ライフサイエンスコーパス: Cenozoic

1 ca over the past 66 million years (i.e., the Cenozoic).

2 a when it collided with Eurasia in the early Cenozoic.

3 s Australia became more arid during the late Cenozoic.

4 while major genera diversified near the mid Cenozoic.

5 g the Cretaceous and, at a smaller size, the Cenozoic.

6 North American terrestrial mammals over the Cenozoic.

7 attern of fauna replacement in SA during the Cenozoic.

8 e Northern or Southern Hemisphere during the Cenozoic.

9 ic era and survived to the beginnings of the Cenozoic.

10 inated the world's terrestrial biotas in the Cenozoic.

11 tern for oceanic diatom diversity across the Cenozoic.

12 faunal turnover of the first 15 m.y. of the Cenozoic.

13 o form diverse assemblages once again in the Cenozoic.

14 imately 0.15% every million years during the Cenozoic.

15 , during one of the warmest intervals of the Cenozoic.

16 l complexity and alpha diversity in the Meso-Cenozoic.

17 e size of marine pelagic diatoms through the Cenozoic.

18 ed marine planktonic diatom species over the Cenozoic.

19 ed temperatures in the latter portion of the Cenozoic.

20 gen content over short time intervals in the Cenozoic.

21 of these faunas remains stable in the latest Cenozoic.

22 itively over solitary species throughout the Cenozoic.

23 ic, their abundance declined markedly in the Cenozoic.

24 most dramatic global climatic cooling of the Cenozoic.

25 independent clades that radiated during the Cenozoic.

26 h decreasing paleotemperature throughout the Cenozoic.

27 he Cretaceous and achieving dominance in the Cenozoic.

28 s between South America and Australia in the Cenozoic.

29 resent in eastern Australia over much of the Cenozoic.

30 s driven by sustained aridification over the Cenozoic.

31 strial ecosystems in the Late Cretaceous and Cenozoic.

32 e organisms through most of the Mesozoic and Cenozoic.

33 n on classical oxygen isotope records of the Cenozoic.

34 was warmer and wetter than any period in the Cenozoic.

35 c, and remained comparatively high until the Cenozoic.

36 nstruct mantle structure at the start of the Cenozoic.

37 d global average temperature trends over the Cenozoic.

38 r five typical geological periods during the Cenozoic.

39 ust experienced strong shortening during the Cenozoic.

40 genian, Late Ordovician, late Paleozoic, and Cenozoic.

41 system toward a glacial tipping point in the Cenozoic.

42 hanging Southern Ocean conditions during the Cenozoic.

43 h at least the first 24 million years of the Cenozoic.

44 rtial pressure of atmospheric CO2 during the Cenozoic.

45 h periods of global warmth such as the Early Cenozoic.

46 ntly rose dramatically in the Cretaceous and Cenozoic (145 million years ago-present), indicating tha

47 y over water from South America in the early Cenozoic (47-29 million years ago, Mya), is more likely.

48 Using this proxy, we reconstruct LAI for the Cenozoic (49 million to 11 million years ago) of middle-

49 ikely due to the glacial pressure during the Cenozoic, a deep-sea group with fewer species emerged ex

50 It persists throughout the Cenozoic, accounting for the gradual overall increase in

51 rved lymexylid fossils in mid-Cretaceous and Cenozoic ambers from Myanmar (ca. 99 million years ago [

52 square meter, three times greater than mean Cenozoic and Early Cretaceous-Late Jurassic dipole momen

53 tages of atmospheric CO(2) variations in the Cenozoic and explore the possibility of a causal link be

54 odulation (AM) cycle during the Mesozoic and Cenozoic and indicate the usefulness of the ~173-ka cycl

55 ale pattern of plate tectonic motions during Cenozoic and late Mesozoic time, provided that subducted

56 tle convection constrained by the history of Cenozoic and Mesozoic plate motions explain some deep-ma

57 olution of seeds and cones at least over the Cenozoic and perhaps over much of the later Mesozoic.

