S. Mills, A. Kampf, K. Momma, R. Housley, J. Marty
Müllerite (IMA2019–060) is a new mineral found at several workings on Otto Mountain, 2.5 km NW of Baker, San Bernardino County, California, USA. Müllerite occurs as hexagonal tablets and thin plates up to 0.2 mm across, intergrown ball-like clusters, and scattered flakes. Crystals are yellow, tending to reddish-orange, and have a pale-yellow streak and subadamantine to greasy luster. Crystals are brittle with an irregular fracture and have a hardness of ∼2 and perfect cleavage on {001}. The main forms observed are {100} and {001}. The calculated density is 5.812 g/cm3. The empirical formula (based on 7 O + Cl + I apfu) is Pb1.83Ag0.26Fe0.93Al0.03Cu0.02Te6+0.95O5.56Cl1.30I0.14; the endmember formula is Pb2Fe3+(Te6+O6)Cl. Müllerite is trigonal, space group P312, with the unit cell parameters a = 5.2040(5), c = 8.9654(12) Å, V = 210.23(3) Å3, and Z = 1. The crystal structure of müllerite was refined using Rietveld analysis and converged to Rwp = 4.861%, S = 0.1873, RB = 1.800%, and RF = 0.691%. Müllerite is the Fe-analogue of backite, Pb2Al3+(Te6+O6)Cl.
{"title":"Müllerite, the Fe-analogue of backite from Otto Mountain, California, USA","authors":"S. Mills, A. Kampf, K. Momma, R. Housley, J. Marty","doi":"10.3749/canmin.2000026","DOIUrl":"https://doi.org/10.3749/canmin.2000026","url":null,"abstract":"\u0000 Müllerite (IMA2019–060) is a new mineral found at several workings on Otto Mountain, 2.5 km NW of Baker, San Bernardino County, California, USA. Müllerite occurs as hexagonal tablets and thin plates up to 0.2 mm across, intergrown ball-like clusters, and scattered flakes. Crystals are yellow, tending to reddish-orange, and have a pale-yellow streak and subadamantine to greasy luster. Crystals are brittle with an irregular fracture and have a hardness of ∼2 and perfect cleavage on {001}. The main forms observed are {100} and {001}. The calculated density is 5.812 g/cm3. The empirical formula (based on 7 O + Cl + I apfu) is Pb1.83Ag0.26Fe0.93Al0.03Cu0.02Te6+0.95O5.56Cl1.30I0.14; the endmember formula is Pb2Fe3+(Te6+O6)Cl. Müllerite is trigonal, space group P312, with the unit cell parameters a = 5.2040(5), c = 8.9654(12) Å, V = 210.23(3) Å3, and Z = 1. The crystal structure of müllerite was refined using Rietveld analysis and converged to Rwp = 4.861%, S = 0.1873, RB = 1.800%, and RF = 0.691%. Müllerite is the Fe-analogue of backite, Pb2Al3+(Te6+O6)Cl.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-07-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.2000026","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"49385840","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
The Kiglapait Intrusion on the north coast of Labrador is a bowl-shaped body dominated by troctolite about 3500 km3 in initial volume and was created during an intrusive event perhaps lasting thousands of years. It was emplaced into anorthosite and metasedimentary rocks at an estimated roof depth of 9.6 km and a magma depth of 8.4 km; hence with a floor at 18 km depth. The primary magma for the intrusion is thought to have been of harzburgite composition; a large volume of olivine crystallized in transit, to the extent that the magma became saturated with plagioclase by the time it reached the site of emplacement or soon after. To test this hypothesis, piston-cylinder experiments were made at 5–15 kbar in graphite using the Kiglapait Intrusion bulk composition with Fo-rich olivine added. Results at 13 kbar yielded saturation with garnet, olivine, spinel, orthopyroxene, clinopyroxene, plagioclase, and melt. This assemblage is compatible with a lherzolite solidus at 1375 °C. A postulated harzburgite solidus at 15 kbar would be hotter, perhaps 1410 °C. Partial melt from this harzburgite rising into a hot, thinned lithosphere is presumed to have shed large amounts of olivine to produce the plagioclase-saturated troctolitic basal Lower Zone of the intrusion. Conditions of emplacement are schematically developed in ternary Al–Ca–Fe diagrams. Some high-pressure experimental compositions of clino- and orthopyroxene are metastably enriched in Al but do not affect the interpretation of the magmatic history. We show that olivine fractionation will pass through the compositions of these aluminous minerals to reach a relatively evolved saturation with only plagioclase and olivine, resulting in the voluminous Lower Zone of troctolite. The amount of olivine crystallized to reach this result is calculated, using multiphase Rayleigh fractionation and a standard MELTS routine, to between 30% and 50%. Previously published argon-argon mineral dates on hornblende, biotite, and feldspars have captured a cooling history from ∼1258 °C to the ambient ∼100 °C over the time interval 1307 to 1220 Ma, hence the 87 million year history claimed in the title.
