bluuebunny/crossref_metadata_2025_split huggingface dataset:
Byrudite, (Be,〈)(V3+,Ti)3O6, a
new mineral from the Byrud emerald mine, South Norway
Authors: Raade G. , Balić-Žunić T. , Stanley C. J. 
Published: July 2015

AbstractByrudite (IMA 2013-045, Raade et al., 2013), with
simplified formula (Be,〈)(V3+,Ti)3O6,
occurs in emerald-bearing syenitic pegmatites of Permian age at Byrud farm,
Eidsvoll, Akershus, South Norway. It has a norbergite-type structure,
Pnma, with a = 9.982(1),
b = 8.502(1), c = 4.5480(6) Å,
V = 385.97(9) Å3, Z = 4. The structure
was refined to R1 = 0.045 for 1413 unique reflections. Twinning occurs on {210}.
The occupancy of the tetrahedral Be site refined to
0.84(1). The presence of Be was verified by secondary ion mass spectrometry
but could not be quantified. Electron-microprobe analyses of the crystal
used for structure determination gave the empirical formula
(Be0.84〈0.16) (V1.323+Ti1.25Cr0.29Fe0.09Al0.07)Σ3.02O6.
There is a strong inverse correlation between V and Cr. The ideal endmember
formula is BeV23+TiO6. The mineral is black and opaque with a
metallic lustre. Reflectance data in air are reported from 400 to 700 nm.
The Commission on Ore Mineralogy required wavelengths are
[R1, R2(λ in nm)]:16.6,17.5(470), 16.7,17.9(546), 16.8,18.3(589) and
16.8,18.6(650). The Mohs hardness is ∼7, based on indentation measurements.
The mineral is brittle with an uneven fracture; cleavage is not present.
D(calc.) = 4.35 g cm–3 for the empirical
formula with 0.84 Be a.p.f.u. The strongest reflections of the calculated
powder X-ray diffraction pattern are [d in Å
(Irel)(hkl)]: 3.721(72)(111),
2.965(100)(121), 2.561(50)(311), 2.464(41)(230), 2.167(24)(231),
1.681(34)(402), 1.671(66)(232), 1.435(23)(630).
Almeidaite,
Pb(Mn,Y)Zn2(Ti,Fe3+)18O36(O,OH)2,
a new crichtonite-group mineral, from Novo Horizonte, Bahia,
Brazil
Authors: Menezes Filho Luiz A. D. , Chukanov Nikita V. , Rastsvetaeva Ramiza K. , Aksenov Sergey M. , Pekov Igor V. , Chaves Mário L. S. C. , Richards R. Peter , Atencio Daniel , Brandão Paulo R. G. , Scholz Ricardo , Krambrock Klaus , Moreira Roberto L. , Guimarães Frederico S. , Romano Antônio W. , Persiano Aba C. , de Oliveira Luiz C. A. , Ardisson José D. 
Published: July 2015

AbstractAlmeidaite (IMA 2013-020), ideally Pb(Mn,
Y)Zn2(Ti,Fe3+)18O36(O, OH)2,
from Novo Horizonte, Bahia, Brazil, occurs in association with quartz,
rutile, anatase, hematite, kaolinite, muscovite, xenotime-(Y) and
bastnaesite-(La). Almeidaite forms isolated, black, opaque, sub-metallic,
platy crystals flattened on [0001], measuring up to 30 mm 6 30 mm 6 6 mm in
size, dominated by the basal pinacoid {0001}, which is bounded by various,
mostly steep, rhombohedra and the hexagonal prism {1120}. Most of the
crystals are multiply twinned, with non-planar contact surfaces that are
approximately parallel to the c axis. The streak is brown. Reflectance
values are [(Ro, Re) λ (nm)]: (12.78, 15.39) 470; (12.86, 15.43) 546; (12.91,
15.55) 589; (13.04, 15.75) 650. The empirical formula is
(Pb0.59Sr0.12Ca0.04La0.03)Σ0.78(Mn0.54Y0.46)Σ1.00Zn1.43(Ti13.02Fe4.983+)Σ18.00(Fe0.323+Mn0.15)Σ0.47[O37.18(OH)0.82]Σ38.00.
It is trigonal, space group R3, with the unit-cell
parameters a = 10.4359(2), c = 21.0471(4)
Å, V = 1985.10(7) Å3 and Z = 3.
The crystal structure was solved (R1 = 0.039) using 2110 unique reflections with I
> 3σ(I). Almeidaite is a member of the crichtonite group
with Pb dominant in the A site (with 12-fold coordination)
and Zn dominant in the T site (with 4-fold coordination).
It is a Zn analogue of senaite and a Pb analogue of landauite. The mineral
is named after Professor Fernando Flávio Marques de Almeida (1916–2013).
Equation of state of hercynite, FeAl2O4, and high-pressure systematics of Mg-Fe-Cr-Al spinels
Authors: Nestola F. , Periotto B. , Anzolini C. , Andreozzi G. B. , Woodland A. B. , Lenaz D. , Alvaro M. , Princivalle F. 
Published: July 2015

