ライフサイエンスコーパス: sea ice

1 o accurately model low-polarity compounds in sea ice.

2 lynya is a large ice-free area surrounded by sea ice.

3 fluence of natural climate drivers on Arctic sea ice.

4 nfrared flux and accelerates the freezing of sea ice.

5 ions in light, temperature and the extent of sea ice.

6 m developed in situ despite the snow-covered sea ice.

7 nkton environment is constrained by seasonal sea ice.

8 m trends are harder to monitor than those of sea ice.

9 ary production than in the region covered by sea ice.

10 c dipole linked to the recent loss of Arctic sea ice.

11 only indirectly contribute to AA by melting sea-ice.

12 in Arctic Alaska were characterized by less sea ice, a greater contribution of isotopically heavy Ar

13 greatest sea ice concentration and earliest sea ice advance, while males foraged longer in polynyas

14 ce extent continues to increase, with autumn sea ice advances in the western Ross Sea particularly an

15 e spring, and in turn triggered the positive sea-ice albedo feedback process and accelerated the sea

16 support the extremophilic lifestyle of this sea ice alga include massively expanded gene families in

17 due to its extensive climate-driven loss of sea ice and accelerated growth of other stressors, inclu

18 The loss of sea ice and acceleration of ocean currents after 2007 re

19 ern Ross Sea dominate increases in Antarctic sea ice and are outside the range simulated by climate m

20 We suggest Antarctic sea ice and Atlantic overturning conditions favoured aby

21 The contrasting albedo of sea ice and dark melted surface areas is the key compone

22 is usually found in the bottom few cm of the sea ice and dominated by pennate diatoms attached to the

23 ave can also initiate widespread fracture of sea ice and further increase the likelihood of subsequen

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

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

26 mining sea level rise, the fate of Antarctic sea ice and its effect on the Earth's albedo, ongoing ch

27 Sea ice and its snow cover are critical for global proce

28 ons in the surface albedo, following loss of sea ice and land snow.

29 e consistent with future projections of less sea ice and more precipitation in Arctic Alaska.

30 were attributed to increase in temperature, sea ice and phytoplankton.

31 , we present evidence that the microbiota of sea ice and sea ice-influenced ocean are a previously un

32 layers and the atmosphere than to underlying sea ice and seawater.

33 m use of open water (predator-free) to dense sea ice and shorelines (predators present) was exhibited

34 ssure over the region arising from decreased sea ice and snow cover.

35 le component might reflect co-variability of sea ice and tundra productivity due to a common forcing,

36 lowing warm Atlantic Layer water, ice sheet, sea-ice and ice-shelf feedbacks, and sensitivity to high

37 Mean concentrations in seawater, sea-ice and snow were generally greater at the Arctic si

38 sion, the legacy of Arctic winter storms for sea-ice and the ice-associated ecosystem in the Atlantic

39 estrial snow cover, snow cover fraction over sea ice, and sea ice extent appear to contribute equally

40 se a positive feedback mechanism between the sea ice anomaly and atmospheric river activity, with ano

41 ivity, with anomalous south winds toward the sea ice anomaly potentially leading to more warm water i

42 pothesise that the late autumn Bering Strait sea-ice anomaly and Pacific atmospheric rivers were part

43 important implications for global sea level, sea ice area, and ocean circulation.

44 r tropospheric circulation data on September sea-ice area indicates that convection episodes produce

45 on of intermediate water, and the buildup of sea-ice around Antarctica, with implications for the glo

46 re, we demonstrate the primary importance of sea ice as a control on Greenland ice core [Formula: see

47 harbored the highest quantities, indicating sea ice as a possible transport vehicle.

48 The apparent use of sea ice as a predator refuge also has implications for h

49 so revealed that chemicals are released from sea ice at variable rates.

50 ntarctic, possibly due to full submersion of sea-ice at the former.

51 arts increasing in early winter, well before sea ice begins to retreat.

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

53 f the sea ice behavior and to predict future sea ice behavior.

