ライフサイエンスコーパス: glacial

1 consistent with proxy evidence for the last glacial.

2 schger (D-O) climate changes during the last glacial.

3 and 30 degrees C) and four concentrations of glacial acetic acid (0.5%, 1%, 2%, and 3%).

4 Hexane: methanol: acetone: glacial acetic acid (8:2:0.5:0.1, by volume) is proposed

5 Kafirin was dissolved in glacial acetic acid (GAA) and simple coacervation was pe

6 Dissolving the prolamins in glacial acetic acid apparently enabled protonation and c

7 itation, involving dissolution in ethanol or glacial acetic acid followed by precipitation by additio

8 In contrast, precipitation from glacial acetic acid resulted in a highly plasticized, co

9 ea-bed landform imprint of a shelf-wide last glacial advance and progressive deglaciation.

10 ccurred during MIS 4, with another prominent glacial advance at 37-33 kyr BP.

11 western Greenland Ice Sheet (GIS) during the glacial advance of marine oxygen isotope stage 4 (MIS4).

12 both regions having served as refugia during glacial advances in the late Quaternary Period.

13 prominent positive delta(13)C excursions and glacial advances.

14 has only been identified for the most recent glacial and deglacial periods and is thought to be absen

15 ocean circulation and stratification between glacial and interglacial climates can be interpreted as

16 ts were grounded below sea level during both glacial and interglacial periods, with grounding lines a

17 limate has undergone dramatic shifts between glacial and interglacial time periods, with high-latitud

18 indings support the hypothesis that repeated glacial and landslide damming in this region inhibited h

19 spread As and Mn contamination including the Glacial Aquifer in the U.S., the Ganges-Brahmaputra-Meht

20 -latitude climate variations during the last glacial are expected to propagate globally in a complex

21 bution of allochthonous migrants in the post-glacial assembly of Europe is unparalleled in other plan

22 coalescent simulations showed that the post-glacial assembly of European bryophytes involves a compl

23 ss mixing dominated the distribution of deep glacial Atlantic Nd isotopes, our results would imply a

24 inct South Indian fingerprints on (early de-)glacial atmospheric CO(2) change.

25 Here, we present data showing that glacial Ca also reduces grain yield in both crop types.

26 his hypothesis, previous work has shown that glacial Ca limits vegetative growth in the wild progenit

27 Yet, the volumetric extent of the glacial carbon pool and the deglacial mechanisms contrib

28 m an iron and silicate mineral-rich basaltic glacial catchment were an order of magnitude higher than

29 riglacial habitats and water bodies within a glacial catchment.

30 netic diversity are likely influenced by the glacial climate cycle and recent history of whaling.

31 vier shells would need to be precipitated in glacial climates in order for these organisms to remain

32 We modelled vegetation for glacial climates under different levels of CO(2) and fir

33 Earth has experienced warm ice-free and cold glacial climates, but it is unknown whether transitions

34 nt a major challenge to our understanding of glacial climates.

35 In this study we show that low glacial CO(2) levels, similar to those at the MPT, lead

36 uatm across the MPT, mainly because of lower glacial CO2 levels.

37 deficit and temperature were decreased under glacial conditions at La Brea, and these have compensati

38 possible due to reduced drought stress under glacial conditions at La Brea.

39 or millennia before a gradual return to full glacial conditions.

40 h implications on ocean productivity at peak glacial conditions.

41 ht to constrain the magnitude and pattern of glacial cooling from palaeothermometers(1,2), but the un

42 set of climate model simulations of the last glacial cycle (120 kyr), that compares well against a co

43 ironmental histories that span the last full glacial cycle and are representative of regional change

44 onounced ice-sheet asymmetry within the last glacial cycle and significant variations in ice-marginal

45 treme Greenland shelf glaciation of the last glacial cycle occurred during MIS 4, with another promin

46 After the last glacial cycle, temperate European trees migrated northwa

47 emergence of the high-amplitude 100,000-year glacial cycle.

48 margin and relative sea level over the last glacial cycle.

49 nges in tropical circulation during the last glacial cycle.

