ライフサイエンスコーパス: Archaean

1 en the upper and lower atmosphere during the Archaean.

2 at of preceding and following periods in the Archaean.

3 ves, a single Gram-negative bacterium and an archaean.

4 ifferent crustal generation processes in the Archaean.

5 r to as the radA gene, for each of the three archaeans.

6 ent conditions and define two isochrons, one Archaean (2.95 Ga) and one Proterozoic (1.15 Ga).

7 dered segments are found to occur in 2.0% of archaean, 4.2% of eubacterial and 33.0% of eukaryotic pr

8 This Archaean age for recycled oceanic crust also provides ke

9 te magnetic inclusions capable of preserving Archaean-age magnetizations.

10 te was not in equilibrium with the oxygen in Archaean air and that its presence in palaeosols provide

11 on the partial pressure of carbon dioxide in Archaean air.

12 that carbon dioxide was abundant in the late Archaean and early Proterozoic atmosphere and that metha

13 ed blasts on Earth, however, extend into the Archaean and early Proterozoic eons, in the form of impa

14 mosphere's radiative balance during the late Archaean and early Proterozoic eons.

15 osited in the world's oceans during the late Archaean and early Proterozoic eras.

16 However, although Archaean and Phanerozoic lithosphere differ in their thi

17 uggest oxygen fugacities similar to those of Archaean and present-day mantle-derived lavas as early a

18 ification of greenhouse gases present in the Archaean atmosphere is critical for understanding the ev

19 at place approximate concentration limits on Archaean atmospheric gases, including methane, carbon di

20 rganic carbon, differential transport in the Archaean biosphere would have had an effect just the opp

21 ow the extreme CO(2) levels required for hot Archaean climates.

22 r is thick ( approximately 150 km) under the Archaean core and tapers out on the surrounding Palaeozo

23 The inference that not all Archaean crust developed a strong and thick thermal boun

24 -granodiorite magmatism and a thin preserved Archaean crust.

25 The Archaean diamond suite formed from relatively cool fluid

26 D) of sun's ultraviolet C light by oxygen in Archaean earth's anoxic atmosphere followed by chirally

27 D of biomolecules and accepted magnitude for Archaean earth's magnetic field.

28 tic field where prebiotic life originated on Archaean earth.

29 ce are consistent with clement conditions on Archaean Earth.

30 s cycle and evolved biologic activity on the Archaean Earth.

31 tinental crust that can be dated back to the Archaean eon (4 billion to 2.5 billion years ago) compri

32 e 'Faint Young Sun' paradox, during the late Archaean eon a Sun approximately 20% dimmer warmed the e

33 wise atmospheric oxidation at the end of the Archaean eon provides a significant temporal link betwee

34 rief period of genetic innovation during the Archaean eon, which coincides with a rapid diversificati

35 as not required to produce TTGs in the early Archaean eon.

36 med near the boundary of the Proterozoic and Archaean eons, some 2.5 Gyr ago, show many hallmarks of

37 d suggest that ocean temperatures during the Archaean era ( approximately 3.5 billion years ago) were

38 The Earth's atmosphere during the Archaean era (3,800-2,500 Myr ago) is generally thought

39 er analysed crustal sediments from the early Archaean era to the Recent epoch and find no systematic

40 he centres of continents which formed in the Archaean era, 4.0-2.5 Gyr ago.

41 cause the predominant sink for oxygen in the Archaean era-enhanced submarine volcanism-was abruptly a

42 age of oceanic mantle lithosphere during the Archaean era.

43 spheric oxygen fluctuated greatly during the Archaean era; (2) the atmosphere has remained oxic since

44 e composition of the lower atmosphere in the Archaean era; to date no method has been developed to sa

45 The archaeans examined were a hyperthermophilic acidophile,

46 unctional analysis of genes born during this Archaean expansion reveals that they are likely to be in

47 understand how changing heat flux influenced Archaean geodynamics, but records of systematic geochemi

48 ltramafic rocks provide a valuable record of Archaean geodynamics.

