ライフサイエンスコーパス: snow

1 terized by short-stature plants and seasonal snow.

2 re portion, 26 taxa occurred in both air and snow.

3 e albedo, following loss of sea ice and land snow.

4 analysing trials only moving over very hard snow.

5 es, atmospheric lows or troughs, and melting snow.

6 on polysaccharide particles modeling marine snow.

7 atologic knowledge in the cities impacted by snow.

8 ution of species that overwinter beneath the snow.

9 ertime temperature can modify this effect of snow.

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

11 f four cities that are exposed to wintertime snow.

12 esent within the dissolved organic matter of snow.

13 nts (ASVs), 70 from the air and 142 from the snow.

14 ion (VRS, Station Nord) in a large number of snow (15) and air (51) samples.

15 ore wet-season moisture as rain (and less as snow), a longer fire season, and higher temperatures, le

16 was amplified by the intensification of the snow accumulation (+50% at Dasuopu) likely linked to the

17 The snow accumulation decreased and dry winters were reestab

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

19 clones are stronger in the Atlantic, Pacific snow accumulation is more sensitive to cyclone strength.

20 isms controlling the timing and magnitude of snow accumulation on sea ice is crucial for understandin

21 n average, 44% of the variability in monthly snow accumulation was controlled by cyclone snowfall and

22 ss gains over ice sheet interiors (increased snow accumulation).

23 We recovered local adaptation under snow addition treatments, which reflect historical condi

24 of freshwater (lakes and rivers), seawater, snow, air, and zooplankton for a range of legacy polychl

25 re highly correlated with the product of the snow-air partition coefficient and the Henry's law const

26 woody debris darkens the snowpack and lowers snow albedo for 15 winters following fire, using measure

27 ransmission through the canopy and decreased snow albedo from deposition of light-absorbing impuritie

28 Snow algae are found in snowfields across cold regions o

29 pported by two field campaigns revealed 1679 snow algae blooms, seasonally covering 1.95 x 10(6) m(2)

30 ples to measure the metabolic composition of snow algae communities and determined the species compos

31 bolic and species diversity of green and red snow algae communities from four locations in Ryder Bay

32 ata show the complexity and variation within snow algae communities in Antarctica and provide initial

33 We present the first estimate of green snow algae community biomass and distribution along the

34 mall islands, resulting in a net increase in snow algae extent and biomass as the Peninsula warms.

35 rameters, such as temperature, rainfall, and snow amount have already been observed.

36 only considering air-water partitioning, as snow amplification influences, and may even control, the

37 simultaneous field measurements, showed that snow amplification is relevant for diverse families of P

38 enry's law constant (K(SA) H'), a measure of snow amplification of fugacity.

39 imated as the ratio of POP concentrations in snow and air from previously reported simultaneous field

40 chlorine pesticides (OCPs) concentrations in snow and air were close to equilibrium.

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

42 Greenland's high-elevation interior, porous snow and firn accumulate; these can absorb surface meltw

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

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

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

48 regions are changing rapidly due to loss of snow and ice in response to ongoing climate change.

49 Our results are indicative that changes in snow and ice melt across glacial environments will influ

50 Arctic soils are covered by snow and ice throughout most of the year.

51 In Arctic ungulates, extreme rain-on-snow and ice-locked pastures have led to severe populati

52 ntion of the long-chain compounds in melting snow and ice.

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

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

55 monstrate that high-elevation streams fed by snow and other cold-water sources continue to serve as c

56 sorbing impurities were measured in seasonal snow and permanent snowfields in the Chilean Andes durin

57 ass AGB was stabilized under deepened winter snow and plant community composition remained unchanged.