58 ally weaker than it is today for most of the Cenozoic and the robust modern LDG of North American mam

59 lineages steadily accumulated throughout the Cenozoic and underwent a significant expansion of among-

60 as a major driver of global tectonics in the Cenozoic and, we argue, of atmospheric CO(2) concentrati

61 ethyan Ocean during the Cretaceous and early Cenozoic, and identifies an eastward movement of ancestr

62 t structures are well documented for recent, Cenozoic, and some Mesozoic foraminifera, the diagnostic

63 versity and complexity occurred in the early Cenozoic, and the overall rate of ecospace expansion has

64 ase in (87)Sr/(86)Sr in seawater through the Cenozoic apparently had no effect on central Pacific dee

65 e for a burst of fern diversification in the Cenozoic, apparently driven by the evolution of epiphyti

66 We suggest that mid-Cenozoic ( approximately 35-25 Myr ago) to Recent magmat

67 ing from 3.0-3.5 kilometres during the early Cenozoic (approximately 55 million years ago) to 4.6 kil

68 enigmatic-terrestrial predators of the late Cenozoic are the Machairodontinae, a diverse group of bi

69 ex ecosystems are far more common among Meso-Cenozoic assemblages than among the Paleozoic assemblage

70 se in marine animal biodiversity through the Cenozoic at the genus level has been attributed to a sam

71 t accommodates both the long-term decline of Cenozoic atmospheric CO(2) levels and the effects of orb

72 sland, in northernmost Canada are the oldest Cenozoic avian fossils from the Arctic.

73 rpretation of bioalteration trace fossils in Cenozoic basalt glasses and their putative equivalents i

74 -habitat diversity measure Fisher's alpha of Cenozoic benthic foraminifera from the temperate Central

75 aternary) history of the four major Mesozoic-Cenozoic brachiopod orders (Terebratulida, Rhynchonellid

76 al losses of tropical rainforests during the Cenozoic, but not to the cumulative area of tropical rai

77 Cenozoic calderas in western North America and in other

78 s predecessors generated a treasure trove of Cenozoic climate and carbon cycle dynamics.

79 ving diaspora associations persisted through Cenozoic climate change and plate movements as the const

80 Here we propose a mechanism by which Cenozoic climate change could have caused the rise of th

81 We show that late Cenozoic climate change induced phylogenetically selecti

82 ar ice volume plays in the predictability of Cenozoic climate dynamics.

83 r obstacle in understanding the evolution of Cenozoic climate has been the lack of well dated terrest

84 Much of our understanding of Cenozoic climate is based on the record of delta(18)O me

85 that episodic pCO2 drawdown drove this major Cenozoic climate transition.

86 esults help fill a gap in understanding past Cenozoic climates and the way long-term climate sensitiv

87 omparative phylogenetic methods to infer how Cenozoic climatic change shaped the morphological and ph

88 rds was influenced by Bergmann's rule during Cenozoic climatic change.

89 au and their temporal relationships with the Cenozoic climatic changes.

90 to have been fully glaciated as a result of Cenozoic climatic cooling.

91 aves have the potential to help resolve late Cenozoic climatic, speleologic, and tectonic questions.

92 In our model, declining Cenozoic CO2 first leads to the formation of small, high

93 are thought to be highly dynamic during the Cenozoic collision of India and Eurasia, but the drainag

94 esser Himalayan sedimentary rocks during the Cenozoic collision of India and Eurasia.

95 st that global climate change throughout the Cenozoic, combined with tropical niche conservatism, pla

96 om leaf cuticles of some Late Cretaceous and Cenozoic conifers.

97 During the early Cenozoic, continental assemblages are dominated by mid-s

98 Cenozoic convergence between the Indian and Asian plates

99 hat the absence of major extinctions and the Cenozoic cooling have been essential in making the IAA t

100 The magnitude of size increase due to Cenozoic cooling is consistent with temperature-size rel

101 rease in solid Earth carbon emissions during Cenozoic cooling requires an increase in continental sil

102 cates a major climate shift within long-term Cenozoic cooling.

103 uted to this group, however, no complete pre-Cenozoic crown-scincid specimens have been found.

104 restricted toward the tropics throughout the Cenozoic, culminating in relatively narrow circumtropica

105 ith a fossil record is influenced largely by Cenozoic data.

106 A compilation of Cenozoic deep-sea sedimentary phosphorus speciation data

107 en isotope records indicates that changes in Cenozoic deep-water circulation patterns were the conseq

108 ture thermochronometry reveals regional Late Cenozoic denudation in Fiordland, New Zealand, consisten

109 rn margin of the Tibetan Plateau heralds the Cenozoic development of high topography.

