ライフサイエンスコーパス: glacial

1 , which took place in the course of the last glacial.

2 consistent with proxy evidence for the last glacial.

3 or marine biological productivity during the glacials.

4 deglaciation had risen, which led to longer glacials.

5 rope around 14,500 years ago during the Late Glacial, a period of climatic instability at the end of

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

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

8 the exchange of the 4-O-acetyl group by the glacial acetic acid that serves as external nucleophile

9 nd kafirin preparations by coacervation from glacial acetic acid.

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

11 surrounds the extent and timing of the last glacial advance and termination on sub-Antarctic South G

12 iwi diversification events date to the major glacial advances of the Middle and Late Pleistocene.

13 eriods are overrun and eroded by more recent glacial advances, and are therefore usually rare, isolat

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

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

16 s is because terrestrial deposits of ancient glacial and interglacial periods are overrun and eroded

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

18 C4 crops (foxtail and broomcorn millets) at glacial and postglacial Ca , measuring grain yield and t

19 ieve a UAS7 </= 6 was 6 weeks (ASTERIA I and GLACIAL) and median time to achieve a UAS7 = 0 was 12 or

20 that atmospheric CO2 pulses during the last glacial- and deglacial periods were consistently accompa

21 remained difficult to quantify the effect of glacial- and millennial-scale climate variability on ear

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

23 lie beyond the reach of most lacustrine and glacial archives.

24 " between intermediate and deep water in the glacial Atlantic Ocean, which indirectly points to an in

25 mmonly invoked as the primary cause of lower glacial atmospheric CO2.

26 in the basin responds closely to changes in glacial boundary conditions in terms of temperature and

27 role in atmospheric CH4 changes and that the glacial budget is not dominated by these sources.

28 Development under glacial Ca also impacted negatively on the subsequent ge

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

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

31 Interestingly, the C4 species at glacial Ca showed some evidence that photosynthetic capa

32 law size-frequency distributions observed at glacial calving fronts and lognormal size-frequency dist

33 These findings constrain parts of the glacial carbon pool to the deep South Pacific.

34 propose an internally consistent picture of glacial carbon storage and equatorial Pacific Ocean wate

35 acial Maximum (LGM), the exact nature of the glacial circulation and its implications for global carb

36 e ocean's persistent, central role in abrupt glacial climate change.

37 to a better perception of the impact of Last Glacial climate changes on European paleoenvironments.

38 ivity, are observed in the Holocene and last-glacial climates.

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

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

41 ults challenge current paradigms on the post-glacial CO2 rise and, at the same time, serve as a harbi

42 l proxies for aridity and with the timing of glacial cold" periods as recorded by marine proxies, suc

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

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

45 covering the entire Arctic Ocean during peak glacial conditions was proposed nearly half a century ag

46 Dust supply peaked under glacial conditions, consistent with previous studies, wh

47 roduction of North Atlantic Deep Water under glacial conditions, indicating that southern-sourced wat

48 h implications on ocean productivity at peak glacial conditions.

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

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

51 e show a dramatic bottleneck during the last glacial cycle in all but one kiwi lineage, as expected i

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

53 c carbon in deep-sea sediments over the last glacial cycle.

54 respired carbon storage throughout the last glacial cycle.

55 ich explains the beginning of the past eight glacial cycles and might anticipate future periods of gl

56 our understanding of the mechanisms driving glacial cycles and our ability to predict the next glaci

57 echanism of, the shift to quasi-100,000-year glacial cycles at the mid-Pleistocene transition.

58 vide direct evidence of orbitally controlled glacial cycles between 34 million and 31 million years a

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

60 actors, in North America during the past two glacial cycles is limited in part by the scarcity of lon

61 heets were typically largest during repeated glacial cycles of the mid-Oligocene ( approximately 28.0

62 time, and continuous reconstructions across glacial cycles remain elusive.

63 hat global cooling during recent Pleistocene glacial cycles resulted in a burst of species diversific

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

65 cal and temperate zones both show impacts of glacial cycles, the former primarily through changing se

66 rs (-900 to 6600 yr range) over the last two glacial cycles.

67 centrations have been closely coupled across glacial cycles.

68 repeated carbon storage over the last three glacial cycles.

69 The water mass structure of the glacial deep Atlantic Ocean and the mechanism by which i

70 During the last glacial/deglacial period, megadrought episodes were obse

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

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

73 he peninsula to be increasingly regulated by glacial discharge, altering food-web interactions.

