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Journal articles on the topic 'Archaean'

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Published: 4 June 2021
Last updated: 20 February 2023

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1

Sleep, Norman H. "Archaean palaeosols and Archaean air." Nature 432, no. 7016 (November 2004): 1. http://dx.doi.org/10.1038/nature03167.

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2

Ohmoto, Hiroshi, and Yumiko Watanabe. "Archaean palaeosols and Archaean air (reply)." Nature 432, no. 7016 (November 2004): 1–2. http://dx.doi.org/10.1038/nature03168.

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3

Sandaa, Ruth-Anne, Øivind Enger, and Vigdis Torsvik. "Abundance and Diversity of Archaea in Heavy-Metal-Contaminated Soils." Applied and Environmental Microbiology 65, no. 8 (August 1, 1999): 3293–97. http://dx.doi.org/10.1128/aem.65.8.3293-3297.1999.

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ABSTRACT The impact of heavy-metal contamination on archaean communities was studied in soils amended with sewage sludge contaminated with heavy metals to varying extents. Fluorescent in situ hybridization showed a decrease in the percentage of Archaea from 1.3% ± 0.3% of 4′,6-diamidino-2-phenylindole-stained cells in untreated soil to below the detection limit in soils amended with heavy metals. A comparison of the archaean communities of the different plots by denaturing gradient gel electrophoresis revealed differences in the structure of the archaean communities in soils with increasing heavy-metal contamination. Analysis of cloned 16S ribosomal DNA showed close similarities to a unique and globally distributed lineage of the kingdom Crenarchaeota that is phylogenetically distinct from currently characterized crenarchaeotal species.
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4

Herzberg, Claude. "Archaean drips." Nature Geoscience 7, no. 1 (December 1, 2013): 7–8. http://dx.doi.org/10.1038/ngeo2033.

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5

WINDLEY, B. "Archaean Geochemistry." Earth-Science Reviews 24, no. 1 (March 1987): 67. http://dx.doi.org/10.1016/0012-8252(87)90051-1.

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6

Imachi, Hiroyuki, Masaru K. Nobu, Nozomi Nakahara, Yuki Morono, Miyuki Ogawara, Yoshihiro Takaki, Yoshinori Takano, et al. "Isolation of an archaeon at the prokaryote–eukaryote interface." Nature 577, no. 7791 (January 15, 2020): 519–25. http://dx.doi.org/10.1038/s41586-019-1916-6.

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Abstract The origin of eukaryotes remains unclear1–4. Current data suggest that eukaryotes may have emerged from an archaeal lineage known as ‘Asgard’ archaea5,6. Despite the eukaryote-like genomic features that are found in these archaea, the evolutionary transition from archaea to eukaryotes remains unclear, owing to the lack of cultured representatives and corresponding physiological insights. Here we report the decade-long isolation of an Asgard archaeon related to Lokiarchaeota from deep marine sediment. The archaeon—‘Candidatus Prometheoarchaeum syntrophicum’ strain MK-D1—is an anaerobic, extremely slow-growing, small coccus (around 550 nm in diameter) that degrades amino acids through syntrophy. Although eukaryote-like intracellular complexes have been proposed for Asgard archaea6, the isolate has no visible organelle-like structure. Instead, Ca. P. syntrophicum is morphologically complex and has unique protrusions that are long and often branching. On the basis of the available data obtained from cultivation and genomics, and reasoned interpretations of the existing literature, we propose a hypothetical model for eukaryogenesis, termed the entangle–engulf–endogenize (also known as E3) model.
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7

Cockell, Charles S. "Photobiological uncertainties in the Archaean and post-Archaean world." International Journal of Astrobiology 1, no. 1 (January 2002): 31–38. http://dx.doi.org/10.1017/s1473550402001003.

