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 ed by kinetic dissolution rates of dicalcium silicate.

3 tion for adsorption sites in the presence of silicate.

4 ble radical intermediates or hypercoordinate silicates.

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

6 high concentrations of respirable silica and silicates.

7 ferentiate distinct phases of failure in two silicates.

8 delta(30)Si(EC-silicates) = -0.33 +/- 0.11 per mille, Mg/Si = ~1.01) an

9 sults highlight that large (>95-um) external silicate abrasives lead to distinct microscopic wear wit

10 Silicate addition also significantly reduced the dissolu

11 ite dissolution rate was reduced by 98% upon silicate addition at pH 7.4 with little effect at pH 3.0

12 In contrast, the effect of silicate addition increased with increasing pH and was g

13 combined effect of galvanic interaction and silicate addition on the dissolution of pyrite, the majo

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

15 These results suggest that silicate addition, for reducing both pyrite dissolution

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

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

18 ts performed on both dry and fluid-permeated silicate and carbonate bearing-rocks, at normal effectiv

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

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

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

22 ver, Si possess a bimodal distribution among silicate and metallic fractions of EC because of its for

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

24 and nanoindentation to determine the role of silicate and tin (two experimental nonphosphate corrosio

25 ing the interfacial energy between the boron silicate and zinc phase.

26 ce of a key mechanism to synthesize water in silicates and advancing our understanding on the origin

27 The interaction of solar-wind protons with silicates and oxides has been proposed as a key mechanis

28 oxo-anions (phosphate, sulfate, bicarbonate, silicate, and nitrate) were selected due to their potent

29 ocarbon lakes; dynamic rings containing ice, silicates, and organics; and Saturn's differential rotat

30 Rare earth silicate apatites are one-dimensional channel structures

31 o observe the mechanisms that fail different silicate architectures, engineering has relied on extern

32 Interfaces between water and silicates are ubiquitous and relevant for, among others,

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

34 Its chemical interaction with calcium-rich silicates at high temperatures give rise to the formatio

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

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

37 inflammatory state faster than inert calcium silicate-based materials thereby accelerating stem cell

38 This implies OM deposition in silicate-bearing BIF would have been minimal, this conse

39 rger pores and connections were found in the silicate biofilms compared to those in tin and groundwat

40 The silicate biofilms had the greatest overall porosities an

41 thickness normalized by the growth time for silicate biofilms was highest at 38 +/- 7.1 mum/month, c

42 d that the thicker and more porous biofilms (silicate biofilms) were potentially less resistant to de

43 ater biofilms were the stiffest, followed by silicate biofilms.

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

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

46 Specifically, we predict that silicate-bridging [AlO(2)(OH)(4)](5-) complexes are favo

47 n a narrow (27)Al NMR signal at 5 ppm to the silicate-bridging [AlO(2)(OH)(4)](5-) sites and show tha

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

49 demonstrate that the carbonation of calcium silicates can produce reaction products that dramaticall

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

51 eratures give rise to the formation of mixed silicate-carbonate minerals, but the structural behavior

52 system for understanding subsurface divalent silicate carbonation reactivity.

53 Calcium silicate (CaSiO(3)) perovskite is believed to be the thi

54 orated into the bridging sites of the linear silicate chains and that at high Ca:Si and H(2)O ratios,

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

56 spite increasing numbers of vacancies in its silicate chains.

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

58 n (386.1) revealed a fiber, sealed by a thin silicate coating, adhering to the surface within a wide

59 s by X-ray diffraction of selected amorphous silicates compressed statically in diamond anvil cells (

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

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

62 oxidation retardation derived from elevated silicate concentrations.

63 interaction processes associated with metal-silicate condensation at high C/O environment (~0.83).

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

65 during the combustion due to its high alkali silicate content.

66 allic core that is overlain by a homogeneous silicate convecting mantle underneath an evolving hetero

67 s groundwater was amended with either tin or silicate corrosion inhibitor (0.5 mg/L as Sn and 20 mg/L

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

69 In this study, highly bioactive Ca-silicate (CSi) bioceramic scaffolds were fabricated by a

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

71 This silicate decrease is primarily attributed to natural mul

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

73 Early silicate differentiation events for the terrestrial plan

74 Evidence for early silicate differentiation in the Hadean (4.6 to 4.0 Ga) h

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

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

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

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

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

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

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

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

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

84 The bulk silicate Earth (BSE), and all its sampleable reservoirs,

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

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

87 the present-day mantle, demonstrating major silicate Earth differentiation within the first 100 My o

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

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

90 The silicate Earth is strongly depleted in moderately volati

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

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

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

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

95 ose similarity with terrestrial mantle (Bulk Silicate Earth, BSE) for numerous isotope systematics.

