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1 iation and inventory relative to P since the Proterozoic.
2 arine sulphate concentrations throughout the Proterozoic.
3  a build-up of atmospheric oxygen before the Proterozoic.
4  the fossil record may be pushed back to the Proterozoic.
5 eaking the long-term static state of the mid-Proterozoic.
6 onate could have been relevant since the mid-Proterozoic.
7 gical and geochemical conditions in the late Proterozoic.
8  for the rise of metazoans at the end of the Proterozoic.
9 on of Earth's surface environment during the Proterozoic.
10 deposits formed during the Archean and early Proterozoic.
11 nental stabilization at the beginning of the Proterozoic.
12 wo isochrons, one Archaean (2.95 Ga) and one Proterozoic (1.15 Ga).
13 xidation of Cr at Earth's surface in the mid-Proterozoic (1.8 to 0.8 billion years ago).
14 he most abundant type of fossil found in the Proterozoic (2,500 to 590 Myr ago), but they then declin
15 mats in benthic environments for most of the Proterozoic (2,500-542 Mya), marine planktonic cyanobact
16 ks from the Archean (4.0 to 2.5 Gyr ago) and Proterozoic (2.5 to 0.5 Gyr ago) Eons.
17 coincident with a major regime change in the Proterozoic acritarch record, including: (i) disappearan
18 cean environmental conditions earlier in the Proterozoic adverse to nitrogen-fixers and their evoluti
19                                          The Proterozoic aeon (2,500-540 million years ago) saw episo
20 exture, and structure of fluvial deposits in Proterozoic-age Torridonian Group, Scotland-a type-examp
21                                 However, the Proterozoic also has a unique magmatic and metamorphic r
22  (Synechococcus sp. PCC 7002), an engineered Proterozoic analog lacking a CO(2)-concentrating mechani
23 a from rocks formed near the boundary of the Proterozoic and Archaean eons, some 2.5 Gyr ago, show ma
24               All phylogenetic dating in the Proterozoic and before is difficult: Significant debates
25 cyanobacteria evolved towards the end of the Proterozoic and early Phanerozoic.
26 oth anomalous climatic stasis during the mid-Proterozoic and extreme climate perturbation during the
27 ntrolling the level of oxygen throughout the Proterozoic and its eventual rise remain uncertain.
28  consistency of its diversification with the Proterozoic and Phanerozoic atmospheric oxygenation.
29                   The transition between the Proterozoic and Phanerozoic eons, beginning 542 million
30  periods of lithospheric thinning during the Proterozoic and Phanerozoic eons, the lithosphere beneat
31  and mean temperature of cold periods within Proterozoic and Quaternary climates, and recent climate
32  the microbially dominated ecosystems of the Proterozoic and the Cambrian emergence of the modern bio
33 ains in the sandstone are Permian, Devonian, Proterozoic, and Archean in age and, with the exception
34 la trace their diversity to the Archaean and Proterozoic, and bacterial families prior to the Phanero
35 approach to geological observations from the Proterozoic, and provide the first quantitative constrai
36 ulphide in injected sands extend back to the Proterozoic, and show that injected sand complexes have
37 organic-walled microfossils extracted from a Proterozoic ( approximately 1.4-gigayear-old) shale in N
38 erstanding of ocean chemistry during the mid-Proterozoic ( approximately 1.8-0.8 Ga).
39 r-filled structures common in early- and mid-Proterozoic ( approximately 2,500-750 million years ago,
40 oncentrations and rates of Fe cycling in the Proterozoic are the largest differences from modern oxyg
41   We propose that the root formed during the Proterozoic assembly of interior East Antarctica (possib
42  was abundant in the late Archaean and early Proterozoic atmosphere and that methane was probably sca
43                                          The Proterozoic basement underlying Somaliland has been affe
44 r highlight that deep chemical weathering of Proterozoic bedrock and denudation associated with the G
45                  The tidal rhythmites in the Proterozoic Big Cottonwood Formation (Utah, United State
46 served crustal thickness across the Archaean/Proterozoic boundary, these data are consistent with a m
47 nts phosphorus and nickel across the Archean-Proterozoic boundary, which might have helped trigger th
48 obialites were common and diverse during the Proterozoic, but declined in abundance and morphological
49 gered by environmental perturbation near the Proterozoic-Cambrian boundary and subsequently amplified
50                   The terminal event, at the Proterozoic-Cambrian boundary, signals the final diminut
51                                          The Proterozoic-Cambrian transition records the appearance o
52 ed to estimate the impact this would have on Proterozoic carbon cycling and global atmospheric compos
53 -cyanobacterium is fully consistent with the Proterozoic carbon isotope record, suggesting that cyano
54                                              Proterozoic carbonate megafacies are composed predominan
55 g events, by a Paleozoic silicic fluid and a Proterozoic carbonatitic fluid, are also encapsulated in
56 eontological data because of the scarcity of Proterozoic chlorophyte fossils.