74 southern and D. richardsoni a more northern glacial distribution than previously thought.

75 aternal lineages, was at the end of the Late Glacial, due to major expansions from one or more refugi

76 were likely the major influences on European glacial dust activity and propose that European dust emi

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

78 Here we show that in the late glacial-early Holocene transition period, when the clima

79 in Arabia; (4) there was likely a minor Late Glacial/early postglacial dispersal from Arabia through

80 history of Mars, including the existence of glacial environments near the locations of the pre-TPW p

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

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

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

84 Our results show evidence of recent and post-glacial expansion.

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

86 esulting from sublimation, condensation, and glacial flow acting over seasonal and geological time sc

87 Surrounding terrains show active glacial flow, apparent transport and rotation of large b

88 t (NAC) at the termination of the third last glacial, for which palaeocurrent information was previou

89 These glacial forefield soils had significantly higher xyloglu

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

91 ere the dominant sources throughout the post-glacial history of the GRK.

92 cal and regional scales; current climate and glacial history play important roles.

93 These small areas of glacial ice are known as meteorite stranding zones, wher

94 the changing climate at the end of the last glacial in Northern Europe.

95 gigatonnes of carbon will postpone the next glacial inception by at least 100,000 years.

96 ined by palaeoclimatic data, we suggest that glacial inception was narrowly missed before the beginni

97 l cycles and our ability to predict the next glacial inception.

98 ycles and might anticipate future periods of glacial inception.

99 mainly reflects conditions of the preceding glacial instead of contemporary interglacial climate.

100 heric cooling which occurred within the Last Glacial Interglacial Transition (LGIT).

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

102 million years, with increased variability as glacial-interglacial change intensified worldwide.

103 as, surrounded by shallow oceans, Quaternary glacial-interglacial changes in climate and sea level ha

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

105 Melt production is apparently modulated by glacial-interglacial changes in sea level, raising the p

106 om cores throughout the Atlantic that reveal glacial-interglacial changes in water mass distributions

107 e climate system and is closely coupled with glacial-interglacial climate oscillations of the Quatern

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

109 om a Greenland ice core over the most recent glacial-interglacial cycle and for two Dansgaard-Oeschge

110 r paleoenvironmental selection over the last glacial-interglacial cycle.

111 The driving force behind Quaternary glacial-interglacial cycles and much associated climate

112 Fluctuations during glacial-interglacial cycles appear superimposed on a lon

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

114 ccounts for the dominance of obliquity-paced glacial-interglacial cycles early in the Quaternary and

115 However, the high-amplitude glacial-interglacial cycles of the mid-Oligocene are hig

116 he mechanisms that control CO2 change during glacial-interglacial cycles remains elusive.

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

118 emoved and extrapolated back to the last two glacial-interglacial cycles, we observe a linear relatio

119 dioxide (CO2) concentration variability over glacial-interglacial cycles.

120 diatom productivity observed during the last glacial-interglacial period.

121 stigate PF-C destabilization during the last glacial-interglacial period.

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

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

124 mmunities tolerate "baseline" variability on glacial-interglacial timescales but are sensitive to lar

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

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

127 cological study challenges this concept over glacial-interglacial timescales.

128 y archive from the lake over the penultimate glacial-interglacial transition (MIS 6-5) and the follow

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

130 Explanations of the glacial-interglacial variations in atmospheric pCO2 invo

131 his case, the dominant control appears to be glacial-interglacial variations in sedimentation rates.

132 1.5 million years (Ma) of orbitally-paced glacial/interglacial cycles (GIC).

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

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

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

136 Superimposed on the glacial/interglacial variations is a marked difference i

137 ronounced during marine isotope stage 3, the glacial interval 25 thousand to 60 thousand years ago.

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

139 50 to 35 ka, are surprisingly high for this glacial interval, and remain unexplained by previous mod

140 o constrain areal extent of ice cover during glacial intervals with sparse geological observables.

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

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

143 induced by recent anthropogenic activity and glacial isostatic adjustment are contributing factors fo

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

145 (OSL) dates to define three stages of rapid glacial lake drainage in the Lago General Carrera/Lago B

146 osed freshwater surface "hosing" to simulate glacial lake drainage suggest that a negative salinity a

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

148 charges expected for floods originating from glacial lake outbursts.

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

150 of the glacier ice, and chemical fate in the glacial lake.