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

59 ects of observation height (e.g. vegetation, snow and soil characteristics) and in habitats varying i

60 Snow and soils with high reflectivity may enhance photod

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

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

63 12 pascals, softer than freshly fallen light snow) and allowing a key estimation to be made of the po

64 Snow assemblages changed markedly throughout the sample

65 DA is the most accurate model for predicting snow avalanche risk.

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

67 This study models the probabilities of snow avalanches, landslides, wildfires, land subsidence,

68 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

69 both positive and negative contributions to snow bias in climate models and provides guidance for fu

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

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

72 iding spectacular resemblance to terrestrial snow-capped mountain chains.

73 In snow, Cladosporium, Pseudogymnoascus, Penicillium, Meyer

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

75 inters following fire, using measurements of snow collected from seven forested sites that burned bet

76 ly to marine snow formation, and that marine snow composed of elongated phytoplankton cells can form

77 able and intertwined drivers of future under-snow conditions (e.g., declining snow depths, rising air

78 ns of migratory species as a response to the snow conditions remains however unexplored.

79 tion is highly dependent on the evolution of snow conditions.

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

81 We controlled for cloud cover, snow cover and evaluated the impact of sensor radiometri

82 atchments in southern Europe; and decreasing snow cover and snowmelt, resulting from warmer temperatu

83 Sea ice and its snow cover are critical for global processes including c

84 e seasonal and circadian use, and identified snow cover as the most important variable predicting khu

85 captured seasonal changes in vegetation and snow cover conditions in finer detail with more certaint

86 to snow cover dynamics using a daily percent snow cover dataset.

87 rich winters, suggesting that high-elevation snow cover displaced dotterel to lower sites.

88 nities to different scenarios of warming and snow cover duration.

89 Here, we examine how changing spring snow cover dynamics and early season forage availability

90 Spring activity date was related to snow cover dynamics using a daily percent snow cover dat

91 6-2018 in order to assess the changes in the snow cover extent across a north-south transect of appro

92 ariability, here we show that the dry-season snow cover extent declined across the entire study area

93 an land surface, causing a steady decline in snow cover extent over the Himalayan-Tibetan Plateau reg

94 We show that the decrease in snow cover fraction is primarily driven by the increase

95 d that reductions of terrestrial snow cover, snow cover fraction over sea ice, and sea ice extent app

96 negative RF, a trend dominated by decreased snow cover in spring months.

97 Snow cover loss related mortality spans approximately 10

98 rees S), where the El Nino signal is weaker, snow cover losses appear to be also influenced by the po

99 ming climate, but studies on one key factor, snow cover, are almost totally lacking.

100 not been the driver of changes in the Arctic snow cover, ice cover, and surface albedo since the 1980

101 We find that reductions of terrestrial snow cover, snow cover fraction over sea ice, and sea ic

102 Our results show that decreasing snow cover, together with warming temperatures, can subs

103 emote Antarctic continent, due to periods of snow cover, which limit remote sensing, and the small si

104 ites previously unavailable due to extensive snow cover, while changes associated with nitrogen depos

105 s, growing-season soil moisture, and days of snow cover.

106 relation to the spatio-temporal dynamics of snow cover.

107 colder, more humid conditions and prolonged snow-coverage at north exposure likely influenced the de

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

109 Although none of the species avoided snow-covered areas, they presumably used snow presence a

110 and OCPs shifted from equilibrium during ice/snow-covered conditions toward a clear net volatilizatio

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

112 ts agree on 46% of the non-permanent ice- or snow-covered land as having low human influence.

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

114 d the transition of the glacial surface from snow-covered to bare-ice.

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

116 terrestrial surface, minus permanent ice and snow, currently has low human impact.

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

118 emperatures are increasing and the number of snow days has generally diminished over time with perenn

119 t monitoring and assessment by examining two snow deficits that posed large socioeconomic challenges

120 otential was consistent with detrital marine snow degradation.

