ライフサイエンスコーパス: glaciation

1 3-2.2 Ga Makganyene "snowball Earth" (global glaciation).

2 f the Wrangel mammoth at the end of the last glaciation.

3 wing the Pennsylvanian Gondwanan continental glaciation.

4 h ice and can survive extensive and repeated glaciation.

5 urface at this time, as well as tendency for glaciation.

6 acial sediments is, thus far, unique to this glaciation.

7 ago, after the onset of Northern Hemispheric glaciation.

8 nd synchronous event postdating the Gaskiers glaciation.

9 , through the Late Ordovician-Early Silurian glaciation.

10 ne family evolution driven by Southern Ocean glaciation.

11 fossil record, and the onset of the Sturtian glaciation.

12 rature would drop to ~291 K, consistent with glaciation.

13 ssumptions regarding the initiation of cloud glaciation.

14 during the last 10,000 years since the last glaciation.

15 s pre-dating the termination of the Marinoan glaciation.

16 a geologically recent period of midlatitude glaciation.

17 ty that Oi-1 represents a precursory bipolar glaciation.

18 ominent withdrawal in response to Hirnantian glaciation.

19 cal past of Mars, after the period of active glaciation.

20 e sheet and the onset of Northern Hemisphere glaciation.

21 y permanent mid-latitude Northern Hemisphere glaciation.

22 a massive methane release after the Marinoan glaciation.

23 lier, after the onset of Northern hemisphere glaciation.

24 once initiated, promotes cooling and further glaciation.

25 asynchronous warming at the end of the last glaciation.

26 the Paleoproterozoic low-latitude Makganyene glaciation.

27 certain boreal tree species during the last glaciation.

28 urentide Ice Sheet after the end of the last glaciation.

29 insolation are generally thought to control glaciation.

30 ent Miocene Climate Transition and Antarctic glaciation.

31 us global cooling and/or Northern Hemisphere glaciation.

32 ntilation and the global carbon cycle during glaciation.

33 s after the onset of the Northern Hemisphere glaciation.

34 tions into globally disparate refugia during glaciation.

35 infer an apparent lack of extensive mountain glaciation.

36 n the evolution of this major prePleistocene glaciation.

37 ntrol of mean annual temperature on tropical glaciation.

38 flat bed, formed before permanent Antarctic glaciation.

39 ic CO2 at the termination of the penultimate glaciation.

40 l sediment records during and since the last glaciation.

41 d climatic cooling associated with Antarctic glaciation.

42 ributions were correlated with the extent of glaciation.

43 n became habitable following the most recent glaciation.

44 ively) and the extent of Northern Hemisphere glaciation.

45 d from southerly (temperate) areas following glaciation.

46 illion years ago with the onset of Greenland glaciation.

47 O(2) decline and continental-scale Antarctic glaciation.

48 e the climate, triggering a transient global glaciation.

49 ght have accelerated the Northern Hemisphere Glaciation.

50 ne in marine productivity following the last glaciation.

51 fluctuations that took place during the last glaciation.

52 vironment in western Eurasia during the last glaciation.

53 h global cooling and initiation of Antarctic glaciation.

54 e gas hydrate stability zone during the last glaciation.

55 billion years ago, following several global glaciations.

56 by vicariant events, especially Pleistocene glaciations.

57 10-50% of today's rates, during the Snowball glaciations.

58 nism for the series of Neoproterozoic global glaciations.

59 bdivisions were shaped during the Quaternary glaciations.

60 the question of how diverse life can survive glaciations.

61 ate cooling before the Neoproterozoic global glaciations.

62 s specific adaptations to cold during recent glaciations.

63 of widespread, low-latitude 'snowball Earth' glaciations.

64 eres of the Permo-Carboniferous and Cenozoic glaciations.

65 ts are an inevitable consequence of periodic glaciations.

66 n the global carbon cycle and periodicity of glaciations.

67 isted in the Arctic Ocean during Pleistocene glaciations.

68 ver where arctic plants survived Pleistocene glaciations.

