ライフサイエンスコーパス: ice

1 Although structured water adlayers and 2D ice have been imaged, capturing the metastable or interm

2 ermediate edge structures involved in the 2D ice growth, which could reveal the underlying growth mec

3 extensive reporting of two-dimensional (2D) ice on metals(5-11), insulating surfaces(12-16), graphit

4 n liquid water and a comprehensive set of 54 ice phases in simulations, by directly comparing their l

5 at buttress(11-13) the ice sheet accelerates ice flow and sea-level rise(14-16).

6 and included locations that were accessible (ice edge) or inaccessible (solid fast ice) to air-breath

7 isochoric heating of high-density amorphous ice to temperatures of 205 +/- 10 kelvin, using an infra

8 mountaintop location at -46 degrees C and an ice supersaturation of 30% with concentrations ranging f

9 If BC acts as an ice nucleating particle (INP), BC could affect the lifet

10 rocesses explain the relationship between an ice-free Arctic and permafrost thawing before 0.4 Ma.

11 l river of Muchuhar Glacier, which formed an ice-dammed lake and generated a small Glacial Lake Outbu

12 radiocarbon-dated charcoal recovered from an ice deposit accumulated in Cave 29, western New Mexico,

13 Methane hydrate ([Formula: see text]) is an ice-like solid that forms from methane-water mixture und

14 als in the period following a movement to an ice block.

15 emperatures hovered around -80 degrees C and ice particles produced in the anvil were notably small (

16 g both supercooled liquid water droplets and ice particles (mixed-phase clouds).

17 satellite images of resuspension events and ice cover, wave hindcasts, and continuous turbidity meas

18 The gas and ice giants in our solar system can be seen as a natural

19 Blue carbon change with sea ice and ice shelf losses has been estimated, but not how blue ca

20 centrations of cloud condensation nuclei and ice nucleating particles.

21 is losing mass at an accelerating pace, and ice loss will likely continue over the coming decades an

22 ity could make the boundary between rock and ice layers fuzzy.

23 intessential habitat for bowhead whales, and ice-covered areas have frequently been interpreted as pr

24 at anomalous precipitation affects Antarctic ice mass loss estimates, and thus the precipitation cont

25 es in satellite imagery across all Antarctic ice shelves.

26 excess loss from the Greenland and Antarctic ice sheets during the LIG, causing global mean sea level

27 sulfate concentrations recorded in Antarctic ice cores imply that the cooling would have been more pr

28 this study, we revisit changes in Antarctic ice mass over recent decades and examine precipitation c

29 reenland (increased surface melt), Antarctic ice shelves (increased ocean melting), and Greenland and

30 ins most inter-annual anomalies of Antarctic ice mass change during the GRACE period (2003-2017).

31 gh the Eocene and the expansion of Antarctic ice sheets close to their modern size near the beginning

32 nly brief interruptions, while the Antarctic ice sheet waxed and waned.

33 many fields including anti-biofouling, anti-icing, anti-corrosion, drag reduction, droplet manipulat

34 dated volcanic fallout records in six Arctic ice cores that one of the largest volcanic eruptions of

35 Leads are a key feature of the Arctic ice pack during the winter owing to their substantial co

36 After a year-long expedition into the Arctic ice, the research vessel Polarstern returns with further

37 nments that became increasingly available as ice retreated.

38 Insights into energy flow dynamics at ice surfaces are essential for understanding chemical dy

39 Bacterial ice-nucleating proteins (INPs) promote heterogeneous ice

40 nematophycean "glacier algae" lower the bare ice albedo of the Greenland Ice Sheet (GrIS), amplifying

41 acier algae to thrive on and darken the bare ice surface.

42 he glacial surface from snow-covered to bare-ice.

43 th only about 0.2% of its overall area being ice-free.

44 to competing effects between Arctic biomes (ice, tundra, taiga).

45 While energy expenditures and peak body ice content were predicted to decline in Wood Frogs acro

46 The photoproducts found desorbing from both ice layers to the gas phase during the irradiation conve

47 Heterogeneous ice nucleation caused by ice-nucleating particles (INPs) enables cloud glaciation

48 atography that showed antifreeze property by ice recrystallization inhibition.

