ライフサイエンスコーパス: glacier

1 e.g. factors linked to treeline position and glaciers).

2 of the total ice loss expected from Thwaites Glacier.

3 +/-0.2 muM) over a 14 day period at Leverett Glacier.

4 2 for Jakobshavn, Helheim, and Kangerlussuaq glacier.

5 ts and decreased with distance away from the glacier.

6 Jakobshavn Isbrae, Greenland's major outlet glacier.

7 nge can instigate surges of Arctic tidewater glaciers.

8 involve a transient increase due to melting glaciers.

9 community with the complete disappearance of glaciers.

10 rrent simulations of ice loss from tidewater glaciers.

11 ng increased discharge of marine-terminating glaciers.

12 ribution to sea level rise of PIG and nearby glaciers.

13 ils of known age exposed upon the retreat of glaciers.

14 vance and retreat of Pleistocene continental glaciers.

15 ive the retreat of modern marine-terminating glaciers.

16 of 8.1 +/- 1.1 millimetres from these three glaciers.

17 and climate from a global compilation of 38 glaciers.

18 erated by physical comminution of bedrock by glaciers.

19 athway of BC from distant regions to the HTP glaciers.

20 that may be present in many Arctic tidewater glaciers.

21 7 glaciers (85% of D) and indirectly for 110 glaciers (15%) using velocity-scaled reference fluxes.

22 anisms driving the observed retreat of these glaciers, 2 ~32-m-long ice cores to bedrock recovered in

23 grounding line migration of 38% for Thwaites Glacier 350 years in the future, or 26.8% reduction in c

24 trace metal ice core record from the Dasuopu glacier (7,200 m, central Himalayas), the highest drilli

25 ischarge, D, into the ocean directly for 107 glaciers (85% of D) and indirectly for 110 glaciers (15%

26 In 2017-2019 a surge of Shispare Glacier, a former tributary of the once larger Hasanabad

27 state-of-the-art ice sheet model of Thwaites Glacier, a marine-terminating glacier in West Antarctica

28 Surge-type glacier accelerations often occur with a decadal to cent

29 on (~10%), the recession of lake-terminating glaciers accounted for up to 32% of mass loss in differe

30 thropogenic black carbon (BC) to snowmelt in glacier accumulation zones of Central Asia based on in-s

31 nmental features that limit L. tumana and Z. glacier across the northern Rocky Mountains.

32 e determined volume changes for 400 mountain glaciers across the Southern Alps, New Zealand for three

33 resulting from interaction between previous glacier advance, recession and outburst flooding.

34 wave periods upscaled to Greenlandic outlet glaciers agree with field observations.

35 On the GrIS, glacier algae direct only ~1 to 2.4% of incident energy

36 driven by the direct and indirect impacts of glacier algae on ice albedo, with a significant negative

37 the photophysiological mechanisms that allow glacier algae to thrive on and darken the bare ice surfa

38 e cellular content of chlorophyll a) enables glacier algae to tolerate extreme irradiance (up to ~4,0

39 Blooms of Zygnematophycean "glacier algae" lower the bare ice albedo of the Greenlan

40 GrIS may be attributable to the presence of glacier algae.

41 ution Imaging Spectroradiometer [MODIS]) and glacier algal biomass (R (2) = 0.75, n = 149), indicatin

42 ased 50-fold by phenolic pigmentation, while glacier algal chloroplasts positioned beneath shading pi

43 Dozens of cirque and valley glaciers, along with the southern margin of the CIS, adv

44 eness of this event, we extend the record of glacier and ocean changes back 1700 years by analyzing a

45 Climate warming-induced glacier and snow loss clearly imperils the persistence o

46 Pine Island Glacier and Thwaites Glacier in the Amundsen Sea Embayme

47 ow fjords that front many marine-terminating glaciers and can reduce calving by buttressing.

48 ediments, especially cryoconite, in European glaciers and Greenland.

49 Ongoing changes in glaciers and ice sheets are driven by submarine melting

50 Ice loss from the world's glaciers and ice sheets contributes to sea level rise, i

51 ts in an increased flux of ice from adjacent glaciers and ice streams, thereby raising sea level glob

52 ade aggravates the BC pollution over the HTP glaciers and may cause significant climate change there.