110 A preference for Cenozoic dispersal origins has replaced the classical vi

111 sent a high-resolution reconstruction of the Cenozoic diversity history of the IAA by inferring speci

112 new terrestrial record for this significant Cenozoic environmental event.

113 Consequently, the extent to which major Cenozoic environmental shifts affected neoselachian dive

114 The history of the Arctic Ocean during the Cenozoic era (0-65 million years ago) is largely unknown

115 position events have occurred during the mid-Cenozoic era (34 to 7 million years ago) in the northern

116 Their evolutionary expansion during the Cenozoic era (66 Ma to present) has been associated with

117 ed non-Gaussian tails throughout much of the Cenozoic era (66 Ma to present), suggesting an intrinsic

118 c carbon dioxide concentrations in the early Cenozoic era (about 60 Myr ago) are widely believed to h

119 during the warmest climatic interval of the Cenozoic era (approximately 65 to 40 million years (Myr)

120 e southern Andes (40 degrees S) by the early Cenozoic era (around 55 million year ago).

121 s in global ocean circulation throughout the Cenozoic era (from about 65 million years ago to the pre

122 ttributable to anagenesis is <19% during the Cenozoic era (last 65 Myr) and <10% during the Neogene p

123 e undergone significant extension during the Cenozoic Era (since approximately 65 Myr ago).

124 lored these responses during portions of the Cenozoic era (the most recent 65.5 million years (Myr) o

125 d dramatic instance of global warming in the Cenozoic era and has been proposed to be a geologic anal

126 thoroughly categorize climate states of the Cenozoic era and to study their dynamics.

127 ing the evolution of global climate over the Cenozoic Era is reviewed.

128 Here, using the exceptional fossil record of Cenozoic Era macroperforate planktonic foraminifera, we

129 from other eudicots at the beginning of the Cenozoic era of the Earth (60 Mya), major diversificatio

130 How the substantial climate shifts of the Cenozoic era shaped the geographical distribution of tro

131 ication of North American mammals across the Cenozoic Era slowed as diversity increased.

132 reversed global convection modeling over the Cenozoic Era which incorporates models of present-day to

133 In the Cenozoic era, continental collisions slowed seafloor spr

134 In the early Cenozoic era, exchange between these two ocean basins wa

135 wever, the effect of cooling during the Late Cenozoic era, including the onset of Pliocene-Pleistocen

136 During the Cenozoic era, spanning approximately the past 66 million

137 frequently have been alkaline during the mid-Cenozoic era.

138 the most important climate transition of the Cenozoic era.

139 he most pronounced climate events during the Cenozoic era.

140 the most dramatic events on Earth during the Cenozoic era.

141 ions were developed with Europe in the early Cenozoic era.

142 t pivotal transition in climate state of the Cenozoic Era.

143 of mammalian fauna in Europe and Asia in the Cenozoic era.

144 Here we show that Cenozoic-era Baffin Island and West Greenland lavas, pre

145 damental to our understanding of the role of Cenozoic-era climate change in the development of topogr

146 d around the transition between Mesozoic and Cenozoic eras and was likely related to the K-Pg mass ex

147 vents during the transition from Mesozoic to Cenozoic eras, including the K-Pg mass extinction event,

148 ock cooling ages signifies much reduced late Cenozoic erosion despite dominantly glacial conditions h

149 ith independent geologic constraints for the Cenozoic evolution of the central Andes, as well as vari

150 Limiting Cenozoic evolution to bathymetry alone leads to predicte

151 ft system is the result of late Mesozoic and Cenozoic extension between East and West Antarctica, and

152 possible lithospheric driving mechanisms for Cenozoic extension in southwestern North America.

