ライフサイエンスコーパス: clay mineral

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

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

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

4 luence the sorption processes at surfaces of clay minerals.

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

6 ndant in montmorillonite and other expanding clay minerals.

7 n aquatic environment will be with suspended clay minerals.

8 ctroscopic signatures of water in two unique clay minerals.

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

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

11 mmediately that initiates release of As from clay minerals.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

45 Clay minerals are efficient sinks for heavy metals in th

46 Clay minerals are layer type aluminosilicates that figur

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

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

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

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

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

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

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

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

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

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

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

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

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

60 Clay mineral-bearing locations have been targeted for ma

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

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

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

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

65 39Ar during neutron irradiation in dating of clay minerals can produce erroneously old ages.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

97 Clay minerals inter-finger with calcium phosphate that c

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

117 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

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

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

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

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

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

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

124 Clay minerals often contain redox-active structural iron

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

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

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

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

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

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

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

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

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

134 0.15) owing to the presence of the smectite clay mineral saponite, which is one of the weakest phyll

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

136 to electron equivalents retained within the clay mineral structure.

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

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

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

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

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

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

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

144 eral dissolution and surface complexation on clay mineral surfaces.

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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

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