ライフサイエンスコーパス: ice sheet

1 duits connecting the surface and base of the ice sheet).

2 necting supraglacial water to the bed of the ice sheet).

3 cial discharge from the surrounding grounded ice sheet.

4 hic habitats on the surface of the Greenland ice sheet.

5 kably robust net autotrophy on the Greenland Ice Sheet.

6 nd highlands and a diminished continent-wide ice sheet.

7 uto of non-brittle deformation within the N2-ice sheet.

8 balance during the retreat of the Laurentide Ice Sheet.

9 ta set to simulate the flow of the Greenland Ice Sheet.

10 ameters of cryoconite holes on the Greenland Ice Sheet.

11 torage even in this melt-prone region of the ice sheet.

12 r can be trapped and stored at the bed of an ice sheet.

13 nputs of surface meltwater to the bed of the ice sheet.

14 rface meltwater to the base of the Greenland Ice Sheet.

15 out a certain collapse of the West Antarctic Ice Sheet.

16 eshening due to mass loss from the Antarctic ice sheet.

17 , or the annual mass loss from the Greenland Ice Sheet.

18 accelerated future retreat of the Antarctic Ice Sheet.

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

20 indings can be directly translated to modern ice sheets.

21 constitute the arterial drainage network of ice sheets.

22 high elevation habitats protruding above the ice sheets.

23 sed to infer the time-varying state of major ice sheets.

24 n habitats near the expanding and retracting ice sheets.

25 oximately 1,500-km-long corridor between the ice sheets.

26 and stored in subglacial lakes beneath large ice sheets.

27 ning of Late-Pleistocene Northern Hemisphere ice sheets.

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

29 These drainage events drive transient ice-sheet acceleration and establish conduits for additi

30 stability of marine sectors of the Antarctic Ice Sheet (AIS) in a warming climate has been identified

31 Sea, Antarctica, indicate that the Antarctic ice sheet (AIS) was highly variable through this key tim

32 O2 levels of >/=600 ppm, a smaller Antarctic Ice Sheet (AIS), restricted to the terrestrial continent

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

34 irst direct geological evidence of Antarctic ice-sheet (AIS) expansion at the MSC onset and use a del

35 Here we use a model coupling ice sheet and climate dynamics-including previously unde

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

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

38 n extraterrestrial platinum in the Greenland Ice Sheet and of the earliest age of the Younger Dryas c

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

40 ing model data conflict of Miocene Antarctic ice sheet and sea level variability.

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

42 Mass contributions from ice sheets and glaciers (1.37 +/- 0.09 mm/y, acceleratin

43 the sea-level budget into contributions from ice sheets and glaciers, the water cycle, steric expansi

44 gional-scale forcings, including insolation, ice sheets and ocean circulation, modulated glacier resp

45 Ice streams drain large portions of ice sheets and play a fundamental role in governing thei

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

47 ice sheet has a stabilizing influence on the ice sheets, and previous studies have established the im

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

49 r findings suggest that these sectors of the ice sheet are more resilient to the dynamic impacts of e

50 Due to climate change, Arctic ice sheets are retreating.

51 re-dated the increase in the maximum size of ice sheets around 0.9 million years ago.

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

53 crucial to interpreting the past behavior of ice sheets, as well as to predicting their future evolut

54 e for millions of years at the center of the ice sheet at Summit, Greenland.

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

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

57 Growth of the first permanent Antarctic ice sheets at the Eocene-Oligocene Transition (EOT), app

58 If this water is delivered to the ice sheet base it may have important consequences for ic

59 bility of the early to mid-Miocene Antarctic ice sheet because of three developments in our modeling

60 termine the distribution of meltwater at the ice-sheet bed before, during, and after three rapid drai

61 t enables water to drain from regions of the ice-sheet bed that have a high basal water pressure.

62 stent with distinct signatures of changes in ice sheet behaviour coincident with major climate transi

63 kes should be considered when predicting how ice sheet behaviour will change in a warming climate.

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

65 es in the oxygen isotopic composition of the ice sheet by using isotope-enabled climate and ice sheet

66 A more stable, continental-scale ice sheet calving at the coastline did not form until ~3

67 onclude that (i) the interior surface of the ice sheet can be efficiently drained under optimal condi

68 , suggesting that small perturbations to the ice sheet can be substantially enhanced, providing a pos

69 This implies that as a minimum, a regional ice sheet centred on the Ellsworth-Whitmore uplands may

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

71 olution atmospheric component to account for ice sheet-climate feedbacks.

