ライフサイエンスコーパス: ice

1 sponses based on the Hubel and Wiesel (1972) ice-cube model of visual cortex.

2 The early 2000s accelerated ice-mass loss from large outlet glaciers in W and SE Gre

3 kilometres from grounded ice onto and across ice shelves, feeding vast melt ponds up to 80 kilometres

4 observations of deposition growth of aligned ice crystals on feldspar, an atmospherically important c

5 ly of CO or CO2 ices, or contained amorphous ice, which could have triggered activity at greater dist

6 er exists in high- and low-density amorphous ice forms (HDA and LDA), which could correspond to the g

7 high-to-low-density transition in amorphous ice at 1 bar.

8 An ice-hosted sedimentation and weathering model may provid

9 Saturn's moon Enceladus has an ice-covered ocean; a plume of material erupts from crack

10 loci where intense melting occurs to thin an ice shelf, these findings expose a novel link between su

11 copepod individual-based model coupled to an ice-ocean-biogeochemical model was utilized to simulate

12 ce cream microstructure was studied using an ice crystal dispersion method.

13 ,400 years ago until 7,500 years ago-when an ice-shelf collapse may have caused rapid ice-sheet thinn

14 ence highlighting the sensitivity of ancient ice sheets to volcanism is scarce.

15 lity, cultivability, metabolic activity, and ice-nucleation activity.

16 hers with reliable access to fish buyers and ice and likely impact rural fisher livelihoods and flood

17 se linked systems of subglacial conduits and ice-shelf channels have been changing over the past few

18 kers are essential to correlate sediment and ice cores from the terrestrial, marine and glacial realm

19 tween subglacial drainage, sedimentation and ice-shelf stability.

20 at the production of metabolites in snow and ice algae is driven mainly by nitrogen and less so by ph

21 r supply during summer from melting snow and ice as well as thawing permafrost, contrasting earlier n

22 arbon (BC) in haze and deposited on snow and ice can have strong effects on the radiative balance of

23 or those that experience periods of snow and ice cover.

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

25 Earth-system and ice-sheet modelling suggests these contrasting trends we

26 We used radio-tracking and ice drift data to quantify the influence of increased dr

27 preferential condensation between vapor and ice has never been directly measured at temperatures bel

28 vability, metabolic activity, viability, and ice-nucleation activity of investigated bacteria.

29 res the density difference between water and ice Ih at ambient conditions, as well as many important

30 ations in deep-sea temperature and Antarctic ice volume in response to the approximately 110-ky eccen

31 lt to assess relationships between Antarctic ice-sheet (AIS) dynamics, climate change and sea level.

32 ion of New Zealand volcanic ash in Antarctic ice.

33 linear tracts of thin ice found on Antarctic ice shelves.

34 As ice surfaces-particularly the two prism faces-come under

35 nd the resistance to ice flow that arises as ice deforms to negotiate bed topography.

36 Freeze casting, also known as ice-templating, is a technique that has received conside

37 The amount of intracellular ice as well as ice crystal size played a role in determining whether or

38 Because ice-shelf channels are loci where intense melting occurs

39 face, englacial interior, subglacial bedrock-ice interface, proglacial streams and glacier forefields

40 ersus water has changed considerably between ice ages and interglacial periods.

41 servations to show that interactions between ice flow, glacial erosion, and sediment transport drive

42 t was proposed that lattice matching between ice and the surface controls their ice-nucleating effici

43 A bulk ice I h or ice VI sample is homogeneously heated by a pi

44 g and south in fall were frequently aided by ice motion.

45 on immobilization, were mainly influenced by ice scour.

46 nter with rainfall (rain-on-snow) can cause 'icing', restricting access to forage, resulting in starv

47 Regulated by the control climate ice coverage, models with greater (lesser) ice coverage

48 CO2 ice sublimation mechanisms have been proposed for a host

49 e if the interaction between sublimating CO2 ice blocks and a warm, porous, mobile regolith can gener

50 olatile inventory, particularly of CO or CO2 ices, or contained amorphous ice, which could have trigg

51 al ice crystals and no entrapment in control ice creams was observed.

