ライフサイエンスコーパス: clay mineral

1 phobic basal surfaces of kaolinite, a common clay mineral.

2 icients to one reference OM material and one clay mineral.

3 nts and to be poorly adsorbed onto untreated clay mineral.

4 iosity rover, which also identified smectite clay minerals.

5 as amorphous iron phases, organic matter and clay minerals.

6 sociated with clay minerals, and (iii) Fe in clay minerals.

7 c matter (OM) and sorption to phyllosilicate clay minerals.

8 ndant in montmorillonite and other expanding clay minerals.

9 n aquatic environment will be with suspended clay minerals.

10 ctroscopic signatures of water in two unique clay minerals.

11 the substituting cations in the TOT-layer of clay minerals.

12 interlayer region of swelling 2:1 layer type clay minerals.

13 REE are inferred to be weakly adsorbed onto clay minerals.

14 f redox sensitive elements on the surface of clay minerals.

15 ell-ordered member of the kaolin subgroup of clay minerals.

16 layer typically contains water and hydrated clay minerals.

17 idence that C compounds were associated with clay minerals.

18 ansformations and microstructural changes in clay minerals.

19 h the dominant constituents of soils such as clay minerals.

20 luence the sorption processes at surfaces of clay minerals.

21 quid water during this time to form hydrated clay minerals.

22 o study directly due to dilution by detrital clay minerals.

23 also adsorbed to clay minerals and OM-coated clay minerals.

24 mmediately that initiates release of As from clay minerals.

25 in barite, sphene, chalcedony, apatite, and clay minerals.

26 d in the U(VI) sorption curves for the three clay minerals.

27 by bioreduced (and pasteurized) iron-bearing clay minerals.

28 mechanism for Fe atom exchange in Fe-bearing clay minerals.

29 d different reduction potentials (Eh) of the clay minerals.

30 The citrate (10 mM) + Mn(II) (182.02 muM) + clay minerals (3% w/v) system in SDOC accounted for comp

31 Clay minerals abound in sedimentary formations and the i

32 el shows that sorption of organic cations to clay minerals accounts for more than 90% of the overall

33 he reductant, Mn(II) was a catalyst, and the clay minerals acted as an accelerator for both the reduc

34 mestone) and aluminosilicate (e.g., calcined clay) mineral additives are routinely used to partially

35 ell as in engineered environments, and while clay minerals' adsorption properties have been studied e

36 The clay minerals also serve as a sink for Cr(III).

37 Water in clay minerals, ammoniated phyllosilicates, or a mixture

38 aqueous Cr(VI) with two abiotically reduced clay minerals: an Fe-poor montmorillonite and an Fe-rich

39 e electron transfer between structural Fe in clay minerals and a vitreous carbon working electrode in

40 erent forms of structural clay-Fe(II) in the clay minerals and different reduction potentials (Eh) of

41 These results suggest the coevolution of clay minerals and early metabolites in our planet could

42 ifficult due to a lack of reactivity between clay minerals and electrodes.

43 between aqueous Fe(II) and structural Fe in clay minerals and electron conduction in octahedral shee

44 scribe for the first time synthetic smectite clay minerals and Fe-sulfide microspheres that reproduce

45 As clay minerals and humic substances are important soil co

46 cs of Cr(VI) reduction by Fe(II/III)-bearing clay minerals and may improve predictions of Cr(VI) beha

47 ssociated with palaeosols, the weathering of clay minerals and microbially induced sedimentary struct

48 for further studies on the sorption of Tl to clay minerals and Mn-oxides and its impact on Tl solubil

49 Surprisingly, U was also adsorbed to clay minerals and OM-coated clay minerals.

50 m, oxytetracycline) with two aluminosilicate clay minerals and one soil.

51 tals can be associated with soil components (clay minerals and organic matter), biosolid application

52 the high capacity for binding of arsenic to clay minerals and oxides of iron and aluminum in subsoil

53 Clay minerals and pedogenic metal (oxyhydr)oxides are th

54 are remarkably preserved by a combination of clay minerals and phosphate, with clay minerals providin

55 the fossils are composed of aluminosilicate clay minerals and some carbon, a composition comparable

56 s, Zn incorporated in dioctahedral layers of clay minerals and Zn sorbed to amorphous silica.

57 fundamental structure and composition of the clay minerals) and "external" (caused by a force externa

58 ticles, (ii) Fe-(hydr)oxides associated with clay minerals, and (iii) Fe in clay minerals.