50 a warmer climate state with sawtooth-shaped glacial cycles in the Early Miocene was brought about by

51 These glacial cycles occurred during large environmental chang

52 as been continually important throughout the glacial cycles of recent Earth history.

53 Only with global cooling and the onset of glacial cycles some 3 Mya, toward the end of the Pliocen

54 Between about 2.8 and 1.2 million years ago, glacial cycles were smaller in magnitude and shorter in

55 c divergences relative to the timing of past glacial cycles, including collapses of the West Antarcti

56 ions in ice-marginal positions between older glacial cycles.

57 a, reflecting population contractions during glacial cycles.

58 repeated carbon storage over the last three glacial cycles.

59 ed climate amplifier in the late Pleistocene glacial cycles.

60 pansion and local extirpation in response to glacial cycling.

61 pt and large-amplitude climate change of the glacial D-O events.

62 Conversely, regions of bedrock confined by glacial deposits yielded significantly lower median N2O-

63 onstraint for the youngest Palaeoproterozoic glacial deposits, the Rietfontein diamictite in South Af

64 We find that glacial discharge - sourced primarily from ice shelf and

65 Here we present a 6,250 year record of glacial discharge based on the oxygen isotope compositio

66 ween being primarily regulated by sea ice or glacial discharge from the surrounding grounded ice shee

67 A marked acceleration in the rate of glacial discharge is also observed in the early part of

68 An increasing trend in glacial discharge occurs after 550 cal.

69 Enhanced glacial discharge, particularly after the 1700s is linke

70 e infer that reduced vegetation cover during glacials drove higher sediment flux from the rift flanks

71 The record shows that variations in glacial dust deposition variability on centennial-millen

72 ive that changes in snow and ice melt across glacial environments will influence the abundance and di

73 sotope data from a Neoproterozoic (Marinoan) glacial episode.

74 matic conditions, including interglacial and glacial episodes, between 670 and 650 (i.e., MIS17/MIS16

75 Miocene was brought about by subsidence and glacial erosion in West Antarctica during the Late Oligo

76 Glacial erosion rate is usually modelled as a function o

77 surface, but there is uncertainty about how glacial erosion should be parameterised in landscape evo

78 ecipitation has received little attention in glacial erosion studies, but our data illustrate its imp

79 ed by spatially heterogeneous Neoproterozoic glacial erosion totaling a global average of 3-5 vertica

80 to show that interactions between ice flow, glacial erosion, and sediment transport drive these cycl

81 l Earth and therefore cannot be a product of glacial erosion.

82 ndings can be used to improve models of past glacial, eustatic, tectonic, and geomorphic processes on

83 urasia, in addition to the better-known late-glacial event.

84 n the deep Atlantic, similar in magnitude to glacial events, have been relatively common and occasion

85 show a similar relationship beyond the last glacial, extending to at least 70,000 years.

86 ariation of the abiotic environment in these glacial-fed streams.

87 sediments than deep horizons, bare soils or glacial flours.

88 We identify the location of immediate pre-glacial fluvially derived sandy systems where rivers fro

89 Centennial-scale mineral dust peaks in last glacial Greenland ice cores match the timing of lowest G

90 ture in the grass's western spread, although glacial history and environmental heterogeneity also cou

91 e is very low and is sourced from melting of glacial ice and direct release of occluded CO(2) gases i

92 spheric carbon dioxide behind climate during glacial inception and deglaciation.

93 nd modelling evidence indicate that the last glacial inception in North America was in NE Canada, lit

94 Antarctic ice cores document glacial-interglacial and millennial-scale variability in

95 hat have remained more stable in response to glacial-interglacial changes in climate were also more s

96 LSTs, superimposed on the fundamental global glacial-interglacial changes.

97 ld have accounted for as much as half of the glacial-interglacial CO2 change.

98 During the succeeding glacial-interglacial cycles (MIS 100 to 95), sea levels

99 Pleistocene glacial-interglacial cycles are correlated with dramatic

100 el varied on average by 13 +/- 5 metres over glacial-interglacial cycles during the middle-to-late Pl

101 The pacing of glacial-interglacial cycles during the Quaternary period

102 Our data reveal clear glacial-interglacial cycles in global ice volume and sea

103 siderably across and within millennia during glacial-interglacial cycles of the Late Quaternary.