49 d pressor tests (CPT; hand in ~0.4 degrees C ice bath for 2 min) pre- and 5 min post-drug administrat

50 e we use historical photographs to calculate ice loss from 1880-2012 for Jakobshavn, Helheim, and Kan

51 Great Acceleration in the Elbrus, Caucasus, ice core.

52 Raspberry chocolate chip ice cream was statistically associated with illness in t

53 ns of abrupt climate change and to constrain ice-core chronologies.

54 hereas the presence of extensive continental ice sheets predicts a tidally energetic Snowball ocean d

55 ntarctica remains in the grip of continental ice sheets, with only about 0.2% of its overall area bei

56 ng from the instability of polar continental ice sheets represents a major socioeconomic hazard arisi

57 cial hydrological system critically controls ice motion at the margins of the Greenland Ice Sheet.

58 facial water molecules and the corresponding ice nucleation activity.

59 on of the ice margin, which-assuming current ice volumes-would have contributed about 3 to 4 metres(1

60 l examples to map the ages from a well-dated ice core to a nearby core, and by tracing isochronous la

61 well-known physics model for two-dimensional ice) and their relations to certain classes of plane par

62 d to consumption of commercially distributed ice cream at multiple venues.

63 round beef, ground pork, hamburger, hot dog, ice cream, liver, luncheon meat, margarine, meat-free di

64 nge in current understanding of algal-driven ice sheet darkening through quantification of the photop

65 dark organic-rich material, has a local dust/ice mass ratio of [Formula: see text], matching values p

66 conceptual model that expresses how earlier ice break-up dates influence within lake habitat product

67 We show that earlier ice break-up conditions created a "resource-rich" littor

68 pelagic habitat during periods with earlier ice break-up when pelagic resources were least abundant.

69 aximum in the Northern Hemisphere, expanding ice sheets forced a large number of plants, including tr

70 We simulate, experimentally, ice processing in disks under realistic conditions, that

71 cient to counteract all but the most extreme icing events.

72 sible (ice edge) or inaccessible (solid fast ice) to air-breathing predators.

73 KOH at low temperature, the transition to FE ice takes place, but its microscopic mechanism still nee

74 Because few ice core records from the Himalayas exist, understanding

75 the IRI efficiency of PVA and other flexible ice-binding polymers hinders the design of more potent I

76 e unified estimates of grounded and floating ice mass change from 2003 to 2019 using NASA's Ice, Clou

77 l periods, with grounding lines and fringing ice shelves extending onto continental shelves(8).

78 a-level change as a result of mass loss from ice sheets is strongly nonuniform, owing to gravitationa

79 us layers within the ice sheet measured from ice-penetrating radar between the two ice core sites.

80 ization and export in subglacial runoff from ice sheets is poorly constrained at present.

81 Furthermore, existing projections of future ice extent are based solely on the location of the 0- de

82 g the radiative forcing of greenhouse gases, ice sheets and mineral dust aerosols, this cooling trans

83 y low and is sourced from melting of glacial ice and direct release of occluded CO(2) gases into the

84 Glacier ice in the Southern Alps has become restricted to higher

85 marine benthic delta(18)O record for global ice volume and deep-sea temperature variations.

86 clear glacial-interglacial cycles in global ice volume and sea level largely driven by the growth an

87 remains unclear what makes a material a good ice former.

88 ian Sea sediment cores and an East Greenland ice core to resolve and constrain sea ice variations dur

89 r in a well-dated, high-resolution Greenland ice-core record that is >7,000 km from Ilopango; and cal

90 Losses outpaced gains, with grounded-ice loss from Greenland (200 billion tonnes per year) an

91 the progressive decay of Northern Hemisphere ice-sheets.

92 Heterogeneous ice nucleation caused by ice-nucleating particles (INPs)

93 als through a process known as heterogeneous ice nucleation.

94 eating proteins (INPs) promote heterogeneous ice nucleation more efficiently than any other material.

95 the edge structures of 2D bilayer hexagonal ice grown on a Au(111) surface.

96 ws regarding the growth of bilayer hexagonal ices and 2D hexagonal matter in general.

