ライフサイエンスコーパス: ice sheet

1 be (46.5 degrees S) of the former Patagonian Ice Sheet.

2 topographic features beneath and within the ice sheet.

3 when considering the future evolution of the ice sheet.

4 enland, with a total 13.7 +/- 1.1 mm for the ice sheet.

5 m of a subglacial catchment of the Greenland ice sheet.

6 cial discharge from the surrounding grounded ice sheet.

7 ffect the pace of mass loss of the Antarctic Ice Sheet.

8 accelerated future retreat of the Antarctic Ice Sheet.

9 of exposed rock, melting and thinning of the ice sheet.

10 iginated beneath the adjacent East Antarctic Ice Sheet.

11 s ice motion at the margins of the Greenland Ice Sheet.

12 influence oceanic heat flux to the Greenland ice sheet.

13 udies exist from fast-flowing sectors of the ice sheet.

14 bilizing role of solid-Earth uplift on polar ice sheets.

15 ta exist on the current methane footprint of ice sheets.

16 measure conditions within and beneath polar ice sheets.

17 compared to the latitudinal distribution of ice sheets.

18 he Southern Ocean as a consequence of larger ice sheets.

19 n in endemic clades south of the continental ice sheets.

20 necessary for initiating Northern Hemisphere ice sheets.

21 t of Earth's fresh water stored in two large ice sheets.

22 es in the Antarctic(13,14) and Greenland(15) ice sheets.

23 the progressive decay of Northern Hemisphere ice-sheets.

24 ant mechanism for mass loss in the Greenland ice sheet(1-3).

25 quire a contribution from the East Antarctic Ice Sheet(3), which has been argued to have remained sta

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

27 o alternative models, and entry south of the ice sheet after 19.5 kya.

28 ration Pathway (RCP) scenarios and Antarctic Ice Sheet (AIS) melt propagate into uncertainties in pro

29 the highstand, so that substantial Antarctic Ice Sheet (AIS) reduction is implied.

30 eat of marine-based sectors of the Antarctic Ice Sheet (AIS)(1-3).

31 Greenland Ice Sheet (GrIS) and the Antarctic Ice Sheet (AIS).

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

33 cial volcanism can breach the surface of the ice sheet and may pose a great threat to WAIS stability.

34 olution ice-sheet modelling of the Antarctic Ice Sheet and multi-millennial global climate model simu

35 ample, increases in melting of the Greenland Ice Sheet and reductions in sea ice and permafrost distr

36 A significant component of ice sheet and shelf mass balance is iceberg calving, whi

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

38 Optimum, leading to growth of the Antarctic ice sheet and the onset of Northern Hemisphere glaciatio

39 we focus on feedbacks between the Antarctic Ice Sheet and the solid Earth, and the role of these fee

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

41 to the carbon cycle or interactions between ice sheets and climate.

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

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

44 urrent state-of-the-art knowledge of pre-LGM ice sheets and provide a conceptual framework to interpr

45 ptures all solid Earth processes that affect ice sheets and show a projected negative feedback in gro

46 tes of biogeochemical/physical weathering in ice sheets and storage and cycling of organic carbon (>1

47 erg-rafted debris derived from the Antarctic Ice Sheet, and performed both high-spatial-resolution ic

48 ity and accelerated melting of the Antarctic Ice Sheet are among the foremost elements of contemporar

49 Ice sheets are currently ignored in global methane budge

50 Ongoing changes in glaciers and ice sheets are driven by submarine melting and iceberg c

51 at assumptions about the complex behavior of ice sheets are the primary drivers of flood hazard diver

52 Our data indicate that ice sheets are very sensitive to warming and provide imp

53 s sensitive to the history of the Laurentide Ice Sheet as the coastline lies along the ice sheet's pe

54 Our reconstructions illustrate pronounced ice-sheet asymmetry within the last glacial cycle and si

55 ing the melting history of the Fennoscandian Ice Sheet at the end of the last deglaciation ( approxim

56 n contributing to the expansion of Antarctic Ice Sheet at the Eocene-Oligocene Transition.

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

58 vents, including sea ice, ice shelf buildup, ice sheets, atmospheric circulation, and meltwater chang

59 rise may accelerate significantly if marine ice sheets become unstable.

60 e-supersaturated waters (CH(4(aq))) from the ice-sheet bed during the melt season.

