ライフサイエンスコーパス: glaciation

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

2 ago, after the onset of Northern Hemispheric glaciation.

3 , through the Late Ordovician-Early Silurian glaciation.

4 ne family evolution driven by Southern Ocean glaciation.

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

6 ssumptions regarding the initiation of cloud glaciation.

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

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

9 a geologically recent period of midlatitude glaciation.

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

11 ominent withdrawal in response to Hirnantian glaciation.

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

13 y permanent mid-latitude Northern Hemisphere glaciation.

14 a massive methane release after the Marinoan glaciation.

15 lier, after the onset of Northern hemisphere glaciation.

16 once initiated, promotes cooling and further glaciation.

17 asynchronous warming at the end of the last glaciation.

18 the Paleoproterozoic low-latitude Makganyene glaciation.

19 certain boreal tree species during the last glaciation.

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

21 insolation are generally thought to control glaciation.

22 us global cooling and/or Northern Hemisphere glaciation.

23 ntilation and the global carbon cycle during glaciation.

24 s after the onset of the Northern Hemisphere glaciation.

25 infer an apparent lack of extensive mountain glaciation.

26 n the evolution of this major prePleistocene glaciation.

27 ntrol of mean annual temperature on tropical glaciation.

28 flat bed, formed before permanent Antarctic glaciation.

29 ic CO2 at the termination of the penultimate glaciation.

30 l sediment records during and since the last glaciation.

31 d climatic cooling associated with Antarctic glaciation.

32 ributions were correlated with the extent of glaciation.

33 n became habitable following the most recent glaciation.

34 ively) and the extent of Northern Hemisphere glaciation.

35 ght have accelerated the Northern Hemisphere Glaciation.

36 fluctuations that took place during the last glaciation.

37 vironment in western Eurasia during the last glaciation.

38 h global cooling and initiation of Antarctic glaciation.

39 e gas hydrate stability zone during the last glaciation.

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

41 wing the Pennsylvanian Gondwanan continental glaciation.

42 h ice and can survive extensive and repeated glaciation.

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

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

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

46 eres of the Permo-Carboniferous and Cenozoic glaciations.

47 ts are an inevitable consequence of periodic glaciations.

48 n of carbon sequestration during Pleistocene glaciations.

49 n the global carbon cycle and periodicity of glaciations.

50 nd in both initiating and terminating global glaciations.

51 unctuated by two low-latitude Snowball Earth glaciations.

52 isted in the Arctic Ocean during Pleistocene glaciations.

53 ver where arctic plants survived Pleistocene glaciations.

54 35 Ma) is marked by extensive Snowball Earth glaciations.

55 e, comparable in magnitude to the Quaternary glaciations.

56 buting to climate cooling and an interval of glaciations.

57 by vicariant events, especially Pleistocene glaciations.

58 nism for the series of Neoproterozoic global glaciations.

59 the question of how diverse life can survive glaciations.

60 ate cooling before the Neoproterozoic global glaciations.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

80 Alpine glaciation and river incision control the topography of

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

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

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

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

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

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

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

88 The snowball Earth glaciations and Neoproterozoic oxidation are both sugges

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

138 increasing drought and aridity and transient glaciation events.

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

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

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

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

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

144 Pleistocene glaciations have played a major role in species divergen

145 Pleistocene glaciations have profoundly affected patterns of genetic

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

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

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

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

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

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

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

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

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

155 Glaciation in the humid tropical Andes is a sensitive in

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

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

158 0-year reconstruction of climate history and glaciation in the Venezuelan Andes using lake sediments.

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

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

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

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

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

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

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

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

167 Antarctic glaciation is attributed to a threshold response to slow

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

192 The glaciation of Antarctica has hitherto been thought to re

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

210 Pleistocene glaciations played an additional geomorphological role,

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

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

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

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

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

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

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

218 geographers have debated whether Pleistocene glaciations shaped evolutionary patterns.

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

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

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

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

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

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

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

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

227 centration, apparently inconsistent with the glaciations that followed.

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

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

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

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

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

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

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

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

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

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

238 As glaciation waned, debris-covered glaciers ceased flowing

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

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

241 The glaciation was initiated, after climatic preconditioning

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

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

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

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

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

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

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

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

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

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

252 Although global glaciation would have drastically curtailed biological p

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

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