ライフサイエンスコーパス: pyrite

1 d independent from, inorganic proxies (e.g., pyrite).

2 sorption experiments with local Tl-rich coal pyrite.

3 d to the oxidative dissolution of As-bearing pyrite.

4 ther with smaller quantities of siderite and pyrite.

5 and complete sorption of monothioarsenate to pyrite.

6 line ferrihydrite, goethite, mackinawite, or pyrite.

7 be explained by abiological precipitation of pyrite.

8 dark red-to-black fragments of hematite and pyrite.

9 s and increasing the oxidative weathering of pyrite.

10 al distribution and chemistry of sedimentary pyrite.

11 nd to NOM thiol groups and incorporated into pyrite.

12 record of seawater sulfates and sedimentary pyrites.

13 ntal tellurium, or a plating of magnetite or pyrites.

14 We studied the reaction between pyrite (5-125 mM) and nitrite (40-2000 muM) at pH 0, 5.5

15 s were found alongside two fragments of iron pyrite-a mineral used in later periods to strike sparks

16 ope differences in size-sorted aerosols from pyrite ablation are not analytically resolvable.

17 In the case of pyrite acting as reductant, however, denitrification is

18 ization of transition metals, which produced pyrite and copious appended sulfur functionality.

19 opose a structure that is isostructural with pyrite and has the stoichiometry PtN2.

20 nderstanding the phase selection between the pyrite and marcasite polymorphs of FeS2.

21 ead to suggestions to improve single crystal pyrite and nanocrystalline or polycrystalline pyrite fil

22 crobially mediated oxidation of arsenic-rich pyrite and organic matter coupled to nitrate reduction r

23 1%), and exceeds the CO(2) flux generated by pyrite and petrogenic organic matter oxidation (~0.2 mol

24 21% of Se is present as selenide (Se(2-)) in pyrite and sphalerite, 19% of Se is present as selenite

25 ant source minerals for aqueous-phase Se are pyrite and sphalerite.

26 Mackinawite, greigite, pyrite and sulfate coexist in the sediments, indicating

27 arcasite has a band gap at least as large as pyrite and that the two polymorphs share similar absorpt

28 a(33)S in trace-metal-poor, early diagenetic pyrite and the unusually enriched organic carbon at low

29 Fe minerals can still be present along with pyrite and vivianite, and that ferric Fe-bound P pool ca

30 c reaction of FeS with H(2)S to form FeS(2) (pyrite) and H(2) was postulated to have operated as an e

31 here are among the largest ever observed in pyrite, and are in phase with glacial-interglacial sea l

32 cles containing pyrite, Cu and Zn-containing pyrite, and iron in hydrothermal vent black smoker emiss

33 nsions (2.0 g L(-1)) of magnetite, siderite, pyrite, and mackinawite.

34 e of geological materials such as clay, ore, pyrite, and potentially, hydrocarbons.

35 ) for the reduction of arsenite, As(III), by pyrite are incompletely understood.

36 tructure (EXAFS) spectra of these As-bearing pyrites are explained by local structure models obtained

37 However, the performance of pyrite as an absorber material in photovoltaic devices h

38 d on the observation of natural hydrothermal pyrites, As(-I) is usually assigned to the occupation of

39 (99)Tc(VII) uptake by synthetic pure pyrite at 21 degrees C was studied in a wide pH range fr

40 ectroscopy for As(II,III) incorporation into pyrite at octahedral Fe(II) sites and for As(-I) at tetr

41 ch reactions show that As(III) is reduced on pyrite at the Eh-pH predicted by the electrochemical stu

42 rals (chalcopyrite, chalcocite, bornite, and pyrite) at different flotation pulp conditions (feed, co

43 ord of remarkable biological preservation in pyrite back to the Paleoproterozoic and provides criteri

44 ciated with the primary minerals sphalerite, pyrite, barite, and chalcopyrite and secondary Fe oxyhyd

45 vothermal process was used to synthesize new pyrite-based composites.