AbstractIn this work a single crystal of synthetic hercynite, FeAl2O4, was investigated by X-ray diffraction up to 7.5 GPa and at room temperature, in order to determine its pressure–volume equation of state. The unit-cell volume decreases non-linearly with a reduction of 3.4% (i.e. 18.43 Å3). The pressure–volume data were fitted to a third-order Birch-Murnaghan equation of state providing the following coefficients:V0= 542.58(3)Å3,KT0= 193.9(1.7) GPa,K' = 6.0(5). These results are consistent with previous investigations of Cr and Al spinels measured with the same experimental approach but theKT0differs significantly from the experimental determination carried out more than 40 years ago by Wang and Simmons (1972) by the pulse echo overlap method. Our new results were used to redetermine the FeAl2O4(hercynite)= FeO(wüstite)+ Al2O3(corundum)equilibrium inP–Tspace and obtain geobarometric information for Cr-Al spinels found as inclusions in diamond.
Palladosilicide, Pd2Si, a new mineral from the Kapalagulu Intrusion, Western Tanzania and the Bushveld Complex, South Africa
Authors: Cabri L. J. , McDonald A. M. , Stanley C. J. , Rudashevsky N. S. , Poirier G. , Wilhelmij H. R. , Zhe W. , Rudashevsky V. N. 
Published: July 2015

AbstractPalladosilicide, Pd2Si, is a new mineral (IMA 2014-080) discovered in chromite-rich samples from the Kapalagulu intrusion, western Tanzania (30°03′51′′E 5°53′16′′S and 30°05′37′′E 5°54′26′′S) and from the UG-2 chromitite, Bushveld complex, South Africa. A total of 13 grains of palladosilicide, ranging in size from 0.7 to 39.1 μm (equivalent circle diameters), were found. Synthetic Pd2Si is hexagonal, space groupP62m, witha= 6.496(5),c= 3.433(4) Å,V= 125.5(1) Å3,c:a= 0.529 withZ= 3. The strongest lines calculated from the powder pattern (Anderko and Schubert, 1953) are [din Å (I) (hkl)] 2.3658 100 (111); 2.1263 37 (120); 2.1808 34 (021); 3.240 20 (110); 1.8752 19 (030); 1.7265 12 (002); 1.3403 11 (122); 1.2089 10 (231). The calculated density for three analyses varies from 9.562 to 9.753 g cm–3. Palladosilicide is considered to be equivalent to synthetic Pd2Si based on results from electron backscattered diffraction analyses. Reflectance data in air for the four Commission on Ore Mineralogy wavelengths are [λ nm,R1(%)R2(%)] 470 49.6 52.7; 546 51.2 53.8; 589 51.6 53.7; 650 51.7 53.3 and the mineral is bright creamy white against chromite, weakly bireflectant and displays no discernible pleochroism or twinning. It is weakly anisotropic, has weak extinction and rotation tints in shades of blue and olive green. Electron probe microanalyses of palladosilicide yield a simplified formula of Pd2Si.
The crystal structure of cyanotrichite
Authors: Mills Stuart J. , Christy Andrew G. , Colombo Fernando , Price Jason R. 
Published: July 2015