54 y about two weeks and covaried strongly with sea ice break-out timing for all reproductive categories

55 n January and were primarily associated with sea-ice break-up.

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

57 smaller litters following years with earlier sea-ice breakup.

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

59 rily by atmospheric deposition and inflow of sea ice brine and that they form a snow-specific assembl

60 Results from a 1-D sea ice brine dynamics model supported this, but also in

61 The expulsion of relatively nutrient-rich sea ice brine into basal snow might have stimulated the

62 Accurate pH measurements in polar waters and sea ice brines require pH indicator dyes characterized a

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

64 southern Greenland is explained by DO event sea ice changes.

65 Future ocean and sea-ice changes affecting the distribution of such speci

66 We assess sea-ice changes in KB together with changes in polar bea

67 ukchi seas during two periods with different sea ice characteristics.

68 , we examine how inter-annual variability in sea ice concentration and advance affect the foraging be

69 ed longer in pack ice in years with greatest sea ice concentration and earliest sea ice advance, whil

70 y, we use spatially explicit remotely sensed sea ice concentration and high-resolution terrestrial pr

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

72 cillation (ENSO), and negatively affected by sea ice concentration and pelagic longline effort.

73 We found that mean sea ice concentration at breeding colonies (i.e., "preva

74 sition (KMD) is applied to satellite data of sea ice concentration for the Northern and Southern hemi

75 centration and observe decreases in the mean sea ice concentration from early to later periods, as we

76 nsight into spatial and temporal dynamics of sea ice concentration not apparent in traditional approa

77 The response of clouds to the changing sea ice concentration was directly observed.

78 tent, and also perform predictions of future sea ice concentration.

79 oraged longer in polynyas in years of lowest sea ice concentration.

80 that undergo significant annual variation in sea ice concentration.

81 a set of environmental parameters including sea-ice concentration (SIC) and mercury contamination.

82 s evident in recent years, whereas Antarctic sea-ice concentration exhibits a generally increasing tr

83 A decreasing trend in Arctic sea-ice concentration is evident in recent years, wherea

84 s, the leading mode of variability of global sea-ice concentration is positively correlated with the

85 s that contribute to the opposite changes in sea-ice concentration.

86 We examine sea ice concentrations at their known foraging grounds t

87 Pacific sea surface temperatures (STWCPSST), sea ice concentrations in the Beaufort Sea (SICBS), and

88 -term time series of observed and reanalysis sea-ice concentrations data suggest the possibility of t

89 Combining the influence of changing sea ice conditions and isotopic fractionation by phytopl

90 rticular, the biological effects of changing sea ice conditions are poorly understood.

91 biting southern coastlines affected by heavy sea ice conditions during the Last Glacial Maximum (LGM)

92 as during cold stadials and reduced seasonal sea ice conditions during warmer interstadials.

93 ber of days gray whales can forage, and thus sea ice conditions may be one limiting factor affecting

94 ter genera associated with low nutrients and sea ice conditions.

95 gional atmospheric and ocean temperatures or sea-ice conditions, although the colony population maxim

96 ng the 40-y record as a whole, the Antarctic sea ice continues to have a positive overall trend in ye

97 de lower than microplastic concentrations in sea ice cores (2-17 particles L(-1)).

98 c abundance, distribution and composition in sea ice cores (n = 25) and waters underlying ice floes (

99 ertical distribution of microplastics within sea ice cores.

100 aising the question of whether reductions in sea ice could increase contact between Arctic and sub-Ar

101 In contrast, it took the Arctic sea ice cover a full 3 decades to register a loss that g

102 t proxy records of Arctic Ocean temperature, sea ice cover and circulation.

103 These differences may result from the higher sea ice cover and decreased NPP during +SAM/La Nina peri

104 Sea ice cover and duration predetermine levels of phytop

105 n from the other 4 sectors and the Antarctic sea ice cover as a whole).