53 haea) in distinct surface habitats and on 12 glaciers and permanent snow fields in Svalbard and Arcti

54 cover five to 15 times the area of permanent glaciers and snow, highlighting their eco-hydrological i

55 Climate warming is causing rapid loss of glaciers and snowpack in mountainous regions worldwide.

56 Mass loss from glaciers and the Greenland Ice Sheet explains the high r

57 ats, ranging from hot springs and deserts to glaciers and the open ocean.

58 ely consumed CO(2) up to 42 km downstream of glaciers, and cumulatively transformed the High Arctic's

59 main contributors to sea-level rise (oceans, glaciers, and ice sheets) respond to climate change on t

60 f previously stored Hg from thawing sea-ice, glaciers, and permafrost.

61 lt its floating ice shelves, destabilize the glaciers, and raise sea level.

62 The Taylor Glacier, Antarctica, periodically expels iron-rich brine

63 lysis as the key to decipher so far untapped glacier archives of the last millennium.

64 makes this region vulnerable to drought, but glaciers are a uniquely drought-resilient source of wate

65 le economically and socially to drought, but glaciers are a uniquely drought-resilient source of wate

66 ems.The reason some of the Earth's tidewater glaciers are advancing despite increasing temperatures i

67 systems, and demonstrate that debris-covered glaciers are among the most sensitive recorders of obliq

68 Moraine-dammed lakes at debris-covered glaciers are becoming increasingly common and pose signi

69 Glaciers are highly effective agents of erosion that hav

70 Glaciers are important drivers of environmental heteroge

71 mountain stream insects, particularly where glaciers are likely to vanish on contemporary timescales

72 Across the Arctic, glaciers are melting and permafrost is thawing at unprec

73 Glaciers are melting rapidly.

74 Worldwide, glaciers are receding rapidly due to climate change, wit

75 Moreover, mountain glaciers are typically steeper, more dependent upon basa

76 Arctic, located proximal to ice sheet outlet glaciers, are required.

77 functional genes was mainly associated with glacier area proportion, glacier source proportion, tota

78 Recently, many surging tidewater glaciers around the Arctic Barents Sea region question w

79 arch needle within the ice of Schaufelferner glacier at 2,870 m asl (Stubai Alps, Austria) allows for

80 The ice blocks obtained at Chli Titlis glacier at 3,030 m asl (Swiss Alps) have been dated by s

81 -Beringia dispersal after the melting of the glaciers at the end of the Pleistocene.

82 fer direct access to the stratigraphy at the glacier base and validation against existing age constra

83 up-glacier, mobilizing the entire 450 km(2) glacier basin over a few days as the till entered an uns

84 ith our main conclusion that friction at the glacier bed does not control fast glacier flow.

85 sported 4.8 x 10(6) m(3) of meltwater to the glacier bed in ~5 h, reducing the lake to a third of its

86 e 20(th) century high SSTs in magnitude, the glacier behaved differently during the 20(th) century.

87 Contrasting climatic settings influence glacier behaviour at the regional scale, but high intra-

88 involved the near-complete disappearance of glaciers below 4700 masl in the eastern Andean cordiller

89 ptobiosis during six centuries of cold-based glacier burial in Antarctica, 2) after re-exposure due t

90 he highest elevation streams primarily below glaciers, but also snowfields and groundwater springs.

91 e in these regions that currently have large glaciers, but few lakes, if future projected ice loss ge

92 1900 AD followed by elevated 20(th) century glacier calving due to the loss of the tongue.

93 ent and have been obtained at two artificial glacier caves.

94 e, we combine high-resolution biological and glacier change (ca. 1850-2015) datasets for Glacier Nati

95 However, predictions of glacier change largely rest on unconstrained theory for

96 ring the large-scale and yet region-specific glacier changes taking place over the HK.

97 demonstrates the potential for using alpine glacier chronologies in the Transantarctic Mountains as

98 iment and meltwater delivery from changes in glacier configuration may impact interpretations of mari

99 Inclusion of thermal expansion and glacier contributions results in a global total SLR esti

100 t a 70 km-diameter crater into a continental glacier could release between 8.7 x 10(13) to 5.0 x 10(1

101 Glaciers cover approximately 10% of the Earth's land sur

102 s and slow advances typical of the tidewater glacier cycle observed in modern systems.