104 Over the past eight hundred thousand years, glacial-interglacial cycles oscillated with a period of

105 ive amplitude of sea-level variations within glacial-interglacial cycles remains poorly constrained.

106 nal hydroclimate records that cover multiple glacial-interglacial cycles(2,3) with different orbital

107 ficantly across decades and centuries during glacial-interglacial cycles, likely causing rapid region

108 get, and Antarctic ice-sheet dynamics across glacial-interglacial cycles.

109 palaeotemperature information over multiple glacial-interglacial cycles.

110 otemperature proxy time series over multiple glacial-interglacial cycles.

111 ng by Earth's climatic precession, with each glacial-interglacial period spanning four or five cycles

112 he past 500,000 y and spanning the last five glacial-interglacial periods.

113 er observed in pyrite, and are in phase with glacial-interglacial sea level and temperature changes.

114 ing the strength of the biological pump, the glacial-interglacial shift in the Si cycle may present a

115 drologic seesaw is apparent over orbital and glacial-interglacial timescales, but its existence over

116 of carbon exchanging with the atmosphere on glacial-interglacial timescales, the deep ocean has been

117 bfossil chironomid records spanning the last glacial-interglacial transition (~15,000-11,000 years ag

118 r, wetter, and more isolated during the last glacial-interglacial transition from approximately 15 to

119 lation bottleneck hypothesis during the Last Glacial-Interglacial transition, providing a demographic

120 models of demographic growth during the Last Glacial-Interglacial transition.

121 ally significant difference between previous glacial-interglacial transitions and the very last one w

122 tion rests on two assumptions: that previous glacial-interglacial transitions were similar to the end

123 why did these large mammals survive previous glacial-interglacial transitions, only to vanish at the

124 Our results confirm that the amplitudes of glacial-interglacial variations in atmospheric greenhous

125 f applications, including ocean circulation, glacial/interglacial climates, and anthropogenic climate

126 st 1.5 million years (Ma) of orbitally-paced glacial/interglacial cycles (GIC).

127 Their area has varied dramatically over the glacial/interglacial cycles of the last million years, b

128 ensitivity and GHG levels over the past four glacial/interglacial cycles.

129 rk provides a clear sign of sea level-driven glacial/interglacial oscillations in biogeochemical flux

130 ies probably colonized Abaco during the last glacial interval but were eliminated when the island bec

131 50 to 35 ka, are surprisingly high for this glacial interval, and remain unexplained by previous mod

132 the plants that were present during the last glacial interval, including all of the arctic-alpines, a

133 However, glacial iron inputs are thought to be dominated by icebe

134 es an independent constraint on the combined Glacial Isostatic Adjustment - the Earth's delayed visco

135 These records capture spatial variations in glacial isostatic adjustment and paleotidal range, yet b

136 The stresses resulting from glacial isostatic adjustment appear to be much smaller t

137 is sea-level record using a revised model of glacial isostatic adjustment characterized by a peak glo

138 ences of penultimate and LIG deglaciation on glacial isostatic adjustment, this excess loss of polar

139 med an ice-dammed lake and generated a small Glacial Lake Outburst Flood (GLOF).

140 of the ice core could have implications for glacial lake outburst risk.

141 s to expand to a fully formed moraine-dammed glacial lake, the degradation of the ice core could have

142 ctic watersheds spanning alpine, tundra, and glacial-lake landscapes in Alaska.

143 ne the influence of surface debris cover and glacial lakes on glacier mass loss across the Himalaya s

144 oat and therefore shares similarities to sub-glacial lakes where they are sealed to the atmosphere.

145 The continued expansion of established glacial lakes, and the preconditioning of land-terminati

146 ape from the Mesozoic overburden and carving glacial landforms down to Plio-Pleistocene times.

147 variation in P. leucopus indicates two post-glacial lineages are separated by the St. Lawrence River

148 We also compared isotope ratios between glacial-marine and more oceanic habitats.

149 d a divergence in food web structure between glacial-marine and oceanic sites.

