ライフサイエンスコーパス: Archean

1 red from the atmosphere to the mantle in the Archean.

2 e of a vast microbial ecosystem in the early Archean.

3 the oceans as continents formed in the late Archean.

4 f the cratonic lithosphere at the end of the Archean.

5 PO(2)) and O(2) production fluxes during the Archean.

6 O(2)-free atmosphere throughout most of the Archean.

7 tant crustal silica since at least the early Archean.

8 d mobile-lid (arc-like) regimes in the early Archean.

9 at formed the continental lithosphere in the Archean.

10 ore reducing conditions prevalent during the Archean.

11 those identified several times later in the Archean.

12 for the Hadean (pre-3,800 Myr ago) and Early Archean (3,800 to 3,400 Myr) impact flux can be derived

13 he scarcity of well-preserved rocks from the Archean (4.0 to 2.5 Gyr ago) and Proterozoic (2.5 to 0.5

14 Archean (4.0-2.5 Ga) tonalite-trondhjemite-granodiorite

15 Late Archean accretionary events involving an oceanic lithosp

16 nt porosity, limiting the potential for post-Archean additions of organic matter to the samples.

17 oxides and molecular oxygen generated during Archean and earliest Proterozoic non-Snowball glacial in

18 n--although often overlooked--constituent of Archean and Early Proterozoic sedimentary successions.

19 e-Ni) sulfide ore deposits formed during the Archean and early Proterozoic.

20 proposed a more uniformitarian view in which Archean and Hadean continents were only slightly more ma

21 idges contrasting (182)W isotope patterns in Archean and modern mantle-derived rocks.

22 fractionation of sulfur isotopes (S MIF) in Archean and Paleoproterozoic rocks provides strong evide

23 cales, with the thickest crust formed in the Archean and Phanerozoic.

24 l availability in anoxic seawater during the Archean and Proterozoic eons (4.0-0.541 billion years ag

25 ing microbes had already evolved by the late Archean and were present before oxygen first began to ac

26 matic plagioclase megacrysts from 3.7-2.8 Ga Archean anorthosites and leucogabbros.

27 in bedded carbonaceous cherts from the Early Archean Apex Basalt and Towers Formation of northwestern

28 scovered in a bedded chert unit of the Early Archean Apex Basalt of northwestern Western Australia.

29 asinal environments adjacent to a major Late Archean ( approximately 2.6-2.5 Ga) marine carbonate pla

30 nk diminished greatly towards the end of the Archean as ultramafic rocks became less common and helpe

31 mentary rocks to examine changes in the Late Archean atmosphere immediately prior to the Great Oxidat

32 The low O2 content of the Archean atmosphere implies that methane should have been

33 on of sulfur isotopes that took place in the Archean atmosphere of Earth.

34 The Archean atmospheric Xe is mass-dependently fractionated

35 Furthermore, we determine an Archean atmospheric Xe/Kr ratio, 2.3 times higher than t

36 Then, we isolated DNA from 124 archean, bacterial, fungal, plant, and mammalian species

37 Here, we show that the early Archean banded rocks from Isua, Akilia, and Innersuartuu

38 is a tonalite intrusion associated with the Archean Barberton Greenstone Belt.

39 at the atmospheric oxygen level rose from an Archean baseline of essentially zero to modern values in

40 rker preservation, so future exploration for Archean biomarkers should screen for rocks with milder t

41 On average, therefore, the Archean biosphere may have been oxidizing at the bottom

42 ous ages, as well as modern, Cretaceous, and Archean black shales.

43 a single tectonomagmatic process during the Archean but was operative during the reworking of Hadean

44 lisms using sulfide oxidation emerged in the Archean, but those involving thiosulfate emerged only af

45 cally-mediated iron precipitation during the Archean by illustrating that it took place on the shallo

46 ndicate that the titanite formed during late Archean ca. 2.9 Ga thermal contact metamorphism and not

47 Mesoproterozoic, Paleoproterozoic, and some Archean conical stromatolites.

48 raining thickness and geothermal gradient of Archean continental crust are crucial to understanding g

49 Evolution of Archean continental crust involved partial melting of ma

50 We posit that much Archean continental crust is made of hybrid magmas that

51 Our study suggests that Archean continental crust, such as that in the EB, most

52 ks were thus derived from the once-extensive Archean continental keels that have been dislodged and r

53 (-1) via low-temperature serpentinization of Archean continents and seafloor is possible.

54 The crustal remnants of Earth's Archean continents have been shielded from mantle convec

55 heric oxygen, oxidative pyrite weathering on Archean continents was controlled by the exposure of lan

56 Archean cratons represent stable continental domains whi

57 t compositionally resemble the deep keels of Archean cratons.

