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1 pper and zinc cofactors (CuZnSOD) during the Archaean.
2 h the operation of subduction throughout the Archaean.
3 en the upper and lower atmosphere during the Archaean.
4 at of preceding and following periods in the Archaean.
5 ves, a single Gram-negative bacterium and an archaean.
6 ifferent crustal generation processes in the Archaean.
7 r to as the radA gene, for each of the three archaeans.
8 ent conditions and define two isochrons, one Archaean (2.95 Ga) and one Proterozoic (1.15 Ga).
9 in Western Australia, Earth's best-preserved Archaean (4.0-2.5 billion years ago (Ga)) continental re
10 lobal geodynamic regime operating during the Archaean (4.0-2.5 billion years ago [Ga]).
11 dered segments are found to occur in 2.0% of archaean, 4.2% of eubacterial and 33.0% of eukaryotic pr
12                                         This Archaean age for recycled oceanic crust also provides ke
13 (SG-3, 12,262 m depth) gold-bearing rocks of Archaean age have been located at depths of 9,500 to 11,
14 te magnetic inclusions capable of preserving Archaean-age magnetizations.
15 te was not in equilibrium with the oxygen in Archaean air and that its presence in palaeosols provide
16 on the partial pressure of carbon dioxide in Archaean air.
17 that carbon dioxide was abundant in the late Archaean and early Proterozoic atmosphere and that metha
18 ed blasts on Earth, however, extend into the Archaean and early Proterozoic eons, in the form of impa
19 mosphere's radiative balance during the late Archaean and early Proterozoic eons.
20 osited in the world's oceans during the late Archaean and early Proterozoic eras.
21                            However, although Archaean and Phanerozoic lithosphere differ in their thi
22 uggest oxygen fugacities similar to those of Archaean and present-day mantle-derived lavas as early a
23 rruginous sediment was widespread during the Archaean and Proterozoic Eons, playing an important role
24 positional and thickness differences between Archaean and Proterozoic lithosphere on deep-carbon flux
25                    In low-oxygen ferruginous Archaean and Proterozoic oceans, therefore, sedimentary
26 bacterial phyla trace their diversity to the Archaean and Proterozoic, and bacterial families prior t
27 ification of greenhouse gases present in the Archaean atmosphere is critical for understanding the ev
28 at place approximate concentration limits on Archaean atmospheric gases, including methane, carbon di
29 nomic analyses of 164 Viridiplantae and 2993 Archaean, bacterial, fungal, and Metazoan aquaporins rat
30                    Using an average enriched Archaean basaltic source composition, we predict Ba conc
31  continental Fe that may have contributed to Archaean BIF formation.
32 rganic carbon, differential transport in the Archaean biosphere would have had an effect just the opp
33 rare Earth element data from three different Archaean carbonate platforms preserved in greenstone bel
34 ow the extreme CO(2) levels required for hot Archaean climates.
35 r is thick ( approximately 150 km) under the Archaean core and tapers out on the surrounding Palaeozo
36 He/(4)He ratios as the rift transitions from Archaean (cratonic) to Proterozoic (orogenic) lithospher
37 tion from ancient crustal nuclei into mature Archaean cratons is unclear, primarily owing to the pauc
38                   The inference that not all Archaean crust developed a strong and thick thermal boun
39 -granodiorite magmatism and a thin preserved Archaean crust.
40                                          The Archaean diamond suite formed from relatively cool fluid
41 nised temporal and spatial biases within the Archaean-early-Palaeoproterozoic MSI record, we demonstr
42 D) of sun's ultraviolet C light by oxygen in Archaean earth's anoxic atmosphere followed by chirally
43 D of biomolecules and accepted magnitude for Archaean earth's magnetic field.
44 ce are consistent with clement conditions on Archaean Earth.
45 s cycle and evolved biologic activity on the Archaean Earth.
46 tic field where prebiotic life originated on Archaean earth.
47 tinental crust that can be dated back to the Archaean eon (4 billion to 2.5 billion years ago) compri
48 e 'Faint Young Sun' paradox, during the late Archaean eon a Sun approximately 20% dimmer warmed the e
49 wise atmospheric oxidation at the end of the Archaean eon provides a significant temporal link betwee
50 der strictly anaerobic conditions during the Archaean eon would have produced geochemical signals ide
51 rief period of genetic innovation during the Archaean eon, which coincides with a rapid diversificati
52 as not required to produce TTGs in the early Archaean eon.
53 med near the boundary of the Proterozoic and Archaean eons, some 2.5 Gyr ago, show many hallmarks of
54 d suggest that ocean temperatures during the Archaean era ( approximately 3.5 billion years ago) were
55            The Earth's atmosphere during the Archaean era (3,800-2,500 Myr ago) is generally thought
56 er analysed crustal sediments from the early Archaean era to the Recent epoch and find no systematic
57 he centres of continents which formed in the Archaean era, 4.0-2.5 Gyr ago.
58 cause the predominant sink for oxygen in the Archaean era-enhanced submarine volcanism-was abruptly a
59 age of oceanic mantle lithosphere during the Archaean era.
60 spheric oxygen fluctuated greatly during the Archaean era; (2) the atmosphere has remained oxic since
61 e composition of the lower atmosphere in the Archaean era; to date no method has been developed to sa
62                                          The archaeans examined were a hyperthermophilic acidophile,
63 unctional analysis of genes born during this Archaean expansion reveals that they are likely to be in
64 s found to infect Nanoarchaeota, a symbiotic archaean found in acidic hot springs of Yellowstone Nati
65 understand how changing heat flux influenced Archaean geodynamics, but records of systematic geochemi
66 ltramafic rocks provide a valuable record of Archaean geodynamics.