150 assed from lower to higher trophic levels in glacial-marine habitats.

151 During glacial maxima throughout that period, species in Europe

152 minimum carbon dioxide concentrations during glacial maxima.

153 two older interglacials and their preceding glacial maxima.

154 s that were connected to the mainland during glacial maxima.

155 by the Laurentide ice sheet during the Last Glacial Maximum (18,000 years before present [YBP]); aft

156 )of cultural evidence that dates to the Last Glacial Maximum (26,500-19,000 years ago)(18), and which

157 reases the volume of the AIS during the Last Glacial Maximum (about 26,000 to 20,000 years ago), trig

158 efore, during and immediately after the Last Glacial Maximum (about 26.5-19 thousand years ago)(2,3)

159 eastern Ross Sea shelf edge during the Last Glacial Maximum (LGM) and eventually retreated 1000 km t

160 Climatic fluctuations during the Last Glacial Maximum (LGM) exerted a profound influence on bi

161 for this time period, spanning from the Last Glacial Maximum (LGM) to the mid-Holocene.

162 Central Europe during the Last Glacial Maximum (LGM) was dominated by polar desert and

163 by heavy sea ice conditions during the Last Glacial Maximum (LGM) yielded genetic signatures of near

164 olf population that expanded during the last glacial maximum (LGM)(1-3) and replaced local wolf popul

165 )N across the Southern Ocean during the Last Glacial Maximum (LGM), 18-25 thousand years ago.

166 more radiogenic than modern during the Last Glacial Maximum (LGM), and shifted towards modern values

167 The Last Glacial Maximum (LGM), one of the best studied palaeocli

168 During the Late Glacial Maximum (LGM), southern European peninsulas were

169 During the Last Glacial Maximum (LGM), the peninsula formed a periglacia

170 owth potential of Trichodesmium for the last glacial maximum (LGM), the present (2006-2015) and the e

171 ected the Near East to Europe after the Last Glacial Maximum (LGM).

172 of Southern Hemisphere dust during the Last Glacial Maximum (LGM).

173 onfiguration of ice sheets prior to the Last Glacial Maximum (LGM).

174 urers and a discontinuity marked by the Last Glacial Maximum (LGM).

175 and two paleoclimatic environments, the Last Glacial Maximum (LGM, ~ 21 kya) and the Mid-Holocene (MH

176 During the Last Glacial Maximum (LGM; ~20,000 years ago), the global oce

177 arth's history, in particular since the Last Glacial Maximum 20,000 years ago, and are used in this s

178 ons of the extent of the AIS during the Last Glacial Maximum and subsequent ice-sheet retreat, and wi

179 ximus groups having diverged during the last glacial maximum and subsequently expanded, whereas P. ja

180 this region rapidly increased after the Last Glacial Maximum ca. 18 kya.

181 illeran Ice Sheet outlet glacier during Last Glacial Maximum climate transitions.

182 d drainage of Fe-rich waters during the Last Glacial Maximum could have reached the Southern Ocean.

183 wave of megafaunal turnover before the Last Glacial Maximum in Eurasia, in addition to the better-kn

184 During the Last Glacial Maximum in the Northern Hemisphere, expanding ic

185 or divergence prior to the onset of the last glacial maximum shaped the genetic diversity and structu

186 Georgia through the transition from the Last Glacial Maximum to Holocene.

187 ated as tidal channels during the post- Last Glacial Maximum transgression, when the study area was a

188 che modeling to infer current and past (Last Glacial Maximum) environmental suitability across the sp

189 an and Epigravettian layers, across the Last Glacial Maximum, and dated between 31210-33103 and 18334

190 casted species distributions during the Last Glacial Maximum, we hypothesize that Arctic coastal syst

191 ntaining tropical grasslands during the last glacial maximum, which are possible centres of diversifi

192 ed dramatic range reductions during the Last Glacial Maximum, yet refugial populations from which mod

193 lacial periods, particularly during the Last Glacial Maximum.

194 d recent population expansion after the Last Glacial Maximum.

195 ters during ice shelf retreat after the Last Glacial Maximum.