97 s in Arctic sea ice dynamics as historically ice-covered areas become increasingly ice-free during su

98 Marine ice (sea ice, ice shelf and glacier retreat) losses generate a valuabl

99 China that were used to make the implicated ice cream.

100 2019 however, we observe an acceleration in ice motion coincident with atmospheric cooling and a ~15

101 te to our understanding of human activity in ice-marginal environments and have implications for unde

102 Delta(33)S is similar to that discovered in ice core sulphate originating from stratospheric volcani

103 also host epiphytic bacteria; these include ice-nucleating (INA+) bacteria, which induce frost damag

104 thermal expansion of the ocean and increased ice-mass loss from Greenland.

105 ically ice-covered areas become increasingly ice-free during summer.

106 with withheld proxies as well as independent ice core and speleothem delta(18)O measurements.

107 e initiates a feedback process where initial ice shelf weakening triggers the development of damage i

108 the 1977 data, provide valuable insight into ice shelf cavity circulation and aid understanding of th

109 se of CH(4) stored in bubbles in winter lake ice.

110 The Greenland Ice Sheet is the largest land ice contributor to sea level rise.

111 ter stability of the EAIS and increased land-ice volumes in the Northern Hemisphere.

112 under realistic conditions, that is, layered ices irradiated by soft X-rays.

113 es to predation associated with the marginal ice zone (MIZ) of the McMurdo Sound, Antarctica, polynya

114 consumption, (3) they forage in the marginal ice zones, and (4) they feed on prey located closer to p

115 Marine ice (sea ice, ice shelf and glacier retreat) losses gene

116 blue carbon increases with losses of marine ice over high latitude continental shelf areas.

117 ng-term partial collapse owing to the marine ice-sheet instability.

118 alts(10) and bacteria(12) implies that MIS11 ice loss was coupled with marine flooding.

119 grids and that these manifest in nonuniform ice after vitrification.

120 ther evidence of the decline of the northern ice cap.

121 ability of isoprene-derived SOA to nucleate ice under a range of atmospheric conditions.

122 stress that prompt the bacteria to nucleate ice.

123 change from thermal expansion of the ocean, ice-mass loss and changes in terrestrial water storage i

124 y linked to the high catalytic activities of ice surfaces.

125 examination that entailed administration of ice, thin liquid, thick liquid, puree, and cracker bolus

126 s underwater vehicle, enables calculation of ice sheet retreat rates from a complex of grounding-zone

127 The collapse of ice shelves that buttress(11-13) the ice sheet accelerat

128 heet discharge, indicating close coupling of ice-ocean dynamics spanning the past 42,000 years.

129 el largely driven by the growth and decay of ice sheets in the Northern Hemisphere.

130 Furthermore, careful evaluation of ice core records points to the occurrence of several clo

131 ful subzero preservation is the formation of ice at temperatures below freezing.

132 ale wherein participants traversed a grid of ice blocks placed 200 m above the ground.

133 Antifreeze proteins restrict the growth of ice crystals during recrystallization and therefore find

134 Moreover, using the information of ice sputter yield, we successfully conduct 3D molecular

135 olcanic freezer' containing ~3 x 10(9) kg of ice on average with maxima reaching ~10(10) kg.

136 dicate that the main constituent is a mix of ice and refractory materials characterized by high poros

137 As patterns of ice loss around Antarctica become more uniform, there is

138 vaporated due to the lower vapor pressure of ice compared with water, resulting in a frost-free zone

139 e as indicators to predict the production of ice nucleants from the fuel.

140 The accelerating rate of ice loss reflects regional-specific climate conditions a

141 s disk with a composition similar to that of ice giant planets(14) demonstrated that massive planets

142 Three types of ice apple juices and three autochthonous yeast strains w

143 d less bruising, facial swelling, and use of ice pack for the ERL group.

144 Long-term soil warming of ice-rich permafrost can result in thermokarst formation

145 the net impact of hydro-dynamic coupling on ice motion remains poorly understood.

146 , or directly, mostly through its effects on ice shelves.