61 of CH(4(aq)) transported laterally from the ice-sheet bed.

62 sion-making such as (i) representing complex ice sheet behavior, (ii) covering decision-relevant time

63 understand processes that govern longer-term ice-sheet behavior.

64 l lakes are widespread beneath the Antarctic Ice Sheet but their control on ice-sheet dynamics and th

65 s to accelerate the retreat of the Antarctic Ice Sheet by increasing surface melting and facilitating

66 timescale and strength of feedbacks between ice-sheet change and solid Earth deformation, and hence

67 aseline, critical for observing and modeling ice-sheet change on societally relevant timescales.

68 The Cordilleran Ice Sheet (CIS) once covered an area comparable to that

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

70 by high freshwater runoff from the Greenland Ice Sheet coinciding with periods of open water.

71 an accurate coupling between atmosphere and ice sheet components in climate models.

72 s behaviour: that is, the currently observed ice-sheet configuration is not regained even if temperat

73 g simulations of the Greenland and Antarctic ice sheets constrained by satellite-based measurements o

74 Ice loss from the world's glaciers and ice sheets contributes to sea level rise, influences oce

75 The 95th percentile ice sheet contribution by 2200, for the +5 degrees C sce

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

77 al modeling, and the observational record of ice sheet contributions to global mean sea-level rise (S

78 The ensuing freshwater discharge coming from ice sheets could have significant impacts on global clim

79 day emissions owing to the large terrestrial ice sheet cover, lower sea level and extensive permafros

80 dence and numerical models indicate that the ice sheet covered much of westernmost Canada as late as

81 We contend that ice sheets create highly geochemically reactive particul

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

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

84 Here we show that fluctuations in Antarctic Ice Sheet discharge caused by relatively small changes i

85 ntilation synchronous with rapid Cordilleran Ice Sheet discharge, indicating close coupling of ice-oc

86 Ice-sheet discharge was not explicitly included in Coupl

87 with recent results from the West Antarctic Ice Sheet Divide ice core and the sea-level record, allo

88 chemical measurements in the West Antarctic Ice Sheet Divide, Byrd, and other ice cores to document

89 In particular, the West Antarctic Ice Sheet does not regrow to its modern extent until tem

90 adiogenic Nd modulated by the North American Ice Sheet dominated the evolution of the NADW Nd isotope

91 plementary Fe sources, such as the Antarctic ice sheet, due to the difficulty of locating and interro

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

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

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

95 de, and the establishment of permanent polar ice sheets during the Neogene period(1,2) have frequentl

96 e most vulnerable part of the West Antarctic Ice Sheet, during the Holocene epoch (from 11.7 thousand

97 er that the MPT was initiated by a change in ice sheet dynamics and that longer and deeper post-MPT i

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

99 ial lake drainage events influence Greenland Ice Sheet dynamics on hourly to interannual timescales.

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

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

102 Southern Ocean carbon budget, and Antarctic ice-sheet dynamics across glacial-interglacial cycles.

103 the Antarctic Ice Sheet but their control on ice-sheet dynamics and their ability to harbour life rem

104 ll documented, their role in modulating past ice-sheet dynamics remains poorly constrained.

105 its our understanding of past East Antarctic Ice Sheet (EAIS) behaviour and thus our ability to evalu

106 nt of Earth's cryosphere, the East Antarctic Ice Sheet (EAIS), to global warming is poorly understood

107 Mass loss from the Antarctic ice sheet, Earth's largest freshwater reservoir, results

108 fluence on the mass balance of the Antarctic Ice Sheet, either indirectly, by its influence on air te

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

110 Sea sector of West Antarctica and models of ice-sheet evolution in the past 10,000 years have recent

111 Here we show that the Antarctic Ice Sheet exhibits a multitude of temperature thresholds

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

113 We conclude that the Laurentide Ice Sheet experienced a phase of very rapid growth in th

114 Mass loss from glaciers and the Greenland Ice Sheet explains the high rates of global sea-level ri

115 ebergs, demonstrating the potential for high ice sheet export.

116 Thus, we identify another ice-sheet feedback intimately tied to iron biogeochemist

117 global climatic changes are translated into ice-sheet fluctuations and sea-level change is currently

118 ehensive stability analysis of the Antarctic Ice Sheet for different amounts of global warming.

