ライフサイエンスコーパス: snow

1 ed to us identified 22 patients with 'visual snow'.

2 produces memory for a nonstudied word (e.g., snow).

3 turn are strongly influenced by rainfall and snow.

4 nts and geochemical analytes measured in the snow.

5 gnificantly influence Hg(0) flux from Arctic snow.

6 the atmosphere and co-precipitated with the snow.

7 w much Hg is transported with melting Arctic snow.

8 ients had first degree relatives with visual snow.

9 he production of nitrite and nitrous acid in snow.

10 dissolved organic matter (DOM) in Antarctic snow.

11 f consideration of the vertical structure of snow.

12 ertime temperature can modify this effect of snow.

13 n the oceanic water column, sea ice or polar snow.

14 f four cities that are exposed to wintertime snow.

15 atologic knowledge in the cities impacted by snow.

16 sectioned peat cores (4 sites, n = 161), and snow (7 sites, n = 19) from ombrotrophic bogs in the AOS

17 summation operatorPFAS) in freshly deposited snow (760-3600 pg L(-1)) were 1 order of magnitude highe

18 tude higher than those in background surface snow (82-430 pg L(-1)).

19 Here we show that red snow, a common algal habitat blooming after the onset of

20 fate and dynamics and reveals the effect of snow accumulation and melt processes on the fate of semi

21 lly- to annually-resolved ice core record of snow accumulation from Mt.

22 ng feedback, long-term impacts of changes in snow accumulation on CH4 fluxes remain uncertain.

23 the balance between areas with more or less snow accumulation than they are currently facing.

24 rdwood forest to determine how reductions in snow accumulation, expected with climate change, directl

25 but some areas will experience decreases in snow accumulation.

26 ing and subsequent loss of the entire annual snow accumulation.

27 ce mixing model showed that DOC deposited in snow across the Icefield reflects fossil fuel combustion

28 Identical declines in a long-term snow-addition experiment definitively identified increas

29 % and 90-100% in medium- (MS) and high- (HS) snow additions relative to Ambient, contributing to incr

30 e combined with UV irradiation intensity and snow age on Hg(0) flux from Arctic snow and (2) elucidat

31 amber, snow temperature, UV irradiation, and snow age were found to significantly influence Hg(0) flu

32 We estimated that the overall decrease in snow albedo by red pigmented snow algal blooms over the

33 The snow-albedo feedback is controlled largely by the contra

34 strate a relationship between tree cover and snow-albedo feedback that may be used to accurately cons

35 Our data reveal that red pigmented snow algae are cosmopolitan as well as independent of lo

36 all decrease in snow albedo by red pigmented snow algal blooms over the course of one melt season can

37 The patterns for snow algal diversity, pigmentation and, consequently alb

38 nsity and snow age on Hg(0) flux from Arctic snow and (2) elucidate the effect of temperature on snow

39 ack carbon are known to reduce the albedo of snow and enhance melt.

40 ower elevation plots, which accumulated less snow and experienced more soil temperature variability d

41 cedented rate and key drivers are changes in snow and ice albedo.

42 y show that the production of metabolites in snow and ice algae is driven mainly by nitrogen and less

43 abitats on glacial surfaces are dominated by snow and ice algae, which are the critical players and t

44 mple water supply during summer from melting snow and ice as well as thawing permafrost, contrasting

45 Black carbon (BC) in haze and deposited on snow and ice can have strong effects on the radiative ba

46 Measurements of Pb concentration in snow and ice core samples from Antarctica show that rece

47 ng is expected to reduce northern hemisphere snow and ice cover, continued increase in atmospheric gr

48 cularly for those that experience periods of snow and ice cover.

49 Penitentes are snow and ice features formed by erosion that, on Earth,

50 soluble chemical species that are trapped in snow and ice offer the possibility to investigate past c

51 in the photochemical processes that occur in snow and ice, and DOM could be a significant, but to dat

52 to date poorly understood, oxidant source in snow and ice.