{"title":"87 million years of recorded history in Labrador: Birth, life, and sleep of the Kiglapait Intrusion","authors":"S. Morse, J. Brady, D. Banks","doi":"10.3749/canmin.1900043","DOIUrl":"https://doi.org/10.3749/canmin.1900043","url":null,"abstract":"The Kiglapait Intrusion on the north coast of Labrador is a bowl-shaped body dominated by troctolite about 3500 km3 in initial volume and was created during an intrusive event perhaps lasting thousands of years. It was emplaced into anorthosite and metasedimentary rocks at an estimated roof depth of 9.6 km and a magma depth of 8.4 km; hence with a floor at 18 km depth. The primary magma for the intrusion is thought to have been of harzburgite composition; a large volume of olivine crystallized in transit, to the extent that the magma became saturated with plagioclase by the time it reached the site of emplacement or soon after. To test this hypothesis, piston-cylinder experiments were made at 5–15 kbar in graphite using the Kiglapait Intrusion bulk composition with Fo-rich olivine added. Results at 13 kbar yielded saturation with garnet, olivine, spinel, orthopyroxene, clinopyroxene, plagioclase, and melt. This assemblage is compatible with a lherzolite solidus at 1375 °C. A postulated harzburgite solidus at 15 kbar would be hotter, perhaps 1410 °C. Partial melt from this harzburgite rising into a hot, thinned lithosphere is presumed to have shed large amounts of olivine to produce the plagioclase-saturated troctolitic basal Lower Zone of the intrusion. Conditions of emplacement are schematically developed in ternary Al–Ca–Fe diagrams. Some high-pressure experimental compositions of clino- and orthopyroxene are metastably enriched in Al but do not affect the interpretation of the magmatic history. We show that olivine fractionation will pass through the compositions of these aluminous minerals to reach a relatively evolved saturation with only plagioclase and olivine, resulting in the voluminous Lower Zone of troctolite. The amount of olivine crystallized to reach this result is calculated, using multiphase Rayleigh fractionation and a standard MELTS routine, to between 30% and 50%. Previously published argon-argon mineral dates on hornblende, biotite, and feldspars have captured a cooling history from ∼1258 °C to the ambient ∼100 °C over the time interval 1307 to 1220 Ma, hence the 87 million year history claimed in the title.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-07-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.1900043","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"41980805","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
N. Chukanov, S. Aksenov, I. Pekov, D. Belakovskiy, S. A. Vozchikova, S. Britvin
The new eudialyte-group mineral sergevanite, ideally Na15(Ca3Mn3)(Na2Fe)Zr3Si26O72(OH)3·H2O, was discovered in highly agpaitic foyaite from the Karnasurt Mountain, Lovozero alkaline massif, Kola Peninsula, Russia. The associated minerals are microcline, albite, nepheline, arfvedsonite, aegirine, lamprophyllite, fluorapatite, steenstrupine-(Ce), ilmenite, and sphalerite. Sergevanite forms yellow to orange-yellow anhedral grains up to 1.5 mm across and the outer zones of some grains of associated eudialyte. Its luster is vitreous, and the streak is white. No cleavage is observed. The Mohs' hardness is 5. Density measured by equilibration in heavy liquids is 2.90(1) g/cm3. Calculated density is equal to 2.906 g/cm3. Sergevanite is nonpleochroic, optically uniaxial, positive, with ω = 1.604(2) and ε = 1.607(2) (λ = 589 nm). The infrared spectrum is given. The chemical composition of sergevanite is (wt.