59 n surface areas and equilibrium constants of clay minerals, and cation exchange capacity.

60 mentally relevant surfaces (Fe (hydr)oxides, clay minerals, and soil from Arizona and the Saharan Des

61 Fe-bearing clay minerals are abundant in argillaceous rocks as thei

62 In contrast, Fe-(hydr)oxides associated with clay minerals are dispersed by both extractants.

63 Clay minerals are efficient sinks for heavy metals in th

64 Serpentine clay minerals are found in many geological settings.

65 vior of iron (Fe(aq)(2+) -> Fe(surf)(3+)) in clay minerals are fundamental for environmental geochemi

66 Clay minerals are implicated in the retention of biomole

67 Clay minerals are layer type aluminosilicates that figur

68 ics and pathways of Cr(VI) reduction by such clay minerals are poorly understood.

69 Widespread iron-bearing clay minerals are potential materials that can reduce an

70 Clay minerals are principally Fe-Mg illite, mixed layers

71 We also find that clay minerals are relatively unimportant ice nuclei.

72 Assemblages of clay minerals are routinely used as proxies for paleocli

73 idence that Fe(II) uptake characteristics on clay minerals are strongly correlated to the redox prope

74 Illite-smectite interstratified clay minerals are ubiquitous in sedimentary basins and t

75 Among all natural submicrosized phases, clay minerals are ubiquitous in soils and sedimentary ro

76 Clay minerals are ubiquitous in subsurface environments

77 Iron-bearing clay minerals are ubiquitous in the environment, and the

78 ity toward reductive dissolution, Fe-bearing clay minerals are viewed as a renewable source of Fe red

79 On Mars, clay minerals are widespread in terrains that date back

80 Iron(II/III)-bearing clay minerals are widespread potential reductants of Cr(

81 Unique surface properties of aluminosilicate clay minerals arise from anisotropic distribution of sur

82 rals as well as the importance of Fe-bearing clay minerals as a renewable source of redox equivalents

83 lues underscore the importance of Fe-bearing clay minerals as redox-active phases in a wide range of

84 sms of abiotic and microbial Fe reduction in clay minerals as well as the importance of Fe-bearing cl

85 st that iron adsorbs on the edge surfaces of clay minerals at distinct structural sites commonly refe

86 Clay mineral-bearing locations have been targeted for ma

87 biologically formed structural Fe(II) in the clay minerals became increasingly important.

88 Lewis acid, titanium tetrachloride, with the clay mineral Bentonite K-10.

89 surfaces of mica (a common alumino-silicate clay mineral) bridged or "glued" by mfp-3.

90 ecause of its weak interlayer interaction, a clay mineral can be treated as two separate low-dimensio

91 Iron-bearing smectite clay minerals can act as electron sources and sinks in t

92 sequent reduction of U(VI) on Fe(II)-bearing clay minerals can control the mobility of uranium in sub

93 e that electron transfer to structural Fe in clay minerals can occur from Fe(II) sorbed to both basal

94 39Ar during neutron irradiation in dating of clay minerals can produce erroneously old ages.

95 This work shows that clay minerals can provide an exceptionally high fidelity

96 reverse tricarboxylic acid (rTCA) cycle and clay mineral catalysts coevolved remains a mystery in th

97 kely to have played an essential role in any clay mineral-catalyzed prebiotic RNA synthesis.

98 mated cation-exchange capacity attributed to clay minerals (CECCLAY).

99 ing secondary Fe oxyhydroxide, Al(OH)(3), or clay mineral colloids, suggesting that the V is not bioa

100 general term for the dioctahedral mica-like clay mineral common in sedimentary rocks, especially sha

101 Talc, as an important class of clay minerals constituting subducting oceanic crust, has

102 Fe-bearing clay minerals contain structural iron that can be redox-

103 r reaction controlling its mobilization, and clay minerals could mitigate As mobilization with surfac

104 and geochemical evidence for an increase in clay mineral deposition in the Neoproterozoic that immed

105 pidly than biologically reduced iron-bearing clay minerals despite the minerals having similar struct

106 (II) in both low (SWy-2) and high (NAu-1) Fe clay minerals did not reduce PCE or TCE under anoxic con

107 increase in reduction potential results from clay mineral dissolution resulting in increased Fe(III)

108 -toxic ionic aluminium (Al(3+)) species from clay minerals, driving the evolution of counteractive ad

109 that hinders N(2)O(5) uptake as well as 10 A-clay minerals (e.g., Illite) that compete with water and

110 Sr isotope ratios, trace element content and clay mineral evidence, that carbonates bearing the (13)C

111 t exchange by calcium for sodium residing on clay mineral exchange sites.