46 alloys are promising for the development of pyrite-based heterojunction solar cells that feature lar

47 ng minerals but is less well established for pyrite-based records.

48 two field-scale treatments from the Iberian Pyrite Belt (IPB, southwest Spain).

49 sin in the US and three sites in the Iberian Pyrite Belt in Spain and found that the fastest rates of

50 ruces is a base-metal deposit in the Iberian Pyrite Belt, one of the world's best-known ore provinces

51 model suggests that after ~ 10 million years pyrite burial achieves relative long-term stability unti

52 seawater sulfate and reflect an increase in pyrite burial and a crash in the marine sulfate reservoi

53 , this may have resulted in elevated organic-pyrite burial and ocean oxygenation.

54 s that enhanced levels of organic-carbon and pyrite burial continued a few hundred thousand years aft

55 We show that pyrite burial could have resulted in molecular oxygen ex

56 We estimate that this organic carbon and pyrite burial event added approximately 19 x 10(18) mole

57 modelling approach reveals three significant pyrite burial events (i.e. PBEs) in the Triassic.

58 tion rates from the global average record of pyrite burial, highlighting how the local nature of sedi

59 r sulfur represent periods of lower rates of pyrite burial, implying a shift in the location of organ

60 EPME, resulting in a substantial increase in pyrite burial, possibly driven by Siberian Traps volcani

61 ochemical box modeling of organic-carbon and pyrite burial, the sulfur-isotope excursion can be gener

62 ults with a sediment biogeochemical model of pyrite burial, we find a strong relationship between obs

63 e promoted atmospheric oxidation by means of pyrite burial.

64 r abrupt changes to tectonics and associated pyrite burial.

65 entary sulfur isotopic composition of marine pyrite by examining a 300-m drill core of Mediterranean

66 IMS, we conclude that anaerobic oxidation of pyrite by our neutrophilic enrichment culture was mainly

67 chalcogenides and first-row transition metal pyrites catalysts.

68 s have been able to directly link changes in pyrite chemistry to the processes responsible for bonanz

69 We report metallic cobalt pyrite (cobalt disulfide, CoS2) as one such high-activit

70 natural magnetite, siderite, pyrrhotite, and pyrite, collected through cascade impaction, followed by

71 release occurring when sulfide (principally pyrite)-containing rock from mining activities and from

72 ogeochemical processes in a nitrate-polluted pyrite-containing aquifer and its evolution over the las

73 ure, which developed during the oxidation of pyrite-containing coal mining overburden/waste rock (OWR

74 oxidation rates coincided with maxima of the pyrite content, total cell counts, and MPN of iron(II)-o

75 r share the same weathering front depth with pyrite, contrary to models where weathering fronts are s

76 All strains capable of reducing pyrite could also use mackinawite as an iron and sulfur

77 we argue that, in the anoxic Archean oceans, pyrite could form in the absence of ambient sulfate from

78 n of a detailed energy band diagram for iron pyrite crystals.

79 de the formation of nanoparticles containing pyrite, Cu and Zn-containing pyrite, and iron in hydroth

80 Iron pyrite (cubic FeS2) is a promising candidate absorber ma

81 apacity of the aquifers, which is present as pyrite, degradable organic carbon, and geogenic U(IV) mi

82 nvironmental information can be derived from pyrite delta(34)S records.