103 retreat, in a process known as the tidewater glacier cycle.

104 ry inputs to arctic ecosystems downstream of glaciers despite recent reductions in global mercury emi

105 refugia for mountain biodiversity even after glaciers disappear.

106 enic forcing, at the same time that the last glaciers disappeared.

107 Even in years of high SMB, enhanced glacier discharge has remained sufficiently high above e

108 red to bedrock on the summit of one of these glaciers document a rapid pace in the loss of ice cover

109 largest Alaskan Cordilleran Ice Sheet outlet glacier during Last Glacial Maximum climate transitions.

110 eases in meltwater could induce a shift to a glacier dynamic regime characterised by seasonal-scale h

111 melting), and Greenland and Antarctic outlet glaciers (dynamic response to ocean melting) was partial

112 The mass loss is controlled at 66 +/- 8% by glacier dynamics (9.1 mm) and 34 +/- 8% by SMB (4.6 mm).

113 tarctic Peninsula, with unknown impacts upon glacier dynamics at the ice-bed interface.

114 f young organic matter sources released from glacier ecosystems and their surrounding watersheds.

115 Glacier ecosystems are teeming with life on, beneath, an

116 nthesis of the microbial ecology of mountain glacier ecosystems, and particularly those at low- to mi

117 Flow models of the ice sheet and till-bedded glaciers elsewhere require a law that relates slip resis

118 ra subglacial basin, that marine-terminating glaciers existed at the Sabrina Coast by the early to mi

119 a one-month period in early summer 2016, the glacier experienced essentially no calving, and was butt

120 onar surveys to image a subsurface tidewater glacier face and document a time-variable, three-dimensi

121 limnology, to conclusively show that certain glacier-fed freshwater ecosystems are important and prev

122 in the catchment of Lake Brewster, an alpine glacier-fed lake located in the Southern Alps of New Zea

123 Glacier-fed rivers and lakes, however, differ critically

124 Glacier-fed streams also export more acid-soluble iron (

125 Benthic biofilms in glacier-fed streams harbor diverse microorganisms drivin

126 en metabolic pathways and abiotic factors in glacier-fed streams in the Tianshan Mountains in Central

127 e microbial functions of benthic biofilms in glacier-fed streams, we predicted metagenomes from 16s r

128 Because these ice shelves buttress glaciers feeding into them, their ocean-induced thinning

129 Under a wide range of glacier flow conditions and layer counting uncertainty,

130 Glacier flow instabilities can rapidly increase sea leve

131 ion at the glacier bed does not control fast glacier flow.

132 results motivate a generalized slip law for glacier-flow models that combines processes of hard-bedd

133 Over the past 40 years, glaciers flowing into the Amundsen Sea sector of the ice

134 , Svalbard were used to reconstruct Holocene glacier fluctuations.

135 and the preconditioning of land-terminating glaciers for new lake development increases the likeliho

136 edrock-ice interface, proglacial streams and glacier forefields.

137 ocity, and surface mass balance (SMB) of 260 glaciers from 1972 to 2018.

138 ing once the melange mass within 7 km of the glacier front had decreased by >40%.

139 edge that increased in thickness towards the glacier front.

140 king (~18 +/- 0.5 m d(-1)) and resulted in a glacier frontal advance of 1495 +/- 47 m.

141 nderscore the need to account for individual glacier geometry when predicting future behaviour.

142 mountains-have the highest concentration of glaciers globally, and 800 million people depend in part

143 esent on the ice shelf in front of Petermann Glacier, Greenland, but other systems, such as on the La

144 Ice-mass loss-predominantly from glaciers-has caused twice as much sea-level rise since 1

145 For example, European glaciers have retreated during the 20(th) century while

146 of the area; the steeply sloping bed allowed glaciers here to stabilise during retreat.

147 ormer tributary of the once larger Hasanabad Glacier (Hunza region), dammed the proglacial river of M

148 lect stick-slip motion which occurs when the glacier hydrological system is unable to accommodate the

149 re consistent with values measured from cold glacier ice and while this may be feasible, uncertaintie

150 The resistivity signature of glacier ice at the site (100-15 kOmega m) is more consis

151 he entire process chain for dating of alpine glacier ice by argon trap trace analysis (ArTTA).

