ライフサイエンスコーパス: silicate

1 gands (e.g., 10 mg L(-1) of HA or 100 muM of silicates).

2 tion for adsorption sites in the presence of silicate.

3 heets of TBA0.24H0.76Ca2Nb3O10 and a layered silicate.

4 ed by kinetic dissolution rates of dicalcium silicate.

5 high concentrations of respirable silica and silicates.

6 ble radical intermediates or hypercoordinate silicates.

7 be synthesized, and thus their corresponding silicates.

8 t mainly occurs in mineral phases such as Zn silicates.

9 ganic matter (humic acid, HA), and dissolved silicates.

10 ume (1 mL) permits detection limits of 21 nM silicate, 3 nM taurine, 3 nM sulfide, and 13 nM cyanide.

11 With silicate addition, a smooth, continuous, coherent and ap

12 pplication of the technique by measuring the silicate and borate depth profiles in the Pacific Ocean;

13 was shown feasible for very weak acids like silicate and borate with a dedicated element specific de

14 lation between (87)Sr/(86)Sr ratios of rice, silicate and carbonate fractions of soil.

15 tallisation in glasses and mainly focuses on silicate and closely related oxide glasses.

16 e 1.88 Ga Gunflint Iron Formation contain Fe-silicate and Fe-carbonate nanocrystal concentrations in

17 a consequence of rapid weathering of calcium silicate and hydroxide minerals derived from the demolit

18 uilibrium iron isotope fractionation between silicate and iron under core formation conditions in Ear

19 The acidity dissolved silicate and liberated metal ions that balanced OH(-), p

20 est the presence of magnesium-rich grains of silicate and oxide composition, partly with iron inclusi

21 nd Rh oxide/hydroxide nanoparticles with the silicate and poor resistance to sintering.

22 ulted from fungal interactions with both the silicate and the sulfide, largely resulting from organic

23 We show that mantle silicates and core metal have comparable melting tempera

24 ne particles composed of calcium aluminates, silicates and iron condense into atmospheric 'dust', whi

25 n atoms may be retained at defects in mantle silicates and oxides.

26 re of volatiles and denser materials such as silicates and salts.

27 tentially available Zn, organic matter, clay silicate, and iron (hydr)oxide contents and pH.

28 several common groundwater solutes (sulfate, silicate, and phosphate) promote the formation of nonura

29 n our solar system in the form of ice, dust, silicates, and refractory organic material with some int

30 Rare earth silicate apatites are one-dimensional channel structures

31 te glass powder with clay mixes using sodium silicate as binder and borate salt as flux.

32 aphite-saturated COH fluids interacting with silicates at 1-3 GPa and 800 degrees C display unpredict

33 ression mechanisms that take place in liquid silicates at the high pressures and temperatures in the

34 on of emitters on a microscope cover slip of silicate based glass (such as quartz).

35 rally related microporous HKUST-1 as well as silicate-based hierarchical materials.

36 In the case of silicate-bearing rocks the abrupt slip acceleration resu

37 echanism of confined synthesis of surfactant-silicate between two identical thin layers of oils on a

38 This Zn silicate biomineralization has relevant implications for

39 oxysilanes [bis(2-methyl-2,4-pentanediolato) silicate, bis(2,2,4-trimethyl-1,3-pentanediolato) silica

40 we demonstrate that a variety of weak acids (silicate, borate, arsenite, cyanide, carbonate, and sulf

41 Tricalcium silicate (Ca3SiO5), the main constituent of Portland cem

42 rophobicity and hydrolytic lability of these silicates can be (independently) controlled by choice of

43 al dust particles consistent with silica and silicates; carbonaceous coal dust was less prominent.

44 were to assess the effectiveness of calcium silicate cement (Biodentine) versus glass ionomer cement

45 esponses with commercially available calcium silicate cement (white mineral trioxide aggregate; WMTA)

46 fects such as bridging site vacancies in its silicate chains.

47 spite increasing numbers of vacancies in its silicate chains.