147 t the unique properties of free-OH groups on ice, putatively linked to the high catalytic activities

148 Sputter yield of a 20 keV Ar(1800)(+) ion on ice has been determined as 1500 (+/-8%) water molecules

149 are indicative of active iodine recycling on ice in the upper troposphere (UT), support the upper end

150 ater forms morainal banks (marine shoals) or ice-contact deltas that reduce water depth, stabilizing

151 ons for how bowhead whales, and likely other ice-associated Arctic marine mammals, will cope with cha

152 was partially compensated by mass gains over ice sheet interiors (increased snow accumulation).

153 Results demonstrate that multiyear pack ice remained a robust feature of the western and central

154 plification of warming and loss of perennial ice cover are set to dramatically alter available Arctic

155 e suggested that during the late Pleistocene ice ages, surface-deep exchange was somehow weakened in

156 e temperature, sea level and extent of polar ice sheets during Earth's past interglacial warm periods

157 Extensive areas of polar ice sheets were grounded below sea level during both gla

158 n our record reveals the key role that polar ice volume plays in the predictability of Cenozoic clima

159 tarctic Circle, it is disputed whether polar ice could exist under such environmental conditions.

160 We present ice core isotopic measurements of methane (Delta(14)C, d

161 t vigorous updrafts (>50 m/s) and prodigious ice production explain the impressive number of lightnin

162 eport that they are composed of methane-rich ice.

163 Although river ice extent has been shown to be declining in many region

164 : compared with 2009-2029, the average river ice duration declines by 16.7 days under Representative

165 change and predicted future changes in river ice extent and duration have not yet been quantified glo

166 To project future changes in river ice extent, we developed an observationally calibrated a

167 ons, we show that the global extent of river ice is declining, and we project a mean decrease in seas

168 -ice habitat in KB shifted from a year-round ice platform (~50% coverage in summer) in the 1990s to n

169 Mass lost from West Antarctica's ice shelves accounted for more than 30% of that region's

170 h of the buttressing regions of Antarctica's ice shelves are vulnerable to hydrofracture if inundated

171 Quantifying changes in Earth's ice sheets and identifying the climate drivers are centr

172 Sea ice is considered quintessential habitat for bowhead wha

173 Marine microalgae within seawater and sea ice fuel high-latitude ecosystems and drive biogeochemic

174 stiff foams, fiber composites, wood, and sea ice, the effective mode I fracture energy depends strong

175 ndance at most breeding colonies, annual sea ice fluctuations often explained less than 10% of the te

176 ited a mix of thick multiyear and annual sea ice year-round.

177 We suggest Antarctic sea ice and Atlantic overturning conditions favoured abyssal

178 annual variation of Arctic and Antarctic sea ice concentration and observe decreases in the mean sea

179 ammals, will cope with changes in Arctic sea ice dynamics as historically ice-covered areas become in

180 The rapid decrease in Arctic sea ice is motivating development and increasing oil and gas

181 ate change, future loss of summer Arctic sea ice will accelerate the thawing of Siberian permafrost.

182 nce of natural climate drivers on Arctic sea ice.

183 production than in the region covered by sea ice.

184 enland ice core to resolve and constrain sea ice variations during four D-O events between 32 and 41

185 Here we present unprecedentedly detailed sea ice proxy evidence from two Norwegian Sea sediment cores

186 ion is responding to rapidly diminishing sea ice, driven in part by changes in heat flux from the Nor

187 fat index was higher in years of earlier sea ice breakup with no change occurring in polar bears.

188 e sea ice behavior and to predict future sea ice behavior.

189 , and also perform predictions of future sea ice concentration.

190 In the Late Holocene, sea ice expanded and regional climate became drier.

191 Marine ice (sea ice, ice shelf and glacier retreat) losses generate a va

192 undergo significant annual variation in sea ice concentration.

193 ower than microplastic concentrations in sea ice cores (2-17 particles L(-1)).

194 undance, distribution and composition in sea ice cores (n = 25) and waters underlying ice floes (n =

195 in turn leads to sustained anomalies in sea ice extent.

196 cations for the Arctic region, including sea ice loss, increased geopolitical attention, and expandin

197 nsistent with future projections of less sea ice and more precipitation in Arctic Alaska.