AbstractWe report the single-crystal average structure of cyanotrichite,
Cu4Al2[SO4](OH)12(H2O)2,
from the Maid of Sunshine mine, Arizona, USA. Cyanotrichite crystallizes in
space group C2/m, with the unit-cell
parameters a = 12.625(3), b = 2.8950(6),
c = 10.153(2) Å and β = 92.17(3)o. All non-hydrogen
atoms were located and refined to R1 = 0.0394 for all 584 observed reflections [Fo > 4σFo] and 0.0424 for all 622 unique reflections. The cyanotrichite
structure consists of a principal building unit of a three-wide
[Cu2Al(OH)6] ribbon of edge-sharing Cu and Al
polyhedra || b, similar to that found for camerolaite. The ribbons lie in
layers || (001) and between these layers, while SO4 tetrahedra
and H2O molecules form rods running || b. A hydrogen-bonding
scheme is also proposed.A sample of cyanotrichite from the Cap Garonne mine, Le Pradet, France,
showed a 4b superstructure with the following unit cell:
space group P2/m, a =
12.611(2) Å, b = 11.584(16) = 4 × 2.896(4) Å,
c = 10.190(1) Å and β = 92.29(6)o. The supercell could
not be refined in detail, but nevertheless imposes constraints on the local
structure in that while the space-group symmetry prevents full order of
SO4 and H2O in the 4b supercell,
it requires that the sequence of species along any given rod is
[-SO4-SO4-(H2O)2-(H2O)2-]
rather than
[-SO4-(H2O)2-SO4-(H2O)2-].
High-resolution imaging of biotite using focal series exit
wavefunction restoration and the graphene mechanical exfoliation
method
Authors: Bower W. , Head W. , Droop G. T. R. , Zan R. , Pattrick R. A. D. , Wincott P. , Haigh S. J. 
Published: July 2015

AbstractWe have applied mechanical exfoliation for the preparation of ultra-thin
samples of the phyllosilicate mineral biotite. We demonstrate that the
'scotch tape' approach, which was made famous as an early method for
production of single-atom-thick graphene, can be used for production of
sheet-silicate specimens that are sufficiently thin to allow high-resolution
transmission electron microscope (HRTEM) imaging to be achieved successfully
while also being free from the specimen preparation artefacts that are often
caused by ion-beam milling techniques. Exfoliation of the biotite parallel
to the (001) planes has produced layers as thin as two structural TOT units
thick (∼2 nm). The minimal specimen thickness enabled not only HRTEM imaging
but also the application of subsequent exit wavefunction restoration to
reveal the pristine biotite lattice. Exit wavefunction restoration recovers
the full complex electron wave from a focal series of HRTEM images, removing
the effects of coherent lens aberrations. This combination of methods
therefore produces images in which the observed features are readily
interpreted to obtain atomic resolution structural information.
Moraskoite, Na2Mg(PO4)F, a new mineral from the Morasko IAB-MG iron meteorite (Poland)
Authors: Karwowski Łukasz , Kusz Joachim , Muszyński Andrzej , Kryza Ryszard , Sitarz Maciej , Galuskin Evgeny V. 
Published: July 2015

AbstractMoraskoite, a new natural phosphate of composition Na2Mg(PO4)F, has been found in the Morasko IAB-MG iron meteorite. The new phosphate occurs in a graphite-troilite inclusion enclosed in a kamacite-taenite matrix. Associated minerals in the inclusions are chlorapatite, buchwaldite, brianite, merrillite, a new phosphate phase of composition Na4MgCa3(PO4)4, chromite, enstatite (bronzite), kosmochlor, kosmochlor–augite, olivine, albite, orthoclase, quartz, cohenite, schreibersite, nickelphosphide, altaite, pyrrhotite, sphalerite, daubreelite, djerfischerite, whitlockite and native Cu. The inclusions are rimmed by a schreibersite-cohenite halo. Moraskoite forms aggregates up to 1.5 mm in size, with individual grains 20–300 μm across. It is colourless and transparent, with a white streak and vitreous lustre; fluorescence is weak blue in ultraviolet radiation (254 and 360 nm); hardness is 4–5; it has irregular, conchoidal fracture and cleavage is rarely observed. Calculated density (using the empirical formula) is 2.925 g cm–3. The moraskoite structure (Pbcn,a= 5.2117(10),b= 13.711(3),c= 11.665(2) Å,V= 833.6(3) Å3andZ= 8) is similar to that of its synthetic analogue. The strongest diffraction lines of the moraskoite powder diffraction pattern are as follows (dhkl, I): 3.909(75), 3.382(52), 2.955(90), 2.606(100), 2.571(96), 2.545(68), 1.691 (67). In the Raman spectrum, the following characteristic bands are distinguished (cm–1, strong bands bold): 1114, 1027, 962, 589, 438, 336, 308, 279, 262, 244, 193, 184, 147 and 131. The Raman data prove the absence of H2O and CO2. Moraskoite is interpreted as being a primary phosphate, which crystallized together with graphite, troilite and other accessories inside the nodule.
A-type substitution in carbonated strontium fluor-, chlor- and
hydroxylapatites
Authors: Weidner Victoria L. , Carney Molly C. , Schermerhorn Demetra V. , Pasteris Jill D. , Yoder Claude H. 
Published: July 2015