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The notion that ultraviolet (UV) fluxes, and thus biologically weighted irradiances, were higher on Archaean Earth than on present-day Earth has been a pervasive influence on thinking concerning the nature of early Earth. It directly influences calculations concerning protection strategies that may or may not have been required by early life. Our knowledge of the Earth's changing UV radiation climate over time depends upon our knowledge of a diversity of factors, the magnitudes of which are uncertain. Here these uncertainties are explored. During the Archaean Era, calculations of the surface photobiological environment span a three order of magnitude difference in DNA-damage weighted irradiances with consequences for our assumptions concerning the environment for exposed surface life and the role of UV radiation as a mutagen. These differences are primarily caused by uncertainties in the concentrations of trace gases and the partial pressures of carbon dioxide and nitrogen that affect scattering in the atmosphere. To a lesser extent, the luminosity of the Sun in the UV region is also a factor. During the Proterozoic and Phanerozoic, when we know that an ozone column existed, these uncertainties drop to two orders of magnitude and are primarily caused by poor knowledge about the frequency and atmospheric effects of potentially ozone-depleting agents such as volcanism, impact events and supernovae explosions as well as the effects of global temperatures on ozone concentrations and thus surface UV irradiance. Changes in other atmospheric constituents during this time have less of an effect on photobiological consequences, which include a Palaeozoic oxygen pulse. Understanding the cause of photobiological uncertainties and their consequences constitutes a current challenge for atmospheric chemists and photobiologists.
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8

Hattori, Keiko, and Eion M. Cameron. "Archaean magmatic sulphate." Nature 319, no. 6048 (January 1986): 45–47. http://dx.doi.org/10.1038/319045a0.

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9

Rollinson, Hugh, and Martin Whitehouse. "Archaean crustal evolution." Precambrian Research 112, no. 1-2 (November 2001): 1–3. http://dx.doi.org/10.1016/s0301-9268(01)00167-x.

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10

Chin, G. J. "MICROBIOLOGY: Archaean Viruses." Science 294, no. 5544 (November 2, 2001): 959e—961. http://dx.doi.org/10.1126/science.294.5544.959e.

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11

Roberts, D. E. "Archaean Geochemistry: the Origin and Evolution of the Archaean Continental Crust." Precambrian Research 34, no. 3-4 (January 1987): 376–78. http://dx.doi.org/10.1016/0301-9268(87)90011-8.

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12

Kramers, J. D. "Archaean geochemistry: The origin and evolution of the archaean continental crust." Chemical Geology 56, no. 3-4 (October 1986): 336–37. http://dx.doi.org/10.1016/0009-2541(86)90015-x.

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13

Bridgwater, David. "Archaean Geochemistry. The Origin and Evolution of the Archaean Continental Crust." Geochimica et Cosmochimica Acta 50, no. 9 (September 1986): 2119. http://dx.doi.org/10.1016/0016-7037(86)90265-6.

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14

Long, Xi, Hong Xue, and J. Tze-Fei Wong. "Descent of Bacteria and Eukarya From an Archaeal Root of Life." Evolutionary Bioinformatics 16 (January 2020): 117693432090826. http://dx.doi.org/10.1177/1176934320908267.

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The 3 biological domains delineated based on small subunit ribosomal RNAs (SSU rRNAs) are confronted by uncertainties regarding the relationship between Archaea and Bacteria, and the origin of Eukarya. The similarities between the paralogous valyl-tRNA and isoleucyl-tRNA synthetases in 5398 species estimated by BLASTP, which decreased from Archaea to Bacteria and further to Eukarya, were consistent with vertical gene transmission from an archaeal root of life close to Methanopyrus kandleri through a Primitive Archaea Cluster to an Ancestral Bacteria Cluster, and to Eukarya. The predominant similarities of the ribosomal proteins (rProts) of eukaryotes toward archaeal rProts relative to bacterial rProts established that an archaeal parent rather than a bacterial parent underwent genome merger with bacteria to generate eukaryotes with mitochondria. Eukaryogenesis benefited from the predominantly archaeal accelerated gene adoption (AGA) phenotype pertaining to horizontally transferred genes from other prokaryotes and expedited genome evolution via both gene-content mutations and nucleotidyl mutations. Archaeons endowed with substantial AGA activity were accordingly favored as candidate archaeal parents. Based on the top similarity bitscores displayed by their proteomes toward the eukaryotic proteomes of Giardia and Trichomonas, and high AGA activity, the Aciduliprofundum archaea were identified as leading candidates of the archaeal parent. The Asgard archaeons and a number of bacterial species were among the foremost potential contributors of eukaryotic-like proteins to Eukarya.
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15

Sleep, N. H. "The Hadean-Archaean Environment." Cold Spring Harbor Perspectives in Biology 2, no. 6 (May 5, 2010): a002527. http://dx.doi.org/10.1101/cshperspect.a002527.

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16

Kasting, James F. "Archaean atmosphere and climate." Nature 432, no. 7016 (November 2004): 1. http://dx.doi.org/10.1038/nature03166.