48 nt display an anomaly in the position of the silicate Christiansen Feature consistent with reduced sp

49 rch has since been dedicated to the study of silicate clays, layered double hydroxides, believed to b

50 particles such as carbon-based 2D materials, silicate clays, transition metal dichalcogenides (TMDs),

51 , suggesting a CO2-induced dissolution of Fe-silicates/clays and/or reductive dissolution of Fe(3+) t

52 These blooms are terminated by limiting silicate concentrations in summer.

53 a nearshore station, nitrate, phosphate, and silicate concentrations reached 19, 1.4, and 10 microM,

54 oxidation retardation derived from elevated silicate concentrations.

55 well as a variety of other groundwater/high silicate containing natural and engineered sites that mi

56 which is thought to be differentiated into a silicate core with an icy mantle.

57 e crystals of four new salt-inclusion uranyl silicates, [Cs3F][(UO2)(Si4O10)], [Cs2Cs5F][(UO2)2(Si6O1

58 Ocean, clear evidence of a marked pre-bloom silicate decline of 1.5-2 microM throughout the winter m

59 This silicate decrease is primarily attributed to natural mul

60 However, the stability of uranium in opaline silicates, determined in part by the binding mechanism f

61 Dense hydrous magnesium silicate (DHMS) phases play a crucial role in transporti

62 tion of the solar nebula, core formation and silicate differentiation cannot explain these observatio

63 Both features are inherited from metal-silicate differentiation in primitive Earth and depend u

64 This must have been acquired during global silicate differentiation within the first 30 million yea

65 tionation under specific conditions of metal-silicate differentiation.

66 concentrations were controlled by dicalcium silicate dissolution and Ca-Si-H precipitation, leading

67 eleased to solution as V(V) during dicalcium silicate dissolution and some V was incorporated into ne

68 ate surfaces strongly influence the rates of silicate dissolution, hydration, and crystallization.

69 by computational simulation, suggesting that silicate-doping of a pseudoamorphous iron oxyhydroxide (

70 n motif in zeolite chemistry: the box-shaped silicate double-four-ring (D4R).

71 arly the prominence of Diatoms inferred from silicate drawdown, drive interannual differences in the

72 ant to Earth's mantle, iron concentration in silicates drops above 70 GPa before increasing up to 110

73 otopic exchanges occur between carbonate and silicate during subduction remains unclear.

74 and super-Earths, raising the possibility of silicate dynamos in these bodies.

75 ssimilate to weather grains of limestone and silicates each with a combined calcium and magnesium con

76 itional and isotopic resemblance to the bulk silicate Earth (BSE) for many elements, but is considere

77 we include an updated estimate for the bulk silicate Earth (C/N = 49.0 +/- 9.3).

78 ecent (142)Nd isotope data indicate that the silicate Earth (its crust plus the mantle) has a samariu

79 The (142)Nd offset between the accessible silicate Earth and chondrites therefore reflects a highe

80 f the difference in delta(66)Zn between bulk silicate Earth and lunar basalts and crustal rocks, the

81 ic compositions of many elements in the bulk silicate Earth are the same as in chondrites.

82 a limited range, indistinguishable from bulk silicate Earth estimates.

83 pattern of volatile element depletion in the silicate Earth is consistent with partial melting and va

84 The silicate Earth is strongly depleted in moderately volati

85 The high C/N bulk silicate Earth ratio therefore is best satisfied by accr

86 monstrate that the halogen depletion of bulk silicate Earth relative to primitive meteorites is consi

87 ionated Cr isotopes, relative to the igneous silicate Earth reservoir, in metamorphosed banded iron f

88 ult of the incomplete condensation of a bulk silicate Earth vapour at an ambient pressure that is hig

89 t loss, set limits on the composition of the silicate Earth, and provide significant parameter bounds

90 at drive the chemical differentiation of the silicate Earth.

91 are similar to those in the present-day bulk silicate Earth.

92 , notably the overabundance of indium in the silicate Earth.

93 al, but still poorly defined, level of metal-silicate equilibration.

94 synthesis and selected properties of various silicate ester derivatives (tetraalkoxysilanes) of the t

95 tates in nominally acarbonaceous crystalline silicates, even if present at levels at 10-100 ppm, migh

96 The CO2 content of fluids interacting with silicates exceeds the amounts measured in the pure COH s

97 ernal surface of micropores of a microporous silicate exhibit high selectivity and activity in transf

98 new family of mixed anion cesium rare earth silicates exhibiting intense scintillation in several ra

99 This study evaluated the effects of silicate fertilization on plant Si uptake and carbon bio

100 to 1.16-2.17 x 10(6) tonnes CO2 yr(-1) with silicate fertilizer additions.