AbstractCarbonated strontium fluor-, hydroxyl- and chlorapatites (carbonated
Sr10(PO4)6X2 = CSrApX, where
X= OH, Cl and F) were synthesized in aqueous solution. The substitution mode
of carbonate was determined from infrared (IR) stretching frequencies for
carbonate and from the variation in unit-cell axial lengths as a function of
carbonate content. The a-axis lengths of CSrApF and CSrApCl decrease,
whereas the a-axis length of CSrApOH increases slightly
with increasing carbonate substitution. The carbonate IR stretching region
from ∼1390 to 1590 cm–1 contains two doublets for both CSrApOH
and CSrApCl, indicating the presence of both A- and B-type carbonate. The
carbonate spectral region for CSrApF is reminiscent of that for CCaApF,
which contains one doublet for B-type carbonate with a small shoulder
attributable to A-type carbonate. Activity-based Ksp values (assuming B-type substitution) were determined for all
three series of carbonated Sr apatites and show that the solubilities of
CSrApOH and CSrApCl increase at higher carbonate values, whereas those of
CSrApF stay constant. The Ksp values for uncarbonated SrApOH, SrApCl and SrApF were
determined by extrapolation to zero percent carbonate (10–120,
10–112 and 10–113 for SrApOH, SrApCl and SrApF,
respectively).
Imayoshiite,
Ca3Al(CO3)[B(OH)4](OH)6·12H2O,
a new mineral of the ettringite group from Ise City, Mie Prefecture,
Japan
Authors: Nishio-Hamane D. , Ohnishi M. , Momma K. , Shimobayashi N. , Miyawaki R. , Minakawa T. , Inaba S. 
Published: July 2015

AbstractImayoshiite,
Ca3Al(CO3)[B(OH)4](OH)6·12H2O,
occurs in cavities in the altered gabbro xenolith in the sepentinized dunite
exposed at Suisho-dani, Ise City, Mie Prefecture, Japan. Imayoshiite is
colourless and transparent with a vitreous lustre and its aggregates are
white with a silky lustre. Imayoshiite has a white streak. Its Mohs hardness
is 2–3. It is brittle, the cleavage is distinct on {100} and the fracture is
uneven. The mineral is uniaxial (–) with the indices of refraction ω =
1.497(2) and ε = 1.470(2) in white light. Imayoshiite is hexagonal,
P63, a = 11.0264(11),
c = 10.6052(16) Å by powder diffraction and
a = 11.04592(2), c = 10.61502(19) Å by
single-crystal diffraction. The structural refinement converged to
R1 = 2.35%. Imayoshiite is the first member of the ettringite
group with both CO3 and B(OH)4 anions.
Determination of the tegengrenite superstructure: another case
of tetrahedral Mn3+ in spinel-type minerals?
Authors: Bonazzi Paola , Bindi Luca 
Published: July 2015