57  Here we use a simple box model of a generic Proterozoic coastal upwelling zone to show how these fee
58 ents indicate expanded anoxia during the mid-Proterozoic compared to the present-day ocean.
59 is implies not only that cyanobacteria built Proterozoic conical stromatolites but also that fossil b
60 at microaerophilic levels throughout the Mid-Proterozoic, consistent with the prevalence of some clad
61 overt assembly of Rodinia from thickened mid-Proterozoic continental crust via two-sided subduction c
62 r H2S-rich seawaters that were widespread in Proterozoic continental margins.
63 ion beneath Venetia from the Archaean to the Proterozoic.Dating of inclusions within diamonds is used
64 d that the metal enrichment record implies a Proterozoic deep ocean characterized by pervasive anoxia
65                The 1.8 billion years younger Proterozoic diamond suite formed by melt-dominated metas
66                                          The Proterozoic Earth was characterized by a high proportion
67 hermal and chemical evolution of the Archean-Proterozoic Earth.
68 yotes were likely aerobic and established in Proterozoic ecosystems.
69 urred in two rapid steps at both ends of the Proterozoic Eon ( approximately 2.5-0.543 Ga).
70 bon fixation by primary producers in the mid-Proterozoic eon (1.8 to 1.0 Ga ago).
71 road steps near the beginning and end of the Proterozoic eon (2,500 to 542 million years ago).
72 resent atmospheric level through most of the Proterozoic Eon (2.4 to 0.65 Ga).
73       Recent data imply that for much of the Proterozoic Eon (2500 to 543 million years ago), Earth's
74 2.3 billion years ago, Gyr ago) and the late Proterozoic eon (about 0.8 Gyr ago), with the latter imp
75 orus cycle may have occurred during the late Proterozoic eon (between 800 and 635 million years ago),
76 s history, focusing in particular on the mid-Proterozoic Eon (i.e., 1.8 - 0.8 Ga).
77 decay of Earth's dynamo strength through the Proterozoic Eon and could challenge the hypothesis of a
78 and diversification of the eukaryotes in the Proterozoic Eon as viewed through fossils, organic bioma
79 e record of marine carbon indicates that the Proterozoic Eon began and ended with extreme fluctuation
80 surface redox conditions evolved through the Proterozoic Eon is fundamental to understanding how biog
81  low gradient, single-threaded rivers in the Proterozoic eon, at a time well before the evolution and
82 ed Earth's surface and atmosphere during the Proterozoic Eon, pushing it away from the more reducing
83 ich environments in the late Archean Eon and Proterozoic Eon, respectively, by the spread of arsM gen
84 ies a unique ocean chemistry for much of the Proterozoic eon, which would have been neither completel
85 the environmental transformation late in the Proterozoic eon.
86 haps five) discrete ice ages in the terminal Proterozoic Eon.
87 e of major animal clades occurred during the Proterozoic Eon.
88 d gross primary productivity) throughout the Proterozoic Eon.
89 n biosphere and geosphere coevolution in the Proterozoic Eon.
90 genation of Earth's surface ocean during the Proterozoic Eon.
91 al patterns of volcanism, as far back as the Proterozoic eon.
92 ty in anoxic seawater during the Archean and Proterozoic eons (4.0-0.541 billion years ago) would hav
93 wth of landmass in the late Archean to early Proterozoic Eons could have reorganized biogeochemical c
94  of Eucarya occurred in the late Archaean or Proterozoic Eons when atmospheric oxygen levels were low
95 known, with ages ranging from the Hadaean to Proterozoic eons(1-3).
96  however, extend into the Archaean and early Proterozoic eons, in the form of impact spherule beds: g
97 iment was widespread during the Archaean and Proterozoic Eons, playing an important role in global bi
98 e balance during the late Archaean and early Proterozoic eons.
99 e concentrations may have changed during the Proterozoic era (2.5-0.54 Gyr ago).
100 ets may have reached the Equator in the late Proterozoic era (600-800 Myr ago), according to geologic
101 ection of eukaryotic phytoplankton since the Proterozoic era.