101 ed at 0.94 x 10(6) tonnes CO2 yr(-1) without silicate fertilizer additions.

102 Therefore, providing silicate fertilizer during rice production may serve as

103 storage with increasing application rates of silicate fertilizer.

104 e straw with increasing application rates of silicate fertilizer; (2) Strong positive correlations be

105 We further propose that hypervalent silicates form ion-pairs with pentanidinium and bisguani

106 eached surface layer in which cations in the silicate framework are gradually leached out and replace

107 the positions adopted by heteroatoms in the silicate framework-can be extracted from experimental da

108 The transport of magnesium as oxide or silicate from the cooling core to underneath the mantle

109 versal reaction mechanism that controls both silicate glass corrosion and mineral weathering.

110 We show higher melting-point silicate glass cross-cutting lower melting-point Al-Cu-F

111 wires (bulk Tm = 1064 degrees C) embedded in silicate glass fibres (Tg = 567 degrees C) were drawn in

112 Here, we report the discovery of silicate glass spherules in a discrete stratigraphic lay

113 usive propagation of light through a channel silicate glass waveguide.

114 ince it is a highly resistant potash-alumino-silicate glass, colored by magnetite nanocrystals (<200

115 In alumino-silicate glasses and melts, extensively used in industry

116 Aqueous dissolution of silicate glasses and minerals plays a critical role in g

117 Silicate glasses are durable solids, and yet they are ch

118 ental insight into the structural changes of silicate glasses as analogue materials for silicate melt

119 Silicate glasses containing lead, also called lead cryst

120 roscopic measurements of iron-enriched dense silicate glasses, as laboratory analogues for dense magm

121 equilibrated metallic melt does not wet the silicate grain boundaries and tends to reside in isolate

122 If -OH or H2O is generated in rims on silicate grains, there are important implications for th

123 pamine-laced hydroxyapatite collagen calcium silicate (HCCS-PDA) were examined by culturing rat mesen

124 t 300 K in nano-cages consisting of (alumino)silicate hexagonal prisms forming a two-dimensional arra

125 zation and cross-linking of calcium (alumino)silicate hydrate (C-(A-)S-H), which is the primary bindi

126 h scale, the mesoscopic structure of calcium silicate hydrate (C-S-H) plays a critical role in determ

127 on in the depleted layer, concurrent calcium silicate hydrate (CSH) alteration to an amorphous zeolit

128 Calcium silicate hydrate (CSH) is the main binding phase of Port

129 Calciuam-silicate-hydrate (C-S-H) is the principal binding phase

130 Gelation and densification of calcium-silicate-hydrate take place during cement hydration.

131 (90)Sr insertion and decay in C-S-H (calcium-silicate-hydrate) in order to test the ability of cement

132 Magnesium carbonate, phosphate, silicate-hydrate, and oxysalt (both chloride and sulfate

133 ted database of atomic structures of calcium-silicate-hydrate, the binding phase of concrete, against

134 Herein, we focus on crystalline calcium-silicate-hydrates (C-S-H) as a model system with applica

135 concrete rely upon the formation of calcium-silicate-hydrates (C-S-H) during cement hydration.

136 action of Ca3SiO5 with water to form calcium-silicate-hydrates (C-S-H) still hosts many open question

137 sient local molecular composition, extent of silicate hydration and polymerization.

138 Silicate hydration is prevalent in natural and technolog

139 Reduced Arctic silicate import and the projected hemispheric-scale clim

140 3.8-3.9 A) and a small amount of uranyl and silicate in a bidentate, mononuclear (edge-sharing) coor

141 hetic amorphous silica, U was coordinated by silicate in a double corner-sharing coordination geometr

142 The appearance of silicate in a sample put in a glass container as a funct

143 the coordination environment also contained silicate in both edge-sharing and corner-sharing coordin

144 ect determination of dissolved phosphate and silicate in seawater using ion exclusion chromatography

145 the determination of dissolved phosphate and silicate in seawater.

146 Since the discovery of mesoporous silicates in 1990s, organic-inorganic assembly processes

147 water-bearing supercritical CO2 (scCO2) and silicates in reservoir rocks.