67 ssure-temperature conditions relevant to the Archaean geothermal gradient.
68 studies have shown that felsic rocks in both Archaean high-grade metamorphic ('grey gneiss') and low-
69 out geological history on earth, and ancient ARCHAEAN hydrothermal deposits could provide clues to un
70 ranite-greenstone complexes developing along Archaean intraoceanic island arcs by imbricate thrust-st
71                                 Rocks of the Archaean Kaapvaal craton (South Africa) are among the be
72 enesis(5), instead supporting a complexified-archaean, late-mitochondrion sequence for the assembly o
73  Australian soils are derived from weathered archaean laterite and are acidic and copper deficient.
74                  Genetic exchange within one Archaean lineage is a bit like sex in eukaryotes - cells
75 indicate that advection of the root of thick Archaean lithosphere laterally to the base of the much t
76  ocean-island basalts) as well as the hotter Archaean mantle (thereby allowing for early production o
77 consistent with a model in which high-degree Archaean mantle melting produced a thick, mafic lower cr
78 c crust that is predicted to have existed if Archaean mantle temperatures were much hotter than today
79 aline groundwater at 2.8 kilometers depth in Archaean metabasalt revealed a microbial biome dominated
80                             The methanogenic archaean Methanococcus maripaludis can use ammonia, alan
81 s meeting the criteria required of authentic Archaean microfossils, and contrast with other microfoss
82 rine sulfide deposits as evidence that early Archaean microorganisms were not sulfate reducers but in
83 least) many hundreds of millions of years in Archaean (more than 2.5 billion years old) cratonic rock
84                        Similarly, many early Archaean (more than 3,400-Myr-old) cherts have been rein
85  that molybdenum was bioavailable in the mid-Archaean ocean long before the Great Oxidation Event.
86 sitions of cherts, however, makes a case for Archaean ocean temperatures being no greater than 40 deg
87 ep origin and infer that it may be recycled, Archaean oceanic mantle lithosphere that has delaminated
88                                              Archaean oceans were depleted in deuterium [expressed as
89 n formation-never observed in earlier anoxic Archaean oceans-can be attributed to additional temperat
90 part of the Sclavia supercraton and that the Archaean onset of subduction occurred asynchronously wor
91 ersification of Eucarya occurred in the late Archaean or Proterozoic Eons when atmospheric oxygen lev
92 illion years ago (Ga), and currently suggest Archaean origins, approximately 3 Ga or earlier(3-9).
93 arbonate, as the mineral siderite, occurs in Archaean palaeosols (ancient soils).
94 f a permanently oxygenated atmosphere at the Archaean-Proterozoic transition (approximately 2.5 billi
95 of molecular oxygen (O(2)) shortly after the Archaean-Proterozoic transition 2.5 billion years ago wa
96 ruptly and permanently diminished during the Archaean-Proterozoic transition.
97 se in preserved crustal thickness across the Archaean/Proterozoic boundary, these data are consistent
98                                       If the Archaean raindrops reached the modern maximum measured s
99 ve remained stable, whereas some older (late Archaean) regions have been tectonically disturbed, sugg
100 we have shown that an engineered form of the Archaean replicative DNA polymerase 9 degrees N, known c
101 es of life in the highly metamorphosed Early Archaean rock record.
102     Abundant chert from weakly metamorphosed Archaean rocks might retain microscopic clues to the pro
103 m the amounts of organic carbon preserved in Archaean rocks, seem to require the sedimentation of an
104  and include the highest values reported for Archaean rocks.
105 ely anoxic and iron-rich as hypothesized for Archaean seas, nor fully oxic as supposed for most of th
106 the inferred presence of manganese oxides in Archaean sedimentary rocks.
107 dy of black cherts from weakly metamorphosed Archaean sediments.
108 n load largely comprises Mesoproterozoic and Archaean sources, whereas rutile and apatite are dominat
109 bit mass-independent effects, meteorites and Archaean terrestrial samples.
110 antle had a lower ferric to ferrous ratio in Archaean times than today nor that modern melting in the
111 hicknesses are thought to have existed since Archaean times(3,13-15).
112                                From the late Archaean to late Proterozoic eras (some 3-1 billion year
113 l and four non-model organisms, ranging from archaean to mammalian species.
114 s the prevalent anoxic basin states from the Archaean to present day, which are associated with diagn
115 respiration must have developed early in the Archaean to prevent a build-up of atmospheric oxygen bef
116 c diamond formation beneath Venetia from the Archaean to the Proterozoic.Dating of inclusions within
117 low Nb/Ta and high Zr/Sm ratios of 'average' Archaean TTG, but from a source with initially subchondr
118 and trace-element compositions equivalent to Archaean TTG, including the low Nb/Ta and high Zr/Sm rat
119 s, suggesting that the arc-like signature in Archaean TTGs was inherited from an ancestral source lin
120 e no method has been developed to sample the Archaean upper atmosphere.
121 heric micrometeorite oxidation suggests that Archaean upper-atmosphere oxygen concentrations may have
122 ial melting of the rock), whereas the older (Archaean), yet deformed, southern Basin and Range provin

 
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