83 e in the sulfur isotopic record preserved in pyrite (delta(34)Spyr) necessarily corresponds to local

84 ironmental context of exceptionally enriched pyrite-delta(34)S and -delta(56)Fe in bioturbated, storm

85 Pyrite-delta(34)S and -delta(56)Fe isotopes represent hi

86 The persistence of nanoparticulate pyrite demonstrates that it is an important mechanism fo

87 ributions of these pools to the formation of pyrite depend on both the accumulation of the insoluble

88 On average, the amount of pyrite detached was equivalent to 6.5 x 10(-11) mol m(-2

89 st that silicate addition, for reducing both pyrite dissolution and metalliferous drainage, may be ap

90 e effect of galvanic interaction on reducing pyrite dissolution decreased with increasing pH and was

91 The pyrite dissolution rate was reduced by 98% upon silicate

92 e surface layer is observed, with consequent pyrite dissolution rates reduced by more than 90% at neu

93 and weathering fluxes of organic carbon and pyrite driven by either Neogene cooling or increasing Pl

94 its effectiveness as the primary oxidant of pyrite during AMD generation.

95 rric iron oxidizes and dissolves sedimentary pyrite during chemical weathering.

96 However, the modes of As incorporation into pyrite during its crystallization under low-temperature

97 potential for hydrogen electroadsorption on pyrite, E approximately +0.1 V (versus RHE).

98 odified [FeFe](H) cluster stably linked to a pyrite electrode immersed in acidified water.

99 The pyrite electrode readily produces hydrogen from acidifie

100 Sulphur (S) isotope values in pyrite extracted from a Plio- to Holocene sequence of th

101 Arsenopyrite (FeAsS) and arsenian pyrite (FeAsxS2-x) of <25 mum size, which have escaped d

102 ganic framework (MOF) yielded well-dispersed pyrite FeS(2) nanoparticles of ~100 nm diameter linked t

103 lyst containing Co doped earth abundant iron pyrite FeS(2) nanosheets hybridized with carbon nanotube

104 itial incubation and decreased together with pyrite (FeS(2)) after perturbation.

105 been used to show that the band gap of iron pyrite (FeS(2)) can be increased from ~1.0 to 1.2-1.3 eV

106 er, we also demonstrate that nanoparticulate pyrite (FeS(2)) is not removed from the plume and can ac

107 Neutrophilic microbial pyrite (FeS(2)) oxidation coupled to denitrification is

108 Pyrite (FeS(2)) thin films were synthesized using a H(2)

109 ~4% copper and zinc impurities, whereas pure pyrite (FeS(2)) was identified in hydraulic fracturing w

110 8% of greigite (Fe(2+)Fe(3+)(2)S(4)) and 72% pyrite (FeS(2)).

111 introduced as an alternate candidate to iron pyrite, FeS(2).

112 ous sulfur isotope (Delta(33)S) signature of pyrite (FeS2) in seafloor sediments from this period, wh

113 Iron pyrite (FeS2) is considered a promising earth-abundant s

114 Oxidation of pyrite (FeS2) plays a significant role in the redox cycl

115 al sulfate reduction that induce substantial pyrite (FeS2) precipitation.

116 g silver and gold (AgNPs and AuNPs), Fe, Mn, pyrite (FeS2), Ag2S, CuS, CdS, and ZnS, is dictated larg

117 Cu, Zn) with Na2S2 enables the formation of pyrite (FeS2), CoS2, and NiS2 at low temperatures (250-3

118 cles in suspension from mackinawite (FeS) to pyrite (FeS2).

119 yrite and nanocrystalline or polycrystalline pyrite films for successful solar applications.

120 re, large-grain, and uniform polycrystalline pyrite films that are fabricated by solution-phase depos

121 Iron pyrite (fool's gold, FeS(2)) is a promising earth abunda

122 Our results show that pyrite formation can be mediated at ambient temperature

123 Since the Archean, sedimentary pyrite formation has played a major role in the global i

124 d for the d(34)S, supporting the scenario of pyrite formation in sediments before the precipitation o

125 Fe isotope fractionation accompanies abiotic pyrite formation in the absence of Fe(II) redox change.

126 However, the mechanism of sedimentary pyrite formation is still being debated.

127 artial Fe(II)(aq) utilization during abiotic pyrite formation rather than microbial dissimilatory Fe(

128 production, indicating a coupling of overall pyrite formation to methanogenesis.

129 hanges in ocean circulation and/or sustained pyrite formation.