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

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

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

75 dies suggesting that the collapse of a major ice sheet could be imminent or potentially underway in W

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

77 (i) We use a climate-ice sheet coupling method utilizing a high-resolution at

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

79 drainage routes opened up during Patagonian Ice Sheet deglaciation.

80 ams as unstable entities that can accelerate ice-sheet deglaciation, we conclude that ice streams exe

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

82 igh latitudes, eventually led to continental ice sheet development in Antarctica in the early Oligoce

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

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

85 ow that, for a lake on the western Greenland Ice Sheet, drainage events are preceded by a 6-12 hour p

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

87 2) ), was less than half covered by grounded ice sheet during glaciations, is biologically rich and a

88 ticyclone developed above the North American ice sheet during Marine Isotope Stage 4.

89 A clearer constraint on the behaviour of the ice sheet during past and, ultimately, future interglaci

90 ever, the configuration and stability of the ice sheet during past interglacial periods remains uncer

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

92 a level changes, and rapid disintegration of ice sheets during deglaciation.

93 The severe cooling and the expansion of the ice sheets during the Last Glacial Maximum (LGM), 27,000

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

95 ubglacial lake drainage events can induce an ice sheet dynamic response--a process that has been obse

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

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

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

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

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

101 urface meltwater to the bed of the Greenland Ice Sheet each summer causes an initial increase in ice

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

103 used to suggest a diminished East Antarctic Ice Sheet (EAIS) during Pliocene warm periods.

104 ular, the contribution of the East Antarctic Ice Sheet (EAIS) is ill defined, restricting our appreci

105 olar climate that enables the East Antarctic Ice Sheet (EAIS) to remain stable, frozen to underlying

106 Here we show that deep ice-sheet erosion-enough to expose basement rocks-has oc

107 Here we investigate a new indicator of ice sheet evolution: sulfates within the glaciogenic dep

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

109 Here we show that the East Greenland Ice Sheet existed over the past 7.5 million years, as in

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

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

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

113 SO behavior when global boundary conditions (ice sheet extent, atmospheric partial pressure of CO2) w

114 n changes in Chinese loess grain-size and NH ice-sheet extent, we use loess grain-size records to con

115 understood insufficiently to constrain past ice-sheet extents.

116 Here we show that progressive Fennoscandian Ice Sheet (FIS) melting 13,100-12,880 years ago generate

117 he Antarctic Ice Sheet restrain the grounded ice-sheet flow.

118 l increase sea-level rise from the Greenland Ice Sheet for decades to come.

119 ion years ago, Earth's climate cooled and an ice sheet formed on Antarctica as atmospheric carbon dio

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

121 times during deglaciation of the Laurentide Ice Sheet (from about 22,000 to 7,000 years ago) and sho

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

123 Such ice sheet geometry is potentially unstable.

124 The Greenland Ice Sheet (GIS) contains the equivalent of 7.4 metres of

125 The response of the Greenland Ice Sheet (GIS) to changes in temperature during the twe

126 ng land-terminating margins of the Greenland Ice Sheet (GIS) varies considerably in response to fluct

127 This gain partially offset water losses from ice sheets, glaciers, and groundwater pumping, slowing t

128 nt with the sum of individual contributions (ice sheets, glaciers, and hydrology) found in literature

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

130 of bioavailable carbon and iron in Greenland Ice Sheet (GrIS) runoff.

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

132 Snow overlays the majority of the Greenland Ice Sheet (GrIS).

133 in southern high-latitude climate, Antarctic ice sheet growth across the continental shelves, and ass

134 ar the grounding line of a retreating marine ice sheet has a stabilizing influence on the ice sheets,

135 The Greenland ice sheet has become one of the main contributors to glo

136 In both cases the Antarctic ice sheet has been implicated as the primary contributor

137 atop a deep marine basin, the West Antarctic Ice Sheet has long been considered prone to instability.

138 across melt-prone surfaces of the Greenland ice sheet have received little direct study.

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

140 ubglacial melting of the Northern Hemisphere ice sheets have driven the observed (234)U/(238)U evolut

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

142 effect, which results in stability once the ice sheets have reached continental size.