106 Ocean in general and the fate of the Arctic sea ice cover in particular.

107 Sea ice cover in the Arctic and Antarctic is an importan

108 shold response between an extensive seasonal sea ice cover in the Nordic Seas during cold stadials an

109 ur of the 5 sectors into which the Antarctic sea ice cover is divided all also have 40-y positive tre

110 omena, including the evolution of the Arctic sea ice cover, the El Nio Southern Oscillation (ENSO), t

111 oceanic processes, particularly diminishing sea ice cover, upper ocean warming, and increasing and p

112 arctic polynyas-large openings in the winter sea ice cover-are thought to be maintained by a rapid ve

113 ose timing is temporally matched to seasonal sea ice cover.

114 ing, thus explaining the recent reduction in sea-ice cover in the eastern Eurasian Basin.

115 sis is constrained by the limitations of the sea-ice cover record, preliminary statistical analyses o

116 ermediate depth water (AIW) temperatures and sea-ice cover spanning the last 1.5 million years (Ma) o

117 urvival, then increased temperature, reduced sea-ice cover, and stronger winds are affecting the popu

118 ing with increasing temperature and receding sea-ice cover, is tightly connected to lower latitudes t

119 ntents, both bearing information on the past sea-ice cover.

120 the melt seasons in the past 10 years, while sea ice coverage varies significantly year-to-year.

121 3 decades of gradual but uneven increases in sea ice coverage, the yearly average Antarctic sea ice e

122 ice loss is expected to take place over the sea-ice covered polar region, when sea ice is not fully

123 ce thus underpins the cardinal role of rapid sea ice decline and related feedbacks to trigger abrupt

124 mary production will continue to rise should sea ice decline further.

125 ad formation due to thinner and more dynamic sea ice despite projected increases in high-Arctic snowf

126 region is responding to rapidly diminishing sea ice, driven in part by changes in heat flux from the

127 thesize that rapid postglacial reductions in sea ice drove biological shifts across multiple widespre

128 sed land than for bears that remained on the sea ice during summer and fall, while mean concentration

129 xtensive phytoplankton blooms beneath ponded sea ice during summer, indicating that satellite-based A

130 ne mammals, will cope with changes in Arctic sea ice dynamics as historically ice-covered areas becom

131 vection caused by brine rejection in growing sea ice enabled M. rubrum to bloom at the ice-water inte

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

133 exceptional wintertime conditions arose from sea ice expansion and reduced ocean heat losses in the N

134 y in causing the observed Barents Sea winter sea ice extent (SIE) decline since 1979.

135 biting an upward trend since 1979, Antarctic sea ice extent (SIE) declined dramatically during austra

136 The sustained decreases of Antarctic sea ice extent after late 2016 are associated with a war

137 cover, snow cover fraction over sea ice, and sea ice extent appear to contribute equally to the Arcti

138 rends in climate model simulations.Antarctic sea ice extent continues to increase, with autumn sea ic

139 c Arctic regions experienced anomalously low sea ice extent in the early winter.

140 Winter Arctic sea ice extent will remain low but with a general increa

141 s of observed increasing trends of Antarctic sea ice extent, in September-October-November 2016, ther

142 Rapid warming, decline in sea ice extent, increase in riverine input, ocean acidif

143 that contribute to the decrease of Antarctic sea ice extent.

144 rth Pacific Ocean linked to change in Arctic sea ice extent.

145 sure and infection with reductions in Arctic sea ice extent.

146 creased the probability of record-low Arctic sea ice extent.

147 This in turn leads to sustained anomalies in sea ice extent.

148 Associated with this, a rapid decline of sea-ice extent and a decrease of its thickness has been

149 ries of record minima for the winter maximum sea-ice extent since 2015.

150 trend, mostly explained by the reduction in sea-ice extent, is consistent with independent atmospher

151 a ice coverage, the yearly average Antarctic sea ice extents reached a record high of 12.8 x 10(6) km

152 abundance at most breeding colonies, annual sea ice fluctuations often explained less than 10% of th

153 ne sedimentary records to reconstruct Arctic sea-ice fluctuations.