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17

Ebinger, Cindy. "Archaean atmosphere and lithosphere." Astronomy and Geophysics 41, no. 3 (June 2000): 3.27–3.28. http://dx.doi.org/10.1046/j.1468-4004.2000.00327.x.

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18

Nisbetand, E. G., and T. K. Kyser. "Archaean carbon and gold." Nature 331, no. 6153 (January 1988): 210–11. http://dx.doi.org/10.1038/331210b0.

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19

VAN SCHMUS, W. R. "Crustal Geochemistry: Archaean Geochemistry." Science 231, no. 4739 (February 14, 1986): 751–52. http://dx.doi.org/10.1126/science.231.4739.751.

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20

Gomes, Maya L. "An Archaean oxygen oasis." Nature Geoscience 11, no. 2 (January 15, 2018): 84–85. http://dx.doi.org/10.1038/s41561-018-0058-z.

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21

Parman, Stephen. "An Archaean mushy mantle." Nature Geoscience 11, no. 2 (January 22, 2018): 85–86. http://dx.doi.org/10.1038/s41561-018-0060-5.

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22

Johnson, Benjamin W., and Boswell A. Wing. "Limited Archaean continental emergence reflected in an early Archaean 18O-enriched ocean." Nature Geoscience 13, no. 3 (March 2020): 243–48. http://dx.doi.org/10.1038/s41561-020-0538-9.

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23

Pearson, D. G., G. A. Snyder, S. B. Shirey, L. A. Taylor, R. W. Carlson, and N. V. Sobolev. "Archaean Re–Os age for Siberian eclogites and constraints on Archaean tectonics." Nature 374, no. 6524 (April 1995): 711–13. http://dx.doi.org/10.1038/374711a0.

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24

Bridgwater, D., and L. Schiøtte. "The Archaean gneiss complex of northern Labrador A review of current results, ideas and problems." Bulletin of the Geological Society of Denmark 39 (December 20, 1991): 153–66. http://dx.doi.org/10.37570/bgsd-1991-39-06.

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1. The early Archaean rocks in northern Labrador can be subdivided into the ea. 3.78 Ga Nulliak supracrus­tal association, the migmatitic Uivak I gneisses, the dominant phase of which was emplaced at ea. 3.73 Ga, and the Uivak II augen gneiss. Inherited low-U rounded inclusions within igneous zircons in the Uivak I gneisses have ages between 3.73 and 3.86 Ga and are more likely to have been derived from a pre-existing high-grade metamorphic gneiss complex than from the Nulliak association. In the early Archaean there were probably several rapid cycles of sedimentary deposition and volcanism followed by emplacement of major plutons. Mid Archaean gneisses are more abundant in northern Labrador than previously realised. The late Archaean metamorphic history of these gneisses is different from the history of the early Archaean gneisses. Whereas an important part of the mid Archaean suite was emplaced in granulite facies and retrogressed at the time of granitoid veining at ea. 2.99 Ga, the major part of the early Archaean rocks were reworked under granulite facies conditions in a sequence of closely spaced events between 2. 7 and 2.8 Ga. The two groups of gneisses had different metamorphic histories until ea. 2.7 Ga, but late and post-tectonic granites of 2.5- 2. 7 Ga age cut across both. It is suggested that the terrane model in southern West Greenland can be extended to Labrador and that tectonic intercalation of early and mid Archaean gneisses took place around 2.7 Ga. Correlation between the Maggo gneisses around Hopedale, mid Archaean gneisses in northernmost Labrador and gneisses from the Akia terrane in West Greenland is suggested. Like the Malene supracrustals in West Greenland the Upernavik supracrustals in Labrador are composite associations, the youngest of which are thought to have been deposited around 2. 7 Ga.
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25

BOGATYREVA, NATALYA S., ALEXEI V. FINKELSTEIN, and OXANA V. GALZITSKAYA. "TREND OF AMINO ACID COMPOSITION OF PROTEINS OF DIFFERENT TAXA." Journal of Bioinformatics and Computational Biology 04, no. 02 (April 2006): 597–608. http://dx.doi.org/10.1142/s0219720006002016.

