ライフサイエンスコーパス: glacier

1 n 2002 and 2009 beneath the retreating Smith Glacier.

2 d to meltwater-induced relocation within the glacier.

3 nd the erosion rate of a fast-flowing Alpine glacier.

4 tile organic chemicals in a temperate Alpine glacier.

5 d subglacial runoff from a large GrIS outlet glacier.

6 +/-0.2 muM) over a 14 day period at Leverett Glacier.

7 the rapidly changing Smith, Pope and Kohler glaciers.

8 critical grounding zones of the ASE's major glaciers.

9 antified in the accumulation areas of Alpine glaciers.

10 surface melt and flow acceleration in outlet glaciers.

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

12 over other erosion processes in fast-flowing glaciers.

13 ng the ice/bedrock interface of contemporary glaciers.

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

15 and predict the behavior of rapidly changing glaciers.

16 vance and retreat of Pleistocene continental glaciers.

17 ive the retreat of modern marine-terminating glaciers.

18 Mass contributions from ice sheets and glaciers (1.37 +/- 0.09 mm/y, accelerating with 0.03 +/-

19 Pine Island Glacier, a major outlet of the West Antarctic Ice Sheet,

20 orinated biphenyls (PCBs) into the Silvretta glacier, a temperate Alpine glacier located in Switzerla

21 dless of the forcing responsible for initial glacier acceleration and thinning, the response of indiv

22 of Aoraki/Mount Cook, New Zealand, onto the glacier accumulation zone below was invisible to convent

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

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

25 rgence of bacterial communities deposited on glaciers across a wide geographical area and situated in

26 In Alpine regions, glaciers act as environmental archives and can accumulat

27 nclude the westernmost tributary of Thwaites Glacier adjacent to the subaerial Mount Takahe volcano a

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

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

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

31 induced climate response was prolonged by NH glacier and sea ice expansion, increased NH albedo, AMOC

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

33 ework that quantifies mass fluxes of PCBs in glaciers and apply it to the Silvretta glacier (Switzerl

34 reenland ice sheet (GrIS) and its peripheral glaciers and ice caps (GICs) contributes about 43% to co

35 Runoff from glaciers and ice sheets has been acknowledged as a poten

36 nfluenced by meltwater discharge from nearby glaciers and ice shelves, and re-examination of some pre

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

38 owing to the thinning and retreat of outlet glaciers and ice streams.

39 idespread within permafrost and extend below glaciers and lakes.

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

41 d stream temperatures and close proximity to glaciers and permanent snowfields.

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

43 es as they exit the GrIS from a large outlet glacier, and as they enter a downstream river delta duri

44 rtially offset water losses from ice sheets, glaciers, and groundwater pumping, slowing the rate of s

45 sum of individual contributions (ice sheets, glaciers, and hydrology) found in literature.

46 e where lithogenic iron inputs from deserts, glaciers, and rivers are increasing [7-10].

47 n air extracted from ice samples from Taylor Glacier, Antarctica.

48 m air bubbles trapped in polar ice at Taylor Glacier, Antarctica.

49 populate most of North America south of the glaciers [ approximately 11,500 to >/= approximately 10,

50 ver two centuries, and concludes that Alpine glaciers are a small secondary source of PCBs, but that

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

52 glaciers are retreating, but some tidewater glaciers are advancing despite increasing temperatures a

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

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

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

56 Despite the fact that rock glaciers are one of the most common geomorphological exp

57 Most of Earth's glaciers are retreating, but some tidewater glaciers are

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

59 Flow patterns of many outlet glaciers are well captured, illustrating fundamental com

60 Temperate glaciers, in contrast to cold glaciers, are glaciers where melt processes are prevalen

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

62 the mechanisms underlying the variations in glacier area and river flow can be well constrained.

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

64 hough both sites reveal a strong decrease in glacier area, they show a remarkably different hydrologi

65 from glaciers to determine the importance of glaciers as a secondary source of organic chemicals to r

66 sotopic data suggest the presence of Alaskan glaciers as far back as 4.2 Myr ago, while diatom and C3

67 The ongoing retreat of glaciers at southern sub-polar latitudes is particularly

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

69 global climate model suggest that the common glacier behaviour was the result of Atlantic meridional

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

71 f the hydrology, vegetation, permafrost, and glaciers, but effects on wildlife have been difficult to

72 1900 AD followed by elevated 20(th) century glacier calving due to the loss of the tongue.

