tipping point

152 climate sensitivity (excluding long-term ice-albedo feedbacks) for our Pliocene-like future (with CO2

153 the high latitudes (> 6 K) by lower surface albedo feedbacks, and increased E(ss) in the Eocene by 1

154 because of robust SW water vapor and surface albedo feedbacks.

155 rongly by increasing insolation and sediment/albedo feedbacks.

156 used for unambiguous metabolic profiling of albedo, flavedo and juice samples.

157 nodispersions made from yellow passion fruit albedo flour and microalgae carotenoid extract presented

158 Yellow passion fruit albedo flour as a polymeric material in the production o

159 investigated the use of yellow passion fruit albedo flour as an encapsulating material for the produc

160 ar absorption from reductions in the surface albedo, following loss of sea ice and land snow.

161 debris darkens the snowpack and lowers snow albedo for 15 winters following fire, using measurements

162 ction, underestimating the single-scattering albedo for both particle morphologies.

163 Albedo forcings are spatially and temporally heterogeneo

164 solated greenhouse gas, aerosol, and surface albedo forcings.

165 ission through the canopy and decreased snow albedo from deposition of light-absorbing impurities.

166 fine-grained sediments and formation of low-albedo gravel-mantled surfaces leads to an increase in n

167 ng treatments each led to large increases in albedo (>30%).

168 as exposed to a high UV/high visible surface albedo had lost 1.4 and 2.5% more mass than litter expos

169 Our results demonstrate that surface albedo has a small but significant effect on photodecomp

170 We find that the Arctic planetary albedo has decreased from 0.52 to 0.48 between 1979 and

171 plified during hot summer days, when surface albedo has more impact on the Earth's radiative balance

172 e, discrete geological units, and noticeable albedo heterogeneity.

173 Dark material from low-albedo impactors is diffused over time through the Vesta

174 ntify the GWP impacts of increasing pavement albedo in 14 cities across various climate zones in the

175 d the surface temperatures and decreased the albedo in northern Greenland, while inhibiting melting i

176 ffect of vegetation exerts strong control on albedo in northern high latitude ecosystems.

177 bsolute reduction in the Arctic mean surface albedo in spring and summer during 1982 to 2014.

178 sociated with a dramatic increase in surface albedo in the area.

179 deposits are found throughout regions of low albedo in the southern highlands of Mars.

180 e find that the summer cooling from cropland albedo increase is strongly amplified during hot summer

181 ing of 0.25 degrees C associated with a 0.09 albedo increase, and a reduction of 22.8 W m(-2) of net

182 nly coated aggregates, the single scattering albedo increases weakly because of the decreased light a

183 e crop residue cover tends to counteract the albedo-induced cooling, but during hot days the albedo e

184 lavedo (outer coloured part of the peel) and albedo (inner white part) in response to pathogen infect

185 oured part of the peel) when compared to the albedo (inner white part).

186 This study demonstrates that aerosol-cloud-albedo interactions can be directly observed by simultan

187 The influence of fire on surface albedo is a predominantly negative forcing in boreal for

188 However, measured relative precision in albedo is always superior to that which would be mathema

189 For the first time, the enhancement in cloud albedo is directly measured on a cloud-by-cloud basis an

190 r, how these variables interact to influence albedo is not well understood, and quantifying these rel

191 hile the target material efficiency or x-ray albedo is optimized.

192 The range of albedos is among the largest observed on Solar System ro

193 population in general is an even mix of low-albedo (less than ten per cent of incident radiation is

194 rm blackbody models, and may also require an albedo lower than any measured for a planet, very strong

195 fitted by a bare-rock model with a low Bond albedo (lower than 0.2 at two standard deviations).

196 Our results support albedo management as a viable means of reducing DeltaT o

197 rtime, while potentially negative effects of albedo management during winter are mitigated by the sea

198 Lunar swirls are high-albedo markings on the Moon that occur in both mare and

199 The low-albedo material has spectral similarities and compositio

200 High-albedo materials reflect more solar radiation and, there

201 A rise in dryland surface albedo may represent a previously unidentified feedback

202 h as those related to ocean mixing and cloud albedo, may have been responsible for these climate cond

203 relates the contribution of single clouds to albedo measurements and illustrates the significance of

204 Based on empirical albedo measurements and literature data of arable soils

205 etation-rainfall feedback nor its underlying albedo mechanism has been convincingly demonstrated usin

206 tion-rainfall feedbacks dominated by surface albedo mechanism.