154 es: cumulative ocean surface heat fluxes and sea ice formation close to PIIS; and interannual reversa

155 Sea ice formation was shown to result in the entrainment

156 d release of oceanic heat has reduced winter sea-ice formation at a rate now comparable to losses fro

157 redict that by 2050 the Arctic Ocean will be sea ice free each summer.

158 Lomonosov Ridge area experienced seasonally sea-ice-free conditions, at least, sporadically, until a

159 ration timing as related to delayed regional sea ice freeze-up since the 1990s, using two independent

160 ing occurred significantly later as regional sea ice freeze-up timing became later in the Beaufort, C

161 as controlled by cyclone snowfall and 29% by sea-ice freeze-up.

162 Marine microalgae within seawater and sea ice fuel high-latitude ecosystems and drive biogeoch

163 torm deepens the snow pack and insulates the sea-ice, further inhibiting ice growth throughout the re

164 issions of previously stored Hg from thawing sea-ice, glaciers, and permafrost.

165 overning the fate of organic contaminants in sea ice grown from artificial seawater.

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

167 terrestrial food, and as the availability of sea ice habitat increased.

168 The annual cycle of sea-ice habitat in KB shifted from a year-round ice plat

169 ntrasting regional changes in Southern Ocean sea ice have occurred over the last 30 years with distin

170 The consequences of rapid changes in Arctic sea ice have the potential to affect migrations of a num

171 Marine ice (sea ice, ice shelf and glacier retreat) losses generate

172 een proposed to explain DO events, including sea ice, ice shelf buildup, ice sheets, atmospheric circ

173 Pro-glacial melange (a mixture of sea ice, icebergs, and snow) may be tightly packed in th

174 nfidence in their ability to simulate future sea ice in in a rapidly evolving Arctic.

175 0 degrees C per year, freshwater runoff and sea ice in the 1980s) rather than by local changes in th

176 This history mirrors that of year-round sea ice in the Arctic Ocean, which was largely absent be

177 ived from the relatively long persistence of sea ice in the autumn.

178 ard longwave radiation, as well as a loss of sea ice in the Barents and Kara seas, were observed.

179 A large retreat of sea-ice in the 'stormy' Atlantic Sector of the Arctic Oc

180 ear pack-ice north of Svalbard, showcase how sea-ice in this region is frequently affected by passing

181 xplain an important fraction of the observed sea ice increase.

182 evidence that the microbiota of sea ice and sea ice-influenced ocean are a previously unknown signif

183 The fate of persistent organic pollutants in sea ice is a poorly researched area and yet ice serves a

184 the increased permafrost vulnerability when sea ice is absent, can be explained by changes in both h

185 Sea ice is an important component of the global climate

186 ng anthropogenic warming on the Arctic Ocean sea ice is ascertained and closely monitored.

187 Sea ice is considered quintessential habitat for bowhead

188 nce of zooplankton in the seasonally varying sea ice is correlated with the Southern Annular Mode (SA

189 timing and magnitude of snow accumulation on sea ice is crucial for understanding snow's net effect o

190 AA largely disappears when Arctic sea ice is fixed or melts away.

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

192 over the sea-ice covered polar region, when sea ice is not fully recovered in winter.

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

194 permafrost is robust to warming when Arctic sea ice is present, but vulnerable when it is absent.

195 Projected Arctic warming, with more open sea ice leads providing halogen sources that promote AMD

196 The HadCM3 simulations reveal that reduced sea ice leads to a strengthened Aleutian Low shifted wes

197 Until recent declines in Arctic sea ice levels, narwhals (Monodon monoceros) have lived

198 , reflected by more prevalent easterly flow, sea ice loss does not lead to Northern European winter c

199 ly, whereas increases were due to widespread sea ice loss during the first decade, the subsequent ris

200 Historically, sea ice loss in the Arctic Ocean has promoted increased

201 his feedback process; a similar mechanism of sea ice loss is expected to take place over the sea-ice

202 as analogue to predict the effects of Arctic sea ice loss on mid-latitude weather.

203 n proposed as a dynamical pathway for Arctic sea ice loss to cause Northern European cooling.