143 Polar ice sheets hold a significant pool of the world's carbon

144 Here we use a coupled ice-sheet/ice-shelf model to show that if atmospheric wa

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

146 al lake, which drained beneath the Greenland ice sheet in 2011.

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

148 and we cannot distinguish between a remnant ice sheet in the East Greenland highlands and a diminish

149 the structure and long-term evolution of the ice sheet in this region have been understood insufficie

150 o millennial-scale response of the Antarctic ice sheet in which enhanced viscous flow produces a long

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

152 mportant for addressing questions concerning ice sheet (in)stability and changes in global sea level.

153 ial maximum (LGM), the demise of continental ice sheets induced crustal rebound in tectonically stabl

154 below sea level may be vulnerable to marine-ice-sheet instability (MISI), a self-sustaining retreat

155 Thereafter, the marine ice-sheet instability fully unfolds and is not halted by

156 ulations have suggested the initiation of an ice-sheet instability in the Amundsen Sea sector of West

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

158 Melting of Greenland's ice sheet is freshening the North Atlantic; however, whe

159 Seasonal acceleration of the Greenland Ice Sheet is influenced by the dynamic response of the s

160 The Greenland Ice Sheet is losing mass at an accelerating rate due to

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

162 recent interior thickening of the Greenland Ice Sheet is partly an ongoing dynamic response to the l

163 Recent peripheral thinning of the Greenland Ice Sheet is partly offset by interior thickening and is

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

165 imate, surface meltwater production on large ice sheets is expected to increase.

166 ecause the equilibrium-response timescale of ice sheets is longer than those of the atmosphere or oce

167 During the Last Glacial Maximum, continental ice sheets isolated Beringia (northeast Siberia and nort

168 st Barents and Norwegian seas where grounded ice sheets led to thickening of the gas hydrate stabilit

169 es, and sources of sea-level rise from polar ice-sheet loss during past warm periods.

170 to a level associated with significant polar ice-sheet loss in the past.

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

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

173 Large parts of the Antarctic ice sheet lying on bedrock below sea level may be vulner

174 sheet (with a marginal zone near the present ice-sheet margin) and the retreated ice sheet (with the

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

176 e melting of sea ice, icebergs, and terminal ice-sheet margins.

177 eams exerted progressively less influence on ice sheet mass balance during the retreat of the Laurent

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

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

180 Antarctic ice sheet mass loss is largely driven by ice shelf basal

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

182 Climate models show that ice-sheet melt will dominate sea-level rise over the com

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

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

185 t high southern latitudes promoted Antarctic ice-sheet melting that fuelled the last interglacial sea

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

187 Five intervals reflect ice sheet minima and air temperatures warm enough for su

188 (ii) The ice sheet model includes recently proposed mechanisms fo

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

190 Here we show that in the Parallel Ice Sheet Model, a local destabilization causes a comple

191 Here we combine a high-resolution ice-sheet model coupled to uniformly applied models of s

192 CO2 These new drill core data and associated ice sheet modeling experiments indicate that polar clima

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

194 Updated ice-sheet modelling shows significant Pliocene EAIS retr

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

196 e sheet by using isotope-enabled climate and ice sheet models.

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

198 Representative ice-sheet models indicate that the global sea-level incr

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

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

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

202 f the Weddell Sea embayment that suggest the ice sheet, nourished by increased snowfall until the ear

203 laciated state into one that sustained large ice sheets on Antarctica.

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

205 of the behavior of Northern Hemisphere (NH) ice sheets over the past million years is crucial for un

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

207 ed a progressively smaller percentage of the ice sheet perimeter and their total discharge decreased.

208 reveal that subglacial lakes beneath modern ice sheets periodically store and release large volumes

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

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

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

212 ems to be a response to changes in Antarctic ice-sheets rather than to NH cooling.

213 avoid this commitment if the West Antarctic Ice Sheet remains stable.

214 The future evolution of the Antarctic Ice Sheet represents the largest uncertainty in sea-leve

215 conventional wisdom, however, the Greenland ice sheet responds to this energy through a new pathway

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

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

218 oating ice shelves surrounding the Antarctic Ice Sheet restrain the grounded ice-sheet flow.