130 have been substantially overprinted by later pyrite formation.

131 Greenstone Belt, South Africa, show that the pyrite formed by bacterial reduction of seawater sulfate

132 ol and the rate of sulfide production in the pyrite-forming environments.

133 ts revealed Se primarily correlated with the pyrite fraction with exact Se speciation highly dependen

134 noids) are present in very low abundance and pyrite framboids are absent.

135 nd electron microprobe analyses conducted on pyrite from the Brucejack epithermal gold deposit, Briti

136 he same epsilon(205)Tl value was found for a pyrite from the deposit that produced the cocombusted py

137 The gold and rounded pyrites from the conglomerates yield a rhenium-osmium is

138 lena)- and bi-sulfide (pyrite-sphalerite and pyrite-galena) batch dissolution experiments were carrie

139 Our results reveal differences in pyrite grain size and sulfur isotope composition between

140 The effects of pyrite grains and three types of oxyanions-sulfate, phos

141 strate that Se is associated with framboidal pyrite grains as a discrete, independent FeSex phase.

142 esult suggests that mechanical detachment of pyrite grains could be an important pathway for the mobi

143 al detachment, and mobilization, of embedded pyrite grains.

144 brating suspensions containing the nanosized pyrite-greigite solid phase at different pH-values and w

145 n the order: Au-NP-sulfide (originating from pyrite) > Au-NP-sulfate > citrate-Au-NP > Au-NP-arsenate

146 The iron isotope composition of sedimentary pyrite has been proposed as a potential proxy to trace m

147 Iron chalcogenides, in particular iron pyrite, have great potential to be useful materials for

148 tally-relevant iron(III) (oxyhydr)oxides and pyrite, (ii) microbial utilization of nanoparticles as '

149 Bulk pyrite in most sediments carries weak S MIF because of m

150 f the early formation of authigenic arsenian pyrite in subsurface sediments.

151 of oxygenated water causes the oxidation of pyrite in the aquifer matrix, and (ii) the associated re

152 nts evidenced the release of As from NOM and pyrite in the presence of nitrate.

153 ulfur isotope data from carbonate-associated pyrite in the ~2.5-billion-year-old Batatal Formation of

154 he geochemical reactivity of such As-bearing pyrites in low-temperature subsurface environments.

155 The sulphur isotopic compositions of pyrites in the shales show strong variations along a pal

156 Acid mine drainage (AMD) formed from pyrite (iron disulfide) weathering contributes to ecosys

157 Pyrite is a key mineral in the global biogeochemical cyc

158 Pyrite is a ubiquitous iron sulfide mineral that is oxid

159 Pyrite is a ubiquitous mineral in reducing environments

160 Early formation of the pyrite is indicated by the mineralogical composition of

161 the isotopic composition of sulphur in this pyrite is large and shows no evidence of mass-independen

162 Geological studies show that pyrite is locally rare, suggesting it was brought delibe

163 Indeed, As-bearing pyrite is observed in a wide variety of sedimentary envi

164 eports indicated that anaerobic oxidation of pyrite is occurring, but the mechanism remains unclear.

165 We found that syngenetic pyrite is present in organic-rich shales of the 2.32-Gyr

166 h faster than Se substituted in the euhedral pyrite lattice.

167 combined effect was at pH 7.4, with <0.1% of pyrite leached in both bi-sulfide systems.

168 ntial incorporation of sulfur compounds into pyrite leads to preservation of S MIF, which is predicte

169 Zn(CN)2, P6(3)/mmc, P(trans) ~ 0.9 GPa), and pyrite-like (pyr-Zn(CN)2, Pa3, P(trans) ~ 1.8 GPa).

170 and 1.8 Ga, positive iron isotope values of pyrite likely reflect an increase in the precipitation o

171 toresponse observed experimentally for mixed pyrite/marcasite-FeS2 films can be ascribed to the prese

172 ly due to distinct reactive environments for pyrite mineralization, linked to organic matter, sulfate

173 network of Pa3 symmetry, as observed in the pyrite model structure, at variance with the usual, but

174 with exact Se speciation highly dependent on pyrite morphology.