73 We show that the Thwaites Glacier catchment has a minimum average geothermal flux

74 mal flux is particularly problematic for the glacier catchments of the West Antarctic Ice Sheet withi

75 We show that calving at Greenland's Helheim Glacier causes a minutes-long reversal of the glacier's

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

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

78 gal communities in the foreland of an Arctic glacier conforms to either of these models, we collected

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

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

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

82 g has contributed to the regional retreat of glaciers, disintegration of floating ice shelves and a '

83 However, the specific sources of glacier DOC remain unresolved.

84 To assess the origin and nature of glacier DOC, we collected snow from 10 locations along a

85 Dynamics of the major outlet glaciers dominated the mass loss from larger drainage ba

86 incorporation into the entire surface of the glacier, downhill transport with the flow of the glacier

87 In recent decades, hundreds of glaciers draining the Antarctic Peninsula (63 degrees to

88 This relationship between climate, glacier dynamics and erosion rate is the focus of recent

89 ude glaciation has focused on reconstructing glacier dynamics during the last glacial termination, wi

90 on aerosols are a large source of DOC to the glacier ecosystem during the early spring (April-May) to

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

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

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

94 a fundamental role in the biogeochemistry of glacier ecosystems.

95 Microbial photoautotrophs on glaciers engineer the formation of granular microbial-mi

96 Glaciers erode valleys to generate headwall relief, and

97 licit examination of the factors controlling glacier erosion across climatic regimes.

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

99 ciers in the western Arctic, Lyngmarksbraeen glacier experienced several advances during the last mil

100 In the Northern Hemisphere, most mountain glaciers experienced their largest extent in the last mi

101 rmal and hydrologic conditions found only in glacier-fed and snow melt-driven alpine streams.

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

103 iodiversity, and the ecosystem services that glacier-fed rivers provide to humans, particularly provi

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

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

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

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

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

109 ychlorinated biphenyls (PCBs) into an Alpine glacier (Fiescherhorn, Switzerland) and an Arctic glacie

110 strating fundamental commonalities in outlet glacier flow and highlighting the importance of efforts

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

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

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

114 eberg capsize and acceleration away from the glacier front.

115 nce between mid-depth ocean temperatures and glacier-front changes along the ~1000-kilometer western

116 ass loss at the calving margins of tidewater glaciers (frontal ablation rates) are a key uncertainty

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

118 The ongoing retreat of glaciers globally is one of the clearest manifestations

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

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

121 mapping of the fjord suggest that the Crane Glacier grounding zone was well within the fjord before

122 unt of the total PCB burden in the Silvretta glacier has been released to the environment.

123 Incorporation of PCBs into cold glaciers has been quantified in previous studies.

124 However, the fate of PCBs in temperate glaciers has never been investigated.

125 Ice mass loss of the marine-terminating glaciers has rapidly accelerated from close to balance i

126 In previous work, Alpine glaciers have been identified as a secondary source of p

127 In many tectonically active mountain ranges, glaciers have been inferred to be highly erosive, and co

128 Most outlet glaciers have been thinning during the last two decades,

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

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

131 s that were repeatedly covered by Quaternary glaciers hinges upon whether the gorges are fluvial form

132 congeners, the main processes are storage in glacier ice and removal by particle runoff.

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

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

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

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

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

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

139 re inconsistent with the high resistivity of glacier ice or dry permafrost in this region.

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

141 ier, downhill transport with the flow of the glacier ice, and chemical fate in the glacial lake.

142 clearly showing the presence (or absence) of glacier ice.

143 deposition and then is incorporated into the glacier ice.

144 synchronous but diverse evolutions of these glaciers illustrate how combinations of oceanography and

145 Glaciers impart unique footprints on river flow at times

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

147 xclusively with enhanced thawing of the rock glacier in recent years.

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

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

150 imately 350-kg polar ice samples from Taylor Glacier in the McMurdo Dry Valleys, Antarctica, and date

151 distinct glacial moraines alongside Stocking Glacier in the McMurdo Dry Valleys, Antarctica.