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

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

98 at drive the chemical differentiation of the silicate Earth.

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

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

101 The carbonation of divalent silicates exposed to humidified scCO(2) occurs in angstr

102 arried out with addition of 0.8 mM dissolved silicate for comparison to previously published data.

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

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

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

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

107 +)-doped silicates (melilite, cyclosilicate, silicate garnet, oxyorthosilicate, and orthosilicate) ul

108 with silicon etched NEG cavities and alumino-silicate glass (ASG) windows and demonstrate the observa

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

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

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

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

113 attribute fast transport to phosphorus-doped silicate glass, the nanochannel material known to have v

114 ween N bonding in metal alloys (Fe-N) and in silicate glasses (as molecular N(2) and NH complexes).

115 The X-ray diffraction patterns of silicate glasses and liquids reveal similar characterist

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

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

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 einforce the widely used assumption that the silicate glasses studies are appropriate structural anal

121 mon, homogeneous ionic solids such as alkali silicate glasses when subjected even to moderate fields

122 opic fractionations between metal alloys and silicate glasses, i.e., from -257 +/- 22 per mille to -4

123 imulations to predict the Young's modulus of silicate glasses.

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

125 Hydrophobic voids within titanium silicates have long been considered necessary to achieve

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

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

128 years) promote the leaching of RAM from the silicate host rocks.

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

130 he main hydration product, calcium aluminate silicate hydrate (C-A-S-H), remains elusive.

131 ate the constitutive relationship of calcium-silicate-hydrate (C-S-H) gel-the primary binding phase i

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

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

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

135 react to form a range of crystalline calcium silicate hydrates (CCSHs) at intermediate pH.

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

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

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

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

140 Silicate hydration is prevalent in natural and technolog

141 g like micrometeorite impacts into anhydrous silicates implanted with solar-wind protons.

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

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

144 signal correlates to (29)Si NMR signals from silicates in C-A-S-H, conflicting with its conventional

145 The silicates in NWA 7983 record a high degree of shock meta

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

147 ogen species, thus limiting the hydration of silicates in the bulk MTZ.

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

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

150 the relatively low water content in bulk MTZ silicates inferred from electrical conductivity studies.

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

154 Silicate is structurally incorporated within this layer

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

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

157 olated Ti(IV) catalytic centers supported on silicates is investigated for olefin epoxidation.

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

159 n the early Earth was surrounded by a molten silicate layer, a basal magma ocean that may have surviv

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

161 We report a silicate, Li(2) BaSiO(4) , with edge-sharing LiO(4) -SiO

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

163 ns to predict the electrical conductivity of silicate liquid at the conditions of the basal magma oce

164 on a significant fraction of carbon from the silicate liquid, leading to carbon transport into the Ea

165 00 S/m, more than 100 times that measured in silicate liquids at low pressure and temperature.

166 for understanding the atomic arrangement of silicate liquids at these high pressures.

167 ong enough to efficiently float magnetite in silicate magma, decompression experiments were conducted

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

169 However, transport of these metals within silicate magmas primarily occurs within dense sulfide li

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

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

172 We show that the delta(15)N value of the silicate mantle could have increased by ~20 per mille du

173 s not equally well homogenized and that some silicate mantle signatures from an early differentiated

174 e whereby a metal-rich core is enclosed by a silicate mantle, which is itself overlain by a crust con

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

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

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

178 ncluding the potential for excess industrial silicate materials (basalt mine overburden, concrete, an

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

180 Here we report five types of Pr(3+)-doped silicates (melilite, cyclosilicate, silicate garnet, oxy

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

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

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

184 re the hot (and so relatively low viscosity) silicate melt cooled to form glass.

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

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

187 ate that magnetite-bubble pairs do ascend in silicate melt, accumulating in an upper layer that grows

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

189 hat magnetite must settle gravitationally in silicate melt.

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

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

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

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

194 or major structural changes occurring in the silicate melts studied up to pressures and temperatures

195 structureless compared to more "polymerized" silicate melts.

196 lasting regions containing both metallic and silicate melts.

197 Magadiite, a rare hydrous sodium-silicate mineral [NaSi(7)O(13)(OH)(3).4(H(2)O)], was dis

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

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

200 oncentrations in meltwaters from an iron and silicate mineral-rich basaltic glacial catchment were an

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

202 ogeochemical weathering of subsurface Fe(II)-silicate minerals at the Luquillo Critical Zone Observat

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

204 e been identified as a significant source of silicate minerals, which can undergo carbonation reactio

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

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

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

208 e of the Mg isotopic composition of the bulk silicate Moon (BSM).