112 production of pedogenic clay minerals (the "clay mineral factory"), leading to increased marine buri

113 aster HCA reduction occurred with decreasing clay mineral Fe content.

114 -content clay mineral SWy-2, suggesting that clay mineral Fe controlled the formation of the reactive

115 taminant reduction, yet our knowledge of how clay mineral Fe reduction pathways and Fe reduction exte

116 tion pathways and Fe reduction extent affect clay mineral Fe(II) reactivity is limited.

117 Our data suggest that clay mineral Fe(III) is a sink for electrons from added

118 In addition to clay minerals, Fe(III) oxides particles have recently be

119 iments motivated by the hypothesis that some clay mineral formation may have occurred under oxidized

120 arly Hesperian or younger age indicates that clay mineral formation on Mars extended beyond Noachian

121 tmosphere, and the (18)O/(16)O of authigenic clay minerals formed in these environs reflect those enr

122 Authigenic clay minerals formed on or in the seafloor occur in ever

123 Fe(II)-rich clay minerals found in subsurface redox transition zones

124 ic composition of hydroxyl groups (OH(-)) in clay minerals from a highly expanded PETM section in the

125 admixed with less soluble salts, the lack of clay minerals from acid-rock reactions, high sphericity

126 E distinguishes Fe(III) reduction of layered clay minerals from that of Fe oxyhydroxides, where accum

127 redox interactions between sorbed Fe(II) and clay minerals gained in this study is essential for futu

128 Among clay minerals, halloysite nanotubes (HNTs) possess a neg

129 tics of redox reactions involving Fe-bearing clay minerals has been challenging due to the inability

130 e of simple oxide surfaces: edge surfaces of clay minerals have a variable proton surface charge aris

131 e is a degree of site masking in the ternary clay mineral-humic acid-bacteria composite.

132 This work investigated REE adsorption to the clay minerals illite and kaolinite through pH adsorption

133 Sorption to the phyllosilicate clay minerals Illite, kaolinite, and bentonite has been

134 In montmorillonite (MMT), a common clay mineral in soils, sediments, and muds, the swelling

135 ndings provide new insights into the role of clay minerals in As transformation, which is significant

136 Iron occurs in clay minerals in both ferric and ferrous forms.

137 tering or preservational effects of detrital clay minerals in modern marine continental margin depoce

138 Our results demonstrate the significance of clay minerals in the (trans)formation of Mn-containing p

139 i(4)O(10)(OH)(2)), one of the representative clay minerals in the alumina-silica-water (Al(2)O(3)-SiO

140 f depositional heterogeneous distribution of clay minerals in the pores.

141 ium are mobilized from exchangeable sites on clay minerals in the shale formations during the hydraul

142 ificant role of kaolinite (Kln), a pervasive clay mineral, in enhancing As(V) immobilization during f

143 lution of the smectite-to-illite sequence of clay minerals, including the nature of coexisting specie

144 Our finding of 5-20% Fe atom exchange in clay minerals indicates that we need to rethink how Fe m

145 Clay minerals inter-finger with calcium phosphate that c

146 e insights into how atmospheric dust-derived clay minerals interact with marine microorganisms to enh

147 e the importance of soil pH, enzyme-, and OP-clay mineral interactions in controlling the mineralizat

148 Such comprehensive knowledge of PFAS at the clay mineral interface is critical to developing novel s

149 aveling the surface geochemistry of hydrated clay minerals is an abiding, if difficult, topic in eart

150 Structural Fe in clay minerals is an important redox-active species in ma

151 Structural Fe in clay minerals is an important, albeit poorly characteriz

152 Structural Fe in clay minerals is an important, potentially renewable sou

153 Herein, the crystallization of clay minerals is catalyzed by succinate, an example of a

154 ise the question whether Fe interaction with clay minerals is more dynamic than previously thought.