151 d-latitudes of the Southern Hemisphere major glacial lakes also formed and drained during deglaciatio

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

153 New and previously mapped glacial landforms together reveal flow of a spatially co

154 However, as a glacial lengthens, the energy needed for deglaciation de

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

156 tudy of the internal structure of mega-scale glacial lineations (MSGLs) formed at the bed of a palaeo

157 l lakes and channels are preserved on top of glacial lineations, indicating long-term re-organization

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

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

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

161 We suggest that glacial maxima and lowering of sea level caused anomalou

162 eep sea was consistently higher (50%) during glacial maxima than during interglacials.

163 During glacial maxima throughout that period, species in Europe

164 two older interglacials and their preceding glacial maxima.

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

166 in the region was about 58% during the Last Glacial Maximum (around 21,000 years ago) and 142% durin

167 oncentration of 375 p.p.b.v. during the last glacial maximum (LGM) 21,000 years ago, to 680 p.p.b.v.

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

169 ral East Antarctica (Dome C) during the last glacial maximum (LGM) and the Holocene.

170 western Atlantic hydrography during the Last Glacial Maximum (LGM) calls for transport and intermixin

171 flecting modern, future (year 2100) and last glacial maximum (LGM) conditions.

172 cluding climatic fluctuations since the last glacial maximum (LGM) have also contribute to population

173 st Antarctic ice sheet (WAIS) since the last glacial maximum (LGM) is important for addressing questi

174 ntarctica was covered by ice during the Last Glacial Maximum (LGM) it has been speculated that endemi

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

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

177 acial (LIG) and the present than in the last glacial maximum (LGM), probably due to topography.

178 Following the last glacial maximum (LGM), the demise of continental ice she

179 nt under the climatic conditions of the Last Glacial Maximum (LGM), the exact nature of the glacial c

180 Cryptotis mexicanus) at present and the Last Glacial Maximum (LGM).

181 climate record, particularly during the Last Glacial Maximum (LGM).

182 retreat and habitat extension after the Last Glacial Maximum (LGM).

183 A lineage M in individuals prior to the Last Glacial Maximum (LGM).

184 10 mya), the Pliocene (~3 mya), and the Last Glacial Maximum (LGM, 0.021 mya).

185 th these replacement events, around the Last Glacial Maximum (LGM, approximately 21-18 kya).

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

187 about 7,300 to 9,800 (at the end of the last glacial maximum about 15,000 YBP), then more quickly to

188 Atlantic overturning circulation at the Last Glacial Maximum and its impact on respired carbon storag

189 comparing them with velocities from the Last Glacial Maximum and the present, we show that the stage

190 e not as spatially extensive during the Last Glacial Maximum as previously believed.

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

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

193 Climatic conditions at the Last Glacial Maximum did not explain additional variation in

194 that links population expansions to the Last Glacial Maximum fit for 14 of the 24 demographic expansi

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

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

197 . tenuis might follow the post-LGM (the Last Glacial Maximum) expansion pattern for temperate species

198 e and pace of climate shifts, since the Last Glacial Maximum, are often used to determine whether pat

199 During the Last Glacial Maximum, continental ice sheets isolated Beringi

200 tmospheric CO2 concentration before the Last Glacial Maximum, have remained unclear.

201 d growth in the 15 kyr leading into the Last Glacial Maximum, thus highlighting the potential of mid-

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

203 which it presumably replaced after the last glacial maximum.

204 -gatherers both pre- and postdating the Last Glacial Maximum.

205 been shown to have occurred during the Last Glacial Maximum.

206 dominantly southern-sourced cell at the Last Glacial Maximum.

207 ored in the abyssal Atlantic during the Last Glacial Maximum.

208 igh abyssal salinities inferred for the last glacial maximum.

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

210 elt, and varying contributions of input from glacial melt and streamwater, created pulses in pesticid

211 ios, the concentration pulse was altered and glacial melt made a greater contribution (as mass flux)

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

213 sion or from the transport of sediment-laden glacial melt waters to the polynya.

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

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

216 gical and fossil data and features prominent glacial migration waves across the Arabian Peninsula and

217 se refugia and the timing and routes of post-glacial migrations that ultimately established modern pa

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

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

220 We mapped six distinct glacial moraines alongside Stocking Glacier in the McMur

221 2 weeks) or placebo or 300 mg of omalizumab (GLACIAL: n = 335, 24 weeks).