52 rom offshore Svalbard to constrain a coupled ice sheet/gas hydrate model, we identify distinct phases

53 voring the formation of nuclei rich in cubic ice, which, as demonstrated by us earlier, are more like

54 observational evidence that rapid deglacial ice-sheet retreat into Pine Island Bay proceeded in a si

55 ubstrates lead to the formation of different ice polytypes.

56 d hexagonal layers makes stacking-disordered ice the stable phase for crystallites up to a size of at

57 indicating that this catchment, which drains ice to the Sabrina Coast, may be sensitive to climate pe

58 sponse to an earlier perturbation in driving ice-sheet loss.

59 The emergence of continental shelves during ice ages and their flooding during interglacials have be

60 global climate change, demonstrating earlier ice breakup, longer ice-free seasons, and increased wate

61 led an additional cohort in years with early ice breakup, lowering the mean size of age 0 fish.

62 We suggest that enhanced ice sheet runoff is primarily associated with albedo eff

63 similar to that observed beneath the extant ice sheet, was also active during the last glacial perio

64 between the cell membrane and extracellular ice result in IIF.

65 Reduced fast ice after 2006 ramped iceberg scouring, killing half the

66 ween loess sedimentation rate, Fennoscandian ice sheet dynamics, and sea level changes is proposed.

67 ts emphasize the importance of the ocean for ice sheet stability under the current changing climate.

68 to lower-resolution data currently used for ice-sheet models, these data show a contrasting topograp

69 veloped using annual layer counting and four ice-flow thinning models.

70 ra, it is also likely to cause more frequent icing events.

71 buted to sea breeze (cold air advection from ice-covered ocean onto adjacent land during the growing

72 carbonyl sulfide (COS) records, derived from ice-core, firn and ambient air samples.

73 th other North American mercury records from ice and lake sediment cores.

74 on and projecting global sea-level rise from ice-sheet loss.

75 For given ice water path, the CTT of dust-mixed cloud is warmer th

76 s as proxies for retreat of grounded glacier ice in the Ross Embayment.

77 is method, all LA-ICP-MS analyses of glacier ice involved a single element per ablation pass or spot.

78 for ultrahigh-resolution sampling of glacier ice is needed.

79 n/evaporation, freshwater inputs) and global ice volume.

80 denced by fast and strong linkages to global ice volume and Arctic paleoclimate indicators.

81 m (Pt) anomaly was reported in the Greenland ice sheet at the Younger Dryas boundary (YDB) (12,800 Ca

82 pproximately 25% increase in total Greenland ice sheet mass loss ( approximately 1.4 m sea-level equi

83 e kilometers) suggests that potential ground-ice presence may have contributed to the formation of Ve

84 ing water up to 120 kilometres from grounded ice onto and across ice shelves, feeding vast melt ponds

85 cial discharge from the surrounding grounded ice sheet.

86 g of random sequences of cubic and hexagonal ice layers.

87 t results from a highly-resolved 'horizontal ice core' from the Weddell Sea Embayment, which records

88 ur isotope anomalies and marked decreases in ice core bromine consistent with increased surface UV ra

89 al biodiversity occurs almost exclusively in ice-free areas that cover less than 1% of the continent.

90 s, reflecting the increase in seasonality in ice cover.

91 l the impacts on coastal areas of increasing ice mass loss and the associated freshwater runoff and l

92 Larger individual ice crystals and no entrapment in control ice creams was

93 of ice-nucleating proteins (INPs) to induce ice formation at relatively warm temperatures in microfl

94 pure, amphipathic metallohelicies inhibited ice growth at just 20 muM.

95 ecules, including ribose, in an interstellar ice analog experiment.

96 The amount of intracellular ice as well as ice crystal size played a role in determi

97 ing of cells demonstrated that intracellular ice formation (IIF) was common and did not necessarily r

98 sidents live on the 1% of Antarctica that is ice free, whilst the largest animals that have ever live

99 Isolated ice-free areas will coalesce, and while the effects on b

100 or several millions of years, with most land ice-covered and much of the ocean seasonally freezing.