148 g mineral group, fundamentally distinct from silicates in the Earth's crust in that carbon binds to t

149 ortland cement, is amongst the most reactive silicates in water.

150 Ceres' dry exterior displays hydroxylated silicates, including ammoniated clays of endogenous orig

151 icrostructural analysis shows that the metal-silicate interface has characteristics expected for a te

152 ize non-topotactically through a nanolayered silicate intermediate during hydrothermal synthesis.

153 t between the C-Br bond and C-Si bond in the silicate intermediate.

154 These marked fluctuations in pre-bloom silicate inventories will likely have important conseque

155 Here we provide evidence that silicate is deposited on extracellular polymeric substan

156 Silicate is structurally incorporated within this layer

157 The interaction of deep aqueous fluids with silicates is a novel mechanism for controlling the compo

158 Complete dehydration of silicates is expected before plate subduction, contrasti

159 m isotope fractionation of these elements in silicates is expected to be negligible at magmatic tempe

160 es, and -mesylates with alkylbis(catecholato)silicates is presented.

161 s on clays, layered transition metal oxides, silicates, layered double hydroxides, metal(iv) phosphat

162 and non-silicifying plankton at the onset of silicate limitation.

163 ed by the physical properties of constituent silicate liquids.

164 ually considered to reside unobserved in the silicate lower mantle.

165 bent (LSS) for CO2 capture using the layered silicate magadiite and organo-magadiite modified with po

166 s for planetary magnetic-field generation in silicate magma layers deep inside such planets.

167 bout the incorporation and role of carbon in silicate magmas is crucial for our understanding of the

168 c magmas and reduced eruptibility of hydrous silicate magmas relative to dry rift volcanics.

169 during synthesis and why specifically uranyl silicates make excellent frameworks for salt-inclusion p

170 High-pressure silicates making up the main proportion of the earth's i

171 h radial seismic models, and leaves behind a silicate mantle that matches the observed mantle abundan

172 a maximum of 0.5 +/- 0.2 per cent of Earth's silicate mass, cannot solely account for present-day ter

173 Here we show that complex silicate material dissolution behaviors can emerge from

174 structure type MFI is an aluminosilicate or silicate material that has a three-dimensionally connect

175 l geochemical systems and developing durable silicate materials for various engineering applications.

176 the basis of the pervasiveness of the SW and silicate materials, that the production of radiolytic SW

177 U may bind directly to the opaline silicate matrix, or to materials such as iron (hydr)oxid

178 tiometric thermometer based on a very stable silicate matrix.

179 Hence, it is likely that silicate melt above and below the mantle transition zone

180 g towards possible exsolution of carbon from silicate melt at reduced oxygen contents.

181 behaviour of the H-C-O-S-Cl-F system in the silicate melt causes unmixing of the fluid phase to form

182 Al-Cu-Fe alloys, and Al2O3 enrichment in the silicate melt surrounding the alloys.

183 ion of metallic Al to Al2O3, occurring where silicate melt was in contact with Al-Cu-Fe alloys.

184 a hydrosaline phase in equilibrium with the silicate melt, both responsible for buffering the chlori

185 reaction history between Al-Cu-Fe alloys and silicate melt.

186 CO2 bearing silicate melting and its relevance in the upper mantle r

187 nano-structure and the dynamic properties of silicate melts and glasses is fundamental to both Earth

188 f silicate glasses as analogue materials for silicate melts at ultrahigh pressures.

189 While viscosity of depolymerized silicate melts increases with pressure consistent with t

190 A defining characteristic of silicate melts is the degree of polymerization (tetrahed

191 the radiative thermal conductivity of dense silicate melts may decrease with pressure and so may be

192 However, the thermal transport properties of silicate melts under relevant high-pressure conditions a

193 lasting regions containing both metallic and silicate melts.

194 top of the D'' layer contains ferromagnesian silicate [(Mg,Fe)SiO3] with nominally 10 mole percent Fe

195 ich may possibly coexist in equilibrium with silicate mineral assemblages.

196 ferences can lead to spatial distribution of silicate mineral dissolution and carbonate mineral preci

197 e reaction of aqueous CO2 with the magnesium silicate mineral forsterite was studied in systems with

198 amorphous rims produced by SW irradiation of silicate mineral grains on the exterior surfaces of inte

199 gen ((18)O), appears to be critical for this silicate mineral to carbonate in low water environments.

