ライフサイエンスコーパス: Cenozoic

1 tern for oceanic diatom diversity across the Cenozoic.

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

3 o form diverse assemblages once again in the Cenozoic.

4 imately 0.15% every million years during the Cenozoic.

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

6 ust experienced strong shortening during the Cenozoic.

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

8 e size of marine pelagic diatoms through the Cenozoic.

9 ed marine planktonic diatom species over the Cenozoic.

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

11 ed temperatures in the latter portion of the Cenozoic.

12 system toward a glacial tipping point in the Cenozoic.

13 gen content over short time intervals in the Cenozoic.

14 c, and remained comparatively high until the Cenozoic.

15 hanging Southern Ocean conditions during the Cenozoic.

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

17 rtial pressure of atmospheric CO2 during the Cenozoic.

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

19 nstruct mantle structure at the start of the Cenozoic.

20 s Australia became more arid during the late Cenozoic.

21 while major genera diversified near the mid Cenozoic.

22 d global average temperature trends over the Cenozoic.

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

24 North American terrestrial mammals over the Cenozoic.

25 attern of fauna replacement in SA during the Cenozoic.

26 e Northern or Southern Hemisphere during the Cenozoic.

27 r five typical geological periods during the Cenozoic.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

52 Cenozoic calderas in western North America and in other

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

54 We show that late Cenozoic climate change induced phylogenetically selecti

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

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

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

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

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

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

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

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

63 Cenozoic convergence between the Indian and Asian plates

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

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

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

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

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

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

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

71 new terrestrial record for this significant Cenozoic environmental event.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

88 the most important climate transition of the Cenozoic era.

89 he most pronounced climate events during the Cenozoic era.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

113 riggered convergent cheek-tooth evolution in Cenozoic herbivores.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

148 t extinctions of marine invertebrates in the Cenozoic period.

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

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

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

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

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

154 A Cenozoic record of hafnium isotopic compositions of cent

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

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

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

158 eported from many localities in Mesozoic and Cenozoic rocks.

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

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

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

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

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

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

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

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

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

168 Late Cenozoic terrestrial fossil records of North America are

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

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

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

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

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

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

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

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

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

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

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

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

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

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