%; electron microprobe, H2O determined by HCN analysis): Na2O 13.69, K2O 1.40, CaO 7.66, La2O3 0.90, Ce2O3 1.41, Pr2O3 0.33, Nd2O3 0.64, Sm2O3 0.14, MnO 4.15, FeO 1.34, TiO2 1.19, ZrO2 10.67, HfO2 0.29, Nb2O5 1.63, SiO2 49.61, SO3 0.77, Cl 0.23, H2O 4.22, –O=Cl –0.05, total 100.22. The empirical formula (based on 25.5 Si atoms pfu, in accordance with structural data) is H14.46Na13.64K0.92Ca4.22Ce0.27La0.17Nd0.12Pr0.06Sm0.02Mn1.81Fe2+0.58Ti0.46Zr2.67Hf0.04Nb0.38Si25.5S0.30Cl0.20O81.35. The crystal structure was determined using single-crystal X-ray diffraction data. The new mineral is trigonal, space group R3, with a = 14.2179(1) Å, c = 30.3492(3) Å, V = 5313.11(7) Å3, and Z = 3. In the structure of sergevanite, Ca and Mn are ordered in the six-membered ring of octahedra (at the sites M11 and M12), and Na dominates over Fe2+ at the M2 site. The strongest lines of the powder X-ray diffraction pattern [d, Å (I, %) (hkl)] are: 7.12 (70) (110), 5.711 (43) (202), 4.321 (72) (205), 3.806 (39) (033), 3.551 (39) (220, 027), 3.398 (39) (313), 2.978 (95) (), 2.855 (100) (404). Sergevanite is named after the Sergevan' River, which is near the discovery locality.
{"title":"Sergevanite, Na15(Ca3Mn3)(Na2Fe)Zr3Si26O72(OH)3·H2O, a new eudialyte-group mineral from the Lovozero alkaline massif, Kola Peninsula","authors":"N. Chukanov, S. Aksenov, I. Pekov, D. Belakovskiy, S. A. Vozchikova, S. Britvin","doi":"10.3749/canmin.2000006","DOIUrl":"https://doi.org/10.3749/canmin.2000006","url":null,"abstract":"\u0000 The new eudialyte-group mineral sergevanite, ideally Na15(Ca3Mn3)(Na2Fe)Zr3Si26O72(OH)3·H2O, was discovered in highly agpaitic foyaite from the Karnasurt Mountain, Lovozero alkaline massif, Kola Peninsula, Russia. The associated minerals are microcline, albite, nepheline, arfvedsonite, aegirine, lamprophyllite, fluorapatite, steenstrupine-(Ce), ilmenite, and sphalerite. Sergevanite forms yellow to orange-yellow anhedral grains up to 1.5 mm across and the outer zones of some grains of associated eudialyte. Its luster is vitreous, and the streak is white. No cleavage is observed. The Mohs' hardness is 5. Density measured by equilibration in heavy liquids is 2.90(1) g/cm3. Calculated density is equal to 2.906 g/cm3. Sergevanite is nonpleochroic, optically uniaxial, positive, with ω = 1.604(2) and ε = 1.607(2) (λ = 589 nm). The infrared spectrum is given. The chemical composition of sergevanite is (wt.