53 Snow and lake water Cl(-)/ClO4(-) ratios suggest evapoco

54 Enhanced concentrations were observed in snow and meltpond samples, implying atmospheric depositi

55 ow depths, and collected over 100 samples of snow and meltwater for chemical analysis in 2008 and 200

56 om the Central Arctic Ocean and shelf water, snow and meltwater samples were collected in 2012; 13 PF

57 ative experiment with additions of rainfall, snow and N was conducted to test their effects on ECE in

58 t limited water resources (such as dew, fog, snow and rain), yet the mechanisms for water collection

59 that sea-ice OCP burdens originate from both snow and seawater.

60 ere detected at large distances (>100 km) in snow and surface lake sediments, suggesting that the imp

61 en support by diffusion from the surrounding snow and the clearance of CO2 by diffusion and absorptio

62 lifornia, water storage deforms the crust as snow and water accumulates during the wet winter months.

63 active environment and chemical processes in snow, and a lack of consideration of the vertical struct

64 dry world, even a small amount of rain, fog, snow, and even atmospheric humidity can be adequate for

65 e influenced Hg photoreduction kinetics when snow approached the melting point (>-2 degrees C), where

66 sediments, coastal marine waters and surface snow are known sites for MeHg production.

67 e distribution of mercury within sea ice and snow are poorly understood.

68 nfirmed large petcoke particles (>10 mum) in snow at near-field sites.

69 nd their masking effect of highly reflective snow, available energy is lower in wetlands, especially

70 Breathing under snow, e.g. while buried by a snow avalanche, is possible in the presence of an air po

71 8 (95% CI, 1.50-5.94; P = .002), presence of snow banking had an adjusted HR of 3.71 (95% CI, 1.18-11

72 whole-community microbial DNA from Antarctic snow, brine, sea ice and sea water to elucidate potentia

73 C7-14 perfluoroalkyl carboxylates (PFCAs) in snow but limited to the transited areas of the research

74 Photochemical reactions in snow can have an important impact on the composition of

75 warm spells in winter with rainfall (rain-on-snow) can cause 'icing', restricting access to forage, r

76 event involving the genetic admixture of the snow-capped (Lepidothrix nattereri) and opal-crowned (Le

77 Crown patches are highly reflective white (snow-capped manakin) or iridescent whitish-blue to pink

78 of over snow vehicles (OSV), including five snow coaches and one snowmobile, were measured on a desi

79 eposition, surface snow, streams from melted snow, coastal seawater, and plankton samples were collec

80 Snow core samples had a mean ClO4(-) concentration of 0.

81 However, the factors that generate the TP snow cover (TPSC) anomalies at the intraseasonal time-sc

82 at High Arctic sites with sufficient winter snow cover and ample water supply during summer from mel

83 and attributing the phenological changes in snow cover are essential for meteorological, hydrologica

84 perature that is tightly interconnected with snow cover distribution and persistence.

85 d to increasing air temperatures and reduced snow cover duration in spring and fall.

86 a possible influence of decrease in seasonal snow cover duration, which could have exposed larger bas

87 olour molting species confronting decreasing snow cover duration.

88 Snow cover loss related mortality spans approximately 10

89 We focus on wintertime snow cover over the central and eastern TP, where the in

90 However, snow cover phenology changes have not been well document

91 Changes in the snow cover phenology led to contrasting anomalies of sno

92 ntrasting changes in the Northern Hemisphere snow cover phenology.

93 the growing season as a result of decreased snow cover will not necessarily result in greater tundra

94 ), known as the third pole of the Earth, has snow cover with intraseasonal to decadal variability tha

95 gional abrupt changes in the ocean, sea ice, snow cover, permafrost, and terrestrial biosphere that a

96 and elevates disease incidence under reduced snow cover.

97 a deep thawed layer as can occur with thick snow cover.

98 he region arising from decreased sea ice and snow cover.

99 soil temperatures, historically buffered by snow cover.

