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1 dying the climate and biogeochemistry of the Precambrian.
2 e ecdysozoan body fossils are known from the Precambrian.
3 rlier history that possibly extends into the Precambrian.
4 s, and their fossil record dates back to the Precambrian.
5 raw inferences about aerobiosis in the early Precambrian.
6  of carbon cycle perturbations unique to the Precambrian.
7  elongated sinuous grooves or furrows in the Precambrian.
8 re, climate, and evolution of animals in the Precambrian.
9 t determination of the lunar distance in the Precambrian.
10  fixation, especially towards the end of the Precambrian.
11 s been approximately constant since the late Precambrian.
12 sented a major carbonate sink throughout the Precambrian.
13 inctive Ptychographic nanotomography data of Precambrian (1.88 Ga) rocks, we recovered the morphology
14 vely high Na+ concentrations during the Late Precambrian [544 to 543 million years ago (Ma)], Permian
15 l to understanding the prokaryote-dominated, Precambrian 85% of life's history, can require more than
16 y the inverse [Formula: see text] pattern of Precambrian acyclic isoprenoid and n-alkane biomarkers.
17  RuBisCO, all of them theoretically dated as Precambrian), and used them as a proxy to search for any
18 us conditions persisted throughout the later Precambrian, and were even a feature of Phanerozoic ocea
19      Putative metazoan body fossils from the Precambrian are curiously lacking morphological characte
20 of the enigmatic Ediacaran biota of the late Precambrian as giant protists.
21 rms that sponges diverged and existed in the Precambrian as non-biomineralizing animals with an organ
22 used to trace the evolution of oxygen in the Precambrian atmosphere and to document past volcanic eru
23 een used to trace the redox evolution of the Precambrian atmosphere and to document the photochemistr
24 oxidative weathering under ostensibly anoxic Precambrian atmospheres.
25 ng the conformational dynamics of a putative Precambrian B-lactamase, we engineer enzyme specificity
26 that likely contributed to the deposition of precambrian banded iron formations, globally important s
27 he continental geological record, separating Precambrian basement from Phanerozoic sedimentary rocks.
28                              Deep within the Precambrian basement rocks of the Earth, groundwaters ca
29 ediment input derived from south Greenland's Precambrian bedrock terranes, probably reflecting the ce
30 thern Sudan follows a contorted path through Precambrian bedrock.
31                                      For the Precambrian (before ~540 Ma), however, dust emission mig
32 tionary biology approaches into the study of Precambrian biota remains a significant challenge.
33 mats was not carbon-limited during the early Precambrian, but became carbon-limited as the supply of
34 um-isotope values reflects a transition from Precambrian carbon and silicon cycles to those character
35 d in terms of the greater sensitivity of the Precambrian carbon cycle to the loss of shallow-water en
36 Stable oxygen isotope ratios (delta(18)O) of Precambrian cherts have been used to establish much of o
37 iple oxygen isotope composition ( '(17)O) of Precambrian cherts.
38                   The long-term stability of Precambrian continental lithosphere depends on the rheol
39 find that the H2 production potential of the Precambrian continental lithosphere has been underestima
40 our estimate of H2 production rates from the Precambrian continental lithosphere of 0.36-2.27 x 10(11
41 xplorations of saline fracture waters in the Precambrian continental subsurface have identified envir
42 nological perspective on the habitability of Precambrian cratons through time.
43 portray the extent and architecture of older Precambrian cratons, re-enforcing their linkages in East
44 se environments to account for the fact that Precambrian crust represents over 70 per cent of global
45 ree and Kidd Creek mines within the Canadian Precambrian crust.
46     Here we examine results from an expanded Precambrian database of palaeomagnetic intensity measure
47 can explain the lack of secular trend in the Precambrian delta(13)C record, and reopens the possibili
48 tions are superimposed on the usual range of Precambrian delta(15)N values, the Nitrogen Isotope Even
49  resulted in rapid and temporally concurrent Precambrian diversifications of the ancestors of several
50 ure modeling and geological investigation of Precambrian Earth-Moon system evolution.
51 ction regimes, we show that over most of the Precambrian, Earth likely operated in a distinct "sluggi
52 he potential for attaining new insights into Precambrian ecosystems and the composition of Earth's ea
53 c rocks are elevated (by +1.1) compared with Precambrian equivalents, consistent with our proposal fo
54 3+)/SigmaFe ratios are elevated by 0.12) vs. Precambrian equivalents.
55 duals, but nothing was known of the possible Precambrian evolution of comparable microorganisms until
56 icrobial lineages leave a fossil record, the Precambrian evolution of life remains shrouded in myster
57 ch bilaterian metazoans might have arisen in Precambrian evolution.
58 thousands of carbon isotope analyses of late Precambrian examples have been published to correlate th
59                                          The Precambrian explosion led to the rapid appearance of mos
60            Northward-flowing segments follow Precambrian fabrics, whereas east-west segments follow f
61 the dominant dipolarity of the time-averaged Precambrian field, a crucial requirement for palaeomagne
62                                              Precambrian genes exhibit a more pronounced difference i
63 omologs in invertebrate and protist genomes (Precambrian genes) with those that do not have such dete
64 es by which it formed remain major issues in Precambrian geology.
65 lion-year timescales that is compatible with Precambrian glaciations and biological constraints and s
66        For more than 100 years, the "missing Precambrian history of life" stood out as one of the gre
67 vidence an opportunistic response to the mid-Precambrian increase of environmental oxygen that result
68 eld and much of Egypt and parts of the small Precambrian inliers in the Sahara including the Ahaggar
69 cting potential geodynamo regimes during the Precambrian is currently impeded by the sparsity of high
70 ils within rocks of non-marine origin in the Precambrian is exceedingly rare.