102  and subaerially exposed habitats during the Proterozoic era.
103               From the late Archaean to late Proterozoic eras (some 3-1 billion years ago), much of t
104 's oceans during the late Archaean and early Proterozoic eras.
105                      The global diversity of Proterozoic eukaryote fossils is poorly quantified despi
106 ay thus help to explain observed patterns of Proterozoic evolution.
107           Claims of fossilized organelles in Proterozoic fossils can no longer be dismissed on ground
108 preserved and distinctive assemblage of Late Proterozoic fossils from subtidal marine shales.
109                  Exceptional preservation of Proterozoic fossils is not unknown, but it is usually as
110                                We describe a Proterozoic, fully biomineralized metazoan from the Omky
111                                              Proterozoic glacial deposits laid down in near-equatoria
112 this redox syntrophy in anoxic and microoxic Proterozoic habitats LECA evolved.
113 spheric oxygen concentration during the late Proterozoic has been inferred from multiple indirect pro
114 idence for such low O2 concentrations in the Proterozoic helps explain the late emergence and diversi
115 mains the most viable model for low-latitude Proterozoic ice ages.
116      Our temporal framework for the terminal Proterozoic is a critical step for testing hypotheses re
117              However, empirical estimates of Proterozoic levels of atmospheric carbon dioxide concent
118 arest and most taxonomically varied views of Proterozoic life yet reported.
119 lly to the base of the much thinner adjacent Proterozoic lithosphere creates a zone of highly concent
120 d thickness differences between Archaean and Proterozoic lithosphere on deep-carbon fluxes remains un
121  the Sierran batholith formed on preexisting Proterozoic lithosphere, most of the original lithospher
122        Recent evidence for H(2)S in some mid-Proterozoic marine basins suggests, however, that the de
123                         Trace metal data for Proterozoic marine euxinic sediments imply that the expa
124 ere we present iron data from a suite of mid-Proterozoic marine mudstones.
125 ve anoxia in the subsurface ocean during the Proterozoic may have allowed large fluxes of biogenic CH
126 /188Os ratios (0.1193 to 0.1273), which give Proterozoic model ages of 820 to 1230 million years ago.
127 s after about 1,800 Myr ago maintained a mid-Proterozoic molybdenum reservoir below 20 per cent of th
128 oxygen generated during Archean and earliest Proterozoic non-Snowball glacial intervals could have dr
129  would have influenced oceanic redox and the Proterozoic O(2) budget.
130            Additionally, modeling favors mid-Proterozoic O(2) exceeding [Formula: see text] to [Formu
131 he iron-replete reducing environments of the Proterozoic ocean [1].
132                   The oxidation state of the Proterozoic ocean between these two steps and the timing
133 nktonic productivity, various models for mid-Proterozoic ocean chemistry imply different effects on t
134 e to show how these feedbacks caused the mid-Proterozoic ocean to exhibit a spatial/temporal separati
135 Here, we link geologic information about the Proterozoic ocean to microbial processes in modern low-o
136 y the major primary producers in the pelagic Proterozoic ocean, despite atmospheric CO(2) levels up t
137 diverse palaeogeographic settings in the mid-Proterozoic ocean, inviting new models for the temporal
138 stem-group cnidarians that lived in the late Proterozoic ocean.
139 much dissolved oxygen was present in the mid-Proterozoic oceans between 1.8 and 1.0 billion years ago
140                       The redox chemistry of Proterozoic oceans has important implications for evolut
141  Thus, a redox structure similar to those in Proterozoic oceans may have persisted or returned in the
142  suggest that subsurface water masses in mid-Proterozoic oceans were predominantly anoxic and ferrugi
143       In low-oxygen ferruginous Archaean and Proterozoic oceans, therefore, sedimentary methane produ
144 modern oxygen minimum zones as an analog for Proterozoic oceans, we explore the effect of low oxygen
145 olved more than 1.5 billion years ago in the Proterozoic oceans.
146 ndicating low sulphate concentrations in mid-Proterozoic oceans.
147 ation of organic sulfur cycling from the Mid-Proterozoic onwards, with implications for climate regul
148 ented the occurrence of microborings in late Proterozoic ooids from central East Greenland.
149                                      The mid-Proterozoic or "boring billion" exhibited extremely stab
150                                         Late Proterozoic organisms must have been diverse and widely
151 rift transitions from Archaean (cratonic) to Proterozoic (orogenic) lithosphere.
152 s C) and show evidence for heating and yield Proterozoic Os model ages, whereas the deeper portions (
153 harply constraining the magnitude of the end-Proterozoic oxygen increase.