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Archaea, bacteria and eukaryotes represent the main kingdoms of life. Is there any trend for amino acid compositions of proteins found in full genomes of species of different kingdoms? What is the percentage of totally unstructured proteins in various proteomes? We obtained amino acid frequencies for different taxa using 195 known proteomes and all annotated sequences from the Swiss–Prot data base. Investigation of the two data bases (proteomes and Swiss–Prot) shows that the amino acid compositions of proteins differ substantially for different kingdoms of life, and this difference is larger between different proteomes than between different kingdoms of life. Our data demonstrate that there is a surprisingly small selection for the amino acid composition of proteins for higher organisms (eukaryotes) and their viruses in comparison with the "random" frequency following from a uniform usage of codons of the universal genetic code. On the contrary, lower organisms (bacteria and especially archaea) demonstrate an enhanced selection of amino acids. Moreover, according to our estimates, 12%, 3% and 2% of the proteins in eukaryotic, bacterial and archaean proteomes are totally disordered, and long (> 41 residues) disordered segments are found to occur in 16% of arhaean, 20% of eubacterial and 43% of eukaryotic proteins for 19 archaean, 159 bacterial and 17 eukaryotic proteomes, respectively. A correlation between amino acid compositions of proteins of various taxa, show that the highest correlation is observed between eukaryotes and their viruses (the correlation coefficient is 0.98), and bacteria and their viruses (the correlation coefficient is 0.96), while correlation between eukaryotes and archaea is 0.85 only.
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26

Halla, Jaana. "Highlights on Geochemical Changes in Archaean Granitoids and Their Implications for Early Earth Geodynamics." Geosciences 8, no. 9 (September 17, 2018): 353. http://dx.doi.org/10.3390/geosciences8090353.

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The Archaean (4.0–2.5 Ga) continental crust is mainly composed of granitoids, whose geochemical characteristics are a function of their formation mechanisms and components, as well as physical conditions of their source. Therefore, revealing changes in Archaean geodynamic processes requires understanding of geochemical changes in Archaean granitoids. This paper compares key geochemical signatures in granitoid occurrences from the Eoarchaean to Neoarchaean Eras and aims to highlight changes or variations in their geochemical signatures. The study is performed by exploring and comparing geochemical and geochronological datasets of Archaean granitoids compiled from literature. The results show that two end-members of sodic TTGs (tonalite–trondhjemite–granodiorite) occur throughout the Archaean: low- and high-HREE (heavy rare earth elements) types. A profound change in granitoid geochemistry occurred between 3.0 and 2.5 Ga when multi-source high-K calc-alkaline granitoid batholiths emerged, possibly indicating the onset of modern-type plate tectonics.
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27

Shestakov, Sergey V. "The role of archaea in the origin of eukaryotes." Ecological genetics 15, no. 4 (December 25, 2017): 52–59. http://dx.doi.org/10.17816/ecogen15452-59.

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A key role of particular evolutionary branch of archaea in the emergence of eukaryotic cell is considered on the basis of phylogenomics. Genomes of recently discovered uncultivated proteoarchaea belonging to Lokiarchaea and Asgard-group contain a large sets of eukaryotic-like genes. This allows to suggest that ancient forms of such archaean could participate in symbiotic fusion with bacteria serving as a mitochondrial progenitor. The open questions concerning properties of LECA (so-called last eukaryotic common ancestor) are discussed in the frame of endosymbiotic hypothesis of eukaryogenesis.
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28

Andersson, U. B., L. A. Neymark, and K. Billström. "Petrogenesis of Mesoproterozoic (Subjotnian) rapakivi complexes of central Sweden: implications from U–Pb zircon ages, Nd, Sr and Pb isotopes." Transactions of the Royal Society of Edinburgh: Earth Sciences 92, no. 3 (September 2001): 201–28. http://dx.doi.org/10.1017/s0263593300000237.

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ABSTRACTU-Pb zircon geochronology of Mesoproterozoic (Subjotnian) rapakivi complexes in central Sweden yields: 1526 ± 3 Ma (Mullnäset), 1524 ± 3 Ma (Mårdsjö), 1520 ± 3 Ma (Nordsjö) and 1497 ± 6 Ma (Rödön). Together with complexes further S in Sweden, they constitute the westernmost, youngest (1·53−1·47 Ga) belt of rapakivi magmatism in the Fennoscandian shield.The low initial εNd values (−8·9 to −4·8) of all studied Subjotnian basic, intermediate and silicic rocks, require an input from an old (Archaean) low-radiogenic source component, as evidence for Palaeoproterozoic protoliths in the age range 2·5−2·1 Ga is lacking in this region. Crustal, early Svecofennian + Archaean (roughly 30−40%) sources are suggested for the Subjotnian A-type granites and syenites, where the granites derive from undepleted, granodioritic, and the syenites from monzodioritic (±depleted crustal) protoliths. The basic rocks originate from a depleted mantle acquiring the enriched Nd isotopic signatures during interaction with an Archaean lower crust (20−40%), largely depleted after rapakivi melt extraction. Pb isotope data from feldspars (207Pb/204Pb to 15·018−15·542) support the presence of Archaean components in the magmas.The results indicate that an Archaean basement is underlying relatively wide areas of Svecofennian formations in central Sweden. This old basement section was most likely rifted off the Archaean craton in the NE in Palaeoproterozoic times.
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29