100 s except for strong wintertime dependence on snow covered conditions and corresponding variation in a

101 emisphere live in regions that are regularly snow covered in winter, there is little hydro-climatolog

102 s controlled largely by the contrast between snow-covered and snow-free albedo (Deltaalpha), which in

103 and tree cover differ substantially between snow-covered and snow-free periods, and among plant func

104 phytoplankton spring bloom observed beneath snow-covered Arctic pack ice.

105 ct on the composition of the atmosphere over snow-covered areas as well as on the composition of the

106 Phytoplankton blooms beneath snow-covered ice might become more common and widespread

107 g the spring flood compared to the preceding snow-covered period.

108 that the bloom developed in situ despite the snow-covered sea ice.

109 Median fluxes over litter- and snow-covered soils were lower than over bare soils, and

110 drological conditions: during the snow-free, snow-covered, and spring-flood seasons.

111 n logging, which was done during winter with snow covering the ground.

112 We show that the presence of snow critically changes the impact that city design has

113 ms ordered hexagonally symmetric structures (snow crystals) in its solid state, however not as liquid

114 n freshly deposited snow relative to surface snow (CSD/CSnow), snowmelt (CSD/CSM), and seawater (CSD/

115 c BC causes the majority (60% on average) of snow darkening.

116 e observations with climate reanalysis data, snow data assimilation model output, and satellite spect

117 otential was consistent with detrital marine snow degradation.

118 se in CO2 were mainly associated with higher snow densities and led to premature interruption due to

119 However, subjects in the low snow density group demonstrated a higher frequency of te

120 ing into snow with an artificial air pocket, snow density had a direct influence on ventilation, oxyg

121 into soils (i.e., soil moisture, snow depth, snow density).

122 To evaluate the role of snow deposition as an input of PFAS to Maritime Antarcti

123 These trends suggest that snow deposition, scavenging sea-salt aerosol bound PFAS,

124 input of PFAS to Maritime Antarctica, fresh snow deposition, surface snow, streams from melted snow,

125 rom ice and snow melting and consistent with snow depositional inputs.

126 ce (Normalized Difference Vegetation Index), snow depth and temperature, and the best fit model inclu

127 ly observed responses of plants to increased snow depth at the same experimental site, the ECM fungal

128 ance, but at this intermediate canopy level, snow depth had negative effects on winter survival of se

129 son (Jun-Aug) after 18 years of experimental snow depth increases and decreases.

130 canopy closure, prescribed fire, and winter snow depth on demographic transitions of each species.

131 Here, we focus on the effects of increased snow depth, and as a consequence, increased winter soil

132 gs as a function of both winter coldness and snow depth, both of which are expected to decline with c

133 explanations, including forest disturbance, snow depth, or permafrost melting, could not explain pat

134 Snow depth, probably associated with digging for winter

135 o diffusion into soils (i.e., soil moisture, snow depth, snow density).

136 We measured discharge, made 10000 snow depths, and collected over 100 samples of snow and

137 Robert W. Snow discusses the importance of empirical evidence, suc

138 ic receiving lake, background lake water and snow distal from the mine.

139 lvic and humic acids and an authentic Arctic snow DOM sample isolated by solid phase extraction, indi

140 The problem is akin to the snow-drift problem in game theory; that is to say, if en

141 Dominated by changes in De, snow duration days (Dd) was shorter in duration by 5.57

142 Breathing under snow, e.g. while buried by a snow avalanche, is possible

143 s data from 2001 to 2014 points out that the snow end date (De) advanced by 5.11 (+/-2.20) days in no

144 Deeper snow enhanced CH4 production within newly thawed soils,

145 trongly, and negatively, related to 'rain-on-snow' events.

146 001-0.004 d(-1)) and nondetectable in melted snow, except at one site (km = 0.0007 d(-1)).

147 tmospheric conditions lead to greater winter snow fall, changes in the ECM fungal community will like

148 data from soil samples taken at a long-term snow fence experiment in Northern Alaska.

149 ce habitats and on 12 glaciers and permanent snow fields in Svalbard and Arctic Sweden.