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

120 Surface meltwater drains across ice sheets, forming melt ponds that can trigger ice-shel

121 scharge of 176 basins draining the Antarctic Ice Sheet from 1979 to 2017.

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

123 ial response of the nearby western Greenland Ice Sheet (GIS) during the glacial advance of marine oxy

124 The Greenland Ice Sheet (GIS) has been losing mass at an accelerating

125 The Greenland Ice Sheet (GIS) is losing mass at a high rate(1).

126 a potential disintegration of the Greenland ice sheet (GIS).

127 delta(15)N rose at 35 Ma ago, as ice sheets grew, sea level fell, and continental shelves

128 Melting of the Greenland ice sheet (GrIS) and its peripheral glaciers and ice cap

129 ents in subglacial waters from the Greenland Ice Sheet (GrIS) and the Antarctic Ice Sheet (AIS).

130 Greenland Ice Sheet (GrIS) contributions were insufficient to expl

131 s have been identified beneath the Greenland Ice Sheet (GrIS) despite extensive documentation in Anta

132 icroorganisms are flushed from the Greenland Ice Sheet (GrIS) where they may contribute towards the n

133 " lower the bare ice albedo of the Greenland Ice Sheet (GrIS), amplifying summer energy absorption at

134 t during the rise and fall of the retreating ice sheet grounding line during successive tidal cycles.

135 ies, causing high ice shelf melting near the ice sheet grounding lines, accelerating ice flow, and co

136 to unloading over short time scales close to ice-sheet grounding lines (areas where the ice becomes a

137 We propose that lower sea levels driven by ice-sheet growth in the Northern Hemisphere decreased EA

138 Finally, we document the transition to full ice-sheet growth over Scandinavia from the ice sheet's e

139 flowing into the Amundsen Sea sector of the ice sheet have thinned at an accelerating rate, and seve

140 veral ice cores retrieved from the Greenland ice sheet have verified the existence of 25 abrupt clima

141 Although ice sheets have been proposed to contain large reserves

142 Antarctica's continental-scale ice sheets have evolved over the past 50 million years.

143 d accelerate future retreat of the Antarctic Ice Sheet if ice shelves that buttress grounding lines m

144 potential partial collapse of the Antarctic ice sheet in assessing future coastal inundation.

145 ut their distribution on the world's largest ice sheet in East Antarctica.

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

147 Here we assess the active role of ice sheets in the global carbon cycle and potential rami

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

149 tool, we show mathematically that the marine ice sheet instability greatly amplifies and skews uncert

150 te that the retreat becomes unstable (marine ice-sheet instability) and thus accelerates.

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

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

153 The Antarctic Peninsula Ice Sheet is currently experiencing sustained and accele

154 The evolution of the Antarctic Ice Sheet is driven by a combination of climate forcing

155 The more stable East Antarctic Ice Sheet is larger and older, rests on higher topograph

156 The Antarctic Ice Sheet is losing mass at an accelerating pace, and ic

157 The West Antarctic Ice Sheet is one of the largest potential sources of ris

158 of the volume of the present East Antarctic Ice Sheet is required to explain many of the approximate

159 The less stable West Antarctic Ice Sheet is smaller and younger and was formed on what

160 The Greenland Ice Sheet is the largest land ice contributor to sea lev

161 Mass balance analysis of ice sheets is a key component to understand the effects

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

163 d marine-based sectors of the East Antarctic ice sheets is required.

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

165 ede ice discharge events from the Laurentide Ice Sheet, known as Heinrich events.

166 nt reduction in the extent of the Laurentide Ice Sheet (LIS) during MIS 3, implying that global sea l

167 surface warming may also have contributed to ice-sheet loss(9-12) analogous to ongoing changes in the

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

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

170 entration record we infer the East Greenland ice sheet margin advanced from 113.4 +/- 0.4 to 111.0 +/

171 nd to constrain the timing of changes to the ice sheet margin and relative sea level over the last gl

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

173 Switzerland, less than 50 km from the Alpine ice sheet margin.

174 al calcites from close to the East Antarctic Ice-Sheet margin, which together suggest that volcanical

175 at one species likely expanded from close to ice sheet margins near the site of a previously describe

176 Supraglacial lakes are important to ice sheet mass balance because their development and dra

177 despite its crucial importance for Antarctic ice sheet mass balance, the response of the Southern Oce

178 h a surface mass balance model to deduce the ice sheet mass balance.