222 t two glacial periods, indicating persistent glacial O2 depletion at the heart of the carbon engine o

223 This hypothesis is consistent with a glacial ocean that hosted globally lower rates of fixed

224 r carbonate chemistry between the modern and glacial ocean.

225 nd (14)C-depleted deep waters with a maximum glacial offset to atmospheric (14)C (DeltaDelta(14)C=-1,

226 re we show that Antarctic krill sampled near glacial outlets at the island of South Georgia (Southern

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

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

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

230 with iron during the last ice age--the Last Glacial Period (LGP)--but the effect of increased ice-ag

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

232 ennial-scale climate changes during the last glacial period and deglaciation were accompanied by rapi

233 asing proportion of softer ice from the last glacial period and the deglacial collapse of the ice bri

234 from the southern Indian Ocean over the last glacial period do not suggest a dominant role of Souther

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

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

237 an increase in (234)U/(238)U since the last glacial period, but the timing and amplitude of its vari

238 nd ice core records for the most of the last glacial period, except during the last deglaciation.

239 antic was therefore enhanced during the last glacial period, primarily due to an increase in the resi

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

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

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

243 al North Africa rainfall record for the last glacial period.

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

245 sity hotspot of eastern South America during glacial periods has been ignored in the literature.

246 , forest retraction and fragmentation during glacial periods would have promoted reproductive isolati

247 Colder glacial periods, and possibly associated reductions in a

248 increase in diversification rates during key glacial periods, comparable with levels observed in clas

249 ll below 70 mumol kg(-1) during the last two glacial periods, indicating persistent glacial O2 deplet

250 if any, in this biodiversity hotspot during glacial periods.

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

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

253 ector of the WAIS contributed little to late-glacial pulses in sea-level rise but was involved in mid

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

255 influenced by global climate change in a key glacial refuge, Lake Ohrid (Albania, Macedonia).

256 d effects of permafrost persistence, distant glacial refugia and fire.

257 en interpreted as supporting expansions from glacial refugia.

258 ighting the role of at least one Pleistocene glacial refugium, perhaps on the Red Sea plains; (3) the

259 a UAS7 = 0 was 12 or 13 weeks (ASTERIA I and GLACIAL, respectively).

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

261 lted in an expanded polar EAIS and a limited glacial response to Pliocene warmth in the Aurora subgla

262 lex in novel periglacial habitats created by glacial retreat in the Jakobshavn Isbrae area of western

263 Benthic biofilms are vulnerable to glacial retreat induced by climate change.

264 escribe the ecological implications of rapid glacial retreat under climate change and resolve the rel

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

266 icles deriving from aeolian dust deposition, glacial runoff, or river discharges can form an importan

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

268 on biogeographic model, with a poleward post-glacial shift revealed in current genetic structure.

269 tilization of the Southern Ocean during peak glacial stages.

270 Glacial-state greenhouse gas concentrations and Southern

271 CB release and the PCB concentrations in the glacial stream are estimated to be small but persistent

272 n an ice core, a lake sediment core, and the glacial streamwater.

273 Distinct microbial habitats on glacial surfaces are dominated by snow and ice algae, wh

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

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

276 arctic ice sheets to warming during the Last Glacial Termination (LGT; 18,000-11,650 yrs ago) allows

277 ographic variability through the penultimate glacial termination (TII) and last interglacial, by appl

278 independent, radioisotopic age constraint on glacial termination VI and on the duration of MIS 13 sea

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

280 rolonged ice buildup and delayed, but rapid, glacial terminations.

281 ed hydrothermal activity during the last two glacial terminations.

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

283 the storage of CO2 in the deep ocean during glacial times.

284 critical role in carbon sequestration during glacial times.

285 CO2 decline, drove the Earth system toward a glacial tipping point in the Cenozoic.

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

287 roximately 430 ka during the transition from glacial to interglacial conditions.

288 The most recent glacial to interglacial transition constitutes a remarka

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

290 ape changes contributed to a non-linear post-glacial trajectory of novelty with jumps corresponding t

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

292 o effects from the preceding interglacial on glacial vegetation are detected.

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

294 rce for the atmospheric CO2 rise during post-glacial warming.

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

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

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

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

299 dominant chemical reactions associated with glacial weathering, and explore the implications for lon

300 owing in southern California during the last glacial, when the ambient atmospheric [CO2] (ca) was 18