101 We propose that the appearance of larger ice sheets over the past million years was a consequence

102 The transition from the last ice age to the present-day interglacial was interrupted

103 d the climate system's descent into the last ice age.

104 th landmasses were covered by the Laurentide ice sheet during the Last Glacial Maximum (18,000 years

105 e ice coverage, models with greater (lesser) ice coverage generally possess a colder (warmer) and dri

106 ne retreat may have been a highly non-linear ice sheet response to relatively continuous external for

107 e, demonstrating earlier ice breakup, longer ice-free seasons, and increased water temperatures.

108 er seasonal stratification related to longer ice-free periods in Lake Superior due to anthropogenic c

109 lacier (PIG) terminates in a rapidly melting ice shelf, and ocean circulation and temperature are imp

110 Conservative minimum ice volume estimates show that waxing and waning of at l

111 flow, and present a challenge for modelling ice-sheet evolution and projecting global sea-level rise

112 he possibility that Ceres experienced modest ice-rock fractionation, resulting in differences between

113 However, most ice-sheet models estimate basal traction from satellite-

114 apidly transforming from a thicker multiyear ice cover to a thinner and largely seasonal first-year i

115 We argue that neither ice sheet dynamics nor CO2 change in isolation can expla

116 nced warming, with a retreat of the northern ice margin behind its present position in the mid Holoce

117 played a role in determining whether or not ice inside the cell was a lethal event.

118 eria enriched with magnesium in the obtained ice cream was lower in comparison to the control samples

119 ivity (and then possible feedback) and ocean-ice sheet dynamics, respectively, rather than simple pro

120 l control has precluded precise alignment of ice, atmospheric and marine records, making it difficult

121 ace drainage could deliver water to areas of ice shelves vulnerable to collapse, as melt rates increa

122 The cause of ice expansion is uncertain, but most likely it is relate

123 lysis shows that significant enhancements of ice nucleation can emerge both when the geometry of a we

124 g current icehouse conditions, the extent of ice versus water has changed considerably between ice ag

125 mages plant tissues through the formation of ice crystals at or below freezing temperatures.

126 iomacromolecules which prevent the growth of ice crystals.

127 tic Ocean, leaving behind distinct layers of ice-rafted debris in the ocean sediments.

128 ster represents more than three millennia of ice-stream sedimentation.

129 Based on these results a model of ice crystals aggregates formation in the presence of IBP

130 and remain unexplained by previous models of ice age adjustment or other local (for example, tectonic

131 Heterogeneous nucleation of ice induced by organic materials is of fundamental impor

132 ese fluctuations assist in the nucleation of ice.

133 ics and provides insight into the origins of ice-growth inhibition.

134 that resembles the one in the basal plane of ice, it was proposed that lattice matching between ice a

135 al nucleation of prismatic crystal planes of ice on high-energy (100) surface planes of feldspar.

136 imate forecasts hinge on good predictions of ice nucleation rates.

137 biological production, and the melt rate of ice shelves.

138 We find that the premelted surface of ice has unique solvation properties, different from thos

139 Here, we report the use of ice-nucleating proteins (INPs) to induce ice formation a

140 cal features in the nucleation from vapor of ice and various organic crystals.

141 ct of twenty-first century climate change on ice-free areas under two Intergovernmental Panel on Clim

142 t the discovery of an ion-specific effect on ice recrystallization.

143 erse subglacial landscapes have an impact on ice flow, and present a challenge for modelling ice-shee

144 hane sequestration and subsequent release on ice sheet retreat that led to the formation of a suite o

145 A bulk ice I h or ice VI sample is homogeneously heated by a picosecond in

146 g mechanism, interfacial gelation process or ice.

147 Females foraged longer in pack ice in years with greatest sea ice concentration and ear

148 es originating from open water and open pack ice increased the cloud condensation nuclei concentratio

149 e and carbon cycle during the late Paleozoic ice age and the climatic significance of the fossil carb

150 ng their analysis process, not in the parent ice.