150 tures occur frequently in nature as flowers, snow-flakes, leaves and so on.

151 Here, we show that, for the snow flea antifreeze protein (sfAFP), stability and coop

152 ation and was likely conducive to marine oil snow formation, analysis of the MiSeq-derived 16S rRNA d

153 A significant amount of marine oil snow formed in the water column of the northern Gulf of

154 ely by the contrast between snow-covered and snow-free albedo (Deltaalpha), which influences predicti

155 iffer substantially between snow-covered and snow-free periods, and among plant functional type.

156 Watering during the snow-free season alleviated some negative effects of war

157 s particularly strong towards the end of the snow-free season, and it has intensified in recent years

158 ifferent hydrological conditions: during the snow-free, snow-covered, and spring-flood seasons.

159 The observed distributions of snow frequency show that snow-rain transition zones are

160 igin and nature of glacier DOC, we collected snow from 10 locations along a transect across the Junea

161 These results suggest that surface snow from western regions of Greenland contains exogenou

162 from measurements in air, sea ice, seawater, snow, frost flowers, and brine.

163 ions and case studies (influenza A in lesser snow geese and Yersinia pestis in coyotes), we argue tha

164 g these actions, the increasing abundance of snow geese has since induced a state of satiation in har

165 dance and destructive foraging behaviours of snow geese have created a trophic cascade that reduces (

166 read of the devastating trophic cascade that snow geese have triggered.

167 Historically, juvenile snow geese suffered from density-related degradation of

168 With the aim of controlling overabundant snow geese, the Conservation Order amendment to the Inte

169 Snow goose family groups eventually responded to their o

170 Canada and snow goose goslings fed low-protein diets had reduced gr

171 red growth trajectories of Canada and lesser snow goose goslings raised on grass-based diets that dif

172 In contrast, snow goose goslings were unable to survive on the low-pr

173 In contrast, snow goslings were similar in mass and structural size t

174 able to support Canada goslings better than snow goslings which require higher-quality forage to sur

175 5 change in emissivity due to mineralogy and snow grain size can cause a 1.8-2.0 W m(-2) difference i

176 Our observations show that lava-snow heat transfer is slow, and that styles of lava prop

177 in snowpack; however, DOM photochemistry in snow/ice has received little attention in the literature

178 ts further imply that local accumulations of snow/ice within gullies were much more voluminous than c

179 Deeper snow increased soil wetness and warming, reducing soil %

180 Since snow insulates soil, a decreased snow pack can increase

181 inside the snowpack, producing rigorous lava-snow interaction via meltwater percolation down into the

182 he rigid, snowpack substrate with minor lava-snow interaction.

183 Our data suggest that 'visual snow' is a unique visual disturbance clinically distinct

184 d areas as well as on the composition of the snow itself.

185 The aromatic fractions of snow, lake sediment, and air samples collected during 20

186 he same heterocyclic aromatics identified in snow, lake sediments, and air were observed in extracts

187 central Greenland was extracted from recent snow layers at NorthGRIP (75.1 degrees N, 042.3 degrees

188 e hybridization between the ancestors of the snow leopard and lion lineages.

189 must have accreted material from beyond the 'snow line', which is the distance from the Sun at which

190 Signatures of the carbon monoxide snow-line (at temperatures of around 20 kelvin) have rec

191 The spectral behaviour across the snow-line confirms recent model predictions: dust fragme

192 A snow-line is the region of a protoplanetary disk at whic

193 But the water snow-line of a protoplanetary disk (at temperatures of m

194 nclude that the outburst has moved the water snow-line.

195 ur results imply that highly dynamical water snow-lines must be considered when developing models of

196 Snow-lines play a crucial role in disk evolution by prom

197 ied, emerging drivers of disturbance such as snow loss and subsequent mortality are much less documen

198 Climate warming-induced glacier and snow loss clearly imperils the persistence of L. tumana

199 region has been linked to warmer winters and snow loss.

200 moval than control plots during all years of snow manipulation.