207 cant negative relationship between broadband albedo (Moderate Resolution Imaging Spectroradiometer [M

208 of incident radiation is reflected) and high-albedo (more than ten per cent of incident radiation is

209 ubsequent cloud formation cycles and aerosol albedo near cloud edges.

210 , which explains the apparent excess of high-albedo near-Earth objects and suggests that low-albedo a

211 hundreds of megaelectronvolts) is cosmic-ray albedo neutron decay (CRAND).

212 phere interact with neutral atoms to produce albedo neutrons, which, being prone to beta-decay, are a

213 We conclude that the deficit of low-albedo objects near the Sun arises from the super-catast

214 mean radius of about 102 metres assuming an albedo of 0.04.

215 very low reflectance of the nucleus (normal albedo of 0.060 +/- 0.003 at 0.55 micrometers), the spec

216 We also derive a Bond albedo of 0.18(-0.12)(+0.07) and an altitude dependence

217 planets' received radiation, assuming a Bond albedo of approximately 0.3.

218 ing through evaporative cooling, but the low albedo of boreal forests is a positive climate forcing.

219 in allergies as well, and that pectin in the albedo of Citrus unshiu may induce anaphylaxis.

220 is case was induced by pectin present in the albedo of Citrus unshiu, but not by the fruit itself.

221 surface temperatures through increasing the albedo of crop plants; and fertilizing the oceans to inc

222 hat no-till management increases the surface albedo of croplands in summer and that the resulting coo

223 Due to the lower albedo of forests and their masking effect of highly ref

224 sible elliptical shapes, we find a geometric albedo of in the V photometric band, which establishes t

225 Finally, we estimate that the spherical albedo of Kepler-7b over the Kepler passband is in the r

226 reprocessing model with a bolometric (Bond) albedo of less than 0.54 at the 2sigma confidence level,

227 The contrasting albedo of sea ice and dark melted surface areas is the k

228 ust and black carbon are known to reduce the albedo of snow and enhance melt.

229 Single scattering albedo of soot particles depends largely on their organi

230 ter vapor, and clouds in the troposphere and albedo of the Earth's surface.

231 tophycean "glacier algae" lower the bare ice albedo of the Greenland Ice Sheet (GrIS), amplifying sum

232 ould potentially shift the single-scattering albedo of the particle from negative to positive radiati

233 for the mechanism seems to be the increased albedo of the umbrella effect.

234 We quantify this by modifying the canopy albedo of vegetation in prescribed cropland areas in a g

235 naphylaxis after eating a Citrus unshiu, the albedo of which is rich in pectin, have been reported.A

236 ary 2005 that reveal that the mean geometric albedos of satellites embedded within the E ring approxi

237 articles, it accounts for the unusually high albedos of the other satellites orbiting within Saturn's

238 usea only after eating fruit, along with the albedo, of Citrus unshiu.

239 a surface temperatures, altitude and surface albedo on local temperatures, which were then calibrated

240 examined the influence of different surface albedos on the photodegradation of two varieties of sorg

241 arctic sea ice and its effect on the Earth's albedo, ongoing changes in global deep-ocean ventilation

242 condensation nuclei concentration, and cloud albedo over oceans.

243 se of this historical record, many classical albedo patterns have long been known to shift in appeara

244 anisms are a factor in modifying terrestrial albedo, potentially impacting biosphere feedbacks on pas

245 find direct evidence of increased planetary albedo primarily through increased drop concentration ([

246 Here we developed a MODIS-derived 'blue sky' albedo product and a novel machine learning modeling fra

247 Flavedo, albedo, pulp, seeds, and oil gland content of lemon and

248 The resulting single-scattering albedos ranged from 0.5 to 0.6.

249 ountain environments in Kyrgyzstan, based on albedo reduction and snowmelt models.

250 of surface humidity, an average mean annual albedo reduction of 0.05 has been calculated for applyin

251 data are used to unravel the causes of this albedo reduction.