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

210 exadecyl and phenyl functionalized magnesium silicates (MSil-C16 and MSil-Ph) were confirmed by X-ray

211 viscosifiers-organically modified magnesium silicates (MSils)-for reservoir drilling fluids where or

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

213 To make full use of external radiation, the silicate nanoscintillators are conjugated with photosens

214 By simply adjusting the metal dopants, silicate nanoscintillators with controllable size and X-

215 cale preparation of monodisperse and uniform silicate nanoscintillators.

216 and in vivo experiments demonstrate that the silicate nanosensitizers can accumulate effectively in t

217 (SHAP), which reveals that the influence of silicate network on all the elastic constants of C-S-H i

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

219 ransverse response is mainly governed by the silicate network.

220 cy of the applied signal, and in the case of silicate, on the pH of the solution.

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

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

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

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

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

226 Without silicate, oxidized pyrite particles form an overlayer of

227 mined N-isotopic fractionations during metal-silicate partitioning (analogous to planetary core forma

228 Using metal-silicate partitioning experiments in a laser-heated diam

229 Here, we present a series of metal-silicate partitioning experiments of Nb and Ta in a lase

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

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

232 sometimes majoritic garnet or former calcium silicate perovskite.

233 0.09 per mille, Mg/Si = ~0.001) whereas its silicate phases are isotopically heavier (Av.

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

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

236 8)) from naturally occurring minerals (e.g., silicate, phosphate, sulfate) follows energy-intensive c

237 stabilized by graphene oxide and including a silicate precursor to grow a strong, mesoporous capsule

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

239 involving the attachment of complex (alumino)silicate precursors to crystal surfaces, yet recurrent i

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

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

242 ctive components of mineral surfaces such as silicate radicals and ferrous iron.

243 Most calcium silicates react with CO(2) to form solid carbonates but

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

245 tion and mass transport controls on divalent silicate reactivity in wet scCO(2) could be advantageous

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

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

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

249 Enhanced silicate rock weathering (ERW), deployable with cropland

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

251 sequestration through application of crushed silicate rocks, such as basalt, to croplands and foreste

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

253 od capable of nearly eliminating CaSO(4) and silicate scaling on electrically conducting membrane dis

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

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

256 nanoparticles to create an insoluble calcium silicate shell.

257 penetrating peptides attached to the calcium silicate shell.

258 parates suggest that processes such as metal-silicate Si isotope fractionation at reduced nebular env

259 ption of nutrients such as phosphate (P) and silicate (Si) by ferric iron (oxyhydr)oxides (FeOx) modu

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

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

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

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

264 IV) chloride to provide bis(trimetaphosphate)silicate, [TBA](2)[Si(P(3)O(9))(2)], characterized by NM

265 Tricalcium silicate (TCS)-based materials produce calcium hydroxide

266 omplex mix of metallic oxides, fluorides and silicates that can cause or exacerbate health problems i

267 ransition from aerosol surfaces dominated by silicates that react efficiently with N(2)O(5) and produ

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

269 Silicates-the largest constituent of the earth's crust-a

270 CO(2) concentrations, these wastes have high silicate to carbonate conversion rates.

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

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

273 Properties of liquid silicates under high-pressure and high-temperature condi

274 nce of tropical mountainous rivers on global silicate weathering and suspended sediment transport.

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

276 ic water column with plagioclase and alumino-silicate weathering contributing < 5% of the Ca(2+)-Na(+

277 Through the water-mediated carbonate-silicate weathering cycle, atmospheric CO(2) partial pre

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

279 We find that the global silicate weathering flux remained constant, even as the

280 n being extended by limitation of the global silicate weathering flux.

281 cycle and without requiring increases in the silicate weathering flux.

282 ning of denudation and consequent changes in silicate weathering intensity reconcile marine isotope a

283 g flux remained constant, even as the global silicate weathering intensity-the fraction of the total

284 M, which couples a global climate model to a silicate weathering model with spatially resolved lithol

285 Using a coupled climate and carbonate-silicate weathering model, we quantify the likely scatte

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

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

288 inuted sediments available for carbonate and silicate weathering reactions that can consume atmospher

289 ficant organic carbon burial, in addition to silicate weathering, is necessary to account for the pos

290 ion of mountains and consequent increases in silicate weathering, which removes atmospheric carbon di

291 e total denudation flux that is derived from silicate weathering-decreased, sustained by an increase

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

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

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

295 form iron hydride or molecular hydrogen and silicate with less than tens of parts per million (ppm)

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

297 enides, fluorides, phosphides, nitrides, and silicates with specific emphasis on spinel metal oxides

298 The SHG intensity is the largest for silicates without second-order Jahn-Teller cations, and

299 data of texturally distinct calcite in calc-silicate xenoliths from arc volcanics in a case study fr

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