151 climates of the Pliocene to the Pleistocene ice ages between 3.2 and 2.6 million years ago.

152 Melting glaciers release previously ice-entrapped chemicals to the surrounding environment.

153 MICI is triggered when this retreat produces ice cliffs above the water line with heights approaching

154 Climate models project ice-free conditions during summer this century under rea

155 lly sharp, concave wedge can further promote ice nucleation with special wedge geometries.

156 A in the free and upper troposphere, promote ice nucleation and facilitate long-range transport of re

157 Exotic forms of these pure ices have been revealed at extreme ( megabar) pressures,

158 an ice-shelf collapse may have caused rapid ice-sheet thinning further upstream-and since the 1940s.

159 e and precipitation, associated with reduced ice extent in the nearby Ross Embayment.

160 Asia, based on a continuous high-resolution ice-core Hg record from the Belukha glacier in the Siber

161 present [YBP]); after the glacier retreated, ice patches remained on the island until ca. 9,000 calib

162 ra subglacial basin before continental-scale ice sheets were established about 34 million years ago.

163 Under the strongest forcing scenario, ice-free areas could expand by over 17,000 km(2) by the

164 Sea ice cover and duration predetermine levels of phytoplank

165 Sea ice is an important component of the global climate syst

166 rate pH measurements in polar waters and sea ice brines require pH indicator dyes characterized at ne

167 scopic examination of fixed seawater and sea ice samples revealed chytrids parasitizing diatoms colle

168 Ross Sea dominate increases in Antarctic sea ice and are outside the range simulated by climate model

169 s in climate model simulations.Antarctic sea ice extent continues to increase, with autumn sea ice ad

170 a, including the evolution of the Arctic sea ice cover, the El Nio Southern Oscillation (ENSO), the A

171 consequences of rapid changes in Arctic sea ice have the potential to affect migrations of a number

172 nalogue to predict the effects of Arctic sea ice loss on mid-latitude weather.

173 scale NAO- events are affected by Arctic sea ice loss.

174 Reductions in Arctic sea ice may promote the negative phase of the North Atlantic

175 The effects of declining Arctic sea ice on local ecosystem productivity are not well underst

176 Atlantic Ocean water to melt all Arctic sea ice within a few years, a cold halocline limits upward h

177 As sea ice retreats and dissolved organic carbon inputs to the

178 xtent continues to increase, with autumn sea ice advances in the western Ross Sea particularly anomal

179 Autumn sea ice trends in the western Ross Sea dominate increases in

180 tes between being primarily regulated by sea ice or glacial discharge from the surrounding grounded i

181 icient zone in the oceanic water column, sea ice or polar snow.

182 veloped in situ despite the snow-covered sea ice.

183 i seas during two periods with different sea ice characteristics.

184 atest sea ice concentration and earliest sea ice advance, while males foraged longer in polynyas in y

185 flected by more prevalent easterly flow, sea ice loss does not lead to Northern European winter cooli

186 onger in pack ice in years with greatest sea ice concentration and earliest sea ice advance, while ma

187 Subarctic, i.e. the northern hemisphere, sea ice now exhibits similar levels of seasonality to the An

188 First, given current reductions in sea ice and increases in Arctic killer whale sightings, kill

189 examine how inter-annual variability in sea ice concentration and advance affect the foraging behavi

190 udy clarifies the range of mechanisms in sea ice/terrestrial productivity coupling, allowing the gene

191 bored the highest quantities, indicating sea ice as a possible transport vehicle.

192 ed longer in polynyas in years of lowest sea ice concentration.

193 can also initiate widespread fracture of sea ice and further increase the likelihood of subsequent ca

194 omponent might reflect co-variability of sea ice and tundra productivity due to a common forcing, suc

195 Recent decline of sea ice habitat has coincided with increased use of land by

196 estrial food, and as the availability of sea ice habitat increased.

197 from the relatively long persistence of sea ice in the autumn.

198 in light, temperature and the extent of sea ice.