%; electron microprobe, H2O determined by HCN analysis): Na2O 13.69, K2O 1.40, CaO 7.66, La2O3 0.90, Ce2O3 1.41, Pr2O3 0.33, Nd2O3 0.64, Sm2O3 0.14, MnO 4.15, FeO 1.34, TiO2 1.19, ZrO2 10.67, HfO2 0.29, Nb2O5 1.63, SiO2 49.61, SO3 0.77, Cl 0.23, H2O 4.22, –O=Cl –0.05, total 100.22. The empirical formula (based on 25.5 Si atoms pfu, in accordance with structural data) is H14.46Na13.64K0.92Ca4.22Ce0.27La0.17Nd0.12Pr0.06Sm0.02Mn1.81Fe2+0.58Ti0.46Zr2.67Hf0.04Nb0.38Si25.5S0.30Cl0.20O81.35. The crystal structure was determined using single-crystal X-ray diffraction data. The new mineral is trigonal, space group R3, with a = 14.2179(1) Å, c = 30.3492(3) Å, V = 5313.11(7) Å3, and Z = 3. In the structure of sergevanite, Ca and Mn are ordered in the six-membered ring of octahedra (at the sites M11 and M12), and Na dominates over Fe2+ at the M2 site. The strongest lines of the powder X-ray diffraction pattern [d, Å (I, %) (hkl)] are: 7.12 (70) (110), 5.711 (43) (202), 4.321 (72) (205), 3.806 (39) (033), 3.551 (39) (220, 027), 3.398 (39) (313), 2.978 (95) (), 2.855 (100) (404). Sergevanite is named after the Sergevan' River, which is near the discovery locality.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-07-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.2000006","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"49596749","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Gahnite (ZnAl2O4) is a common accessory mineral at the Lalor auriferous Zn-Cu metamorphosed VHMS deposit (Snow Lake, Manitoba). To evaluate factors influencing its crystal chemistry, gahnite representing a range of textures, host mineral assemblages, and whole-rock compositions were analyzed for major, minor, and trace elements. The analyzed grains span the range of Ghn63-75Her15-22Spl10-18 and are un-zoned with respect to Zn, Fe, and Mg. A moderate positive correlation exists between Mg in gahnite and whole-rock MgO (R2 = 0.66). The minor- and trace-element chemistry of the Lalor gahnite is dominated by Mn (400–2600 ppm), Si (<25–250 ppm), and V (<25–2300 ppm). Based on the limited variability in gahnite major-element composition, as well as similar partitioning coefficients of Zn and Fe between sphalerite-gahnite pairs (indicating comparable metamorphic conditions of crystallization for the analyzed gahnite), metamorphic grade is interpreted to have had the strongest influence on gahnite major-element chemistry. Most sphalerite occurs with pyrite and pyrrhotite, an assemblage that would have buffered fS2 and fixed the Zn:Fe ratio in sphalerite, which also could have contributed to the narrow compositional range observed in gahnite. Magnesium was not an essential component of the sphalerite-consuming, gahnite-producing reactions, so its concentration in gahnite was more readily affected by whole-rock Mg. A small proportion of gahnite grains may have formed from the destabilization of silicates (staurolite and biotite), rather than sphalerite. These possible gahnite-forming reactions (sphalerite- versus biotite- or staurolite-consuming) appear to have had the strongest control on gahnite minor- and trace-element chemistry, as gahnite formed from sphalerite desulfidation reactions shows a range in Mn (450–2600 ppm) and restricted V/Mn values (<0.5), while gahnite interpreted to have formed from the dehydration of biotite and staurolite shows restricted Mn (<430 ppm) and a range of V/Mn values (0.75–5.5). Further work is recommended to investigate the possibility of using gahnite trace-element signatures (such as with Mn and V) to discriminate between gahnite that crystallized in sphalerite-rich and sphalerite-barren environments, as this concept has potential for application to exploration using detrital gahnite.