69 n of carbon sequestration during Pleistocene glaciations.

70 nd in both initiating and terminating global glaciations.

71 unctuated by two low-latitude Snowball Earth glaciations.

72 35 Ma) is marked by extensive Snowball Earth glaciations.

73 e, comparable in magnitude to the Quaternary glaciations.

74 buting to climate cooling and an interval of glaciations.

75 nd after the Neoproterozoic 'snowball' Earth glaciations (0.75 to 0.63 billion years ago).

76 after the Palaeoproterozoic Huronian global glaciations (2.45 to 2.2 billion years ago), leading to

77 which also caused some diachronous regional glaciations; (2) a permanent climate cooling period betw

78 ater in the Bering Sea beginning with the M2 glaciation (3.3 Myr ago).

79 treme climatic fluctuations and global-scale glaciation [3], and the emergence of metazoan life in th

80 nvironmental changes that promoted Antarctic glaciation ~33.7 million years ago.

81 were already diversified before the Sturtian glaciation (720 mya), supporting the hypothesis that mas

82 diments of South China prior to the Sturtian glaciation (820~720 Ma).

83 vironmental changes associated with the last glaciation (90,000 to 10,000 years before the present; 9

84 d may have been the precursor to Pleistocene glaciation about 2.75 Myr ago.

85 The cause of Northern Hemisphere glaciation about 3 million years ago remains uncertain.

86 ermination of the late Cryogenian (Marinoan) glaciation about 635 million years ago.

87 of Pliocene-Pleistocene Northern Hemisphere glaciation (about two to three million years ago), on gl

88 rds, especially during the onset of the last glaciation, about 120 kyr ago.

89 ind that Oi-1 is best explained by Antarctic glaciation alone, combined with deep-sea cooling of up t

90 It has been proposed that during Pleistocene glaciations, an ice cap of 1 kilometre or greater thickn

91 rs in the Arctic Ocean since the most recent glaciation and a persistent contribution of Arctic water

92 s a strong correlation between the extent of glaciation and arc-continent collisions in the tropics.

93 herto unrecognized negative feedback between glaciation and atmospheric CO2 predominantly controlled

94 rds termination of the global-scale Marinoan glaciation and is coeval with similar dated rocks from N

95 he geological records of Northern Hemisphere glaciation and model results that indicate that the thre

96 rk sheds new light on the mechanisms linking glaciation and ocean acidity change across arguably the

97 go coeval with the onset of major Patagonian glaciation and retreat of deformation from the easternmo

98 Alpine glaciation and river incision control the topography of

99 t CO(2) declined before and during Antarctic glaciation and support a substantial CO(2) decrease as t

100 on postulated for this phase of low-latitude glaciation and that trophic complexity survived through

101 mpact of the proposed driving mechanisms for glaciation and the influence of orbital variations on th

102 show that the first Paleoproterozoic global glaciation and the onset of the GOE occurred between ca.

103 ibuted to past vicariance during Pleistocene glaciations and a secondary contact associated to demogr

104 Paleoproterozoic in association with global glaciations and continued until the end of the Lomagundi

105 of falling and rising sea levels during the glaciations and interglaciations of the last one million

106 The snowball Earth glaciations and Neoproterozoic oxidation are both sugges

107 and where in the ocean CO2 was stored during glaciations and released during (de)glacial millennial-s

108 terpretation of the origin of the Quaternary glaciations and the impact of the monsoon.

109 suitable climatic conditions during the last glaciation, and contrasting historical movements along t

110 e and associated mass gain of the AIS during glaciation, and grounding-line retreat and mass loss dur

111 arge carbon-isotopic excursions, continental glaciation, and stratigraphically anomalous carbonate pr

112 ecies from refugia subsequent to Pleistocene glaciation, and such studies have been instructive in un

113 rn refugia as its host plant during the last glaciation, and that little long-distance dispersal has

114 gly oxygenated after the end of the Marinoan glaciation, and they allow us to identify three distinct

115 The precise timing and rate of glaciation, and thus its impacts on ocean circulation, r

116 rbital-scale climate variability during past glaciations, and are likely to be important in future cl

117 tigating termination of the Paleoproterozoic glaciations, and highlight the possible role of impact c

118 Further, we argue that periodic glaciations, and particularly the Neoproterozoic low-lat

119 the onset of significant Northern Hemisphere glaciation approximately 2.75 million years ago, but the

120 t the intensification of Northern Hemisphere glaciation approximately 3 million years ago did not int

121 rn Brazil during low-latitude Neoproterozoic glaciation approximately 740 to 700 million years ago.