200 n the shallow aquifer is dominated mainly by silicate mineral weathering, and no CO2 leakage signals

201 F comprise 85-90% by volume of the magnesium silicate mineral, talc.

202 eric carbon dioxide through the breakdown of silicate minerals and is thought to stabilize Earth's lo

203 utralization from on-site available reactive silicate minerals may be used to maintain neutral pH, af

204 Reactions of CO2 with magnesium silicate minerals to precipitate magnesium carbonates ca

205 te product sensitive to the particle size of silicate minerals.

206 r rocks, and the reactive surface area ar of silicate minerals.

207 rization) in influencing SIP measurements of silicate minerals.

208 lly created urban soils containing Ca and Mg silicate minerals.

209 ing of trace sulfide minerals in addition to silicate minerals.

210 9) Si bonds between intermediate nanolayered silicate moieties and the crystallizing MFI zeolite nano

211 e), tellurium (Te), and antimony (Sb) in the silicate Moon can instead reflect core-mantle equilibrat

212 -linked hydrated network using biocompatible silicate nanoparticles (SiNPs).

213 Novel silicate nanoplatelets that induce osteogenic differenti

214 llowed by an in situ repolymerization of the silicate network.

215 ate, bis(2,2,4-trimethyl-1,3-pentanediolato) silicate or Si(eg)2 polymer with 5-98% conversion, as go

216 raction of two low-solubility phases-Cr(III) silicates or (hydr)oxides and Mn(III/IV) oxides-that lea

217 ed to similar sorbed amounts of NA, FLU, SA, silicates or HA as compared to the stoichiometric magnet

218 ong contrast to common glass formers such as silicates or phosphates.

219 demonstrate the simple one-pot synthesis of silicate organic frameworks based on octahedral dianioni

220 An organic-modified silicate (OrMoSils) sol-gel doped with a pH-sensitive dy

221 Without silicate, oxidized pyrite particles form an overlayer of

222 bsolute bulk concentrations on heterogeneous silicate particle surfaces at early stages of hydration.

223 f low-surface-area ( approximately 1 m(2)/g) silicate particles.

224 Here, we use high-pressure metal-silicate partitioning experiments to show that the obser

225 e,Al)(Al,Fe,Si)O3 bridgmanite (also known as silicate perovskite), has hampered any conclusive result

226 sometimes majoritic garnet or former calcium silicate perovskite.

227 , conclusions consistent with condensates of silicates, perovskite, and silica of submicron radii.

228 woodite, the thermodynamically stable uranyl silicate phase, was slow.

229 eal the formation of an intermediate layered silicate phase, which subsequently transforms into zeoli

230 ered region in which free lime and dicalcium silicate phases were absent and Ca-Si-H was precipitated

231 ar only been observed in a few high pressure silicate phases.

232 consisting of centimetre-sized metallic and silicate phases.

233 he density contrast between solid and liquid silicate phases.

234 ons and increases in surf zone turbidity and silicate, phosphate, and dissolved inorganic nitrogen co

235 itions are consistent with enrichment of the silicate portions of the Moon in the heavier Zn isotopes

236 h-temperature sintering of compacted yttrium silicate powders doped with Pr(3+) and Li(+).

237 voured in sulfate-poor environments where Fe-silicate precipitation could outcompete Fe-sulfide forma

238 ve vegetation with the addition of inorganic silicate precursors and without the addition of extraneo

239 Increasing concentrations of dissolved silicate progressively retard Fe(II) oxidation kinetics

240 Quaternary ammonium methacryloxy silicate (QAMS)-containing acrylic resin demonstrated co

241 Si(eg)2 or bis(2-methyl-2,4-pentanediolato) silicate reacted with EtOH and catalytic acid to give Si

242 Hypercoordinate silicates represent a new and improved class of radical

243 In particular, mixed silicates represent an advancement with practical applic

244 mmol m(-2) d(-1) for nitrate, phosphate, and silicate, respectively, along the shore.