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

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

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

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

125 Irrigated agriculture in snow-dependent regions contributes significantly to glob

126 imate change on irrigated agriculture in the snow-dependent Yakima River Basin (YRB) in the Pacific N

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

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

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

130 ate warming is rapidly leading to changes in snow depth and soil temperatures across mid- and high-la

131 Yet, remote sensing observations of mountain snow depth are still lacking at the large scale.

132 re, we show the ability of Sentinel-1 to map snow depth in the Northern Hemisphere mountains at 1 km2

133 Accurate snow depth observations are critical to assess water res

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

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

136 ngly than tracking spring green-up or autumn snow depth.

137 This is showcased with the contrasting snow depths between 2017 and 2018 in the US Sierra Nevad

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

139 uture under-snow conditions (e.g., declining snow depths, rising air temperatures, shortening winters

140 Deepened snow did not affect aboveground plant biomass (AGB) but

141 In the Arctic, snow directly influences resource availability.

142 ive forcing in 2018 causing earlier melt and snow disappearance in > 11% of forests in the western se

143 forests burned since 1984, and 5 day earlier snow disappearance persisting for >10 years following fi

144 Size often increased with earlier snow disappearance, with larger increases in meadow soil

145 Survival often declined with earlier snow disappearance, with somewhat smaller declines in me

146 mmer precipitation, especially if coupled to snow drought and earlier soil moisture recession, but su

147 biogeochemical processes; however, no global snow drought assessments currently exist.

148 hat likely contribute to observed changes in snow drought characteristics.

149 d decreases (percent changes) in the average snow drought duration (-4, -7, -8, and -16%, respectivel

150 roughts, experiencing ~2, 16, and 28% longer snow drought durations, respectively, in the latter half

151 to the first half of the record) of having a snow drought exceed the average intensity from the first

152 e characterize the duration and intensity of snow droughts (snow water equivalent deficits) worldwide

153 We find that snow droughts became more prevalent, intensified, and le

154 Europe, and the WUS emerged as hot spots for snow droughts, experiencing ~2, 16, and 28% longer snow

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

156 Distinct drifts of light and dark snow (enriched with light absorbing particles, LAPs) fac

157 reindeer, we show that more frequent rain-on-snow events actually reduce extinction risk and stabiliz

158 ndicating that increasingly frequent rain-on-snow events could destabilize populations.

159 Extreme rain-on-snow events mainly suppress vital rates of vulnerable ag

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

161 001-0.004 d(-1)) and nondetectable in melted snow, except at one site (km = 0.0007 d(-1)).

162 e of the strongest overall, due to increased snow exposure in the winter and spring months.

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

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

165 We apply this formula to marine snow formation following a phytoplankton bloom.

166 ocity can contribute significantly to marine snow formation, and that marine snow composed of elongat

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

168 o optimise their arrival time and select for snow-free areas to maximise prey encounter en-route.

169 it the activity of amphibians during ~70% of snow-free days in sunny habitats.

170 s are exceeded in all habitats during 48% of snow-free days, suggesting that there may be limited opp

171 EWL limits are still exceeded during 63% of snow-free days.

172 of these physiological limits during 95% of snow-free days.

173 ower concentrations were detected during the snow-free season (end of July).

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

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

176 Winter snow from four glacial sites on Svalbard was analyzed fo

177 then quantified using radar observations and snow gauge measurements.

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

179 ose that perished in a die-off of Canada and Snow geese in Cambridge Bay, Nunavut, Canada.

180 s ice crystals to produce the aforementioned snow globe effect.

181 a beautiful effect visually reminiscent of a snow globe.

182 purities were 0.0150, 0.0160, and 0.0077 for snow grain radii of 100 um for northern Chile, the regio

183 Light-absorbing soot in snow has been decreasing in past decades over the Arctic

184 inance indices, with the assemblage found in snow having the highest diversity indices.

185 15 times the area of permanent glaciers and snow, highlighting their eco-hydrological importance.

186 gs highlight the heterogeneity in atmosphere-snow-ice interactions across the Arctic, and emphasize t

187 etter understand their effects on the Arctic snow-ice system with anthropogenic warming.