122 ly and maximum phase of southern midlatitude glaciation ( approximately 30-20 ka), to verify the comp

123 ogical record before the end of the Marinoan glaciation ( approximately 635 Myr ago).

124 CO(2) levels during the Permo-Carboniferous glaciation are in agreement with glaciological evidence

125 Ice nucleation and the resulting cloud glaciation are significant atmospheric processes that af

126 rred to be highly erosive, and conditions of glaciation are used to explain both the marked relief ty

127 While the effects of glaciations are relatively well understood, the spatial

128 The Earth's most severe glaciations are thought to have occurred about 600 milli

129 y that the Earth suffered episodes of global glaciation as recently as the Neoproterozoic period, bet

130 uch as Middle to Late Ordovician cooling and glaciation associated with the closure of the Iapetus Oc

131 panded to a ubiquitous global presence after glaciation-associated allopolyploidization.

132 ing step at 2.73 Myr ago and the first major glaciation at 2.15 Myr ago.

133 ng oxygen does not appear during the Pongola glaciation at 2.9 Ga or during the Huronian glaciations,

134 rs formed in a previous climate conducive to glaciation at middle latitudes.

135 a, which may be too high, given evidence for glaciation at roughly this time.

136 ce-nucleating particles (INPs) enables cloud glaciation at temperatures above the homogeneous freezin

137 Thus, we show that the Antarctic glaciation at the Eocene-Oligocene boundary was preceded

138 Moreover, a major transient glaciation at the epoch boundary ( approximately 23 Ma),

139 Mountain glaciation began in the latest Eocene (approximately 37-

140 tly, it was thought that Northern Hemisphere glaciation began much later, between 11 and 5 million ye

141 d as the most likely root cause of Antarctic glaciation, but the mechanism linking glaciation to the

142 the global ice sheet system during the last glaciation, but the timing of its growth to or retreat f

143 ance after the Neoproterozoic Snowball Earth glaciations, but the causes for this consequential evolu

144 were globally deposited directly after these glaciations, but they are usually organic barren or ther

145 h rates of organic carbon burial facilitated glaciation by reducing atmospheric greenhouse capacity.

146 g the culmination of the Northern Hemisphere glaciation, ca. 2.6 million years ago.

147 If glaciation caused all the rapid sea level changes in the

148 sitivity of regional climates to continental glaciation, changing greenhouse gas levels, and insolati

149 Connections between glaciation, chemical weathering, and the global carbon c

150 .4 Ga that operated under the Snowball Earth glaciation conditions.

151 rease as the primary agent forcing Antarctic glaciation, consistent with model-derived CO(2) threshol

152 of 3.5 per mil during each of the past five glaciation cycles, indicators of iceberg discharge and s

153 spheric composition may explain the observed glaciations, demonstrating the importance of high-qualit

154 as a negative feedback, limiting progress of glaciation, dependent on lithology and the concentration

155 years ago), and that the onset of extensive glaciations did not occur until about 3 million years ag

156 ically defined by abrupt cooling and renewed glaciation during the last glacial-interglacial transiti

157 explain this increase in Northern Hemisphere glaciation during the Late Pliocene.

158 s after the Cryogenian helped prevent severe glaciation during the Phanerozoic.

159 a strong population bottleneck likely due to glaciation during the Pleistocene.