199 Projected Arctic warming, with more open sea ice leads providing halogen sources that promote AMDEs,

200 sive phytoplankton blooms beneath ponded sea ice during summer, indicating that satellite-based Arcti

201 on timing as related to delayed regional sea ice freeze-up since the 1990s, using two independent dat

202 occurred significantly later as regional sea ice freeze-up timing became later in the Beaufort, Chukc

203 This contributes to weak western Ross Sea ice trends in climate model simulations.Antarctic sea ic

204 timing is temporally matched to seasonal sea ice cover.

205 of the ice-albedo feedback on summertime sea ice, we find that during some time interval of the seaso

206 oxy records of Arctic Ocean temperature, sea ice cover and circulation.

207 Westward and northward drift of the sea ice used by polar bears in both regions increased betwee

208 a marine biosphere-climate link through sea ice melt and low altitude clouds that may have contribut

209 Future ocean and sea-ice changes affecting the distribution of such species w

210 diate depth water (AIW) temperatures and sea-ice cover spanning the last 1.5 million years (Ma) of

211 othermometry of the ostracode Krithe and sea-ice planktic and benthic indicator species, we suggest t

212 istribution profile between seawater and sea-ice showed a compound-dependency for Arctic samples not

213 ndamental changes in AIW temperature and sea-ice variability.

214 ident in recent years, whereas Antarctic sea-ice concentration exhibits a generally increasing trend.

215 A decreasing trend in Arctic sea-ice concentration is evident in recent years, whereas An

216 Arctic sea-ice loss is a leading indicator of climate change and ca

217 he leading mode of variability of global sea-ice concentration is positively correlated with the AMO

218 at contribute to the opposite changes in sea-ice concentration.

219 ctic, possibly due to full submersion of sea-ice at the former.

220 both observational and proxy records of sea-ice variability, and show persistent patterns of co-vari

221 m time series of observed and reanalysis sea-ice concentrations data suggest the possibility of the h

222 Seasonal sea-ice melt processes may alter the exchange rates of selec

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

224 Findings suggest that sea-ice OCP burdens originate from both snow and seawater.

225 is constrained by the limitations of the sea-ice cover record, preliminary statistical analyses of on

226 plified warming in Arctic regions due to sea-ice loss and other processes, relative to global mean te

227 of Labrador Sea productivity related to sea-ice variability in Labrador, Canada that extends well in

228 al conditions (low temperatures and seasonal ice cover).

229 It has volumetric anomalies-water's solid (ice) floats on its liquid; pressure can melt the solid r

230 ponds are relatively well documented on some ice shelves, we have discovered that ponds often form pa

231 ments of nanoelements called artificial spin ice can lead to specific collective behaviour, including

232 e', is shown to occur experimentally in spin ice, a dipolar lattice system.

233 nes connecting topological monopoles in spin ice.

234 The magnetic properties of the quantum spin ice candidate Yb2Ti2O7 have eluded a global understandin

235 luctuations, including spin liquids and spin ices.

236 the possible microstates in artificial spin ices and related arrays of nanomagnets.

237 In this respect, artificial spin ices are geometrically frustrated magnetic metamaterials

238 agnets Ho2Ti2O7 and Dy2Ti2O7, so-called spin ices, exhibit a classical spin liquid state with fractio

239 ns, for example the magnetic charges in spin ices, also called monopoles.

240 taev spin liquids, skyrmions phases, or spin ices.

241 Here, we demonstrate a spin-ice-based active material in which energy is converted i

242 Subsequently, ice advanced across and retreated from the Sabrina Coast

243 finding implies the existence of substantial ice volume in the Aurora subglacial basin before contine

244 We infer rapid and sustained ice-sheet retreat driven by MICI, commencing around 12,3

245 modelling and the alignment of terrestrial, ice and marine (14)C and (10)Be records, the authors sho

246 This is in contrast to the expectation that ice sheets expand in colder climates and shrink in warme

247 ulations with various water models find that ice nucleated and grown under atmospheric temperatures i

248 ice, confirming theoretical predictions that ice can survive for billions of years just beneath the s

249 rved Heinrich events, but also suggests that ice sheets in contact with warming oceans may be vulnera

250 The ice-air interface is an important locus of environmental

251 rstand the impact of water moving across the ice surface a broad quantification of surface meltwater

252 ata show a contrasting topography across the ice-bed interface.