155 The interaction of Fe(II) with clay minerals is of particular relevance in global geoch

156 that: (1) As desorption/adsorption from/onto clay minerals is the major reaction controlling its mobi

157 Microdiffraction imaging identified the clay mineral kaolinite to play a key role in the immobil

158 th (13)C-labelled amino acids and two common clay minerals (kaolinite and montmorillonite).

159 sequestration by a lanthanum (La) exchanged clay mineral (La-Bentonite), which is extensively used i

160 Instead catalysis is shown to occur at the clay mineral lattice-edge where hydroxyl groups and expo

161 electron transfer from the inner part of the clay mineral layer structure to the reactive sites.

162 onates (<10 percent), olivine (<10 percent), clay minerals (<20 percent), and quartz (<5 percent) in

163 ps developed for these four commonly studied clay minerals may be applied to future studies intereste

164 oxhydroxides, and V-bearing Al(OH)(3) and/or clay minerals may have occurred.

165 ding that the infrared absorptivity of fired clay minerals, measured at the Si-O-Si stretching resona

166 tion can alter the stability of nanoparticle/clay mineral mixtures.

167 electron donor, we found that the Fe-bearing clay minerals montmorillonite SWy-2 and nontronite NAu-2

168 we report that citrate along with Mn(II) and clay minerals (montmorillonite and kaolinite) reduce Cr(

169 on rate constants by bioreduced iron-bearing clay minerals (montmorillonite SWy-2 and nontronite NAu-

170 neral matrix (containing structural water of clay minerals) must be separated from SOM and samples ne

171 A Na-smectite clay mineral (Na-Mt) was exchanged with various amounts

172 n of the sorption properties of three source clay minerals-Na-rich montmorillonite (SWy-2), illite-sm

173 plane-sorbed Fe(II) to structural Fe(III) in clay mineral NAu-1 at pH 4.0 and 6.0 occurred but to a m

174 sorbed to basal planes and edge OH-groups of clay mineral NAu-1.

175 We calculated that 5-20% of structural Fe in clay minerals NAu-1, NAu-2, and SWa-1 exchanged with aqu

176 ditions are needed to synthesize the Fe-rich clay mineral nontronite at low temperatures.

177 h, it closely resembles the structure of the clay mineral nontronite, a representative of the Fe-rich

178 s arsenate) adsorption to the phyllosilicate clay minerals of the aquifer.

179 demonstrated the rapid formation of Fe-rich clay minerals of variable crystallinity from aqueous Fe(

180 pes, chemical index of alteration (CIA), and clay minerals) of two well-dated Triassic-Jurassic (T-J)

181 Clay minerals often contain redox-active structural iron

182 We investigated the role of Fe-bearing clay minerals on the bioreduction of nitrobenzene.

183 s or sheaths, which are instead preserved by clay minerals or francolite.

184 nding to montmorillonite (an aluminosilicate clay mineral) or clay-enriched soils had been shown to e

185 Today most clay minerals originate in biologically active soils, so

186 culations, Fe(II) located at the edge of the clay mineral particles alone cannot account for the fast

187 Here we explore the distribution of natural clay mineral particles in poly(ethylene glycol) (PEG)/de

188 idal size and permanent structural charge of clay mineral particles, which endow them with significan

189 on and suggest that RMI formation depends on clay mineral presence and Fe content.

190 we demonstrate a causal relationship between clay mineral production by the melting Sturtian Snowball

191 Clay minerals provide a useful model system for studying

192 ination of clay minerals and phosphate, with clay minerals providing the highest fidelity of preserva

193 flood inefficiency include low permeability, clay mineral reactivity and fluid incompatibility.

194 chemically reduced (dithionite) iron-bearing clay minerals reduced nitrobenzene more rapidly than bio

195 Here, we evaluated whether Fe(II) in clay minerals reduces tetrachloroethene (PCE) and trichl

196 nonlinear relationship of rate constant and clay mineral reduction potential E(H) have major implica

197 The surface reactivity of clay minerals remains challenging to characterize becaus

198 ce of iron-rich carbonate relative to common clay minerals requires a minimum partial pressure of car

199 0.15) owing to the presence of the smectite clay mineral saponite, which is one of the weakest phyll

200 ell-graded soil grain size distribution, and clay minerals serving as cementing agents in the nest so

201 Moreover, the presence of clay minerals slows methane production and reduces final

202 erlayer cation, the greater the influence of clay mineral structure and hydrophobicity on the configu

203 to electron equivalents retained within the clay mineral structure.