179 Snowfall in Antarctica is a key term of the ice sheet mass budget that influences the sea level at g

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

181 heric warming may have the largest impact on ice-sheet mass balance.

182 This suggests that parts of the ice sheet may be highly sensitive to climate warming.

183 lobally, suggesting that a dynamic Antarctic Ice Sheet may have driven climate fluctuations during th

184 ream effect of a much larger MIS2 Laurentide Ice Sheet may have played an additional role.

185 Some regions of the ice sheet may reach a tipping point, potentially leading

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

187 In our simulations, future ice-sheet melt enhances global temperature variability a

188 levels by 2100, which will lead to enhanced ice-sheet melt.

189 sing and predicting the impacts of Antarctic Ice Sheet melting concerns the vertical distribution of

190 The acceleration of ice sheet melting has been observed over the last few de

191 gether with the likely sensitivity to future ice sheet melting, suggests that their export in glacial

192 dissolved and amorphous silica in Greenland Ice Sheet meltwaters and icebergs, demonstrating the pot

193 ensemble simulations with a state-of-the-art ice sheet model of Thwaites Glacier, a marine-terminatin

194 Here we use an ice sheet model to show that the magnitude and timing of

195 th palaeodata(2) we find, using the Parallel Ice Sheet Model(3-5), that at global warming levels arou

196 Here, using an ice-sheet model coupled to a global sea-level model, we

197 We force a high-resolution ice-sheet model with an ensemble of climate histories co

198 , and performed both high-spatial-resolution ice-sheet modelling of the Antarctic Ice Sheet and multi

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

200 Here we quantify ice-sheet modelling uncertainties for the original MICI

201 d ice sheet provide critical constraints for ice sheet models used to determine Greenland's response

202 hich are currently not accounted for in most ice sheet models, to improve sea level rise projections.

203 tions remain in the predictive capability of ice sheet models.

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

205 ide important calibration targets for future ice-sheet models(7).

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

207 ing Antarctica-contrary to present Antarctic ice-sheet models, which assume that meltwater is stored

208 used to guide development of continent-wide ice-sheet models, which currently do not simulate ice-sh

209 ence in the predictive capability of current ice-sheet models.

210 terminus of the largest Alaskan Cordilleran Ice Sheet outlet glacier during Last Glacial Maximum cli

211 records from the Arctic, located proximal to ice sheet outlet glaciers, are required.

212 of land terminating margins of the Greenland Ice Sheet over multi-annual timescales.

213 explain the synchronous evolution of global ice sheets over ice-age cycles.

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

215 Overall, our results indicate that ice sheets overlie extensive, biologically active methan

216 l of subglacial regolith or interhemispheric ice sheet phase-locking.

217 Ice sheets play a more important role in the global sili

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

219 a lack of knowledge of the configuration of ice sheets prior to the Last Glacial Maximum (LGM).

220 deling correlations between inter- and intra-ice sheet processes and their tail dependences.

221 rise projections due to imperfectly modeled ice sheet processes and unpredictable climate variabilit

222 and computational approaches to identify the ice sheet processes that drive uncertainty in sea-level

223 YDB Pt anomaly is consistent with Greenland Ice Sheet Project 2 (GISP2) data that indicated atmosphe

224 stimates of the past extent of the Greenland ice sheet provide critical constraints for ice sheet mod

225 Our ice-sheet reconstructions illustrate the current state-o

226 consequence, the potential contributions of ice sheets remain the largest source of uncertainty in p

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

228 The growth and decay of the Antarctic Ice Sheet reshapes the solid Earth via isostasy and eros

229 ors to sea-level rise (oceans, glaciers, and ice sheets) respond to climate change on timescales rang

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

231 Ice-sheet responses to decadal-scale ocean forcing appea

232 recludes an Atlantic trigger for Cordilleran Ice Sheet retreat and instead implicates the Pacific as

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

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

235 r in Beringia, indicating a correlation with ice sheet retreat.

236 st that, even when climate forcing weakened, ice-sheet retreat continued.

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

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

239 ocean-induced thinning is driving Antarctic ice-sheet retreat today.