252 Mean albedo reductions due to light-absorbing impurities were

253 ogen concentrations coincide with older, low-albedo regions near the equator, where water ice is unst

254 /high visible and low UV/low visible surface albedo, respectively.

255 n surface albedo and is reinforced by a land albedo-sea ice feedback.

256 per belt, which may help to explain the high albedos shown by some of these bodies.

257 Scytonemin accumulation decreases soil albedo significantly.

258 he Arctic snow cover, ice cover, and surface albedo since the 1980s.

259 nergy budget because of differences in their albedo (solar reflectivity) compared to soils and to nat

260 optical depths (AAOD) and single scattering albedo (SSA) among EC and BrC, using multiwavelength mea

261 d significant absorption with single scatter albedo (SSA) between 0.74 and 0.84.

262 sulting in higher particle single-scattering albedo (SSA).

263 to extinction is known as the single scatter albedo (SSA); thus, the instrument is referred to as the

264 d to calculate the aerosol single scattering albedo (SSA, at 532 nm) for individual truck exhaust plu

265 fficiency, sigma(abs); and single scattering albedo, SSA) from an urban site (Kanpur) in the Indo-Gan

266 ttering versus absorption (single scattering albedo, SSA), along with metrics of the structure of the

267 ate reflectance spectra of the high- and low-albedo surface components.

268 l may be challenging, particularly over high albedo surfaces and rigorous instrument calibration is r

269 The albedo, texture, particle size and roughness are beyond

270 the volcanic plains in Caloris are higher in albedo than surrounding basin materials and lack spectra

271 Small satellites Hydra and Nix have higher albedos than expected.

272 Assuming an Earth-like albedo, the equilibrium temperature of the 21.8-day plan

273 Increasing pavement albedo, therefore, has been considered as a technologica

274 y glaciating supercooled water, can decrease albedo, thus compensating for the increase in albedo due

275 rbance and predisturbance impacts of dust on albedo to estimate the impact on runoff from the UCRB ac

276 creasing low cloud formation, which enhances albedo (umbrella effect).

277 the important cooling effect exerted by ice albedo under high levels of atmospheric carbon dioxide.

278 framework to predict fire-driven changes in albedo under historical and future climate scenarios acr

279 l mean cooling of -1.77 +/- 1.35 W/m(2) from albedo under historical climate conditions (1971-2000) i

280 A spatially dominant high-albedo unit having the strong signature of H2O ice contr

281 form, spherical, blackbody emission and zero albedo (unprecedented for planets) is 1,741 K.

282 eptember 2007 that reveal distinct color and albedo variations across the surface of this large aster

283 rge-scale weather patterns on Mars, and thus albedo variations are a necessary component of future at

284 and reradiated because PV plants change the albedo, vegetation, and structure of the terrain.

285 We quantified changes in shortwave albedo via multi-angle, solar-reflectance measurements.

286 asonal RH variations that relate strongly to albedo (via clouds), and that this covariability is mimi

287 s the net warming effect (+1.5 degrees C) of albedo warming (+2.3 degrees C) and emissivity cooling e

288 lication on the carbon cycle and on the soil albedo was integrated into the greenhouse gas (GHG) bala

289 ht materials, often with extremely different albedos, were recently found on Vesta's surface.

290 nditions will modify the change in planetary albedo when sea ice melts.

291 to agricultural soils can change the surface albedo which could counteract the climate mitigation ben

292 chemical processes, depends strongly on soil albedo, which can be significantly modified by factors s

293 biophysical effects, evapotranspiration and albedo, which in turn are strongly influenced by rainfal

294 the dry season, dramatically increases cloud albedo, which reduces evapotranspiration through its mod

295 ) the cooling effect from long-term postfire albedo will be reduced by 15%-28% due to climate change.

296 This wind-albedo-wind feedback also leads to an increase in the fr

297 Our analyses reveal consistent declines in albedo with increasing tree cover, occurring south of la

298 densation nuclei led to an increase in cloud albedo with the resulting changes in temperature and rad

299 and indirect impacts of glacier algae on ice albedo, with a significant negative relationship between

300 ysical properties of the atmosphere and snow albedo, yet little is known about its emission or deposi