{"title":"Mineral chemistry of gahnite from the Lalor metamorphosed VHMS deposit, Snow Lake, Manitoba","authors":"E. Wehrle, A. McDonald, D. Tinkham","doi":"10.3749/canmin.1900036","DOIUrl":"https://doi.org/10.3749/canmin.1900036","url":null,"abstract":"Gahnite (ZnAl2O4) is a common accessory mineral at the Lalor auriferous Zn-Cu metamorphosed VHMS deposit (Snow Lake, Manitoba). To evaluate factors influencing its crystal chemistry, gahnite representing a range of textures, host mineral assemblages, and whole-rock compositions were analyzed for major, minor, and trace elements. The analyzed grains span the range of Ghn63-75Her15-22Spl10-18 and are un-zoned with respect to Zn, Fe, and Mg. A moderate positive correlation exists between Mg in gahnite and whole-rock MgO (R2 = 0.66). The minor- and trace-element chemistry of the Lalor gahnite is dominated by Mn (400–2600 ppm), Si (<25–250 ppm), and V (<25–2300 ppm). Based on the limited variability in gahnite major-element composition, as well as similar partitioning coefficients of Zn and Fe between sphalerite-gahnite pairs (indicating comparable metamorphic conditions of crystallization for the analyzed gahnite), metamorphic grade is interpreted to have had the strongest influence on gahnite major-element chemistry. Most sphalerite occurs with pyrite and pyrrhotite, an assemblage that would have buffered fS2 and fixed the Zn:Fe ratio in sphalerite, which also could have contributed to the narrow compositional range observed in gahnite. Magnesium was not an essential component of the sphalerite-consuming, gahnite-producing reactions, so its concentration in gahnite was more readily affected by whole-rock Mg. A small proportion of gahnite grains may have formed from the destabilization of silicates (staurolite and biotite), rather than sphalerite. These possible gahnite-forming reactions (sphalerite- versus biotite- or staurolite-consuming) appear to have had the strongest control on gahnite minor- and trace-element chemistry, as gahnite formed from sphalerite desulfidation reactions shows a range in Mn (450–2600 ppm) and restricted V/Mn values (<0.5), while gahnite interpreted to have formed from the dehydration of biotite and staurolite shows restricted Mn (<430 ppm) and a range of V/Mn values (0.75–5.5). Further work is recommended to investigate the possibility of using gahnite trace-element signatures (such as with Mn and V) to discriminate between gahnite that crystallized in sphalerite-rich and sphalerite-barren environments, as this concept has potential for application to exploration using detrital gahnite.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-07-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.1900036","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"43982482","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
The emerald deposits in Rajasthan, northwest India, are situated in a narrow NE–SW belt in the Aravalli Mountains. The studied deposits were formed by the metasomatic reaction between muscovite (± garnet ± tourmaline) pegmatites and lenticular bodies of altered ultramafic rocks that are hosted by the Delhi Group gneisses. This reaction produced phlogopite schists containing the exometasomatic emeralds, as in all other granite-related emerald deposits. Endometasomatic changes of the mineralogy of the pegmatites is indicated by the geochemistry of the muscovite (phengitic substitution) and the feldspars (disappearance of the potassic feldspar and calcification of the plagioclase). The K-Ar analyses of syngenetic phlogopite (from the phlogopite schist) and muscovite (from the pegmatites) give an age of ca. 790 Ma, close to that of the last major orogeny affecting the region. This is in accordance with the ages of other granite-related deposits, which all formed in conditions of active orogeny. The ages of the biotite are lower than those of the muscovite, indicating limited radiogenic argon loss as a result of deformation.