204 mplications for the Arctic region, including sea ice loss, increased geopolitical attention, and expa

205 d to the Arctic ocean and contributes to the sea ice loss, thereby enhancing Arctic warming.

206 uel extraction predicted to accompany Arctic sea ice loss.

207 sea surface exposed to air in the region of sea ice loss.

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

209 , amplified warming in Arctic regions due to sea-ice loss and other processes, relative to global mea

210 Arctic sea-ice loss is a leading indicator of climate change an

211 under unmitigated climate change, continued sea-ice loss is expected to eventually have negative dem

212 We conclude that sea-ice loss is necessary for the existence of large AA

213 We conclude that sea-ice loss of the magnitude expected in the next decad

214 larger sea-ice loss, and models with bigger sea-ice loss produce larger AA.

215 ds with larger AA are associated with larger sea-ice loss, and models with bigger sea-ice loss produc

216 o April and only over areas with significant sea-ice loss.

217 omplexity of the spatio-temporal dynamics of sea ice makes it difficult to assess the temporal nature

218 net effect on the surface energy budget and sea-ice mass balance.

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

220 Reductions in Arctic sea ice may promote the negative phase of the North Atla

221 Natural external forcing causes changes in sea-ice mediated export of freshwater into areas of acti

222 ting a marine biosphere-climate link through sea ice melt and low altitude clouds that may have contr

223 l, Arctic Ocean warming following the summer sea-ice melt drives vertical convection that perturbs th

224 Seasonal sea-ice melt processes may alter the exchange rates of s

225 albedo feedback process and accelerated the sea ice melting in the summer.

226 l modify the change in planetary albedo when sea ice melts.

227 imate, but no studies have examined Holocene sea ice, moisture, and ocean-atmosphere circulation in A

228 Results from the Norwegian young sea ICE (N-ICE2015) expedition, a five-month-long (Jan-J

229 tic-Subarctic, i.e. the northern hemisphere, sea ice now exhibits similar levels of seasonality to th

230 ishing this iconic marine predator as a true sea ice obligate and providing a firm basis for projecti

231 endent observations of the atmosphere, snow, sea-ice, ocean, and ecosystem.

232 he reduction of Ekman pumping due to reduced sea ice-ocean surface stress.

233 At Ryder Bay, West Antarctic Peninsula (WAP) sea ice, oceanography, phytoplankton and encrusting zoob

234 Findings suggest that sea-ice OCP burdens originate from both snow and seawate

235 The effects of declining Arctic sea ice on local ecosystem productivity are not well und

236 racterize multidecadal and annual effects of sea ice on population growth.

237 he understanding of the impact of retreating sea ice on the atmospheric circulation.

238 ernates between being primarily regulated by sea ice or glacial discharge from the surrounding ground

239 -deficient zone in the oceanic water column, sea ice or polar snow.

240 e similar to atmospheric communities than to sea ice or seawater communities.

241 paleothermometry of the ostracode Krithe and sea-ice planktic and benthic indicator species, we sugge

242 asonal lag relationship has implications for sea ice prediction.

243 poleward migratory predator through varying sea ice property and dynamic anomalies.

244 Here we present unprecedentedly detailed sea ice proxy evidence from two Norwegian Sea sediment c

245 e AA and that models need to simulate Arctic sea ice realistically in order to correctly simulate Arc

246 Our independent sea ice records consistently reveal a millennial-scale v

247 resent study, detailed physical mechanism of sea ice reduction in winter (December-February) is ident

248 Sea ice reduction is accelerating in the Barents and Kar

249 egional records of Holocene hydroclimate and sea ice reduction scenarios modeled by the Hadley Centre

250 ngwave radiation is an essential element for sea ice reduction, but can primarily be sustained by exc

251 winter could recur in future years when the sea-ice reduction in the Pacific Arctic interacts with e

252 They document substantial and rapid sea ice reductions that may have happened within 250 y o

253 of ice melting in mid-May through inhibiting sea-ice refreezing in the winter and accelerating the pr

254 re likely to occur under the thinning Arctic sea ice regime.