153 In contrast to northern continents, the Cenozoic faunal history of SA was characterized by a lon

154 ss is independent of geological age, as even Cenozoic feathers can comprise primarily alpha-helices a

155 This anomaly suggests that Cenozoic flood basalt volcanism in the Afar region and a

156 Thus, examination of Cenozoic fossil coral collections from these regions sho

157 om eastern Africa's rich and well-dated late Cenozoic fossil record documents communities of large-bo

158 as and insect faunas that are known, but its Cenozoic fossil record of insects and insect herbivory i

159 modeling, paleoclimate models, and the early Cenozoic fossil record to examine the influence of clima

160 agree with most early (Palaeozoic) and late (Cenozoic) fossil-based times, but indicate major gaps in

161 here dominates our knowledge of Mesozoic and Cenozoic fossilized tree resin (amber) with few findings

162 During the Mesozoic and Cenozoic, four distinct crocodylomorph lineages colonize

163 arity stratigraphy at Gran Barranca with the Cenozoic geomagnetic polarity time scale indicate that B

164 The long-standing view of Earth's Cenozoic glacial history calls for the first continental

165 d atmospheres of the Permo-Carboniferous and Cenozoic glaciations.

166 etween permanently glaciated areas and early Cenozoic global climate reorganization-is uncertain.

167 nding mammalian evolution in response to the Cenozoic global climatic and tectonic changes.

168 ntially born from selective pressures during Cenozoic global cooling and eventual ice conditions begi

169 edicts that enhanced erosion related to late Cenozoic global cooling can act as a first-order influen

170 various peculiar adaptations during the late Cenozoic global cooling trends.

171 of the Paratethys sea from central Asia and Cenozoic global cooling.

172 ease their evolutionary rate with decreasing Cenozoic global temperatures.

173 p water marine AOA during the Mesozoic-early Cenozoic greenhouse climates.

174 glaciers were present even during the Early-Cenozoic greenhouse world.

175 aleocene origins, i.e. well within the Early Cenozoic greenhouse world.

176 ns are considered the primary driver for the Cenozoic Greenhouse-Icehouse transition, ~34 million yea

177 oanseran affinities of several bizarre early Cenozoic groups such as the 'pseudotoothed birds' (Pelag

178 ominated forests in the Cretaceous and early Cenozoic had a profound effect on terrestrial biota by c

179 ge terrestrial mammals of the North American Cenozoic has previously been quantitatively summarized i

180 ging climate and habitat loss throughout the Cenozoic have had strong impacts on the phylogenetic str

181 ges of faunas between continents in the Late Cenozoic have made it challenging to identify general pa

182 riggered convergent cheek-tooth evolution in Cenozoic herbivores.

183 ure of the modern biota, despite the complex Cenozoic history of marine environments.

184 Our results call for a reassessment of the Cenozoic history of ocean temperatures to achieve a more

185 mass co-evolved in proboscideans across the Cenozoic; however, this pattern appears disrupted by two

186 ass extinction, our data show that the early Cenozoic hyperthermals did not have a long-term impact o

187 record significant changes during the early Cenozoic hyperthermals.

188 imate-carbon cycle feedbacks during the Late Cenozoic Ice Age (LCIA).

189 The first Cenozoic ice sheets initiated in Antarctica from the Gam

190 occurred between the late Mesozoic and early Cenozoic, identifying this period as the "Second Age of

191 nstructions of biomes and climate to examine Cenozoic imprints on the phylogenetic structure of regio

192 Subsequent volcanism, through the Cenozoic in Mongolia and North China does not appear to

193 y parts of the western hemisphere during the Cenozoic, including both continents and the West Indies.

194 The hyperthermal events of the Cenozoic, including the Paleocene-Eocene Thermal Maximum

195 the Recent thus accounts for only 5% of the Cenozoic increase in bivalve diversity, a major componen

196 etres at present, consistent with an overall Cenozoic increase in weathering.

197 uration, that occurred during the long early Cenozoic interval of elevated warmth.

198 Here we report high Fe(3+)/EFe values in Cenozoic intraplate basalts from eastern China, which ar

199 Here we present mercury isotope data for Cenozoic intraplate EM1-type basalts from Northeast Asia

200 onty) in herbivorous mammals during the late Cenozoic is classically regarded as an adaptive response

201 in amber exclusively from the Cretaceous and Cenozoic is widely regarded to be a result of the produc

202 house-gas-driven global warming event of the Cenozoic-is central to drawing inferences for future cli

203 theses have been put forward to explain the 'Cenozoic isotope-weathering paradox', and the evolution

204 As a result, reconciling Cenozoic isotopic records with the need for mass balance

205 d against assigning climate a direct role in Cenozoic land mammal faunal changes.