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

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

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

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

223 uplift and sea-surface drop associated with ice-sheet retreat significantly reduces AIS mass loss re

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

225 As the Cordilleran and Laurentide Ice Sheets retreated, North America was colonized by hum

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

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

228 The main drivers of Greenland ice sheet runoff, however, remain poorly understood.

229 The ice sheet's dynamic response to the decreasing proportio

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

231 On the basis of the ice sheet's radiostratigraphy, ice flow in its interior

232 pically span only a few decades, and, at the ice-sheet scale, it is unclear how the entire drainage n

233 influenced ice stream activity, but--at the ice-sheet scale--their drainage network adjusted and was

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

235 Here we use a coupled ice sheet-sea-level model to investigate the impact of t

236 hern latitudes and provide insight regarding ice sheet sensitivity to past climate change.

237 nces and challenges involved in constraining ice-sheet sensitivity to climate change with use of pale

238 res accurate portrayal of outlet glaciers in ice sheet simulations, but to date poor knowledge of sub

239 ns since the Miocene during periods when the ice sheet size was smaller than today, but with an overa

240 magmatic flux acts as a negative feedback on ice-sheet size.

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

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

243 ommitment for different carbon emissions and ice sheet stability scenarios, we compute the current po

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

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

246 nary GIS collapse after it crossed a climate/ice-sheet stability threshold that may have been no more

247 increased iceberg calving and dispersal from ice sheets surrounding the North Atlantic has inspired m

248 nt the response of the present-day Antarctic ice-sheet system to the oceanic and climatic changes of

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

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

251 e longest period of stability of the present ice sheet that is consistent with the measurements is 1.

252 Unlike the ice sheets, the Alpine ice cap developed in an orogen wh

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

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

255 the mass and energy balance of the Greenland ice sheet through its impact on radiative budget, runoff

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

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

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

259 The high sensitivity of the Greenland ice sheet to both ice-only and liquid-bearing clouds hig

260 redict future contributions of the Greenland ice sheet to global sea level rise.

261 the long-term contribution of the Antarctic ice sheet to global sea level.

262 The contribution of the Greenland ice sheet to sea-level rise has accelerated in recent de

263 overestimate true meltwater export from the ice sheet to the ocean.

264 Climate variations cause ice sheets to retreat and advance, raising or lowering s

265 ribution of the Greenland and West Antarctic ice sheets to sea level has increased in recent decades,

266 rtainty when predicting the contributions of ice sheets to sea-level rise.

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

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

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

270 Grounding zones, where ice sheets transition between resting on bedrock to full

271 events are preceded by a 6-12 hour period of ice-sheet uplift and/or enhanced basal slip.

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

273 e coming centuries, but our understanding of ice-sheet variations before the last interglacial 125,00

274 ble interval) over the next few millennia as ice sheets, vegetation and atmospheric dust continue to

275 hat there were major variations in Antarctic ice sheet volume and extent during the early to mid-Mioc

276 etwork adjusted and was linked to changes in ice sheet volume.

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

278 Past fluctuations of the West Antarctic Ice Sheet (WAIS) are of fundamental interest because of

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

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

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

282 trajectory of thinning of the West Antarctic ice sheet (WAIS) since the last glacial maximum (LGM) is

283 lacial implies retreat of the West Antarctic Ice Sheet (WAIS).

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

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

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

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

288 Antarctic ice sheets were typically largest during repeated glacia

289 grain-size records to confirm that northern ice-sheets were restricted during marine oxygen isotope

290 m in less crevassed, interior regions of the ice sheet, where water at the bed is currently less perv

291 s left a direct thermal remnant in the polar ice sheets, where the exceptional purity and continual a

292 id growth of Northern Hemisphere continental ice sheets, which terminated warm and stable climate per

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

294 Here we project that the Antarctic ice sheet will contribute up to 30 cm sea-level equivale

295 The contribution that large ice sheets will make to sea-level rise under such warmin

296 rations, corresponding to the 'modern-scale' ice sheet (with a marginal zone near the present ice-she

297 present ice-sheet margin) and the retreated ice sheet (with the marginal zone located far inland).

298 the glacier catchments of the West Antarctic Ice Sheet within the low topography of the West Antarcti

299 ws the potential for prognostic modelling of ice sheets without the need for spatially varying parame

300 man perturbations no substantial build-up of ice sheets would occur within the next several thousand