AbstractThe crystal structure of the spinel-related, Sb mineral tegengrenite from
the Filipstad district, Värmland, Sweden, has been solved in the space group
R3 [a = 16.0285(9), c
= 14.8144(8) Å, V = 3296.1(3) Å3,
Z = 42] and refined up to R = 0.0484
for 3589 reflections with Fo > 4σ(Fo). Tegengrenite exhibits a rhombohedrally distorted spinel-type
structure with cations occupying 1/8 of the tetrahedral (T) and 1/2 of the
octahedral (M) interstices of a nearly regular cubic close-packing of oxygen
atoms. Due to the cation ordering, which leads to a complex superstructure
with a unit-cell volume of 21/4 that of a common spinel, the M and T sites
of the spinel-type structure split into ten and six independent sites,
respectively. Chemical composition determined by electron microprobe led to
the empirical formula Mg1.26Mn0.852+Zn0.04Mn0.193+Al0.01Si0.12Ti0.03Sb0.505+O4, on the assumption that no vacancies occur in the
mineral (Σcat = 3.00 and Σcharge = 8.00 per formula
unit). Crystal-chemical considerations indicate that octahedra are occupied
mainly by Mg, Mn3+ and Sb5+ (+Al, + Ti), whereas
tetrahedra are filled mainly by Mn2+ and Mg (+Zn) with Si ordered
in a specific site. However, the structure refinement shows a low
site-scattering factor for one octahedral site, implying substantial
vacancies and a larger overall mean Mn valence than stated above. Long mean
distances also suggest some Mn2+ on octahedral sites. Together,
these observations necessitate the presence of substantial Mn3+
on tetrahedral sites.
Alteration of nanocrystalline calcium silicate hydrate (C-S-H) at pH 9.2 and room temperature: a combined mineralogical and chemical study
Authors: Marty Nicolas C. M. , Grangeon Sylvain , Warmont Fabienne , Lerouge Catherine 
Published: July 2015

AbstractCalcium silicate hydrate (C-S-H) alteration was studied with flow-through experiments at 25°C and pH 9.2. Three materials with apparent Ca/Si ratios (C/S ratios) of 1.47, 1.38 and 0.86 were investigated. Physical (thermogravimetric analyses/differential thermal analysis), mineralogical (X-ray diffraction) and chemical (electron probe microanalysis, transmission electron microscopy/energy dispersive X-ray spectrometry) analyses were performed to characterize the reacting minerals. Initial stoichiometric C/S ratios were 1.22, 1.22 and 0.85, respectively. The excess of Ca is attributed mainly to the presence of calcium hydroxide intimately mixed in with C-S-H particles.The C-S-H chemical compositions were monitored during flow-through experiments in order to determine the mineral stoichiometry needed for reaction kinetics. Under our experimental conditions the stoichiometric C/S ratios decreased continuously with time. A close to stoichiometric dissolution was observed after 2 days of experiments. Using an integrated approach, the kinetics was found to be a function of the C/S.A decrease in layer-to-layer distance in the early stage of the alteration process is interpreted as interlayer Ca/Na exchange (Na being part of the pH buffering solution). A second dissolution step, marked by a close to stoichiometric release of Ca and Si, undoubtedly results from layer dissolution. The structural similarity of C-S-H and tobermorite was confirmed.
The tobermorite supergroup: a new nomenclature
Authors: Biagioni Cristian , Merlino Stefano , Bonaccorsi Elena 
Published: July 2015

AbstractThe name 'tobermorites' includes a number of calcium silicate hydrate (C-S-H) phases differing in their hydration state and sub-cell symmetry. Based on their basal spacing, closely related to the degree of hydration, 14, 11 and 9 Å compounds have been described. In this paper a new nomenclature scheme for these mineral species is reported. The tobermorite supergroup is defined. It is formed by the tobermorite group and the unclassified minerals plombièrite, clinotobermorite and riversideite. Plombièrite ('14 Å tobermorite') is redefined as a crystalline mineral having chemical composition Ca5Si6O16(OH)2·7H2O. Its type locality is Crestmore, Riverside County, California, USA. The tobermorite group consists of species having a basal spacing of ∼11 Å and an orthorhombic sub-cell symmetry. Its general formula is Ca4+x(AlySi6–y)O15+2x–y·5H2O. Its endmember compositions correspond to tobermorite Ca5Si6O17·5H2O (x= 1 andy= 0) and the new species kenotobermorite, Ca4Si6O15(OH)2·5H2O (x= 0 andy= 0). The type locality of kenotobermorite is the N'Chwaning II mine, Kalahari Manganese Field, South Africa. Within the tobermorite group, tobermorite and kenotobermorite form a complete solid solution. Al-rich samples do not warrant a new name, because Al can only achieve a maximum content of 1/6 of the tetrahedral sites (y= 1). Clinotobermorite, Ca5Si6O17·5H2O, is a dimorph of tobermorite having a monoclinic sub-cell symmetry. Finally, the compound with a ∼9 Å basal spacing is known as riversideite. Its natural occurrence is not demonstrated unequivocally and its status should be considered as “questionable”. The chemical composition of its synthetic counterpart, obtained through partial dehydration of tobermorite, is Ca5Si6O16(OH)2. All these mineral species present an order-disorder character and several polytypes are known. This report has been approved by the International Mineralogical Association Commission on New Minerals, Nomenclature and Classification.
Selective precipitation of schwertmannite in a stratified acidic pit lake of Iberian Pyrite Belt
Authors: Santofimia E. , López-Pamo E. , Montero E. 
Published: July 2015