253 de Ice Sheet as the coastline lies along the ice sheet's peripheral bulge.

254 a novel accelerated microscope assay and the ice cream microstructure was studied using an ice crysta

255 heless accumulate as dry agglomerates at the ice surface, driven by direct interactions between the o

256 o a water-mediated attraction of ions at the ice surface.

257 which it is derived, namely friction at the ice-bed interface and form drag, and the resistance to i

258 r interface is the smallest area face at the ice-vapor interface.

259 The most stable face at the ice-water interface is the smallest area face at the ice

260 s ridge, forming an ocean cavity beneath the ice shelf, occurred in 1945 (+/-12 years); final ungroun

261 rdered domains and monotonously decrease the ice freezing temperature.

262 ystallization inhibition was assessed in the ice cream mixes using a novel accelerated microscope ass

263 at the total number of microorganisms in the ice cream was higher than in the starter cultures.

264 to occur in supersaturated conditions in the ice-vapor system.

265 plume of material erupts from cracks in the ice.

266 ility of the ion to be incorporated into the ice phase plays a key role in the ultimate size of the i

267 oth when the geometry of a wedge matches the ice lattice and when such lattice match does not exist.

268 , which indicated cavitation events near the ice front upon freezing, were both related to minimum te

269 is widely suspected to underpin much of the ice age decline in atmospheric CO2 concentration, but th

270 -dammed glacial lake, the degradation of the ice core could have implications for glacial lake outbur

271 plays a key role in the ultimate size of the ice grains after recrystallization.

272 inage of meltwater across the surface of the ice sheet through surface streams and ponds (hereafter '

273 tephra were erupted though the center of the ice sheet, deposited near WAIS Divide and preserved in t

274 1945 (+/-12 years); final ungrounding of the ice shelf from the ridge occurred in 1970 (+/-4 years).

275 cate that ions increase the liquidity of the ice surface but hydrophilic organics do not.

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

277 one-tenth of the ice-free land surface is under intense human management,

278 t active drainage has exported water off the ice surface through waterfalls and dolines for more than

279 At tropospheric temperatures, the ice surface is partially premelted.

280 and modeling studies have suggested that the ice sheet contribution to future sea level rise could ha

281 nary downward longwave radiative flux to the ice surface, which may then amplify the Arctic wintertim

282 gate the lower bound duration over which the ice stream would have deposited sediment to account for

283 g between ice and the surface controls their ice-nucleating efficiency.

284 le than hexagonal crystallites, making their ice nucleation rates more than three orders of magnitude

285 channels are long curvilinear tracts of thin ice found on Antarctic ice shelves.

286 We use the TIP4P/ice force field, one of the best existing molecular mode

287 y related to their free energy of binding to ice.

288 terface and form drag, and the resistance to ice flow that arises as ice deforms to negotiate bed top

289 Total ice cover would make an anoxic ocean likely, and would b

290 Plankton were more abundant under ice than expected; mean winter values were 43.2% of summ

291 ute bout of local cryotherapy, delivered via ice cup massage over the anterolateral thigh.

292 cts single apoferritin molecules in vitreous ice with high specificity and determines their orientati

293 to be sustained by the sublimation of water ice and supported by rapid rotation, while at least one

294 gen, consistent with broad expanses of water ice, confirming theoretical predictions that ice can sur

295 near WAIS Divide and preserved in the WDC06A ice core.

296 oister) climate, exhibit a stronger (weaker) ice-albedo feedback, and experience greater (weaker) war

297 polar bears responded to the higher westward ice drift with greater eastward movements, while their m

298 To compensate for more rapid westward ice drift in recent years, polar bears covered greater d

299 which may then amplify the Arctic wintertime ice-surface warming.

300 to a thinner and largely seasonal first-year ice cover with significant consequences for Arctic prima