71 ervation of biogeochemical complexity in the Precambrian is largely limited to cherts, phosphates and
72  history of atmospheric O(2) during the late Precambrian is vital for evaluating potential links to a
73 atic stepwise increase in oxygen in the late Precambrian is widely considered a prerequisite for the
74 ion of photosynthesizing communities on late Precambrian land surfaces.
75                       The natural history of Precambrian life is still unknown because of the rarity
76                                              Precambrian life on land can now be tested with stable i
77 rall, these results support the notions that Precambrian life was thermophilic and that proteins can
78 pens a new window through which to view late Precambrian life.
79 hree billion years of pervasively microbial 'Precambrian' life, and on the other the modern 'Phaneroz
80 in South Africa yields a contribution of the Precambrian lithosphere to global H2 production that was
81 thout significantly modifying the underlying Precambrian lithosphere.
82 cross the GOE provides new insights into the Precambrian marine cycling of this critical micronutrien
83 orm distinct layers with features similar to Precambrian mats and paleosols.
84 on points based on the interpretation of the Precambrian microbial fossil record, and strict molecula
85 -Ga Gunflint biota is one of the most famous Precambrian microfossil lagerstatten and provides a key
86               The existence of a terrestrial Precambrian (more than 542 Myr ago) biota has been large
87 le) leads to ambiguity in defining the early Precambrian nitrogen cycle.
88 rtain, with estimated dates ranging from the Precambrian (no land plants) to the Carboniferous (diver
89 ce reconstruction analysis targeting several Precambrian nodes in the evolution of class-A beta-lacta
90 estimates of phosphate concentrations in the Precambrian ocean, during life's origin and early evolut
91 concentrations seem to have been elevated in Precambrian oceans.
92 as well as the low preservation potential of Precambrian organisms (see Primer by Butterfield, in thi
93                        Some of the enigmatic Precambrian organisms in the Ediacaran Period grew large
94                           This validates the Precambrian origin of Ecdysozoa, reconciling a major gap
95  to reconstruct the structure of some of the Precambrian orogenic belts before biostratigraphy became
96 f methane using sulphate, was limited in the Precambrian period by low sulphate concentrations in sea
97 nidarians diverged from other animals in the Precambrian period, their record from the Ediacaran peri
98 Ediacaran sclerites is evidence against any 'Precambrian prelude' to the explosive diversification of
99  produced contemporary karyotypes from their Precambrian progenitors.
100                     Here, we use resurrected Precambrian proteins as scaffolds for protein engineerin
101 ical potential of laboratory resurrection of Precambrian proteins, as both high stability and enhance
102 e interior of East Antarctica is a mosaic of Precambrian provinces affected by rifting processes.
103  metallogenic processes also operated in the Precambrian remains obscure.
104                                      Barley, Precambrian Res.
105 are conserved, remains extremely rare in the Precambrian rock record.
106 lopment of Archean paleosols and patterns of Precambrian rock weathering suggest colonization of cont
107  and new H2 concentration data obtained from Precambrian rocks and find that the H2 production potent
108 , and delta(36)S from sulfide and sulfate in Precambrian rocks indicate that a change occurred in the
109 nisms, elevated SiO(2)(aq) concentrations in Precambrian seawater would have generated serpentinites
110 so eliminates the only known occurrence of a Precambrian sedimentary carbonate with highly (13)C-depl
111                       Their detection in the Precambrian sedimentary record would then permit an inde
112 setting, mineralogy, and geologic history of Precambrian sedimentary rocks indicates that the Fe isot
113 evolution during the earlier and much longer Precambrian segment of geological time centred on prokar
114 t water lakes such as those underlain by the Precambrian Shield.
115 n the Timmins, Ontario, area of the Canadian Precambrian Shield.
116 nt, varying from 95 +/- 4 kilometers beneath Precambrian shields and platforms to 81 +/- 2 kilometers
117  largely interpreted from the fossils of the Precambrian soft-bodied Ediacara Biota.
118  not least multiple examples of Cambrian and Precambrian soft-bodied fossils.
119 iculogenesis long after their divergences or Precambrian spicules were not amenable to fossilization.
120    This work provides a new search image for Precambrian sponge fossils, which are critical to resolv
121 ecessary criterion for the identification of Precambrian sponge fossils.
122 iomineralized axial filaments, suggests that Precambrian sponges may have had weakly biomineralized s
123 e the Cambrian period(5-8), possibly because Precambrian sponges were aspiculate and non-biomineraliz
124 s to the micritic microstructures typical of Precambrian stromatolites.
125 ons of Laurentia and other landmasses in the Precambrian supercontinent of Rodinia are controversial.
126                     By contrast, resurrected Precambrian thioredoxins express efficiently in E. coli,
127 ro and in vivo analyses of seven resurrected Precambrian thioredoxins, dating back 1-4 billion years,
128                       The implied history of Precambrian tidal friction is in accord with both the mo
129 dicts a more substantial role for AOA during Precambrian time, and may have implications for understa
130 ercontinent centres can be located back into Precambrian time, providing fixed points for the calcula
131 ciation ("snowball Earth" conditions) during Precambrian time.
132 prompts re-evaluation of the significance of Precambrian trace fossils as evidence of the early diver
133  traces bear a remarkable resemblance to the Precambrian trace fossils, including those as old as 1.8
134 ications for MOR hydrothermal systems in the Precambrian, when low-seawater SO4 could help explain lo
135 as the increasing ocean oxygen levels in the Precambrian, which are thought to have influenced the em

 
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