{"title":"Mineral chemistry and geochronology of the Rajasthan emerald deposits, NW India","authors":"P. Alexandre","doi":"10.3749/canmin.1900055","DOIUrl":"https://doi.org/10.3749/canmin.1900055","url":null,"abstract":"\u0000 The emerald deposits in Rajasthan, northwest India, are situated in a narrow NE–SW belt in the Aravalli Mountains. The studied deposits were formed by the metasomatic reaction between muscovite (± garnet ± tourmaline) pegmatites and lenticular bodies of altered ultramafic rocks that are hosted by the Delhi Group gneisses. This reaction produced phlogopite schists containing the exometasomatic emeralds, as in all other granite-related emerald deposits. Endometasomatic changes of the mineralogy of the pegmatites is indicated by the geochemistry of the muscovite (phengitic substitution) and the feldspars (disappearance of the potassic feldspar and calcification of the plagioclase).\u0000 The K-Ar analyses of syngenetic phlogopite (from the phlogopite schist) and muscovite (from the pegmatites) give an age of ca. 790 Ma, close to that of the last major orogeny affecting the region. This is in accordance with the ages of other granite-related deposits, which all formed in conditions of active orogeny. The ages of the biotite are lower than those of the muscovite, indicating limited radiogenic argon loss as a result of deformation.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-05-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.1900055","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"42005546","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
A. Kampf, R. Housley, G. Rossman, Hexiong Yang, R. Downs
Adanite, Pb₂ (Te⁴⁺O₃)(SO₄), is a new oxidation-zone mineral from the North Star mine, Tintic district, Juab County, Utah, and from Tombstone, Cochise County, Arizona, USA. The characterization of the species is based principally on North-Star holotype material. Crystals are beige wedge-shaped blades, up to about 1 mm in length, in cockscomb intergrowths. The mineral is transparent with adamantine luster, white streak, Mohs hardness 2½, brittle tenacity, conchoidal fracture, and no cleavage. The calculated density is 6.385 g/cm³. Adanite is biaxial (–), with α = 1.90(1), β = 2.04(calc), γ = 2.08(calc), 2V(meas) = 54(1)°. The Raman spectrum is consistent with the presence of tellurite and sulfate groups and the absence of OH and H₂O. Electron-microprobe analyses gave the empirical formula Pb_(1.89)Sb³⁺_(0.02)Te⁴⁺_(0.98)S⁶⁺_(1.04)Cl_(0.02)O_(6.98). The mineral is monoclinic, space group P2₁/n, with a = 7.3830(3), b = 10.7545(5), c = 9.3517(7) A, β = 111.500(8)°, V = 690.86(7) A₃, and Z = 4. The four strongest X-ray powder diffraction lines are [dobs A(I)(hkl)]: 6.744(47), 3.454(80), 3.301(100), and 3.048(73). The structure (R₁ = 0.022 for 1906 I > 2σI reflections) contains Te⁴⁺O₃ pyramids that are joined by short (strong) Pb–O bonds to form sheets. Interlayer SO₄ groups link the sheets via long Pb–O and Te–O bonds.
Adanite, Pb₂(Te⁴⁺O₃)(SO₄)是一种新的氧化带矿物，来自犹他州Juab县Tintic区North Star矿和美国亚利桑那州Cochise县Tombstone矿。该物种的特征主要基于北星全模材料。晶体是米黄色的楔形叶片，长度可达1毫米左右，在鸡冠状丛生物中。该矿物透明，具有金刚光泽，白色条纹，莫氏硬度2½，脆韧性，贝壳状断裂，无解理。计算密度为6.385 g/cm³。Adanite双轴(-),α= 1.90(1),β= 2.04(钙)、γ= 2.08(钙),2 v(量)= 54(1)°。拉曼光谱与碲和硫酸盐基团的存在一致，没有OH和h2o。电子探针分析给出了实验式Pb_(1.89)Sb³⁺_(0.02)Te⁴⁺_(0.98)S 26⁺_(1.04)Cl_(0.02)O_(6.98)。该矿物为单斜型，空间群为P2₁/n, a = 7.3830(3)， b = 10.7545(5)， c = 9.3517(7) a， β = 111.500(8)°，V = 690.86(7) a₃，Z = 4。四条最强的x射线粉末衍射线为[dobs A(I)(hkl)]: 6.744(47)、3.454(80)、3.301(100)和3.048(73)。该结构(对于1906 I > 2σI反射，R₁= 0.022)包含Te⁴⁺O₃金字塔，这些金字塔由短(强)Pb-O键连接成薄片。层间的SO₄基团通过长Pb-O和Te-O键连接薄片。
{"title":"Adanite, a new lead-tellurite-sulfate mineral from the North Star mine, Tintic, Utah, and Tombstone, Arizona, USA","authors":"A. Kampf, R. Housley, G. Rossman, Hexiong Yang, R. Downs","doi":"10.3749/canmin.2000010","DOIUrl":"https://doi.org/10.3749/canmin.2000010","url":null,"abstract":"Adanite, Pb₂ (Te⁴⁺O₃)(SO₄), is a new oxidation-zone mineral from the North Star mine, Tintic district, Juab County, Utah, and from Tombstone, Cochise County, Arizona, USA. The characterization of the species is based principally on North-Star holotype material. Crystals are beige wedge-shaped blades, up to about 1 mm in length, in cockscomb intergrowths. The mineral is transparent with