152 We show that the active rock glacier in the mineralized catchment of Lake Rasass (RAS

153 ice-core concentration records from Belukha glacier in the Siberian Altai and emission data from 12

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

155 tions at three locations along the Beardmore Glacier in the Transantarctic Mountains (in order of inc

156 hboring water bodies with and without a rock glacier in their catchments in the European Alps.

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

158 rnal debris within cold-based debris-covered glaciers in Antarctica.

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

160 es occurring at increasing numbers of outlet glaciers in Greenland and Antarctica.

161 level requires accurate portrayal of outlet glaciers in ice sheet simulations, but to date poor know

162 es in digital elevation models indicate that glaciers in Karakoram and Pamir have gained mass, while

163 throughout the core; this demonstrates that glaciers in Koge Bugt remained in tidewater settings thr

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

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

166 tion rates for three dynamically contrasting glaciers in Svalbard from an unusually dense series of s

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

168 Stocking Glacier is one of several alpine glaciers in the Dry Valleys fringed by multiple cold-bas

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

170 moraine chronology in Colombia showing that glaciers in the northern tropical Andes expanded to a la

171 result from the development of ice caps and glaciers in the polar region during the Late Miocene glo

172 Consistent with other glaciers in the western Arctic, Lyngmarksbraeen glacier

173 Ice cores from glaciers in this region serve as unique natural archives

174 melting are the primary cause of retreat for glaciers in this region.

175 ntributed to the relatively stable status of glaciers in this region.

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

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

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

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

180 Temperate glaciers, in contrast to cold glaciers, are glaciers whe

181 luxes, as well as the storage of PCBs in the glacier increase until the 1980s and decrease thereafter

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

183 ence suggest possible collapse of the Totten Glacier into interior basins during past warm periods, m

184 One system emanates from below Taylor Glacier into Lake Bonney and a second system connects th

185 od, New Zealand was repeatedly fragmented by glaciers into a series of refugia, with the tiny geograp

186 This glacier is affected by surface melting in summer.

187 Stocking Glacier is one of several alpine glaciers in the Dry Val

188 ion and thinning, the response of individual glaciers is modulated by local conditions.

189 r long-term ability to lower mountains above glaciers is poorly understood; however, small, frequent

190 We also surveyed 491 glacier lakes for earthquake damage but found only nine

191 to the Silvretta glacier, a temperate Alpine glacier located in Switzerland.

192 in an ice core from the temperate Silvretta glacier, located in eastern Switzerland.

193 Jorge Montt glacier, located in the Patagonian Ice Fields, has under

194 er (Fiescherhorn, Switzerland) and an Arctic glacier (Lomonosovfonna, Norway).

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

196 able gravity combined with reconciled global glacier loss estimates enable a disaggregation of contin

197 he magnitude of this water supply, predicted glacier loss would add considerably to drought-related w

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

199 sture transport over the Tibetan Plateau for glacier mass balance, river runoff and local ecology, ch

200 the ice core, adding the years with negative glacier mass balance, that is, years with melting and su

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

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

203 Our results suggest that temporary mountain glaciers may act as barriers in promoting the lineage di

204 As glacier melting accelerates under future climate warming

205 l-May) together with the pronounced rates of glacier melting in the region suggests that the delivery

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

207 However, no long-term and well-constrained glacier modeling has ever been performed to confirm this

208 The formation of RAS at the toe of the rock glacier most probably began at the onset of acidic drain

209 H. pylori genome from a European Copper Age glacier mummy.

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

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

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

213 of its ice shelf, Zachariae Isstrom, a major glacier of northeast Greenland that holds a 0.5-meter se

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

215 d kilometers of the expanding and retracting glaciers of the Southern Alps of New Zealand.

216 bility that similar-appearing debris-covered glaciers on Mars may likewise hold clues to environmenta

217 he past half century in ice cores from three glaciers on the Tibetan Plateau.

218 the extent to which topography was shaped by glaciers or by rivers.

219 dered with evidence from mid-latitude Andean glaciers, our results argue for a common glacier respons

220 nt PCB fluxes in and from a temperate Alpine glacier over two centuries, and concludes that Alpine gl

221 and geochronological data, that Pine Island Glacier (PIG) also experienced rapid thinning during the

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

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

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

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

226 geologic history, the thermal regimes of its glaciers range from temperate to polar.