175 that for these elements to become mobilized, pyrite must first dissolve.

176 be coordination assembly of anisotropic FeS2 pyrite nanoparticles (NPs) that can facilitate charge tr

177 document metal sulfide particles, including pyrite nanoparticles, within the first meter of buoyant

178 s not expected from the particular model for pyrite nodule formation in a largely closed or semi-clos

179 , and stable sulfur isotopic compositions of pyrite nodules were studied from a section at Taoying, e

180 We focused on pyrite nodules, precipitated in shallow sediments.

181 ted because arsenic acts as an inhibitor for pyrite nucleation at ambient temperature.

182 Remarkably, As(III) reduction on pyrite occurs at similar potentials to those for reducti

183 Variable and negative iron isotope values in pyrites older than about 2.3 Ga suggest that an iron-ric

184 er both 1) alternative oxygen sources during pyrite oxidation and 2) secondary overprinting by microb

185 iments of rocks from the watershed show that pyrite oxidation and carbonate dissolution control the s

186 These findings indicate that microbial pyrite oxidation and metal mobilization preferentially o

187 The mass balance of pyrite oxidation and nitrate reduction revealed a closed

188 te dissolution following proton release from pyrite oxidation and subsequent exchange by calcium for

189 and 2) the coupled carbonate dissolution and pyrite oxidation at depth in the rock.

190 Here, we investigated direct microbial pyrite oxidation by a neutrophilic chemolithoautotrophic

191 Our data imply a cyclic model for pyrite oxidation by Fe(III) on the basis of the oxidatio

192 The rate of pyrite oxidation by ferric iron in sterile suspensions a

193 Inhibition of pyrite oxidation by SMP was shown to be comparable to, b

194 res, [Formula: see text]/[Formula: see text] Pyrite oxidation during chemical weathering on land cons

195 order of magnitude greater than the rate of pyrite oxidation expected under similar conditions.

196 xidation in a wastewater reactor and aerobic pyrite oxidation in acid mine drainage.

197 Under the atmosphere today, pyrite oxidation is rate-limited by diffusion of oxygen

198 Chemolithotrophic denitrification coupled to pyrite oxidation is regarded a key process in the remova

199 Maximal microcalorimetrically determined pyrite oxidation rates coincided with maxima of the pyri

200 onsidered in studies on microbially mediated pyrite oxidation with nitrate.

201 tion headwaters is quantitatively sourced by pyrite oxidation, but resulting Delta'(17)O values imply

202 ocedure typically used to quantify microbial pyrite oxidation, in overestimating Fe(III) production.

203 Due to pyrite oxidation, metals (especially copper) are mobiliz

204 ctively mitigated by reducing or eliminating pyrite oxidation, which decreases the likelihood of dolo

205 ct of phospholipid on the biogeochemistry of pyrite oxidation, which leads to acid mine drainage (AMD

206 nterpret this to reflect overprinting of the pyrite oxidation-derived Delta'(17)O anomaly by microbia

207 la: see text] incorporation into terrestrial pyrite oxidation-derived sulfate, but a mechanistic unde

208 sulfate, but a mechanistic understanding of pyrite oxidation-including oxygen sources-in weathering

209 equesters, on average, 37% of Se released by pyrite oxidation.

210 ed organic matter can play a role in slowing pyrite oxidation.

211 ters, we determined the factors that control pyrite oxidation.

212 bedrock remains reducing, preventing deeper pyrite oxidation.