188 lization of PCBs and most of the OCPs during snow/ice-free conditions.

189 oil moisture increased under deepened winter snow in early growing season, particularly in deeper soi

190 plumage is a crucial adaptation to seasonal snow in more than 20 mammal and bird species.

191 ed species as established from tracks in the snow in previous field studies.

192 d there is a trend towards increasing winter snow in semi-arid regions in China.

193 unctioning require acknowledging the role of snow in tundra vegetation models.

194 Deepened snow increased the net ecosystem exchange of CO(2) (NEE)

195 he presence of nanoplastics in high-altitude snow indicates airborne transport of plastic pollution w

196 le vegetation data with detailed climate and snow information using machine learning methods to model

197 cused on snow microorganisms, the ecology of snow inhabitants remains unclear.

198 spill in the Gulf of Mexico, natural marine snow interacted with oil and dispersants forming marine

199 ow protocols to generate 'artificial' marine snow, into which bacteria can be incorporated to facilit

200 ralogical composition analysis of the Andean snow is a worthwhile effort.

201 Here we show that this loss of snow is undermining winter convective mixing and causing

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

203 eriod, likely because of inputs from the ice/snow layer melting and river runoff.

204 The basal saline snow layer that was in direct contact with the sea ice s

205 line layer was more similar to that of other snow layers and the atmosphere than to underlying sea ic

206 Microbial communities in all snow layers derived from mixed sources, both marine and

207 higher abundance of cells than the overlying snow layers, with a predominance of Alteromonadales and

208 of the leopard (Panthera pardus, 81% loss), snow leopard (P. uncia, 38%), wolf (Canis lupus, 77%) an

209 er controlled conditions in which 16 captive snow leopards (Panthera uncia) were camera-trapped on 40

210 environmental change in Scottish mountains (snow lie, elevated summer temperatures and nitrogen depo

211 enerally diminished over time with perennial snow line now observed at higher elevations.

212 subnival ecosystem (between the treeline and snow line), characterized by short-stature plants and se

213 creased evapotranspiration, mainly driven by snow loss and a consequent decrease in reflection of sol

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

215 on, large ones (>0.05 cm) also called marine snow, make a significant contribution to the global carb

216 Here, we conducted a 5-year winter snow manipulation experiment in a temperate grassland in

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

218 melange (a mixture of sea ice, icebergs, and snow) may be tightly packed in the long, narrow fjords t

219 CP concentrations associated with the spring snow melt (early-mid June), while much lower concentrati

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

221 spring activity date is largely dictated by snow melt characteristics and that changing snow melt co

222 snow melt characteristics and that changing snow melt conditions may result in earlier spring activi

223 Snow melt end date, melt rate, and melt consistency expl

224 allows for rapid infiltration of oxygen-rich snow melt in spring as shown by oxidized iron in porewat

225 Accelerated snow melt occurs in burned forests due to increased ligh

226 increase this ecosystem respiration dominate snow melt period causing larger greenhouse gas losses du

227 The snow melt period coincides with rising ecosystem respira

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

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

230 ximum during the summer that corresponded to snow melt-derived moisture and a transition from winter

231 e the albedo feedback weakens as the ice and snow melt.

232 Snow scavenges air pollutants, and after snow melting, it can induce an unquantified and poorly u

233 th of copiotrophic psychro- and halotolerant snow members.

234 The surface snow metagenomes were characterized by the occurrence of

235 Our below-the-snow microclimate simulations were driven by dynamically

236 Despite an increase in studies focused on snow microorganisms, the ecology of snow inhabitants rem

237 ively nutrient-rich sea ice brine into basal snow might have stimulated the growth of copiotrophic ps

238 with oil and dispersants forming marine oil snow (MOS) that sank from the water column to sediments.