Wang, Yinzhao, Ruize Xie, Jialin Hou, Zhenbo Lv, Liuyang Li, Yaoxun Hu, Hungchia Huang, and Fengping Wang. "The late Archaean to early Proterozoic origin and evolution of anaerobic methane‐oxidizing archaea." mLife 1, no. 1 (March 2022): 96–100. http://dx.doi.org/10.1002/mlf2.12013.

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30

Baofeng, Shen, Peng Xiaoliang, Luo Hui, and Mao Debao. "Archaean Greenstone Belts in China." Acta Geologica Sinica - English Edition 7, no. 1 (May 29, 2009): 15–29. http://dx.doi.org/10.1111/j.1755-6724.1994.mp7001002.x.

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31

Nutman, A. P., and K. Ehlers. "Archaean crust near Broken Hill?" Australian Journal of Earth Sciences 45, no. 5 (October 1998): 687–94. http://dx.doi.org/10.1080/08120099808728426.

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32

de Wit, Maarten J., Cornel E. J. de Ronde, Marian Tredoux, Chris Roering, Rodger J. Hart, Richard A. Armstrong, Rod W. E. Green, Ellie Peberdy, and Roger A. Hart. "Formation of an Archaean continent." Nature 357, no. 6379 (June 1992): 553–62. http://dx.doi.org/10.1038/357553a0.

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33

Nisbet, E. G. "Igneous petrology: Archaean mantle models." Nature 320, no. 6060 (March 1986): 306–7. http://dx.doi.org/10.1038/320306a0.

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34

Towe, Kenneth M. "Aerobic respiration in the Archaean?" Nature 348, no. 6296 (November 1990): 54–56. http://dx.doi.org/10.1038/348054a0.

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35

de Wit, Maarten, and Christien Thiart. "Metallogenic fingerprints of Archaean cratons." Geological Society, London, Special Publications 248, no. 1 (2005): 59–70. http://dx.doi.org/10.1144/gsl.sp.2005.248.01.03.

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36

Nisbet, Euan. "The realms of Archaean life." Nature 405, no. 6787 (June 2000): 625–26. http://dx.doi.org/10.1038/35015187.

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37

Schopf, J. William. "Fossil evidence of Archaean life." Philosophical Transactions of the Royal Society B: Biological Sciences 361, no. 1470 (May 9, 2006): 869–85. http://dx.doi.org/10.1098/rstb.2006.1834.

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Evidence for the existence of life during the Archaean segment of Earth history (more than 2500 Myr ago) is summarized. Data are presented for 48 Archaean deposits reported to contain biogenic stromatolites, for 14 such units reported to contain 40 morphotypes of putative microfossils, and for 13 especially ancient, 3200–3500 Myr old geologic units for which available organic geochemical data are also summarized. These compilations support the view that life's existence dates from more than or equal to 3500 Myr ago.
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38

Smithies, R. Hugh, David C. Champion, and Shen-Su Sun. "The case for Archaean boninites." Contributions to Mineralogy and Petrology 147, no. 6 (July 13, 2004): 705–21. http://dx.doi.org/10.1007/s00410-004-0579-x.

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39

Jansson, B. P. Mattias, Laurence Malandrin, and Hans E. Johansson. "Cell Cycle Arrest in Archaea by the Hypusination Inhibitor N1-Guanyl-1,7-Diaminoheptane." Journal of Bacteriology 182, no. 4 (February 15, 2000): 1158–61. http://dx.doi.org/10.1128/jb.182.4.1158-1161.2000.