49 studies have shown that felsic rocks in both Archaean high-grade metamorphic ('grey gneiss') and low-

50 out geological history on earth, and ancient ARCHAEAN hydrothermal deposits could provide clues to un

51 ranite-greenstone complexes developing along Archaean intraoceanic island arcs by imbricate thrust-st

52 Rocks of the Archaean Kaapvaal craton (South Africa) are among the be

53 Australian soils are derived from weathered archaean laterite and are acidic and copper deficient.

54 Genetic exchange within one Archaean lineage is a bit like sex in eukaryotes - cells

55 ocean-island basalts) as well as the hotter Archaean mantle (thereby allowing for early production o

56 consistent with a model in which high-degree Archaean mantle melting produced a thick, mafic lower cr

57 c crust that is predicted to have existed if Archaean mantle temperatures were much hotter than today

58 aline groundwater at 2.8 kilometers depth in Archaean metabasalt revealed a microbial biome dominated

59 The methanogenic archaean Methanococcus maripaludis can use ammonia, alan

60 s meeting the criteria required of authentic Archaean microfossils, and contrast with other microfoss

61 rine sulfide deposits as evidence that early Archaean microorganisms were not sulfate reducers but in

62 least) many hundreds of millions of years in Archaean (more than 2.5 billion years old) cratonic rock

63 Similarly, many early Archaean (more than 3,400-Myr-old) cherts have been rein

64 that molybdenum was bioavailable in the mid-Archaean ocean long before the Great Oxidation Event.

65 sitions of cherts, however, makes a case for Archaean ocean temperatures being no greater than 40 deg

66 ep origin and infer that it may be recycled, Archaean oceanic mantle lithosphere that has delaminated

67 Archaean oceans were depleted in deuterium [expressed as

68 ersification of Eucarya occurred in the late Archaean or Proterozoic Eons when atmospheric oxygen lev

69 arbonate, as the mineral siderite, occurs in Archaean palaeosols (ancient soils).

70 f a permanently oxygenated atmosphere at the Archaean-Proterozoic transition (approximately 2.5 billi

71 ruptly and permanently diminished during the Archaean-Proterozoic transition.

72 se in preserved crustal thickness across the Archaean/Proterozoic boundary, these data are consistent

73 If the Archaean raindrops reached the modern maximum measured s

74 ve remained stable, whereas some older (late Archaean) regions have been tectonically disturbed, sugg

75 we have shown that an engineered form of the Archaean replicative DNA polymerase 9 degrees N, known c

76 es of life in the highly metamorphosed Early Archaean rock record.

77 Abundant chert from weakly metamorphosed Archaean rocks might retain microscopic clues to the pro

78 m the amounts of organic carbon preserved in Archaean rocks, seem to require the sedimentation of an

79 and include the highest values reported for Archaean rocks.

80 ely anoxic and iron-rich as hypothesized for Archaean seas, nor fully oxic as supposed for most of th

81 dy of black cherts from weakly metamorphosed Archaean sediments.

82 bit mass-independent effects, meteorites and Archaean terrestrial samples.

83 From the late Archaean to late Proterozoic eras (some 3-1 billion year

84 l and four non-model organisms, ranging from archaean to mammalian species.

85 respiration must have developed early in the Archaean to prevent a build-up of atmospheric oxygen bef

86 c diamond formation beneath Venetia from the Archaean to the Proterozoic.Dating of inclusions within

87 low Nb/Ta and high Zr/Sm ratios of 'average' Archaean TTG, but from a source with initially subchondr

88 and trace-element compositions equivalent to Archaean TTG, including the low Nb/Ta and high Zr/Sm rat

89 s, suggesting that the arc-like signature in Archaean TTGs was inherited from an ancestral source lin

90 e no method has been developed to sample the Archaean upper atmosphere.

91 heric micrometeorite oxidation suggests that Archaean upper-atmosphere oxygen concentrations may have

92 ial melting of the rock), whereas the older (Archaean), yet deformed, southern Basin and Range provin