152 of organic aerosol composition preserved in glacier ice cores.

153 sents the first documented advance of alpine glacier ice in the Dry Valleys during Marine Isotope Sta

154 Mountains as proxies for retreat of grounded glacier ice in the Ross Embayment.

155 Glacier ice in the Southern Alps has become restricted t

156 nt of this method, all LA-ICP-MS analyses of glacier ice involved a single element per ablation pass

157 system for ultrahigh-resolution sampling of glacier ice is needed.

158 s recovered beneath the floating Pine Island Glacier ice shelf, and constrain the date at which the g

159 Glaciers impart unique footprints on river flow at times

160 ano, based on ice-core records from Illimani glacier in Bolivia, providing the first complete history

161 n cryoconite and proglacial sediments from a glacier in British Columbia, Canada, and compare values

162 diment core from Sermilik Fjord near Helheim Glacier in SE Greenland.

163 e concentrations in rivers draining Leverett Glacier in southwest Greenland and Kiattuut Sermiat in s

164 Pine Island Glacier and Thwaites Glacier in the Amundsen Sea Embayment are among the fast

165 solution ice-core Hg record from the Belukha glacier in the Siberian Altai, covering the time period

166 at the remnant eastern ice shelf of Thwaites Glacier in West Antarctica had thinned between 10 and 33

167 present thinning and retreat of Pine Island Glacier in West Antarctica is part of a climatically for

168 el of Thwaites Glacier, a marine-terminating glacier in West Antarctica that is thought to be unstabl

169 d the first complete disappearance of modern glaciers in Europe.

170 The limited Holocene retreat of glaciers in Koge Bugt was controlled by the subglacial t

171 We anticipate that glaciers in Koge Bugt will remain in stable configuratio

172 Glaciers in most parts of the world are retreating, rele

173 However, there are no equivalent studies for glaciers in North America.

174 UFG), Wyoming, is one of the few continental glaciers in the contiguous United States known to preser

175 ed at other locations around the world, some glaciers in the High Mountains of Asia appear to have ga

176 d in part on meltwater from the thousands of glaciers in the high mountains of Asia.

177 Glaciers in the Himalaya-Karakoram (HK) are critical for

178 d the Andes, are the last remaining tropical glaciers in the West Pacific Warm Pool (WPWP).

179 rate increases of up to 6.3% (7 cm a(-1)) on glaciers in three different mountain environments in Kyr

180 accelerated ice-mass loss from large outlet glaciers in W and SE Greenland has been linked to warmin

181 unding zones of the Pine Island and Thwaites glaciers in West Antarctica need to retreat only short d

182 ayment are among the fastest changing outlet glaciers in West Antarctica with large consequences for

183 The glaciers in West Kunlun, Eastern Pamir and the northern

184 .e.a(-1)) mass balances for lake-terminating glaciers, in comparison to land-terminating glaciers, wi

185 Our results show that both L. tumana and Z. glacier inhabit an extremely narrow distribution, restri

186 The influence of snowpack and glacier inputs was further evidenced by the correlation

187 ate time-varying elevations near the melange-glacier interface, generating a factor of three or more

188 over a threshold to the lake, only when the glacier is significantly larger than at present.

189 ced meltwater from initial build-up of local glaciers, is also shown.

190 When such dams break, glacier lake outburst floods (GLOFs) can cause catastrop

191 alayas has gradually spawned more than 5,000 glacier lakes that are dammed by potentially unstable mo

192 tion experiments in a wild population of the glacier lily (Erythronium grandiflorum, Liliaceae) from

193 ogy and morphology caused by climate-induced glacier loss are projected to be the greatest of any hyd

194 However, the effects of glacier loss on biodiversity have never been quantified

195 By 17.38 +/- 0.12 cal ka BP, the glacier margin had receded into a deepening proglacial l

196 e melting and iceberg calving from tidewater glacier margins.

197 pact of riverine organic matter subsidies to glacier-marine habitats by developing a multi-trophic le

198 se changes affected precipitation and Andean glacier mass balance.

199 Significant positive glacier mass balances are noted along the edge of the Up

200 of surface debris cover and glacial lakes on glacier mass loss across the Himalaya since the 1970s.