206 mmunity structure during warm periods of the Cenozoic (last 66 million years) reveal that deep-dwelli

207 it is clear that in both the Cretaceous and Cenozoic, leptosporangiate ferns were adept at exploitin

208 ozoic diversity was, in contrast to the Meso-Cenozoic, limited by nutrient-poor phytoplankton resulti

209 Using the unparalleled fossil record of Cenozoic macroperforate planktonic foraminifera, we demo

210 Here we analyse Triton, a global dataset of Cenozoic macroperforate planktonic foraminiferal occurre

211 cular, the model matches the encroachment of Cenozoic magmatism from the margins towards the plateau

212 al Bayesian survival model of North American Cenozoic mammal species durations in relation to species

213 , Kenya, which has produced a rich record of Cenozoic mammalian evolution(10).

214 the duration of bivalve species in the early Cenozoic marine fossil record of the eastern United Stat

215 We documented the occupancy histories of Cenozoic marine mollusks from New Zealand.

216 birds and mammals and 140 species of extinct Cenozoic marine mollusks.

217 tions of entire assemblages in more than 500 Cenozoic marine sediment samples, including more than 1

218 radiation associated with global warming and Cenozoic maximum global temperatures, (ii) moderately an

219 tantial variations of genesis regions in the Cenozoic may affect upper-ocean vertical mixing and henc

220 further decrease in maximum size during the Cenozoic may relate to the evolution of bats, the Cretac

221 Proboscideans were keystone Cenozoic megaherbivores and present a highly relevant ca

222 unct plant communities associated with early Cenozoic mesophytic forests and a boreotropical history.

223 Climatic events in the Cenozoic (Middle Eocene Climate Optimum, Miocene Climate

224 ends to contradict the popular view of rapid Cenozoic monotreme diversification.

225 play an important role in understanding late Cenozoic mountain uplift and global cooling.

226 present a sampling-standardised analysis of Cenozoic neoselachian genus diversity and faunal composi

227 Monte Carlo evaluation finds that late Cenozoic net growth of the carbonate reservoir is very l

228 ese six temporal associations that summarize Cenozoic North American mammalian evolutionary history.

229 over deep time on the diversity patterns of Cenozoic North American mammals.

230 emperature increase to the highest prolonged Cenozoic ocean temperature and a similarly distinctive c

231 gate the compositional systematics of ~ 3500 Cenozoic oceanic and continental sodic basalts to provid

232 likely relictual mammals from earlier in the Cenozoic of SA and Antarctica, Necrolestes demonstrates

233 Later, in the Cretaceous and Cenozoic, ordinal origination of benthic organisms did n

234 below Lesser Himalayan rocks at the onset of Cenozoic orogenesis are flawed, and that some metamorphi

235 Here we present a Cenozoic palaeoceanographic record constructed from >400

236 d global analysis was undertaken of earliest Cenozoic (Paleocene) neogastropods and this does indeed

237 l of interconnected feedbacks in reproducing Cenozoic paleoclimate variability, given that different

238 in fossil record and assembled detailed late Cenozoic paleoclimatic, paleoenvironmental, and paleoeco

239 nvironmental parameters and comparisons with Cenozoic paleoproxy data show a consistently positive co

240 t extinctions of marine invertebrates in the Cenozoic period.

241 ers, our results indicate that, in these two Cenozoic periods of sustained warmth, ODZs were contract

242 aliaforms, Late Cretaceous metatherians, and Cenozoic placentals.

243 -mantle slab penetration events by comparing Cenozoic plate motions at the Earth's main subduction zo

244 We used size measurements from Cenozoic populations of the ostracode genus Poseidonamic

245 are consistent with fossil evidence for mid-Cenozoic presence of sloths in the West Indies and an ea

246 e under the Indian Ocean at the start of the Cenozoic presents a challenge for connecting the event t

247 logical, and climatic changes throughout the Cenozoic, primarily associated with tectonic plate colli

248 crucial intervals of the Mesozoic and early Cenozoic, providing the earliest occurrence(s) of some t

249 shroom diversity started during the Mesozoic-Cenozoic radiation event, an era of humid climate when t

250 xamine whether xylem traits helped shape the Cenozoic radiation of Eupolypod ferns.

251 hought that there was a steep Cretaceous and Cenozoic radiation of marine invertebrates.