198 ration and observe decreases in the mean sea ice concentration from early to later periods, as well a

199 nthropogenic warming on the Arctic Ocean sea ice is ascertained and closely monitored.

200 The apparent use of sea ice as a predator refuge also has implications for how b

201 on (KMD) is applied to satellite data of sea ice concentration for the Northern and Southern hemisphe

202 ht into spatial and temporal dynamics of sea ice concentration not apparent in traditional approaches

203 exity of the spatio-temporal dynamics of sea ice makes it difficult to assess the temporal nature of

204 red flux and accelerates the freezing of sea ice.

205 ends are harder to monitor than those of sea ice.

206 ntral Lomonosov Ridge and that perennial sea ice remained present throughout the present interglacial

207 Chlamydomonas sp. ICE-L thrives in polar sea ice, where it tolerates extreme low temperatures, high s

208 e HadCM3 simulations reveal that reduced sea ice leads to a strengthened Aleutian Low shifted west, p

209 Reduced sea ice may contribute to warming of Arctic air(4-6), which

210 eduction of Ekman pumping due to reduced sea ice-ocean surface stress.

211 production will continue to rise should sea ice decline further.

212 ions suggest the complete loss of summer sea ice by the middle of this century(1).

213 the temporal and spatial dynamics of the sea ice behavior and to predict future sea ice behavior.

214 ng this iconic marine predator as a true sea ice obligate and providing a firm basis for projection u

215 increased permafrost vulnerability when sea ice is absent, can be explained by changes in both heat

216 The robustness of permafrost when sea ice is present, as well as the increased permafrost vuln

217 whereas increases were due to widespread sea ice loss during the first decade, the subsequent rise in

218 Blue carbon change with sea ice and ice shelf losses has been estimated, but not how

219 cal distribution of microplastics within sea ice cores.

220 edimentary records to reconstruct Arctic sea-ice fluctuations.

221 changes in the seasonal cycle of Arctic sea-ice that are forced by orbital variations and volcanic e

222 We assess sea-ice changes in KB together with changes in polar bear mo

223 The mean duration between sea-ice retreat and advance increased from 109 to 160 days (

224 The annual cycle of sea-ice habitat in KB shifted from a year-round ice platform

225 ts, both bearing information on the past sea-ice cover.

226 with increasing temperature and receding sea-ice cover, is tightly connected to lower latitudes throu

227 ons of previously stored Hg from thawing sea-ice, glaciers, and permafrost.

228 , and we project a mean decrease in seasonal ice duration of 6.10 +/- 0.08 days per 1- degrees C incr

229 rrently, KB is transitioning to a seasonally ice-free region because of climate change.

230 variable precipitation, resulting in shorter iced-over periods and variable tributary flows as well a

231 ge, confined at the interface between a spin ice and an isostructural antiferromagnetic pyrochlore ir

232 Reminiscent of those described for spin ice, these impurity-induced strings are proposed to exis

233 ficial) system that realizes the kagome spin ice state.

234 s emergent quasiparticles in pyrochlore spin ice compounds.

235 mited because of volume-dependent stochastic ice formation at subzero temperatures.

236 In contrast, surface ice within the ablation zone and subglacial meltwaters r

237 and subsequent deformation of the suspended ice, with a threshold that depends directly on the shape

238 We contend that ice sheets create highly geochemically reactive particul

239 We find that ice velocity speed-up is greater in marginal areas, and

240 This suggests that ice-nucleation-induced wounding of the wheat leaf provid

241 apse of ice shelves that buttress(11-13) the ice sheet accelerates ice flow and sea-level rise(14-16)

242 edation and/or higher light levels along the ice edge.

243 and the same melting characteristics as the ice cream samples made with commercial gum Arabic.

244 Lowered abundance of krill at the ice edge indicated they were depleted or were responding

245 , amplifying summer energy absorption at the ice surface and enhancing meltwater runoff from the larg

246 Chemistry at the ice surface and ocean-rock interface might provide the b

247 dynamics of these different OH groups at the ice surface are attributed to enhanced intermolecular co

248 nal energy relaxation and dissipation at the ice surface for hydrogen-bonded OH groups.