196 igh abyssal salinities inferred for the last glacial maximum.

197 ions at a scale unprecedented since the last glacial maximum.

198 tope Stage) 2 related to the end of the Last Glacial Maximum.

199 wed by a precipitous decline during the Last Glacial Maximum.

200 population expansions, dated after the last glacial maximum.

201 Since 2001, glacial MeHg and THg inputs to Lake Hazen have increased

202 Pro-glacial melange (a mixture of sea ice, icebergs, and sno

203 atmospheric/oceanic warming and increases in glacial melt over the past half century.

204 cal for understanding how current and future glacial melt seasons may influence downstream environmen

205 consumption in proglacial freshwaters due to glacial melt-enhanced weathering is likely a globally re

206 ectively, in step with dramatic increases in glacial melt.

207 dicated that the pesticide concentrations in glacial meltwater and lake water were strongly correlate

208 aminants in suspended sediments suggest that glacial meltwater and the delivery of cryoconite have li

209 nt export of microbial assemblages alongside glacial meltwater is expected to impact the ecology of a

210 ic climate conditions and suggests that peak glacial meltwater production is imminent if not already

211 The findings suggest that the glacial meltwater recharging the closed-basin and well-s

212 sticides were quantified in air, lake water, glacial meltwater, and streamwater in the catchment of L

213 he scavenging of hydrophobic contaminants in glacial meltwater.

214 Annually, glacial meltwaters accounted for 62-98% of dissolved nut

215 warming since 2007 has increased delivery of glacial meltwaters to the lake by up to 10-times.

216 d during glaciations and released during (de)glacial millennial-scale climate events.

217 The characterization of Last Glacial millennial-timescale warming phases, known as in

218 nce the increased buoyant force of a denser, glacial ocean.

219 .4 +/- 0.4 to 111.0 +/- 0.4 ka BP during the glacial onset and retreated from 12.1 +/- 0.1 to 9.0 +/-

220 The second stage commenced after a glacial outburst that caused the collapse of the Thermoh

221 mperature records, and estimates of the last glacial oxygen isotopic composition of precipitation bas

222 ved regional amount effect variability, last glacial paleotemperature records, and estimates of the l

223 d and Antarctic temperatures during the last glacial period (115,000 to 11,650 years ago) are thought

224 atterns of variability since the penultimate glacial period (140 ka), but the seasonality of this sig

225 Both tephra were erupted during the last glacial period and a widespread increase in subglacial v

226 t largely formed during the late Pleistocene glacial period and shrank in the Holocene Thermal Maximu

227 encompassing the transition between the last glacial period and the current interglacial.

228 Abrupt climate changes during the last glacial period have been detected in a global array of p

229 pheric CO2 (Ca ) experienced during the last glacial period is hypothesized to have been an important

230 of the region, suggests that during the last glacial period such ticks occupied distinct refugia, wit

231 During the termination of the last glacial period the western U.S. experienced exceptionall

232 his hydroclimatic transition from the wetter glacial period to more arid Holocene accompanies a surfa

233 jor atmospheric CO2 drawdown during the last glacial period were linked to iron (Fe) fertilization of

234 em that covers nearly the entire penultimate glacial period, from 195 to 135 ky BP.

235 During the last glacial period, the Laurentide Ice Sheet sporadically di

236 climatic episodes in Alaska during the last glacial period, when permafrost was absent, allowing wat

237 ed by the atmospheric conditions of the last glacial period, with important implications for the orig

238 the Amazon was widely drier during the last glacial period, with much less recycling of water and pr

239 e most prominent feature of the Earth's last glacial period.

240 cies in Europe following the end of the last glacial period.

241 e change events in Greenland during the last glacial period.

242 colonization of northern Eurasia in the last glacial period.

243 t ice sheet, was also active during the last glacial period.

244 therefore not incising, for much of the post-glacial period.

245 er similar oscillations are typical of prior glacial periods, however, has not been well established.

246 rsist in the southern Atlantic Forest during glacial periods, particularly during the Last Glacial Ma

247 would have been especially effective during glacial periods, when the Atlantic Meridional Overturnin

248 promoting atmospheric CO(2) drawdown during glacial periods.