201 Therefore, snow manipulations in this system can be used to predict

202 rray experiment supported the results of the snow manipulations.

203 The snow-masking effect of vegetation exerts strong control

204 However in winter, the presence of snow masks the influence of the built and vegetated frac

205 ctic and the reduction in albedo accelerates snow melt and increases the time and area of exposed bar

206 if decreased water availability from earlier snow melt and warmer summer temperatures lead to earlier

207 climate change is expected to cause earlier snow melt but may not change the last frost-free day of

208 After snow melt, the cities return to being strongly controlle

209 tial, with air temperatures warming prior to snow melt, which preceded forest canopy closure.

210 gic conditions found only in glacier-fed and snow melt-driven alpine streams.

211 warming springs are advancing the timing of snow melt.

212 ue to warmer temperatures and earlier spring snow melt.

213 e salinity, indicating a source from ice and snow melting and consistent with snow depositional input

214 After the summer snow melting, VMS accumulate in the Southern Ocean and A

215 Further, snow meltwater I(-) measurements showed enrichments of u

216 otoreducible Hg retention and transport with snow meltwater.

217 n this study, the structure and diversity of snow microbial assemblages from two regions of the weste

218 The snow microbial assemblages were more similar to communit

219 tellite observations, climate model data and snow model simulations.

220 plored the formation mechanism of marine oil snow (MOS) and the associated transport of oil hydrocarb

221 Furthermore, the formation of marine oil snow (MOS) in oil-amended incubations was consistent wit

222 Snow Mountain virus (GII.2.1976) is the prototype strain

223 able isotope ratio (delta(15)N) in Greenland snow nitrate and in North American remote lake sediments

224 Changes of snow occurrence across the central and eastern United St

225 The percentages of the area losing snow occurrence are also assessed.

226 nce a partial, or even a very large, loss of snow occurrence in the future.

227 istorical (1981-2000) and future (2081-2100) snow occurrence.

228 ion events (AMDEs) that require halogens and snow or ice surfaces.

229 The association with work over snow or water and the lack of association with brimmed h

230 Snow overlays the majority of Antarctica and is an impor

231 Snow overlays the majority of the Greenland Ice Sheet (G

232 using two methods: in 2011-2013 by altering snow pack (snow-removal vs. control treatments), and in

233 particularly sensitive to changes in winter snow pack accumulation and winter soil temperature varia

234 Since snow insulates soil, a decreased snow pack can increase the frequency of soil freezing, w

235 to the higher temperatures, earlier loss of snow packs, longer growing seasons, and associated water

236 ing the definition of "dragon kings." Marine snow particles overwhelmingly contributed to the total p

237 ntly have a 20x greater dependence on winter snow patches than males.

238 rements of sulfate aerosols extracted from a snow pit at the South Pole (1984-2001) showed the highes

239 cean aggregates--colloquially called 'marine snow' - promotes cooperation.

240 Thus, snow properties are co-responsible for survival during a

241 Snow properties determine the oxygen support by diffusio

242 Snow properties influence levels of hypoxia and hypercap

243 corresponded to lower DOC concentrations in snow (R(2) = 0.31) and a decrease in percent humic-like

244 er phenology led to contrasting anomalies of snow radiative forcing, which is dominated by De and acc

245 mean winter temperatures is at or above the snow-rain threshold (>0 degrees C mean winter temperatur

246 ean winter temperatures are currently at the snow-rain threshold and have been warming for approximat

247 all species range and appears linked to this snow-rain transition across its range.