249 at seek to quantify interactions between the ice sheet and the ocean.

250 l surveys of MeHg concentrations, during the ice-covered and open water seasons, across a hydrologic

251 During the ice-covered season, MeHg concentrations in lake waters w

252 ontents of sorbitol and shikimic acid in the ice juices.

253 f the warmest Pleistocene interglacials, the ice sheet margin at the Wilkes Basin retreated to near t

254 t, for Galilean and Saturnian icy moons, the ice shell can undergo hemispheric symmetry breaking only

255 dived deeper, and more frequently, near the ice edge.

256 wer atmospheric carbon dioxide levels of the ice ages.

257 tres inland from the current position of the ice margin, which-assuming current ice volumes-would hav

258 r pressure offset a larger proportion of the ice overburden pressure, leading to reduced effective pr

259 Flow models of the ice sheet and till-bedded glaciers elsewhere require a l

260 Enhanced basal melting of the ice shelves is thought to be the ultimate driver of chan

261 ion, we demonstrate that the presence of the ice-water interface leads to a lowering of the free-ener

262 new microscopic factors help to predict the ice nucleating ability.

263 acial waters of East Antarctica recorded the ice sheet's response to MIS11 warming.

264 Regarding the ice ciders, the apple mixture significantly influenced t

265 Rheological tests showed that the ice cream stabilized by the A. mearnsii gum had a more s

266 We show that the ice-albedo feedback spread explains uncertainties in pol

267 the Antarctic continental shelf towards the ice(4-6).

268 of CH(4) trapped in bubbles in and under the ice during fall freeze (bubble release), and diffusion o

269 Participants interacted with the ice blocks via sensors placed on their feet.

270 and by tracing isochronous layers within the ice sheet measured from ice-penetrating radar between th

271 energies, and vibrational properties of the ices.

272 enefited from using natural colorants in the icing solution, while "beijinhos" became softer and chew

273 These ice rules require each triangle plaquette to have a sing

274 age feedback potentially preconditions these ice shelves for disintegration and enhances grounding li

275 reater acceleration when compared to thicker ice further inland.

276 polar bears in the near-term due to thinner ice with increased biological production, although this

277 We hypothesise that under thinner ice, increases in basal water pressure offset a larger p

278 onas syringae by combining a high-throughput ice nucleation assay with surface-specific sum-frequency

279 the shear zones of Pine Island and Thwaites ice shelves.

280 Our data show that changes to ice break-up drive multi-directional results for resourc

281 Sea-level rise due to ice loss in the Northern Hemisphere in response to insol

282 negut's connection with the lattice match to ice, three new microscopic factors help to predict the i

283 ng step for binding of flexible molecules to ice is not the alignment of the molecule to the surface

284 km(3) or between 41 and 62% of the LIA total ice volume has been lost.

285 d enlarges fractures, potentially triggering ice-shelf collapse(3-5,8-10).

286 d from ice-penetrating radar between the two ice core sites.

287 astic abundance in surface waters underlying ice floes (0-18 particles m(-3)) were orders of magnitud

288 sea ice cores (n = 25) and waters underlying ice floes (n = 22) were assessed in the Arctic Central B

289 r, this standard technique produces vitreous ice with inconsistent thickness from specimen to specime

290 and protein distribution across the vitreous ice.

291 -aimed at preserving thin, uniform vitrified ice and improving protein adsorption-have been considere

292 Water ice was not detected.

293 xposed water ice from outbursts(4) and water ice in shadow(5,6).

294 strings are proposed to exist in doped water ice too, where IRs are even stronger.

295 previously observed in freshly exposed water ice from outbursts(4) and water ice in shadow(5,6).

296 t exposed primitive water ice-that is, water ice from the time of the comet's formation 4.5 billion y

297 It exposed primitive water ice-that is, water ice from the time of the comet's form

298 s made 19 months later found that this water ice, mixed with ubiquitous dark organic-rich material, h

299 g mass, flowing faster, and retreating where ice is exposed to warm ocean waters.

300 ginal areas, and is strongly correlated with ice thickness.