227 hat Pleistocene climatic change and mountain glaciers, rather than the Mekong-Salween Divide, play th

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

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

230 Melting glaciers release previously ice-entrapped chemicals to t

231 Helheim Glacier responded to many of these episodes with increas

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

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

234 ean glaciers, our results argue for a common glacier response to cold conditions in the Antarctic col

235 tial for deriving simple models of tidewater glacier response to oceanographic forcing.

236 ice sheets and ocean circulation, modulated glacier responses regionally, they are unable to account

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

238 he importance of greenhouse gases in driving glacier retreat during the most recent deglaciation, the

239 id submarine melting to hasten mass loss and glacier retreat from West Antarctica.

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

241 Consistent with evidence from glacier retreat in Southern Hemisphere mountain ranges,

242 Glacier retreat likely was the main factor responsible f

243 e consistent with increased temperatures and glacier retreat on Chimborazo since Humboldt's study.

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

245 s coincident with widespread acceleration of glacier retreat.

246 1250 CE, MCA), a period which coincided with glacier retreat.

247 When grounding zones of glaciers retreat onto such slopes, theoretical considera

248 8,000 years before present [YBP]); after the glacier retreated, ice patches remained on the island un

249 nger Dryas, however, northern tropical Andes glaciers retreated owing to abrupt regional warming in r

250 d particles in the atmosphere and within the glacier, revolatilization, diffusion and degradation, an

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

252 lacier causes a minutes-long reversal of the glacier's horizontal flow and a downward deflection of i

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

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

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

256 inferred from sediment yields from 15 outlet glaciers spanning 19 degrees of latitude from Patagonia

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

258 ex Traits Involved in Elevated Disease Risk [GLACIER Study; N=4312] and the Malmo Diet and Cancer Stu

259 ly that fungal community development in this glacier succession follows a directional replacement mod

260 congener is predominantly transferred to the glacier surface by wet deposition and then is incorporat

261 ot dependent on ice dynamics, nor reduced by glacier surface freeze-up, but varies strongly with sub-

262 ntities of PCBs incorporated into the entire glacier surface, and estimate the quantity of chemicals

263 Extensive valley glaciers survived in the Rangitata catchment until at le

264 collected samples from the Midtre Lovenbreen Glacier, Svalbard, along a soil successional series span

265 Bs in glaciers and apply it to the Silvretta glacier (Switzerland).

266 (PCBs) from an Alpine ice core (Fiescherhorn glacier, Switzerland).

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

268 exerting a buttressing force directly on the glacier terminus.

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

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

271 In the south, glaciers that terminate in warm Circumpolar Deep Water h

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

273 udget into contributions from ice sheets and glaciers, the water cycle, steric expansion, and crustal

274 Our findings imply that climate and the glacier thermal regime control erosion rates more than d

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

276 r air and ocean temperatures have caused the glacier to detach from a stabilizing sill and retreat ra

277 we investigated the sensitivity of Thwaites Glacier to ocean melt and whether its unstable retreat i

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

279 mate the quantity of chemicals released from glaciers to determine the importance of glaciers as a se

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

281 g upstream into tributaries feeding the main glacier trunk.

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

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

284 At this time, Stocking Glacier was 20-30% larger than today.

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

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

287 We show that glacier wastage during the 2000s in the Kerguelen was am

288 mulate the climate drivers behind the recent glacier wastage in the Kerguelen.

289 This suggests that future glacier wastage projections should be considered cautiou

290 edistribution of legacy pollutants in Alpine glaciers, we analyzed polychlorinated biphenyls in an ic

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

292 melting and geothermal flux beneath Thwaites Glacier, West Antarctica.

293 surface exposure dating from Lyngmarksbraeen glacier, West Greenland.

294 glaciers, in contrast to cold glaciers, are glaciers where melt processes are prevalent.

295 ated water from the surface (in this case, a glacier), which is a common occurrence during explosive

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

297 ice core recovered in 2012 from the Chongce glacier with the delta(18)O records of two other ice cor

298 sociated with triglyceride concentrations in GLACIER, with each additional BMI unit (kg/m(2)) associa

299 Surprisingly, the presence or the absence of glaciers within a watershed was unrelated to long-term s

300 urred in two regions: the head of the Totten Glacier, within 150 kilometres of today's grounding line