248 The snow-rain transition zone is located around 38-46 degree

249 The probabilistic projections show that the snow-rain transition zone will shift to the north under

250 ed distributions of snow frequency show that snow-rain transition zones are mainly zonally distribute

251 e system through atmospheric temperature and snow recharge, which are known exhibit stochastic variab

252 Deeper snow reduced Fox by 35-40% and 90-100% in medium- (MS) a

253 ix Greenland shallow firn cores from the dry snow region confirms that the most recent prior widespre

254 albedo below a critical threshold in the dry snow region, and caused the melting events in both 1889

255 ual PFAS concentrations in freshly deposited snow relative to surface snow (CSD/CSnow), snowmelt (CSD

256 g the first and second growing seasons after snow removal (P = 0.023 for 2009 and P = 0.005 for 2010)

257 Experimental snow removal advanced flowering phenology by 7 days, whi

258 Snow removal also altered foliar morphology, but in unex

259 ntal treatments, extended growing season via snow removal and extended growing season combined with s

260 Snow removal significantly increased the depth of maxima

261 Plants in the snow removal treatment that escaped frost damage had hig

262 Plants in the snow removal treatment were more likely to experience fr

263 the prediction that plants exposed to early snow removal would resemble individuals from lower eleva

264 We conducted a 2-year snow-removal experiment at Hubbard Brook Experimental Fo

265 lowering occurred approx. 10 days earlier in snow-removal than control plots during all years of snow

266 methods: in 2011-2013 by altering snow pack (snow-removal vs. control treatments), and in 2013 by ind

267 Patients with 'visual snow' report continuous tiny dots in the entire visual f

268 Warmer winters with less snow resulted in longer lags and a more protracted verna

269 s and measurements of CH4 trapped in ice and snow reveal a meteoric rise in concentration during much

270 Reduced snow (RS) increased the fraction of oxidized CH4 (Fox) b

271 ride at trace levels in more than 450 recent snow samples collected during the 1998-1999 Internationa

272 CBs are in agreement with data from seasonal snow samples in the Alps, but are a factor of 100 higher

273 Despite this, the chemical composition of snow samples was consistent with a marine contribution,

274 Complementary sampling of air, snow, sea-ice, and seawater for a range of organochlorin

275 idence indicating the presence of marine oil snow sedimentation and flocculent accumulation (MOSSFA).

276 'Visual snow' should be considered a distinct disorder and syste

277 e, USA, that concurrently monitored climate, snow, soils, and streams over a three-year period and su

278 e Antarctica, fresh snow deposition, surface snow, streams from melted snow, coastal seawater, and pl

279 et survey (n = 275) of self-assessed 'visual snow' subjects done by Eye On Vision Foundation was anal

280 Using a Teflon flux chamber, snow temperature, UV irradiation, and snow age were foun

281 f the dry tundra was more affected by deeper snow than the moist tundra community.

282 in areas where precipitation accumulates as snow, then melts faster than drainage capacity.

283 ult from observed and predicted increases in snow thickness, active layer depth, and soil temperature

284 s imply that large mass transfers of Hg from snow to air may take place during the Arctic snowmelt pe

285 the climate warms, a transition from winter snow to rain in high latitudes will cause significant ch

286 Our aim was to study patients with 'visual snow' to characterize the phenotype.

287 panish broom (Spartium junceum), in the rain-snow transition zone of the Sierra Nevada of California.

288 ry that is consistent with the observed rain-snow transition.

289 nd strength of pollen limitation varied with snow treatments, and among years.

290 f mast seeding using four 40-yr Chionochloa (snow tussock) datasets; and comparing the performance of

291 s of MeHg production in snowpacks and melted snow using mercury stable isotope tracer experiments, as

292 The Delta(14)C-DOC of snow varied from -743 to -420 per thousand showing progr

293 use, and tailpipe exhaust emissions of over snow vehicles (OSV), including five snow coaches and one

294 al covariates, history of work over water or snow was associated with increased odds of XFS (OR, 3.86

295 Snow was found to contain a diverse assemblage of bacter

296 recipitation-evapotranspiration index, April snow water equivalent, and water year streamflow from a

297 Mean concentrations in seawater, sea-ice and snow were generally greater at the Arctic site.

298 Decreases in Fox with deeper snow were partly due to increases in plant-mediated CH4

299 cation in plankton to a thin layer of marine snow widely observed in stratified systems that concentr

300 port that in healthy subjects breathing into snow with an artificial air pocket, snow density had a d