204 ociated with Mg and Al and is likely part of clay minerals such as illite.

205 Our results suggest that Fe-rich clay minerals such as nontronite can form rapidly under

206 (hydr)oxides were dominantly associated with clay minerals, suggesting that their dispersion as free

207 interlayer cations with water molecules and clay mineral surface oxygens is governed largely by cati

208 Adsorption and redox transformations on clay mineral surfaces are prevalent in surface environme

209 Yet, a molecular-level understanding of clay mineral surfaces has been hampered by the lack of a

210 diments, adsorption of carbon compounds onto clay mineral surfaces played a fundamental role in the b

211 electrical double layers formed on hydrated clay mineral surfaces, particularly those in the interla

212 he complexation of inorganic contaminants on clay mineral surfaces, they also evidenced the reliabili

213 /precipitation), and surface complexation on clay mineral surfaces.

214 eral dissolution and surface complexation on clay mineral surfaces.

215 CE after adding 5 mM dissolved Fe(II) to the clay mineral suspensions.

216 y mineral Syn-1 > Fe(OH)(2) > low Fe-content clay mineral SWy-2, suggesting that clay mineral Fe cont

217 e observed in the presence of low Fe-content clay mineral SWy-2.

218 E products decreased in the order of Fe-free clay mineral Syn-1 > Fe(OH)(2) > low Fe-content clay min

219 ons containing 20 mM Fe(II) alone or Fe-free clay mineral (Syn-1), we observed a purely Fe(II)-contai

220 approach is applied to study collections of clay mineral tactoids interacting with two synthetic pol

221 s clays, in particular Illite-a non-swelling clay mineral that naturally contains interlayer K(+) and

222 aining soluble reduced metals and expandable clay minerals that absorb cations, providing a capacity

223 ematic oscillations of various evaporite and clay minerals that can be linked to the variation of reg

224 ould greatly enhance production of pedogenic clay minerals (the "clay mineral factory"), leading to i

225 ic matter is mixed on a nanometer scale with clay minerals, the individual D/H ratios of the two H-be

226 espite the importance of Fe redox cycling in clay minerals, the mechanism and location of electron tr

227 Given the ubiquity of natural clay minerals, the most likely interaction of nanopartic

228 ffect on Cr(VI) reduction kinetics: for both clay minerals, the rate constant of Cr(VI) reduction var

229 many inter-crystalline pores are produced in clay minerals, this type of pores is not the most import

230 nect the synthesis of sauconite, a model for clay minerals, to prebiotic photochemistry.

231 rmination of clay-Fe(II/III) and U(IV/VI) in clay mineral-U suspensions such that advanced spectrosco

232 Cr(VI) by organic ligand in the presence of clay minerals under certain environmental conditions.

233 The stability of clay minerals under such hydrous subduction environment

234 ing the redox properties of structural Fe in clay minerals using electrochemical approaches, however,

235 study, the retention mechanism of Fe(II) on clay minerals was investigated using macroscopic sorptio

236 uction on soil surrogates composed of HA and clay minerals was studied by use of a coated-wall flow r

237 processes between divalent Fe and Zn at the clay mineral-water interface.

238 Using experimental data on an iron-bearing clay mineral, we illustrate how mediated electrochemical

239 Clay minerals were co-located with P only to a lesser ex

240 d structural incorporation into double-layer clay minerals were likely responsible for greater retent

241 Under anoxic conditions, clay minerals were shown to increase Cd retention by fav

242 owever, the correlations between C forms and clay minerals were weakened in the coarse-textured Calci

243 en shown using culture experiments with pure clay minerals, whereas recognition in nature remains dif

244 ity, and ion-exchange capacity properties of clay minerals, which constitute a major fraction of glob

245 It is generally assumed that clay minerals, which contribute approximately two-thirds

246 fraction as U(VI) primarily adsorbed on 2:1 clay minerals, which is in line with X-ray Absorption Sp

247 by creating a hydrogel made from geological clay minerals, which provides an efficient confinement e

248 odels for an illite-smectite interstratified clay mineral with a ratio of 1:1 and a Reichweite parame

249 We discovered that the interaction of clay minerals with dissolved organic matter and a gamma-

250 mpact on Cd retention in the presence of two clay minerals with low Fe contents, a natural kaolinite

251 of organic monomers within the interlayer of clay minerals yields nanocomposites with novel material