201 Heterogeneous glacier mass loss has occurred across High Mountain Asia

202 t projections forced by RCP8.5 underestimate glacier mass loss which could exceed this worst-case sce

203 In contrast to the glacier mass losses observed at other locations around t

204 Sustained glacier melt in the Himalayas has gradually spawned more

205 As glacier melting accelerates under future climate warming

206 Here I show that seasonal glacier meltwater is equivalent to the basic needs of 22

207 ascribed to the delivery of dense and turbid glacier meltwaters mixing PFAS throughout the Lake Hazen

208 iodiversity and functional roles of mountain glacier microbiota; describe the ecological implications

209 The instability propagated rapidly up-glacier, mobilizing the entire 450 km(2) glacier basin o

210 Fluctuations in glacier motion are very common and are thought to be con

211 s detected in 113 streams (175 sites) within Glacier National Park (GNP) and surrounding areas.

212 glacier change (ca. 1850-2015) datasets for Glacier National Park, USA, to test the prediction that

213 , we report the recent, rapid retreat of the glaciers near Puncak Jaya by quantifying the loss of ice

214 The glaciers near Puncak Jaya in Papua, Indonesia, the highe

215 Rapid changes observed today in mountain glaciers need to be put into a longer-term context to un

216 the terminal moraine complex of the Ngozumpa Glacier, Nepal, to aid assessment of future terminus sta

217 riverine organic matter assimilation by the glacier-nesting seabirds Kittlitz's murrelet (Brachyramp

218 vation "island of the cryosphere" before the glaciers of Kilimanjaro disappear forever.

219 theast Greenland, hosts three of the largest glaciers of the Greenland Ice Sheet; these have been maj

220 ge of surface meltwater to the bed of outlet glaciers on the Antarctic Peninsula occurs and triggers

221 he mass loss of debris-covered and clean-ice glaciers over our study period, but substantially more n

222 s that potentially accelerate the retreat of glaciers over the Himalayas and Tibetan Plateau (HTP).

223 Pine Island Glacier (PIG) terminates in a rapidly melting ice shelf,

224 The retreating Pine Island Glacier (PIG), West Antarctica, presently contributes 5-

225 te representing a minor portion of the total glacier population (~10%), the recession of lake-termina

226 sections of cold, alpine streams often below glaciers predicted to disappear over the next two decade

227 ronosequences at the forefront of retreating glaciers provide information about colonization rates of

228 Here I show that these glaciers provide summer meltwater to rivers and aquifers

229 These Papua glaciers provide the only tropical records of ice core-d

230 The region's future, when glaciers reach grounding lines and iceberg production di

231 ates points to factors capable of amplifying glacier recession in addition to climatic change along t

232 Rapid glacier recession is altering the physical conditions of

233 The degree to which debris-covered glaciers record past environmental conditions is debated

234 esert (SD) and greening of the Arctic tundra-glacier region (ArcTG) have been hot subjects under exte

235 Melting glaciers release previously ice-entrapped chemicals to t

236 Helheim Glacier responded to many of these episodes with increas

237 s into the mechanism of the recent divergent glacier response over the HK.

238 poraneous ocean-forced change and of ongoing glacier response to an earlier perturbation in driving i

239 retreating, complicating interpretations of glacier response to climate change.

240 Understanding the long-term glacier response to external forcing is key to improving

241 Renewed glacier resurgence in the fjords between c. 15,170 and 1

242 ble estimate of blue carbon change caused by glacier retreat along Antarctic fjords and thus to estab

243 timated, but not how blue carbon responds to glacier retreat along fjords.

244 We attribute the onset of glacier retreat at 18.0 +/- 0.14 cal ka BP to abrupt sou

245 We derive a testable estimate of glacier retreat driven blue carbon gains by investigatin

246 This observation constrains maximum Holocene glacier retreat here to less than 6 km from present-day

247 We started by multiplying ~40 year mean glacier retreat rates by the number of retreating WAP fj

248 ional Park, USA, to test the prediction that glacier retreat reduces biodiversity in mountain ecosyst

249 Marine ice (sea ice, ice shelf and glacier retreat) losses generate a valuable negative fee

250 l in Antarctica, 2) after re-exposure due to glacier retreat, instead of dying (due to high rates of

251 er year; P < 0.03) and also suggest that the glaciers' retreat is augmented by El Nino-Southern Oscil

252 8,000 years before present [YBP]); after the glacier retreated, ice patches remained on the island un

253 f Alaska originates from landscapes draining glacier runoff, but the influence of the influx of river

254 preconcentrated ice samples from the Belukha glacier, Russian Altai Mountains.