252 ogical diversity of extant species.(1-7) The Cenozoic radiation of placental mammals, the foundationa

253 Here, we show that the Cretaceous-Cenozoic radiation was driven by increased diversificati

254 o the extinction or those originating in the Cenozoic rarely reach higher ranks today, implying long-

255 ve focused on the proto-Icelandic plume, our Cenozoic reconstructions reveal the equally important dy

256 A Cenozoic record of hafnium isotopic compositions of cent

257 China (Xinjiang Province) that is the first Cenozoic record of this clade and renders Deltatheroida

258 nizations of biogenic silica burial over the Cenozoic reduced marine authigenic clay formation, contr

259 -bound delta(15)N during warm periods of the Cenozoic, reflecting decreased water column denitrificat

260 global mean sea level (GMSL) during the late Cenozoic remain uncertain.

261 eau lithosphere over 35-40 Myr following mid-Cenozoic removal of the Farallon plate from beneath Nort

262 year (Quaternary) and 3.6-18.9 mm/year (Late-Cenozoic) respectively.

263 A late Cenozoic rise in diatoms has been causally tied to the r

264 eported from many localities in Mesozoic and Cenozoic rocks.

265 These results enable us to calculate mid-Cenozoic rotation parameters for East and West Antarctic

266 al corrosion textures in volcanic glass from Cenozoic seafloor basalts and the corresponding titanite

267 ndings suggest that global changes since the Cenozoic shaped the patterns of flowering plant diversit

268 vince and Rio Grande rift province underwent Cenozoic shortening followed by extension, the plateau e

269 Growth of the Andes has been attributed to Cenozoic subduction.

270 O2 partial pressure and the evolution of the Cenozoic sulphur cycle, and could be accounted for by ge

271 paleoceanographic model that predicts Early Cenozoic surface currents periodically conducive to raft

272 s and modern stream waters to determine late Cenozoic surface uplift across the Peruvian central Ande

273 s a tectonic setting for several significant Cenozoic tectonic events in the Ross Sea embayment inclu

274 ecies (<100 million years ago) suggests that Cenozoic tectonic history and oceanic circulation patter

275 r rapid-cooling pulses precludes significant Cenozoic tectonic or glacial exhumation of central inter

276 de active orogen with a well-documented late Cenozoic tectonic, climatic and glacial history.

277 ons are more subject to invasion; the latest Cenozoic temperate zones evidently received more invader

278 Late Cenozoic terrestrial fossil records of North America are

279 st 65 My, using 27,903 fossil occurrences of Cenozoic terrestrial mammals from western North America

280 tential solution for mismatches between late Cenozoic terrestrial sedimentation and marine geochemist

281 Anthonotha) may have diverged earlier in the Cenozoic than predicted by molecular phylogenies.

282 e thus a more diverse radiation in the early Cenozoic than previously appreciated.

283 Fe isotopic composition of seawater over the Cenozoic that reflect the influence of several, distinct

284 For the Cenozoic, the key driving mechanism of atmospheric CO(2)

285 Yet, since the Cenozoic, these organisms have experienced major fluctua

286 hat eastern Tibet was elevated before middle Cenozoic time and that the tempo of fluvial incision may

287 ine bivalves shows, in three successive late Cenozoic time slices, that most clades (operationally he

288 s of the 31 included clades in Cretaceous to Cenozoic times.

289 -wave velocity provinces, as in Mesozoic and Cenozoic times.

290 er increase in specific lineages towards the Cenozoic to reach, in the most recently derived lineages

291 interpreted in the subsurface, above the sub-Cenozoic unconformity, bounded by two tear faults.

292 The causes of Cenozoic uplift of the Colorado Plateau, southwestern US

293 an asthenosphere mantle contribution to the Cenozoic volcanic record of the region.

294 long-term geological record reveals an early Cenozoic warm climate that supported smaller polar ecosy

295 e the consequence, not the cause, of extreme Cenozoic warmth.

296 st size of planktic foraminifera through the Cenozoic was an adaptive response to intensifying surfac

297 All such groups arose in parallel during the Cenozoic, when army ants diversified into modern genera

298 on of the Altaids and was rejuvenated in the Cenozoic, which might be a far-field response to the Ind

299 eawater sulfate sulfur isotope curve for the Cenozoic with a resolution of approximately 1 million ye

300 at originated in the tropics during the late Cenozoic, with the contrarian gradient strength at both