213 anaerobically oxidize a putatively nanosized pyrite particle fraction with nitrate as electron accept

214 , and temperature we found that in all cases pyrite particles became detached from the shale surfaces

215 Without silicate, oxidized pyrite particles form an overlayer of crystalline goethi

216 factors between Fe(II)(aq), mackinawite, and pyrite permit the generation of pyrite with Fe isotope s

217 The pyrite phase of Fe(1-x)CoxS(2)/CNT was characterized by

218 rtionation and atomic rearrangement into the pyrite phase.

219 cause of this may be the instability of the pyrite phase.

220 but also from formation of intermediate and pyrite phases.

221 ly controlled formation of the high-pressure pyrite polymorph of CuSe2 (by exposure to air).

222 siently increasing the marine burial rate of pyrite precipitated under euxinic (i.e., anoxic and sulf

223 On a geologic time scale, pyrite precipitation and burial governed a second feedba

224 uld have supported 20 to 100% of sedimentary pyrite precipitation and up to 75% of microbial sulfur r

225 bove + 40.0 per mille indicate at least some pyrite precipitation in the presence of a (34)S-depleted

226 han fossil Conotubus hemiannulatus show that pyrite precipitation was fuelled by the degradation of l

227 d sulfur pools and that the pathways forming pyrite precursors played an important role in establishi

228 s, particularly surface disulfide, to act as pyrite precursors.

229 ts were conducted with nano-porous sulfides (pyrite) produced by sulfate-reducing bacteria grown in t

230 ron and triangle combinations, MOFs based on pyrite (pyr) and rutile (rtl) nets were expected instead

231 However, the poor solubility of pyrite raises questions about its bioavailability and th

232 important as atmospheric oxygen in limiting pyrite reactivity over Earth's history.

233 Combined with the pyrite record, these results show that sulfate does not

234 te the full range of sedimentary delta(56)Fe(pyrite) recorded in Archean to modern sediments.

235 not reduce pyrite, suggesting that microbial pyrite reduction is metabolism-specific.

236 ess, the solar conversion efficiency of iron pyrite remains below 3%, primarily due to a low open cir

237 We found that pyrite removes Tc quantitatively from solution (log K(d)

238 c composition of Neoarchean-Paleoproterozoic pyrites requires both extensive marine iron oxidation an

239 Sulfur isotope evidence from sedimentary pyrites reveals that the exquisite fossilization of orga

240 ing Fe(II)-oxidizing culture enriched from a pyrite-rich aquifer.

241 contents, due to cocombustion of Tl-enriched pyrite roasting waste.

242 om the deposit that produced the cocombusted pyrite roasting waste.

243 iderite (C-rich agglomerates) and pyrrhotite/pyrite (S-rich spheres).

244 al and electrochemical properties to exploit pyrite's full potential for sustainable energy applicati

245 s knowledge opens up a new tactic to address pyrite's known defect problems.

246 d here, showing that the dissolution rate of pyrite significantly changes with the pH, temperature, a

247 e investigation on {100}-faceted n-type iron pyrite single crystals to understand its puzzling low VO

248 and poor photoconversion efficiency of iron pyrite single crystals.

249 ties and solar conversion efficiency of iron pyrite single crystals.

250 sizes of sedimentary Fe(3+)-oxyhydroxide and pyrite sinks for Neoarchean marine iron.

251 The slower Tc uptake was explained by higher pyrite solubility under acidic conditions.

252 Single (pyrite, sphalerite, and galena)- and bi-sulfide (pyrite-

253 te, sphalerite, and galena)- and bi-sulfide (pyrite-sphalerite and pyrite-galena) batch dissolution e

254 or galena (by 10-44%, except at pH 3 for the pyrite-sphalerite system).

255 ds with high HER catalytic activity, such as pyrite structure cobalt disulphide (CoS2), and substitut

256 s the same polyanionic dimer as found in the pyrite structure, which would suggest the possibility of

257 on FeS(2) surface upon Co doping in the iron pyrite structure.