240 ring the Last Glacial Maximum and subsequent ice-sheet retreat, and with relative sea-level change in

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

242 lance simulations show evidence for enhanced ice sheet runoff under volcanically forced conditions de

243 l ice-sheet growth over Scandinavia from the ice sheet's earliest position to the later pattern of de

244 c continental shelf, plays a key role in the ice sheet's mass balance.

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

246 edback processes, fundamentally altering the ice sheet's present and future hydrology.

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

248 driven shifts in atmospheric forcing and the ice sheet's sensitivity to that forcing.

249 The ice sheet's temperature sensitivity is 1.3 metres of sea

250 'ice slabs' that have expanded the Greenland ice sheet's total runoff area by 26 +/- 3 per cent since

251 (AMOC), inflowing warm Atlantic Layer water, ice sheet, sea-ice and ice-shelf feedbacks, and sensitiv

252 ring the last glacial period, the Laurentide Ice Sheet sporadically discharged huge numbers of iceber

253 e interactions between ocean, atmosphere and ice sheet stability during the YD, more high-resolution

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

255 tive of a change in the dynamics that govern ice sheet stability, such as that expected from the remo

256 hindering the assessment of past and future ice-sheet stability.

257 yr period of cycles in Earth's axial tilt as ice sheets stabilize on Antarctica and intensify in the

258 olar radiation receipt (and ablation) at the ice sheet surface.

259 within the eastern sector of the Laurentide Ice Sheet than traditional reconstructions for this inte

260 Numerical models of the Antarctic Ice Sheet that incorporate meltwater's impact on ice she

261 lation splits moved south of the continental ice sheets that covered Canada sometime between ~17.5 an

262 ree of the largest glaciers of the Greenland Ice Sheet; these have been major contributors to ice los

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

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

265 nic eruptions can impact the mass balance of ice sheets through changes in climate and the radiative

266 upply of surface meltwater to the bed of the ice sheet throughout the melt season.

267 nus from subsurface warming and allowing the ice sheet to advance again until, at its most advanced p

268 train the possible response of the Greenland ice sheet to climate forcings.

269 ese feedbacks in shaping the response of the ice sheet to past and future climate changes.

270 a mechanism for this sector of the Antarctic Ice Sheet to respond rapidly to atmospheric warming.

271 st of the contribution of the West Antarctic Ice Sheet to sea level rise.

272 Mass loss from the Antarctic Ice Sheet to the ocean has increased in recent decades,

273 merical modelling results related to pre-LGM ice sheets to produce new hypotheses regarding their ext

274 s insight into the response of sea level and ice sheets to prolonged warming(1).

275 owever, inferences on the response of former ice sheets to sub-millennial palaeoclimate shifts are li

276 The sensitivity of past ice sheets to volcanic ashfall highlights the need for a

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

278 ucting the dynamic response of the Antarctic ice sheets to warming during the Last Glacial Terminatio

279 econstruct the mass balance of the Greenland Ice Sheet using a comprehensive survey of thickness, sur

280 cial meltwater rivers draining the Greenland Ice Sheet, using a recently developed submersible analyz

281 g on greenhouse gas concentrations and polar ice sheet volume.

282 geological data show that the West Antarctic Ice Sheet (WAIS) advanced to the eastern Ross Sea shelf

283 driver of mass loss from the West Antarctic Ice Sheet (WAIS) has been warm ocean water underneath co

284 The West Antarctic ice sheet (WAIS) is highly vulnerable to collapsing beca

285 Moreover, the West Antarctic ice sheet (WAIS) may be much less stable than previous b

286 s, including collapses of the West Antarctic Ice Sheet (WAIS).

287 The mean concentration of cells exiting the ice sheet was 8.30 x 10(4) cells mL(-1) and we estimate

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

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

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

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

292 Retreating palaeo ice sheets were therefore likely responsible for high di

293 Antarctic ice sheets were typically largest during repeated glacia

294 Until recently, ice sheets were viewed as inert components of this cycle

295 he (234)U cycling observed in the Laurentide Ice Sheet, where (234)U accumulated during periods of ic

296 eshwater resources are held by the Antarctic Ice Sheet, which thus represents by far the largest pote

297 Here we present an ice-sheet-wide survey of Greenland subglacial lakes, ide

298 ng that the future response of the Antarctic Ice Sheet will be governed more by long-term anthropogen

299 cial for controlling methane fluxes from the ice sheet, with efficient drainage limiting the extent o

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