255 tive, the contribution from India to the HTP glaciers shows a rapid increasing trend while the contri

256 Here, we synthesize current evidence of how glacier shrinkage will alter hydrological regimes, sedim

257 of impacts in all affected regions caused by glacier shrinkage.

258 273) conclude that fast glacier sliding is independent of basal drag (friction),

259 on rate is usually modelled as a function of glacier sliding velocity, but the empirical basis for th

260 nly associated with glacier area proportion, glacier source proportion, total nitrogen, dissolved org

261 e meltwater stonefly (Lednia tumana) and the glacier stonefly (Zapada glacier) - were recently propos

262 des strongly limit mass replenishment of the glacier, suggesting irreversible consequences.

263 ment produced the highest recorded Karakoram glacier surface flow rate using feature tracking (~18 +/

264 from mixtures of materials collected at the glacier surface.

265 re samples from the high-alpine Fiescherhorn glacier (Swiss Alps), and used high-performance liquid c

266 of the January 2009 collapse of the Nathorst Glacier System (NGS) in Svalbard, we show that an underl

267 al sea-level contributions, regional climate-glacier systems and local landscape evolution.

268 and sediment dynamics: a shoal forms at the glacier terminus, reducing ice discharge and causing adv

269 exerting a buttressing force directly on the glacier terminus.

270 future warming could trigger advance even in glaciers that are steady or retreating, complicating int

271 search, with less attention paid to mountain glaciers that overlap environmentally and ecologically w

272 to the terminal regions of Greenland outlet glaciers that we studied.

273 At many marine-terminating glaciers, the breakup of melange, a floating aggregation

274 Climate plays a paradoxical role as cold glacier thinning and retreat promote basal freezing whic

275 imperils the persistence of L. tumana and Z. glacier throughout their ranges, highlighting the role o

276 By contrast, in front of the retreating Pia Glacier (Tierra del Fuego, Chile), a Nothofagus forest i

277 We show a rare fully instrumented coupled glacier/till record of contrasting summer and winter sti

278 However, the sensitivity of HK glaciers to changes in meteorological forcing remains la

279 ertain response of marine terminating outlet glaciers to climate change at time scales beyond short-t

280 ia was extensive, and the sensitivity of its glaciers to climate variability during the last terminat

281 rence lies in the susceptibility of mountain glaciers to the near-term threat of climate change, as t

282 data from an Icelandic soft-bedded temperate glacier, to show that there are two distinct seasonal st

283 beneath an East Antarctic ice shelf, Shirase Glacier Tongue, driven by southward-flowing warm water g

284 g and associated friction increase under the glacier tongue.

285 ter can reduce till strength under tidewater glacier tongues to orchestrate a temporal clustering of

286 g upstream into tributaries feeding the main glacier trunk.

287 The Upper Fremont Glacier (UFG), Wyoming, is one of the few continental gl

288 erization of samples collected from within a glacier using a melt probe, and the only Antarctic subgl

289 Projections of mass loss for these glaciers, using the worst-case scenario, Representative

290 he authors show that internal dynamics drive glacier variability independent of climate.

291 Zapada glacier was only detected in 10 streams (24 sites), six

292 nia tumana) and the glacier stonefly (Zapada glacier) - were recently proposed for listing under the

293 ions of a rapid lake drainage event at Store Glacier, west Greenland, in 2018.

294 on), dammed the proglacial river of Muchuhar Glacier, which formed an ice-dammed lake and generated a

295 iated with melting permafrost and retreating glaciers, while lowest burial rates occurred during the

296 At the current rate of ice loss, these glaciers will likely disappear within the next decade.

297 Yet, assessing how much and how fast both glaciers will weaken if these changes continue remains a

298 most rapid erosion is achieved at temperate glaciers with high mean annual precipitation, which serv

299 Cultivars such as Stupice and Glacier, with very round leaves, had the highest perform

300 glaciers, in comparison to land-terminating glaciers, with the largest differences occurring after 2