58 ounts of differentiated mantle-derived melt, Archean crust and hydrothermally altered shallow-crustal

59 /kbar, characteristic of overthickened mafic Archean crust at the head of a mantle plume, crustal ove

60 -143)Nd data reveal that this large block of Archean crust formed by reworking of much older (>4.2 bi

61 the addition of deep mantle material to the Archean crust, oceans, and atmosphere, while also provid

62 Archean crust-sourced tonalitic-trondhjemitic-granodiori

63 n years to form an important source rock for Archean crustal genesis.

64 servations, model results indicated that the Archean data reflect low primary productivity (~100-fold

65 ooling, with a recent reconstruction placing Archean delta(18)O(SW) 5 to 10 per mille lower than toda

66 ew lherzolitic and eclogitic diamonds to the Archean diamond suite.

67 reflecting a stably dipolar, core-generated Archean dynamo.

68 ean island basalt, the HIMU source formed as Archean-early Proterozoic subduction-related carbonatite

69 The Archean Earth (3.8 to 2.5 billion years ago) was probabl

70 diation screening required to protect DNA on archean Earth compare well with field and laboratory obs

71 mposition of continental crust on Hadean and Archean Earth is critical to our understanding of the ph

72 average flux (1.2 kg N m(-2) year(-1)), the Archean Earth's surface would need to be 0.0092, and 0.0

73 On the anoxic Archean Earth, the oxidized partner was probably iron.

74 reduced planet such as the late Hadean/early Archean Earth.

75 even under the high UV radiation regimes of archean Earth.

76 timate biologically effective irradiances on archean Earth.

77 oxygenation (O(2)-whiffs) and glaciation on Archean Earth.

78 ulfur allotropes in the anoxic atmosphere of Archean Earth.

79 e arsenic biogeochemical cycle on the anoxic Archean Earth.

80 es of evidence suggest that, during the late Archean, Earth completed its transition from a stagnant-

81 and Hf isotopic mixing arrays show that the Archean EM I material was poor in trace elements, resemb

82 ndamental insights into the chemistry of the Archean environment and evolutionary origin of microbial

83 was an important metabolism in organic-rich Archean environments--even in an Archean ocean basin dom

84 se in mantle (182)W/(184)W occurs during the Archean eon (about four to three billion years ago), pot

85 d into arsenic-rich environments in the late Archean Eon and Proterozoic Eon, respectively, by the sp

86 d archaea likely in the late Hadean or early Archean eon and that the ancestral methanogen was depend

87 Ancient oxidoreductases from the Archean Eon between ca. 3.5 and 2.5 billion years ago ha

88 shallow waters and on continents during the Archean eon in the absence of molecular oxygen.

89 e same S-isotope pattern at both ends of the Archean Eon is unexpected, given the complex atmospheric

90 Rocks of the Archean Eon record at least 16 major impact events, invo

91 The Archean Eon was a time of predominantly anoxic Earth sur

92 The Archean Eon witnessed the production of early continenta

93 Marine life on Earth is known back to the Archean Eon, when life on land is assumed to have been l

94 equired for large periods of time during the Archean eon.

95 ate concentrations persisted for much of the Archean eon.

96 the Cretaceous Oceanic Anoxic Events and the Archean Eon.

97 for the evolution of molecular oxygen in the Archean eon.

98 We therefore conclude that the Archean field was produced by the basal magma ocean.

99 bilized the craton and contributed a younger Archean generation of eclogitic diamonds.

100 ossibilities to improve our knowledge of the Archean geodynamo.

101 water signal may be representative of a late Archean global signature and that it preceded a similar,

102 This Middle Archean gold mineralization event corresponds to a perio

103 rchean in age and, with the exception of the Archean grain, are also matched by the population in the

104 ential for impacts into biosignature-bearing Archean greenstones and the Martian surface.

105 For over 50 y, the high organic content of Archean (>2.5 Ga) mudrocks has puzzled geologists and ev

106 it has been proposed that during the Hadean-Archean heavy bombardment by extraterrestrial impactors,

107 ions trapped and shielded from alteration in Archean high-Mg olivine crystals offer a solution to thi

108 unique geological archive covering 800 Ma of Archean history.

109 In this study, we analyzed noble gases in Archean hydrothermal quartz fluid inclusions and show th

110 in Archean terrigenous sedimentary rocks and Archean igneous/metaigneous rocks to track the bulk MgO

111 tone are Permian, Devonian, Proterozoic, and Archean in age and, with the exception of the Archean gr

112 fur isotope data implying that the sulfur in Archean komatiite-hosted Fe-Ni sulfide deposits was prev

113 show via petrological modeling that hydrous Archean mafic crust metamorphosed in a non-plate tectoni

114 Estimates of fO2 of Archean magmas are not this low, arguing for alternative

115 ble for the rise in oxygen, it requires that Archean magmas had at least two orders of magnitude lowe

116 Here we report that an Archean manganese mineral, rhodochrosite (MnCO(3)), can

117 Middle Archean mantle depletion events initiated craton keel fo

118 Archean mantle evolution is complementary to crustal gro

119 o buoyant, refractory harzburgites formed by Archean mantle melting.