249 e ancient DNA retrieved from the oldest Late Glacial pine forest.

250 nologies are only available for several Last Glacial pollen and rare speleothem archives principally

251 s for emplacing offshore groundwater include glacial processes that drove water into exposed continen

252 ur results indicate a stronger role for post-glacial range expansion, rather than isolation in allopa

253 d ice cores from the terrestrial, marine and glacial realms.

254 nd experienced secondary contact during post-glacial recolonization of spruce in the Holocene.

255 ering of these distinctive features was in a glacial refuge zone on the southern coast 100-70 ka, wit

256 Long-lasting geographic isolation between glacial refugia could have been led to the allopatric sp

257 infer the precise latitude and longitude of glacial refugia in two widespread, codistributed hickori

258 coastal progenitors were likely colocated in glacial refugia.

259 ed in three distinct clades corresponding to glacial refugia.

260 en interpreted as supporting expansions from glacial refugia.

261 e this issue, as it has been considered as a glacial refugium during critical periods of the Neandert

262 was in NE Canada, little is known about the glacial response of the nearby western Greenland Ice She

263 ates in Antarctica and have implications for glacial response to Holocene warming.

264 ing grounding lines and slowing or reversing glacial retreat.

265 m, we found that weathering reactions in the glacial rivers actively consumed CO(2) up to 42 km downs

266 Glacial rivers were the most important source of MeHg an

267 particulate and dissolved organic carbon in glacial runoff and near surface coastal waters was aged

268 sheet melting, suggests that their export in glacial runoff is likely to be important for biological

269 Glacial runoff is predicted to increase in many parts of

270 he existence of complex interactions between glacial sea level changes, volcanic degassing and atmosp

271 dionuclides (FRNs) and other contaminants in glacial sediments, especially cryoconite, in European gl

272 patterns of organic delta(15)N deposited in glacial sediments.

273 ts before these impacts suggests large-scale glacial silt production and supports the previously prop

274 Winter snow from four glacial sites on Svalbard was analyzed for atmospheric d

275 Our findings reveal that in the glacial Southern Ocean, Fe fertilization critically reli

276 the existence of refuge areas during intense glacial stages and raise questions concerning understudi

277 tilization of the Southern Ocean during peak glacial stages.

278 We base our findings on a rare glacial stalagmite deposited between ~106 and ~27 ka, pr

279 Glacial-state greenhouse gas concentrations and Southern

280 assemblages reflected the transition of the glacial surface from snow-covered to bare-ice.

281 dary carotenoids, which cause a darkening of glacial surfaces leading to a decrease in surface albedo

282 cate that a surface-meltwater-rich sub-polar glacial system existed under climate conditions similar

283 ions in atmospheric CO2 were associated with glacial terminations of the Late Pleistocene.

284 Radiometric dating of glacial terminations over the past 640,000 years suggest

285 mispherewide shifts of the SWW suggested for glacial terminations.

286 During glacials, the basin was isolated from the ocean, and sed

287 ve remained spatially stable throughout post-glacial time, although with transform-affinity faults re

288 s substantially drier or remained wet during glacial times has been controversial, largely because mo

289 onic foraminifera shell mass increase during glacial times.

290 heaval that occurred as Earth shifted from a glacial to an interglacial climate.

291 ved, boron isotope CO2 data to show that the glacial to interglacial CO2 difference increased from ap

292 se in unthreshed grain yield of 50% with the glacial to postglacial increase in Ca , which matched th

293 temperature in the 40k world are well above glacial values from the past eight hundred thousand year

294 e present an exceptionally well-dated annual glacial varve chronology recording the melting history o

295 onential population increase during the Late Glacial warming period (c.16.6-12.9 kya).

296 ical and geological evidence shows that post-glacial warming released human populations from their va

297 Our analysis supports the theory that glacial weathering is characterized predominantly by wea

298 Compared with nonglacial weathering, glacial weathering is more likely to yield alkalinity/DI

299 To evaluate the effects of glacial weathering on atmospheric pCO2, we use a solute

300 Iron supplied by glacial weathering results in pronounced hotspots of bio