239 ore than a billion people rely on water from snow, most of which originates in the Northern Hemispher

240 a well-defined stool collection from a GII.2 Snow Mountain Virus (SMV) human challenge study to inves

241 Snow obtained shortly after deposition was kept at room

242 more diverse fungal community in the air and snow of Livingston Island in comparison with studies usi

243 cyclone activity on the seasonal buildup of snow on Arctic sea ice using model, satellite, and in si

244 cence had no effect, but a six-week delay in snow-onset (the observed data range) was estimated to in

245 Snow overlays the majority of Antarctica and is an impor

246 wfall from each sequential storm deepens the snow pack and insulates the sea-ice, further inhibiting

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

248 raphic correction, uncertainties in the rain-snow partitioning threshold, and high ablation biases.

249 sity and distribution of precipitation, rain-snow partitioning, and radiative fluxes.

250 Despite limited evidence of snow-phase methylation, the snowpack is an important MeH

251 Snow plays a fundamental role in global water resources,

252 tributed to greater stability in NEE in deep-snow plots.

253 Maritime Antarctica is recipient of abundant snow precipitation.

254 ded snow-covered areas, they presumably used snow presence as a cue to time their arrival at their br

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

256 Snow properties determine the oxygen support by diffusio

257 Snow properties influence levels of hypoxia and hypercap

258 has therefore evolved current natural marine snow protocols to generate 'artificial' marine snow, int

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

260 ss SWE compared to Landsat-Era Sierra Nevada Snow Reanalysis (SNSR) dataset.

261 populations under simulated climate change (snow removal) across all five experimental gardens.

262 ments, but it was less pronounced than under snow removal.

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

264 curred at lower densities in years following snow-rich winters, suggesting that high-elevation snow c

265 egative effects of stochastic winter rain-on-snow (ROS) events causing icing, with strongest effects

266 tion on sea ice is crucial for understanding snow's net effect on the surface energy budget and sea-i

267 nly present in the air sample and 101 in the snow sample, with only 41 present in both samples; howev

268 eralogy, and chemical enrichment) of surface snow sampled at 21 sites across a transect of about 2,50

269 versity present in air and freshly deposited snow samples obtained from Livingston Island, Antarctica

270 nanometer range for both snowpit and surface snow samples.

271 Snow scavenges air pollutants, and after snow melting, i

272 4) of continuous eddy covariance data from a snow-scoured alpine tundra meadow in Colorado, USA, wher

273 phere, snowpack with four distinct layers of snow, sea ice brine and seawater.

274 independent observations of the atmosphere, snow, sea-ice, ocean, and ecosystem.

275 go, and 2500 ug/m(2) in the south, where the snow season was longer and the snow was deeper.

276 Air, snow, the fugacity in soils and snow, seawater and plankton were sampled concurrently fr

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

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

279 inflow of sea ice brine and that they form a snow-specific assemblage reflecting the particular envir

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

281 sible red and green patches below and on the snow surface.

282 Patients with visual snow syndrome suffer from a continuous pan-field visual

283 for visual and non-visual symptoms in visual snow syndrome.

284 of the visual association cortex for visual snow syndrome.

285 For surface snow, the average mass mixing ratio of BC was 15 ng/g in

286 Air, snow, the fugacity in soils and snow, seawater and plank

287 er, ground warming occurred due to increased snow thickness while air temperature remained statistica

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

289 was high (~10-100 ng/g) and the sub-surface snow was comparatively clean, indicating the dominance o

290 th, where the snow season was longer and the snow was deeper.

291 icate that light-absorption by impurities in snow was dominated by dust rather than BC.

292 eek or more, the BC concentration in surface snow was high (~10-100 ng/g) and the sub-surface snow wa

293 ied markedly with summer plant productivity, snow water equivalent (SWE) and winter period.

294 The simulation of snow water equivalent (SWE) remains difficult for region

295 the duration and intensity of snow droughts (snow water equivalent deficits) worldwide and difference

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

297 ying the long-term vulnerability of mountain snow-water resources to climate change.

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

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

300 in > 11% of forests in the western seasonal snow zone.