120 report the occurrence of phosphite in early Archean marine carbonates at levels indicating that this

121 combined with a thicker oceanic crust in the Archean may have limited the whole-Earth topographic rel

122 Late Archean metamorphism significantly reduced the kerogen's

123 ong with other short-chain alkanes from some Archean metasedimentary rocks, has unique isotopic signa

124 The recognition of Archean microbial methane in this work reveals a biochem

125 and reveal the progressive development of an Archean microcontinent.

126 very substantiates previous reports of Early Archean microfossils in Warrawoona Group strata.

127 n the ancient sedimentary record to quantify Archean Mo cycling, which allows us to calculate lower l

128 f ca 3110 Ma for zircon formation and a late Archean model age of 2610 Ma for the metamorphism that p

129 planetary heat is dissipated, and reasonable Archean-modern heat flow changes account for ~5 per mill

130 In the late Archean, molecular oxygen likely cycled as a biogenic tr

131 on metals molybdenum and rhenium in the late Archean Mount McRae Shale in Western Australia.

132 Iron speciation data for the late Archean Mount McRae Shale provide evidence for a euxinic

133 We found that organic-rich Archean mudrocks were deposited under exceptionally low

134 Archean mutinaite might have become de-aluminated toward

135 We propose that Archean negative Fe isotope excursions reflect partial F

136 st continental lithospheric mantle since the Archean, no change in Delta'(17)O is observed.

137 Archean O(2) levels were vanishingly low according to ou

138 rganic-rich Archean environments--even in an Archean ocean basin dominated by iron chemistry.

139 The Archean ocean is efficient in diluting primary atmospher

140 e for possibly biological uptake in the late Archean ocean, suggesting an active redox cycling of pho

141 ano, Indonesia, a low-sulfate analog for the Archean ocean, we find large (>20 per mil) sulfur isotop

142 h predominantly bound metals abundant in the Archean ocean.

143 bdenum and rhenium were probably supplied to Archean oceans by oxidative weathering of crustal sulfid

144 O) of ancient chemical sediments imply ~70 C Archean oceans if the oxygen isotopic composition of sea

145 Here we argue that, in the anoxic Archean oceans, pyrite could form in the absence of ambi

146 sibly restricting biological productivity in Archean oceans.

147 potentially catalyzed redox reactions in the Archean oceans.

148 ealed modern bacteria, perhaps indicative of Archean ones.

149 that the mantle gradually oxidized from the Archean onwards, leading to speculation that such oxidat

150 lion-year-old (uranium-lead ratio in zircon) Archean ophiolite complex in the North China craton.

151 The documentation of a complete Archean ophiolite implies that mechanisms of oceanic cru

152 radox, by studying the accumulation rates of Archean organic-rich mudrocks.

153 strength is similar to that observed in the Archean paleomagnetic record.

154 high-precision iron isotopic measurements of Archean-Paleoproterozoic sediments and laboratory grown

155 Development of Archean paleosols and patterns of Precambrian rock weath

156 If active during the Archean, pelagic precipitation and subsequent sedimentat

157 vailability of sulfates during Earth's early Archean period proposed that more soluble S(+IV) compoun

158 two critical roles for carbon dioxide in the Archean period.

159 We infer an increase from early Archean pH values between 6.5 and 7.0 and Phanerozoic va

160 e main phosphorus source for life during the Archean, phosphite (HPO(3)(2)(-)) gained importance lead

161 ns of declining phosphate levels through the Archean, possibly linked to phosphate-scavenging Fe(III)

162 have been present on Earth's surface in the Archean, prior to the formation of stratospheric ozone.

163 t nutrients phosphorus and nickel across the Archean-Proterozoic boundary, which might have helped tr

164 on the thermal and chemical evolution of the Archean-Proterozoic Earth.

165 ting in Earth's atmosphere shortly after the Archean-Proterozoic transition during the 'Great Oxidati

166 f noble gases trapped in fluid inclusions of Archean quartz (Barberton, South Africa) that reveal the

167 owth through deep-crustal partial melting of Archean-Rhyacian crust.

168 e mass-independent fractionation line of the Archean rock record.

169 resulted in parallel transposition of Early Archean rocks and significant boudinage, the tails of wh

170 Hopanes and steranes found in Archean rocks have been presented as key evidence suppor

171 Archean rocks may provide a record of early Earth enviro

172 dation state phosphorus compounds in ancient Archean rocks.