160 pproximately 37-34 Ma), contemporaneous with glaciation elsewhere on the continent and a reduction in

161 iving mechanisms that set the stage for this glaciation event are not well constrained, however, owin

162 cooling event at ~34.1-33.9 Ma and the Oi-1 glaciation event at ~33.8-33.6 Ma.

163 mitant increased seasonality before the Oi-1 glaciation event.

164 excursions in marine limestones suggest that glaciation events may have punctuated this episode of ex

165 ld terrestrial species have survived extreme glaciation events on the continent?

166 increasing drought and aridity and transient glaciation events.

167 injection, likely before the 717-Ma Sturtian glaciation for the climate appropriate for regolith form

168 roughly synchronous with a period of global glaciation from approximately 6.2-5.5 Ma and with the Me

169 or both the onset and demise of a Cryogenian glaciation from the same continental margin and suggests

170 rthern Hemisphere experienced only ephemeral glaciations from the Late Eocene to the Early Pliocene e

171 nt debate on records of southern midlatitude glaciation has focused on reconstructing glacier dynamic

172 low latitude, and the onset of the Sturtian glaciation has suggested a tectonic forcing.

173 Pleistocene glaciations have played a major role in species divergen

174 Pleistocene glaciations have profoundly affected patterns of genetic

175 Immediately after the Marinoan glaciation, higher delta(82/76)Se values superpose the g

176 getated land surface without major Antarctic glaciation, highlighting the important cooling effect ex

177 However, the early glaciation history of the Northern Hemisphere is a subje

178 ian mass extinction was related to Gondwanan glaciation; however, it is still unclear whether elevate

179 with high rates of disturbance (i.e., fires, glaciation, hurricanes, and deforestation).

180 cycles') have driven cyclical alternation of glaciations (ice ages) and warmer interglacials.

181 nearly a billion years with no evidence for glaciation, ice advanced to equatorial latitudes at leas

182 y have been one contributor to the prolonged glaciations if these were near-global.

183 , Fe, and P fluxes expected during a partial glaciation in an anoxic world with high-Fe oceans indica

184 lict subglacial lakes formed during the last glaciation in Canada.

185 m changes in migration timing are related to glaciation in headwater streams.

186 ablished before the Pleistocene and survived glaciation in small separated refugia.

187 pecies appeared to have survived Pleistocene glaciation in the eastern Palearctic, much of the Palear

188 Glaciation in the humid tropical Andes is a sensitive in

189 isms responsible for the initiation of major glaciation in the Northern Hemisphere at about 2.75 mill

190 sation depth in the world's oceans, and that glaciation in the Northern Hemisphere began much later,

191 0-year reconstruction of climate history and glaciation in the Venezuelan Andes using lake sediments.

192 productivity throughout one of the harshest glaciations in Earth history.

193 em to support a link between the most severe glaciations in Earth's history, the oxygenation of the E

194 multiple climate cooling before the Sturtian glaciations in South China: (1) a series of episodic and

195 group of South Africa suggest that all three glaciations in the Huronian Supergroup of Canada predate

196 lities suggested that CO(2) increased during glaciation, in contradiction to theory.

197 worldwide climatic changes ensuing the last glaciation, increased anthropophilia of the mosquito vec

198 Tunnel valleys associated with half of these glaciations indicate that a surface-meltwater-rich sub-p

199 Additionally, daily glaciation-induced snowfall accumulations reached 15 mil

200 million years ago, when Northern Hemisphere glaciation intensified in association with global coolin

201 Antarctic glaciation is attributed to a threshold response to slow

202 We find that Greenland glaciation is mainly controlled by a decrease in atmosph

203 The ~635 Ma Marinoan glaciation is marked by dramatic Earth system perturbati

204 The intensification of Northern Hemisphere Glaciation is the most obvious result of the Plio-Pleist

205 of climatic conditions prior to the Sturtian glaciations is critical to understanding the trigger mec

206 Although the severity of the historical glaciations is debated, theoretical "hard Snowball" cond

207 an half covered by grounded ice sheet during glaciations, is biologically rich and a key area of both

208 in the expansion of arid zones, rather than glaciation, it could be expected that arid-adapted speci

209 particularly the Neoproterozoic low-latitude glaciation, known as 'snowball Earth', could have been p

210 ic marine biomes persisted through cycles of glaciation, leading to unique assemblages in polar water

211 he Quaternary icehouse climate and extensive glaciations, limnic biodiversity sustained a severe decl

212 c mammal species, complicated by episodes of glaciation, local extinctions, and intercontinental migr

213 During the last glaciation, lower atmospheric CO(2) levels were accompan

214 at enhanced sulfide oxidation as a result of glaciation may act as a source of CO2 to the atmosphere.