AbstractSelective precipitation of schwertmannite was identified in the water column of a chemically stratified acidic lake (pH 2.0 2.5). A set of analytical techniques was used to identify accurately the mineral phase (X-ray diffraction, X-ray fluorescence spectrometry, scanning electron microscopy coupled with energy dispersive spectroscopy). The lake has two clearly differentiated layers: a thin superficial layer that extends to ∼2 m in depth with less dissolved solid content and, therefore, lower density, which contrasts with a thicker lower layer that extends to 34 m in depth. The upper layer is strongly influenced by climatic factors, triggering dilution (rainfall), concentration (dry season) and intense seasonal thermal fluctuations, while the lower layer is more compositionally and thermally stable.Schwertmannite precipitate was initially observed only in the upper layer, adhered to a plastic buoy and the anchor line. The latter was confirmed through a test involving a precipitation device that consisted of maintaining a series of plastic plates at different depths over a period of several months. Only the plates located in the upper layer became covered with precipitate, whereas the plates that were submerged in the lower layer remained clean. These observations clearly differed from the saturation indices of schwertmannite (SIsch) calculated usingPHREEQCand using Bighamet al.(1996) or Kawano and Tomita (2001) solubility products. Schwertmannite would not precipitate in the lake with the former but would precipitate in both layers with the latter. It is the constant provided by Yuet al.(1999) that makes SIschin both layers approach the observed behaviour: SIsch>0 displays oversaturation in the upper layer while SIsch<0 displays undersaturation in the lower layer. The value of the product of solubility that better adjusts to this situation is log Ksch= 9.5 10. Using the method by Yuet al.(1999) to establish the apparent solubility, a range of log Kschvalues was defined between 10.5 and 11.5 for the system studied.
Platelet binding sites for factor VIII in relation to fibrin and phosphatidylserine
Authors: Gilbert Gary E. , Novakovic Valerie A. , Shi Jialan , Rasmussen Jan , Pipe Steven W. 
Published: July 2015

Key PointsCoagulation fVIII binds to a protein complex, including fibrin, on stimulated platelets rather than to membrane PS. Anti-fVIII antibodies inhibit function on platelets differently than on phospholipid vesicles used in clinical assays.
Disease evolution and outcomes in familial AML with germline CEBPA mutations
Authors: Tawana Kiran , Wang Jun , Renneville Aline , Bödör Csaba , Hills Robert , Loveday Chey , Savic Aleksandar , Van Delft Frederik W. , Treleaven Jennifer , Georgiades Panayiotis , Uglow Elizabeth , Asou Norio , Uike Naokuni , Debeljak Maruša , Jazbec Janez , Ancliff Philip , Gale Rosemary , Thomas Xavier , Mialou Valerie , Döhner Konstanze , Bullinger Lars , Mueller Beatrice , Pabst Thomas , Stelljes Matthias , Schlegelberger Brigitte , Wozniak Eva , Iqbal Sameena , Okosun Jessica , Araf Shamzah , Frank Anne-Katrine , Lauridsen Felicia B. , Porse Bo , Nerlov Claus , Owen Carolyn , Dokal Inderjeet , Gribben John , Smith Matthew , Preudhomme Claude , Chelala Claude , Cavenagh Jamie , Fitzgibbon Jude 
Published: July 2015

Key PointsGerm-line CEBPA mutations are highly penetrant, causing early-onset de novo AML associated with favorable survival outcomes. Familial CEBPA-mutated AML displays a unique model of disease progression, with recurrence caused by novel, independent leukemic episodes.