258 evolution electrocatalyst material based on pyrite-structured cobalt phosphosulfide nanoparticles gr

259 and experiments to identify a highly stable, pyrite-structured iron oxide (FeO2) at 76 gigapascals an

260 s the most active HER catalyst based on iron pyrite, suggesting a scalable, low cost, and highly effi

261 or iron oxide-respiring cells did not reduce pyrite, suggesting that microbial pyrite reduction is me

262 ndicating that changes in the burial rate of pyrite sulfur and organic carbon did not singularly cont

263 o the burial histories of organic carbon and pyrite sulfur.

264 tem increased the rate of organic carbon and pyrite sulphur burial and hence atmospheric pO(2).

265 ncreases in the burial of organic carbon and pyrite sulphur in sediments deposited under large-scale

266 richments of molybdenum and vanadium and low pyrite sulphur isotope values (Delta(34)S values >/=65 p

267 ron (oxy)hydroxide to goethite, resulting in pyrite surface passivation.

268 A fundamental question is what role the pyrite surface plays in the reduction process.

269 ) reduction to elemental As(0) occurs on the pyrite surface under suboxic-reducing conditions and is

270 degrees C in slime streamers and attached to pyrite surfaces at a sulfide ore body, Iron Mountain, Ca

271 d be avoided if nitrite was removed from the pyrite suspensions through a washing procedure prior to

272 compositions of microscopic-sized grains of pyrite that formed about 3.4 billion years ago in the Ba

273 and silicate addition on the dissolution of pyrite, the major contributor to acid and metalliferous

274 and experimental study to establish ternary pyrite-type cobalt phosphosulphide (CoPS) as a high-perf

275 drogen-bearing iron peroxide (FeO2Hx) in the pyrite-type crystal structure was recently found to be s

276 sformations to the CaCl(2), alpha-PbO(2) and pyrite-type structures.

277 ility of the material as compared to natural pyrite was evidenced, as deduced from its characterizati

278 Neither pyrrhotite nor pyrite was found.

279 0 with a yield of 100 muM Fe(III) after 5 mM pyrite was incubated with 2000 muM nitrite for 24 h.

280 of aqueous vanadate after 48 h and uptake by pyrite was limited.

281 Significant oxidation of pyrite was measured at pH 0 with a yield of 100 muM Fe(I

282 No oxidation of pyrite was observed at pH 5.5 and 6.8.

283 Nanosized pyrite was readily oxidized to ferric iron and sulfate w

284 In euhedral pyrites, we found Se(-II) substitutes for S in the miner

285 eoproterozoic sediments and laboratory grown pyrites, we show that the triple iron isotopic compositi

286 On the early Earth, pyrite weathering by atmospheric oxygen was severely lim

287 lfur-oxidizing microorganisms control global pyrite weathering fluxes despite their ability to cataly

288 ignal is imperceptible and where terrestrial pyrite weathering occurs predominantly in bedrock fractu

289 uble S, total Fe and total As, implying that pyrite weathering posed a substantial stress on microbia

290 we show an anoxic photochemical mechanism of pyrite weathering that could have provided substantial a

291 gements of crystalline intermediates to form pyrite, which is attributed to partial solvation of the

292 Pyrite, which is common in organic-rich shales, is a pot

293 sulfide-polysulfide promotes Mo fixation in pyrite while promoting formation of organo-Re adducts; t

294 quent reaction of sulfide with iron produces pyrite whose burial in sediments is an important oxygen

295 independent sulphur isotopic compositions of pyrite with Delta(33)S of up to 0.91 per mille in Late O

296 inawite, and pyrite permit the generation of pyrite with Fe isotope signatures that nearly encapsulat

297 nd gap dropped from 2.2 (hematite) to ~1 eV (pyrite), with completely converted layers exhibiting abs

298 ils from ancient vent sites are preserved by pyrite, with no remaining carbonate shell.

299 oporous frameworks: diamondoid WUT-1(Ni) and pyrite WUT-2(Ni).

300 s been proposed as a possible alternative to pyrite, yet has only been studied for interesting magnet