245 47 and 0.31% for the dissolved phosphate and silicate, respectively, were obtained in National Resear

246 ate depth profiles in the Pacific Ocean; the silicate results show an excellent match with results fr

247 oxide persists, the chemical interactions in silicate-rich rocks may curb this transport drastically

248 nced weathering, the spreading of ultramafic silicate rock flour to enhance natural weathering rates,

249 The basement is a calc-silicate rock housing hydrothermal decarbonation reactio

250 The role of pH changes associated with water-silicate rock interactions during diamond formation is u

251 ium isotope record of seawater as a proxy of silicate rock weathering and erosion, we calculate chang

252 Enhanced weathering of (ultra)basic silicate rocks such as olivine-rich dunite has been prop

253 pheric CO2 levels and chemical weathering of silicate rocks that operates over million-year time scal

254 a weathering fluid interacting with dry-land silicate rocks.

255 y Si4O10 sheets with a previously unobserved silicate sheet topology that contains the uncommon cycli

256 The calcium silicate shell traps and protects an siRNA payload, whic

257 nanoparticles to create an insoluble calcium silicate shell.

258 penetrating peptides attached to the calcium silicate shell.

259 on can be produced directly from inexpensive silicates/silicon oxide precursors by a two-step electro

260 rived geotherm also intersects the carbonate-silicate solidus, suggesting that partial melt defines t

261 ection of aqueous zinc sulfate into a sodium silicate solution.

262 paper describes the preparation of a Layered Silicate Sorbent (LSS) for CO2 capture using the layered

263 sis of dilute adsorbed organic molecules and silicate species on low-surface-area particles, which un

264 produced vapor out of which a thick cloud of silicate spherules condensed that were then ground into

265 ism for reduced ARD through the formation of silicate-stabilized iron oxyhydroxide surface layers.

266 t evidence of the presence of carbonate- and silicate-substitutions in the calcium phosphate plaques

267 Ag and Au, and in all metals on the layered silicate support.

268 the behavior of nanoparticles on niobate and silicate supports highlight the importance of d-orbital

269 l oxide nanoparticles on layered niobate and silicate supports.

270 sucrose at distinct nonhydrated and hydrated silicate surface sites and electrostatic interactions wi

271 es of certain organic molecules and water at silicate surfaces strongly influence the rates of silica

272 In silicate systems, such as window glass, it is well-estab

273 s are single- or near single-unit cell thick silicates that can function as molecular sieves.

274 rrent understanding of how graphite, layered silicates, the MAX phases, and many other plastically an

275 The investigations of mesoporous silicates, their nonsilica replicas and composites are d

276 e of silicic acids by guiding them to form a silicate trimer along the surface of micelles.

277 topic fractionation between molten metal and silicate under high pressure-temperature conditions is p

278 ion that the greater hydrophobicity of these silicates (vis-a-vis PTX or DTX itself) should be advant

279 Dissolved silicate was determined by double isotope dilution using

280 the long-term massive erosion of continental silicates was critical to the subsequent success of diat

281 g-term carbon removal fluxes via terrestrial silicate weathering and ocean crust alteration plays a k

282 ormation might be blocked, since kinetics of silicate weathering are typically strongly retarded at t

283 ing Po2 provides distinctive evidence that a silicate weathering feedback stabilizes Pco2 on million-

284 g with the conventional view that the global silicate weathering flux must adjust to equal the volcan

285 acial scouring of the continents and intense silicate weathering in a post-Snowball Earth hothouse.

286 er, which is three times the CO2 drawdown by silicate weathering in this basin.

287 Climate regulation by silicate weathering is thus strongest when global topogr

288 However, the potential influence of silicate weathering on atmospheric pCO2 levels on geolog

289 s a new perspective for predicting long-term silicate weathering rates in actual geochemical systems

290 weathering feedback, we present a model for silicate weathering that regulates climatic and tectonic

291 anges may have stimulated CO2 consumption by silicate weathering, but reconstructions of sea-floor sp

292 Like drawdown by means of silicate weathering, this source is probably enhanced by

293 This was likely due to the silicate weathering-negative feedback and the expansion

294 e strongly than carbon sequestration through silicate weathering.

295 g balanced by the rate of CO2 consumption by silicate weathering.

296 g viability of the basic concept of enhanced silicate weathering.

297 ) sulfate, iron(III) phosphate, and iron(II) silicates were also contributors to aerosol composition.

298 ning borates were found, no transition-metal silicate with useful NLO properties has been reported.

299 Silicates with amorphous rims are observed on interplane

300 together the muskeg, wood fibers, and added silicates yielding a load-bearing and low-subsidence com