173 erse tectonic settings, including five early Archean samples from Isua, Greenland, of which three hav

174 results demonstrate that previously studied Archean samples host mixtures of biomarker contaminants

175 We posit that delta(18)O in the oldest Archean samples provides the best delta(18)O estimate fo

176 ongly with multiple sulfur isotope trends in Archean samples, which exhibit significant (36)S anomali

177 Because the main ingredient of the Archean sea was sodium bicarbonate, neither archeobacter

178 r conditions that model the chemistry of the Archean sea.

179 We speculate that Archean seafloor vents were nanoparticle "factories" tha

180 Models suggesting lower d(18)O(sw) of Archean seawater due to intense continental weathering a

181 n anoxic systems, suggesting that Hadean and Archean seawater featured phosphate concentrations ~10(3

182 d by sulfur cycling in Lake Matano, we infer Archean seawater sulfate concentrations of less than 2.5

183 fur isotope fractionations into estimates of Archean seawater sulfate concentrations.

184 es predict uniformly negative Delta(33)S for Archean seawater sulfate, this remains untested through

185 After subduction, this Archean sediment apparently remained stored in the deep

186 erial was poor in trace elements, resembling Archean sediment.

187 at archaea and bacteria were present in Late Archean sedimentary environments.

188 sotopes (reported as Delta(33)S) recorded in Archean sedimentary rocks helps to constrain the composi

189 Since the Archean, sedimentary pyrite formation has played a major

190 The presence of these anomalies in Archean sediments [(4-2.5 billion years ago, (Ga)] impli

191 Large fractionations in post-Archean sediments are congruent with a decline of favora

192 Since Archean sediments lack fractionation exceeding the Apr v

193 ude of minor sulfur isotope fractionation in Archean sediments remain unexplained.

194 such as the elevated (49)Ti/(47)Ti ratios in Archean shales, has been used to argue for ongoing subdu

195 arbon for a 150 million-year section of late Archean shallow and deepwater sediments of the Hamersley

196 re determined by the size of the preexisting Archean siderite reservoir, which was consumed through o

197 e mass-independent fractionation (S-MIF), an Archean signature of atmospheric anoxia that begins to d

198 we show that subduction processes formed the Archean Slave craton in Canada.

199 Proterozoic rocks exist, no currently known Archean strata lie within the appropriate thermal maturi

200 Archean subduction, even if generally short-lived, was c

201 candidate traces of life can be confirmed in Archean subseafloor environments.

202 to the sediments likely results from a Late Archean subsurface hydrothermal biosphere of archaea and

203 malies, thus questioning the significance of Archean sulfate deposits.

204 mosphere but identify variability within the Archean sulfate isotope record that suggests persistence

205 ch allows us to investigate the diversity of Archean sulfate texture and mineralogy with unprecedente

206 planation for the low range of delta(34)S in Archean sulfides, and raise a possibility that sulfate s

207 regions, allowing for reconstruction of the Archean sulfur cycle and possibly offering insight into

208 ng an integrated biogeochemical model of the Archean sulfur cycle, we find that the preservation of m

209 ass-anomalous fractionations expected of the Archean sulfur cycle, whereas values show large fraction

210 n on to deconvolute the ocean and atmosphere Archean sulfur cycle.

211 atmosphere has implications for interpreting Archean sulfur deposits used to determine the redox stat

212 o early episodes of transient oxygenation of Archean surface environments.

213 ractionated (MIF) sulfur isotopes that trace Archean surficial signatures into the mantle.

214 We used Ni/Co and Cr/Zn ratios in Archean terrigenous sedimentary rocks and Archean igneou

215 Here we show that in the Archean, the formation and stabilization of continents a

216 evated atmospheric CO2 concentrations in the Archean, the sustained methane fluxes necessary for haze

217 olumes of mantle lithosphere that existed in Archean time (>2.5 Ga) has apparently been lost somehow.

218 ence with a slow carbon cycle cadence during Archean time.

219 ocks has increased by 10 to 15 per mil since Archean time.

220 emains untested through the vast majority of Archean time.

221 he reaction would have continued through the Archean to at least the early phases of the Great Oxidat

222 Growth of landmass in the late Archean to early Proterozoic Eons could have reorganized

223 ccount evidence from sulfur isotope data for Archean to early Proterozoic surface material in the dee

224 t full-vector paleointensity measurements of Archean to Hadean zircons bearing magnetic inclusions fr

225 sedimentary delta(56)Fe(pyrite) recorded in Archean to modern sediments.

226 arly monotonically by ~15 per mille from the Archean to present.

227 s resembling-but not always matching-natural Archean TTGs.

228 o determine the concentration of O(2) in the Archean upper atmosphere.

229 cks to track the bulk MgO composition of the Archean upper continental crust.

230 we show that these data imply that reducing Archean volcanic gases could have prevented atmospheric

231 enesis may have evolved during or before the Archean, when methane could have been key to Earth's ear

232 In the low-oxygen Archean world (>2400 million years ago), seawater sulfat