215 st carbon (PF-C) accumulated during the last glaciation may have been an important source for the atm

216 ozoic 2.45 to 2.2 billion years ago, several glaciations may have produced Snowball Earths.

217 We show that, after the last glaciation, melting of residual snow and ice in alcoves

218 llion years was the rapid onset of Antarctic glaciation near the Eocene/Oligocene epoch boundary (app

219 than today, to extensive Northern Hemisphere glaciation (NHG) ~2.73 million years ago (Ma).

220 Had such a transient global glaciation occurred in the distant past when solar lumin

221 e development of continental-scale Antarctic glaciation occurred in the late middle Eocene to early O

222 The first major build-up of Antarctic glaciation occurred in two consecutive stages across the

223 At least two global "Snowball Earth" glaciations occurred during the Neoproterozoic Era.

224 Global glaciation occurs at CO2 concentrations <40 ppm, suggest

225 We show that the CO(2) threshold below which glaciation occurs in the Northern Hemisphere ( approxima

226 requently linked to changing paleogeography, glaciation, ocean oxygenation, and biological innovation

227 h the initiation of stepwise global cooling, glaciation of Antarctica and aridification on the northe

228 The sudden, widespread glaciation of Antarctica and the associated shift toward

229 level drop caused by the onset of permanent glaciation of Antarctica at ca. 13.8 Ma.

230 g trend that culminated in continental-scale glaciation of Antarctica from 34 Ma onward.

231 The glaciation of Antarctica has hitherto been thought to re

232 istory calls for the first continental-scale glaciation of Antarctica in the earliest Oligocene epoch

233 We posit that increased glaciation of Antarctica, deduced from the 21 +/- 10-met

234 We conclude that the last glaciation of South Georgia was extensive, and the sensi

235 rs (Myr) ago] by the longest and most severe glaciation of the entire Phanerozoic Eon.

236 rait region the most extreme Greenland shelf glaciation of the last glacial cycle occurred during MIS

237 te state, steering clear of both large-scale glaciation of the Northern Hemisphere and its complete d

238 The glaciations of the Neoproterozoic Era (1,000 to 542 MyBP

239 tiation of the extensive Northern Hemisphere glaciations of the Quaternary Ice Age.

240 ine sediment cores, we resolve the record of glaciation offshore of South Georgia through the transit

241 e behind extinctions in the marine realm and glaciation on Antarctica.

242 Assessing the impact of glaciation on Earth's surface requires understanding gla

243 al erosion rates and, in part, the impact of glaciation on mountainous landscapes during the past few

244 ease in solar output could result in runaway glaciation on the Earth.

245 subsurface ocean helped to prevent snowball glaciation on the Phanerozoic Earth.

246 ection likely limited the extent of the MIS2 glaciation on the SW Greenland shelf.

247 The history of glaciations on Southern Hemisphere sub-polar islands is

248 or atmospheric oxygen following the Marinoan glaciation, or for a direct link between early animal ev

249 t that abrupt climate change during the last glaciation originated through changes in the Atlantic th

250 ast 1.1 million years, perhaps due to global glaciation oscillations during the Pleistocene.

251 d environmental change, including 'snowball' glaciations, oxygenation and the appearance of animals.

252 Pleistocene glaciations played an additional geomorphological role,

253 The severe "Snowball Earth" glaciations proposed to have existed during the Cryogeni

254 pisodes of water-related activity, including glaciation, punctuated the geological history of Mars.