255 recursors released by open water and melting sea ice regions.

256 Excluding perennial sea-ice regions, the mean warming trend is 0.11 K per de

257 mistry is important for the understanding of sea ice related impacts on atmospheric dynamics.

258 Yet, given the weak effects of annual sea ice relative to the large unexplained variance in ye

259 d central Lomonosov Ridge and that perennial sea ice remained present throughout the present intergla

260 Sea-ice retreat allows for an increased transport of hea

261 The mean duration between sea-ice retreat and advance increased from 109 to 160 da

262 accelerate Arctic warming in the context of sea-ice retreat and increasing low-level cloud cover.

263 The date of spring sea-ice retreat in the previous year was positively corr

264 As sea ice retreats and dissolved organic carbon inputs to

265 The observations suggest that when sea-ice retreats, cloud fraction of the ice-free region

266 icroscopic examination of fixed seawater and sea ice samples revealed chytrids parasitizing diatoms c

267 he distribution profile between seawater and sea-ice showed a compound-dependency for Arctic samples

268 systems, particularly through ocean warming, sea-ice shrinkage and enhanced pollution.

269 PM(1) mass originated in open ocean (OO) and sea ice (SI) regions, respectively.

270 tic Ocean temperatures influence ecosystems, sea ice, species diversity, biogeochemical cycling, seaf

271 ow layer that was in direct contact with the sea ice surface harbored a higher abundance of cells tha

272 hich winter storms impact the coupled Arctic sea-ice system.

273 r study clarifies the range of mechanisms in sea ice/terrestrial productivity coupling, allowing the

274 l/sub-regional and large-scale components of sea ice/terrestrial productivity coupling.

275 d by changes in the seasonal cycle of Arctic sea-ice that are forced by orbital variations and volcan

276 ks, stiff foams, fiber composites, wood, and sea ice, the effective mode I fracture energy depends st

277 ual model connecting seasonal loss of Arctic sea ice to midlatitude extreme weather events is applied

278 dings were obtained under seasonally varying sea ice to the north of Alaska during a period of 154 da

279 This contributes to weak western Ross Sea ice trends in climate model simulations.Antarctic se

280 Autumn sea ice trends in the western Ross Sea dominate increase

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

282 ty on the seasonal buildup of snow on Arctic sea ice using model, satellite, and in situ data over 19

283 otope data are recording multidecadal Arctic sea ice variability and through the climate model ensemb

284 Constraining the past sea ice variability in the Nordic Seas is critical for a

285 cord of Labrador Sea productivity related to sea-ice variability in Labrador, Canada that extends wel

286 s to both observational and proxy records of sea-ice variability, and show persistent patterns of co-

287 d fundamental changes in AIW temperature and sea-ice variability.

288 Greenland ice core to resolve and constrain sea ice variations during four D-O events between 32 and

289 nce of the ice-albedo feedback on summertime sea ice, we find that during some time interval of the s

290 c response to a prescribed decline in Arctic sea ice, we show that including interactive stratospheri

291 ction of snowpack microbial communities over sea ice were influenced primarily by atmospheric deposit

292 lga Chlamydomonas sp. ICE-L thrives in polar sea ice, where it tolerates extreme low temperatures, hi

293 nt of brine for controlling chemical fate in sea ice which provides a pathway for exposure to ice-ass

294 ed to explain the accelerated loss of Arctic sea ice, which remains to be controversial.

295 climate change, future loss of summer Arctic sea ice will accelerate the thawing of Siberian permafro

296 Most likely, September Arctic sea ice will effectively disappear at between approximat

297 Our results imply that declining Arctic sea ice will lead to an increasingly energetic Beaufort

298 n association with the formation and melt of sea ice, with distinct microalgal communities that trans

299 warm Atlantic Ocean water to melt all Arctic sea ice within a few years, a cold halocline limits upwa

300 nhabited a mix of thick multiyear and annual sea ice year-round.