154  state of the oceans, generated by the early Proterozoic oxygen revolution and terminated by the envi
155 ain extreme carbon isotope variations in the Proterozoic, Paleozoic, and Triassic.
156 d of the East African orogen during the late Proterozoic pan-African orogenic event.
157 crobial mats-a dominant ecosystem of the mid-Proterozoic period of the Earth history.
158                                       At mid-Proterozoic pH and pCO(2) values, carbon isotope fractio
159       Sedimentary rocks deposited across the Proterozoic-Phanerozoic transition record extreme climat
160 the divergence of living agnathans, near the Proterozoic/Phanerozoic boundary (approximately 550Mya).
161 rovide the first quantitative constraints on Proterozoic plate velocities that substantiate the postu
162 modern DOC is (13)C-enriched relative to the Proterozoic, possibly because of changing autotrophic ca
163 from weak to strong in the Paleozoic and the Proterozoic present challenges in identifying the onset
164                            Even though a few Proterozoic Re depletion ages are locally preserved in t
165 f western North America some younger (middle Proterozoic) regions have remained stable, whereas some
166                            Although suitable Proterozoic rocks exist, no currently known Archean stra
167 yanobacterial sheaths routinely preserved in Proterozoic rocks, this assemblage includes multicellula
168 nt in 13C relative to Phanerozoic or earlier Proterozoic samples.
169 at provided by Ediacaran fossils in terminal Proterozoic sandstones and shales.
170                           Here, we present a Proterozoic seawater sulfate isotope record that include
171                             A compilation of Proterozoic sedimentary delta(15)N data reveals a stepwi
172 ally continuous suites of samples from Upper Proterozoic sedimentary successions of East Greenland, S
173 overlooked--constituent of Archean and Early Proterozoic sedimentary successions.
174 f chromium (Cr) isotope data from a suite of Proterozoic sediments from China, Australia, and North A
175 ere we show that hydrocarbons extracted from Proterozoic sediments in several locations worldwide are
176                                      The mid-Proterozoic, spanning 1.8 to 0.8 billion years ago, is r
177 g-distance correlation between fossiliferous Proterozoic strata of Mexico and the United States.
178 entary changes, including the replacement of Proterozoic-style microbial matgrounds by Phanerozoic-st
179 alt, the HIMU source formed as Archean-early Proterozoic subduction-related carbonatite-metasomatized
180                       Efforts to reconstruct Proterozoic supercontinents are strengthened by this dem
181 rom sulfur isotope data for Archean to early Proterozoic surface material in the deep HIMU mantle sou
182                                   Subsequent Proterozoic tectonic and magmatic events altered the com
183  depth under warm subduction geotherm or the Proterozoic tectonic setting.
184 n hydrated and probably weakened much of the Proterozoic tectospheric mantle beneath the Colorado pla
185 ability of the evolution of Ecdysozoa in the Proterozoic, the otherwise prolific fossil record of the
186 n of animal life on Earth for much of Middle Proterozoic time ( approximately 1.8-0.8 billion years a
187  reviving the faint young Sun paradox during Proterozoic time and challenging existing models for the
188                                       During Proterozoic time, Earth experienced two intervals with o
189 role of CH4 in Earth's climate system during Proterozoic time.
190       To better define the transition from a Proterozoic to a modern-like weathering regime, here we
191                                         Late Proterozoic to modern sediments may reflect greater Fe(I
192 nently oxygenated atmosphere at the Archaean-Proterozoic transition (approximately 2.5 billion years
193 lar oxygen (O(2)) shortly after the Archaean-Proterozoic transition 2.5 billion years ago was more co
194 Earth's atmosphere shortly after the Archean-Proterozoic transition during the 'Great Oxidation Event
195 d permanently diminished during the Archaean-Proterozoic transition.
196 , the assumption of elevated pCH4 during the Proterozoic underlies most models for both anomalous cli
197 Te present in sulfide ores from the Kisgruva Proterozoic volcanogenic deposit.
198 wn, but it is generally assumed that the mid-Proterozoic was home to a globally sulphidic (euxinic) d
199 tionary trajectories and highlight the early Proterozoic, which encompasses the Great Oxidation Event
200 significant non-arc magmatism during the mid-Proterozoic, while fewer occurrences of many other miner
201                             By contrast, the Proterozoic witnessed continuously decreasing crustal th
202  show that higher mantle temperatures in the Proterozoic would have resulted in a larger proportion o

 
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