255 hase feedback arising from a decreased cloud glaciation rate in a warmer climate.

256 re model, we show that the rise of Antarctic glaciation, rather than altered palaeogeography, is best

257 Onset of Antarctic glaciation reflects a critical tipping point for Earth's

258 ern of topographic adjustment to Pleistocene glaciations remain poorly known.

259 ugal from North Africa after the Pleistocene glaciation, respond to selection on a key life-history t

260 h the isotopic signal, as well as the global glaciation, result from enhanced export of organic matte

261 geographers have debated whether Pleistocene glaciations shaped evolutionary patterns.

262 rienced several intervals of intense, global glaciation ("snowball Earth" conditions) during Precambr

263 orts the hypothesis that, during Pleistocene glaciations, some plant refugia were located in the Arct

264 d outside the limits of the last (Wisconsin) glaciation, suggesting that they may have acted as refug

265 ore potentially far more important for cloud glaciation than whole intact spores or hyphae.

266 find rapid transitions into and out of full glaciation that are consistent with the geological evide

267 ng models for the initiation of low-latitude glaciation that depend on the oxidative collapse of a st

268 ated by the inception of a long, progressive glaciation that is attributed to astronomically influenc

269 climate was terminated by a major period of glaciation that resulted in loss of open-ocean habitat s

270 centration, apparently inconsistent with the glaciations that followed.

271 The continent has experienced repeated glaciations that most models indicate blanketed the cont

272 This collapse can be explained by a global glaciation (that is, a snowball Earth), which ended abru

273 More than 10(4) years after the last major glaciation the topography of mountain ranges worldwide r

274 mediate aftermath of a Neoproterozoic global glaciation, the P(CO2) was at its highest level in the p

275 peninsulas in Europe during the Pleistocene glaciations; the importance of vicariance events such as

276 n be sustained for thousands of years during glaciations; the size of this phase lag is probably conn

277 emain above our model's northern-hemispheric glaciation threshold of approximately 280 p.p.m.v. until

278 onmental changes from the height of the last glaciation through to the present day.

279 The transition from temperate, alpine glaciation to a dynamic, polythermal ice sheet took plac

280 arctic glaciation, but the mechanism linking glaciation to the deepening of calcite compensation dept

281 As glaciation waned, debris-covered glaciers ceased flowing

282 indicate that the threshold for continental glaciation was crossed earlier in the Southern Hemispher

283 eolatitudes, which implies that the Sturtian glaciation was global in extent.

284 The glaciation was initiated, after climatic preconditioning

285 e records, indicate that Northern Hemisphere glaciation was not required to accommodate the magnitude

286 ion event in the wake of the severe Marinoan glaciation was the driving factor behind this early dive

287 Instead of bipolar glaciation, we find that Oi-1 is best explained by Antar

288 glaciation at 2.9 Ga or during the Huronian glaciations, we argue that oxygenic cyanobacteria evolve

289 ncentration of atmospheric O2 Future work on glaciation-weathering-carbon cycle feedbacks should cons

290 ~15,000 to 28,000 years ago during the last glaciation when alpine and coastal progenitors were like

291 ering of basalts also triggered the Sturtian glaciation, which accelerated erosion.

292 oxygen increase and Sturtian Snowball Earth glaciation, which accompanied emplacement of LIPs across

293 ls with one or more episodes of low-latitude glaciation, which are probable "Snowball Earth" events.

294 wn of the water table during the Wisconsinan glaciation, which lowered global sea level by nearly 130

295 n shales before and after all Neoproterozoic glaciations, which we interpret as incomplete reduction

296 an periods, an interval marked by two global glaciations with strong consequent changes in the amount

297 with an approximately 200,000-year period of glaciation, with ice sheets of about half the size of th

298 Although global glaciation would have drastically curtailed biological p

299 n Hemisphere immediately following Antarctic glaciation would have required rapid CO(2) drawdown with

300 During the Neoproterozoic, severe "snowball" glaciations would have had an extreme impact on the bios