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ABSTRACT Hypusination is an essential posttranslational modification unique to archaeal and eukaryotic protein synthesis initiation factor 5A (aIF5A and eIF5A, respectively). We have investigated the effect of the efficient hypusination inhibitorN 1-guanyl-1,7-diaminoheptane (GC7) on four archaeal and one bacterial species. We found that (i) archaea are sensitive to GC7, whereas the bacteriumEscherichia coli is not, (ii) GC7 causes rapid and reversible arrest of growth of the archaeon Sulfolobus acidocaldarius, and (iii) the growth arrest is accompanied by a specific reversible arrest of the cell cycle prior to cell division. Our findings establish a link between hypusination and sustained growth of archaea and thereby provide the framework to study molecular details of archaeal cell cycle in connection with in vivo functions of hypusine and of aIF5A and eIF5A.
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40

Nutman, Allen P. "Tectonostratigraphic terranes within Archaean gneiss complexes: examples from Western Australia and southern West Greenland." Bulletin of the Geological Society of Denmark 39 (December 20, 1991): 199–211. http://dx.doi.org/10.37570/bgsd-1991-39-09.

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New field work and isotopic data show that the Godthabsfjord region of West Greenland consists of a collage of tectonostratigraphic terranes, which evolved separately prior to tectonic juxtaposition in the late Archaean. In Western Australia the Narryer Gneiss Complex, which lies on the northwestern margin of the Yilgarn Craton, is, unlike the Godthabsfjord region, very poorly exposed (less than 1 % ). In consequence it is impossible to follow geological boundaries in this complex, and instead the complex has been studied by a very extensive use of within-grain zircon U-Pb geochronology on the ion microprobe SHRIMP. The zircon geochronology suggests that the Narryer Gneiss Complex also consists of several discrete terranes of early to mid Archaean gneisses. In both the Godthabsfjord region and the Narryer Gneiss Complex, late Archaean juxtaposition of terranes was accompanied by intrusion of crustally­derived granites, deformation, and amphibolite facies metamorphism. Thus some Archaean high grade gneiss complexes consist of terranes that underwent independent evolution until they were brought together at a later time. In this respect their anatomy resembles post-Archaean orogenic belts that formed as a consequence of plate tectonic processes.
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41

Kalsbeek, F. "The tectonic framework of the Precambrian shield of Greenland A review of new isotopic evidence." Rapport Grønlands Geologiske Undersøgelse 128 (December 31, 1986): 55–64. http://dx.doi.org/10.34194/rapggu.v128.7924.

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There is now reliable isotopic evidence that most of the crystalline basement of Greenland consists of Archaean (>2500 Ma) rocks: only in the Ketilidian mobile belt of southemmost Greenland no Archaean rocks have yet been found. Proterozoic orogenic activity was widespread in the Nagssugtoqidian and Rinkian mobile belts of central and northem West Greenland, and peaked at c. 1850 Ma. There is some evidence that the Nagssugtoqidian mobile belt may define the boundary between two once separate Archaean continental plates and it is possibie that comparable plate boundaries also exist elsewhere in Greenland.
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42

Schiøtte, L., A. P. Nutman, and D. Bridgwater. "U–Pb ages of single zircons within "Upernavik" metasedimentary rocks and regional implications for the tectonic evolution of the Archaean Nain Province, Labrador." Canadian Journal of Earth Sciences 29, no. 2 (February 1, 1992): 260–76. http://dx.doi.org/10.1139/e92-024.

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Detrital zircons and their postdepositional overgrowths from three units of the "Upernavik" supracrustal association in the northern (Saglek) block of the Archaean Nain Province have been dated with the ion microprobe SHRIMP. In one unit, from the granulite-facies area in inner Saglek Fiord, the zircon population is dominated by early Archaean grains thought to be derived from the Uivak gneisses. Recrystallization and growth of new zircon within this metasediment took place during granulite-facies metamorphism at 2761 ± 12 Ma (2σ), which is also a younger limit on the age of deposition.In a second unit, from the amphibolite-facies area in outer Saglek Fiord, detrital zircons have predominantly mid- and late Archaean ages. The mid-Archaean zircons are comparable in age to the 3235 Ma Lister gneisses. The ages of the late Archaean detrital zircons (2800–2960 Ma) do not correspond to any known rock complex in the Saglek block, but plutonic rocks associated or correlative with the ca. 2840 Ma Kanairiktok Plutonic Suite of the southern (Hopedale) block are a possible source for many of the grains. Overgrowths were dated at 2690–2730 Ma in this sample.A third metasedimentary unit from the Okak Bay area, 100 km south of Saglek Fiord, also contains detrital zircons with ages comparable to that of the Lister gneisses (3235 Ma). The age of recrystallization and zircon overgrowths was dated at ca. 2560 Ma in this sample. A single grain dated at ca. 2780 Ma is considered most likely to be detrital, which would imply an age of deposition between ca. 2780 and 2560 Ma for this unit.The results show that although late Archaean depositional ages are possible for all three units, the "Upernavik" supracrustal association is composite and sediments in different units have widely different sources and metamorphic histories. These conclusions support a new model for the Nain Province according to which separate terranes were tectonically juxtaposed in the late Archaean. In this model, the age of plutonic and supracrustal rocks and their metamorphic histories prior to juxtaposition differ from one terrane to another.
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43

Wilks, M. E., and E. G. Nisbet. "Stratigraphy of the Steep Rock Group, northwest Ontario: a major Archaean unconformity and Archaean stromatolites." Canadian Journal of Earth Sciences 25, no. 3 (March 1, 1988): 370–91. http://dx.doi.org/10.1139/e88-040.

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The Archaean Steep Rock Group of northwest Ontario, situated in the Wabigoon Subprovince of the Superior Province, Canada, comprises five formations: Wagita Formation (clastics), Mosher Carbonate, Jolliffe Ore Zone, Dismal Ashrock, and Witch Bay Formation (metavolcanics). Reinvestigation of the geology of the group has shown that the basal clastics of the Wagita Formation (0–150 m) unconformably overlie the Marmion Complex (a massive tonalite – tonalite gneiss terrane, 3 Ga old). Overlying the basal elastics is the Mosher Carbonate (0–500 m), containing diverse stromatolite morphologies. Extensive zones of carbonate breccia occur adjacent to fault zones and mafic dykes. Stratigraphically above the Mosher Carbonate is the Jolliffe Ore Zone (100–400 m), which is divided into a lower Manganiferous Paint Rock Member and an upper Goethite Member. Within the Jolliffe Ore Zone thin layers of "Buckshot Ore" occur. These are horizons of haematitic pisolites and fragments, set in a lighter ferruginous matrix of kaolinite and gibbsite. Overlying the Jolliffe Ore Zone is the Dismal Ashrock, a dominantly high-Mg pyroclastic rock (22% MgO) with minor interbedded lava flows (15% MgO). In contact with the Dismal Ashrock are the metavolcanics of the Witch Bay Formation. This juxtaposition is not exposed in the Steep Rock mine section, and the Witch Bay Formation may be separated from the Dismal Ashrock by a structural break. The Witch Bay Formation is only provisionally included in the Steep Rock Group.The group is interpreted as a sequence deposited in an extensional or rifting environment. The unconformity has regional significance, and it may be possible to define an extensive cratonic nucleus of 3 Ga or older age in northwest Ontario.
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44

Nisbet, E. G., and C. M. R. Fowler. "Archaean metabolic evolution of microbial mats." Proceedings of the Royal Society of London. Series B: Biological Sciences 266, no. 1436 (December 7, 1999): 2375–82. http://dx.doi.org/10.1098/rspb.1999.0934.

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45

Williams, Neil. "Archaean gold: Exploring for magmatic origins." Nature 321, no. 6073 (June 1986): 812. http://dx.doi.org/10.1038/321812a0.

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46

HENDERSON–SELLERS, A., and B. HENDERSON–SELLERS. "Equable climate in the early Archaean." Nature 336, no. 6195 (November 1988): 117–18. http://dx.doi.org/10.1038/336117b0.

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47

Walker, James C. G. "Was the Archaean biosphere upside down?" Nature 329, no. 6141 (October 1987): 710–12. http://dx.doi.org/10.1038/329710a0.

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48

Snyder, David B. "Imaging Archaean-age whole mineral systems." Precambrian Research 229 (May 2013): 125–32. http://dx.doi.org/10.1016/j.precamres.2011.10.016.

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49

Zadnik, M. G., and P. M. Jeffery. "Radiogenic neon in an Archaean anorthosite." Chemical Geology: Isotope Geoscience section 52, no. 1 (April 1985): 119–25. http://dx.doi.org/10.1016/0168-9622(85)90012-0.

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50

Gee, D. G. "EUROPROBE: Lithosphere dynamics ‐ Archaean to present." GFF 118, sup004 (October 1996): 33–34. http://dx.doi.org/10.1080/11035899609546305.

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