adamantine luster, white streak, Mohs hardness 2½, brittle tenacity, conchoidal fracture, and no cleavage. The calculated density is 6.385 g/cm³. Adanite is biaxial (–), with α = 1.90(1), β = 2.04(calc), γ = 2.08(calc), 2V(meas) = 54(1)°. The Raman spectrum is consistent with the presence of tellurite and sulfate groups and the absence of OH and H₂O. Electron-microprobe analyses gave the empirical formula Pb_(1.89)Sb³⁺_(0.02)Te⁴⁺_(0.98)S⁶⁺_(1.04)Cl_(0.02)O_(6.98). The mineral is monoclinic, space group P2₁/n, with a = 7.3830(3), b = 10.7545(5), c = 9.3517(7) A, β = 111.500(8)°, V = 690.86(7) A₃, and Z = 4. The four strongest X-ray powder diffraction lines are [dobs A(I)(hkl)]: 6.744(47), 3.454(80), 3.301(100), and 3.048(73). The structure (R₁ = 0.022 for 1906 I > 2σI reflections) contains Te⁴⁺O₃ pyramids that are joined by short (strong) Pb–O bonds to form sheets. Interlayer SO₄ groups link the sheets via long Pb–O and Te–O bonds.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-05-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.2000010","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"48314623","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Biotite grains from 22 felsic intrusions in New Brunswick were mapped in situ using a laser ablation-inductively coupled plasma-mass spectrometer (LA-ICP-MS). We investigated the extent to which biotite can retain its magmatic zoning patterns and, where zoning does exist, how it can be used to elucidate early to late stage, syn-magmatic to post-crystallization processes. Although the major element and halogen contents of the examined biotite phenocrysts are homogeneous, two-thirds of the grains display trace-element zoning for Ba, Rb, and Cs. The results also indicated that zoning is better retained in larger grains (i.e., > 500 × 500 μm) with minimal alteration and mineral inclusions. An exceptionally well-zoned Li-rich siderophyllite from the Pleasant Ridge topaz granite in southwestern New Brunswick shows Ti, Ta, Sn, W, Cs, Rb, and V (without Li or Ba) zoning. Cesium values increase from 200 to 1400 ppm from core to rim. Conversely, Sn and W values decrease toward the rim (50 to 10 and 100 to 10 ppm, respectively). Tantalum and Ti values show fewer variations but drop abruptly close to the rim of the grain (100 to 20 and 2000 to 500 ppm, respectively). These observations may indicate crystallization of mineral phases with high partition coefficients for these highly incompatible elements (except Ti) (e.g., cassiterite and rutile) followed by fractionation of a fluid phase at a later stage of magma crystallization. The preservation of zoning may indicate rapid cooling post-crystallization of the parent magma.
{"title":"High-resolution LA-ICP-MS trace-element mapping of magmatic biotite: A new approach for studying syn- to post-magmatic evolution","authors":"Z. Azadbakht, D. Lentz","doi":"10.3749/canmin.1900101","DOIUrl":"https://doi.org/10.3749/canmin.1900101","url":null,"abstract":"\u0000 Biotite grains from 22 felsic intrusions in New Brunswick were mapped in situ using a laser ablation-inductively coupled plasma-mass spectrometer (LA-ICP-MS). We investigated the extent to which biotite can retain its magmatic zoning patterns and, where zoning does exist, how it can be used to elucidate early to late stage, syn-magmatic to post-crystallization processes. Although the major element and halogen contents of the examined biotite phenocrysts are homogeneous, two-thirds of the grains display trace-element zoning for Ba, Rb, and Cs. The results also indicated that zoning is better retained in larger grains (i.e., > 500 × 500 μm) with minimal alteration and mineral inclusions.\u0000 An exceptionally well-zoned Li-rich siderophyllite from the Pleasant Ridge topaz granite in southwestern New Brunswick shows Ti, Ta, Sn, W, Cs, Rb, and V (without Li or Ba) zoning. Cesium values increase from 200 to 1400 ppm from core to rim. Conversely, Sn and W values decrease toward the rim (50 to 10 and 100 to 10 ppm, respectively). Tantalum and Ti values show fewer variations but drop abruptly close to the rim of the grain (100 to 20 and 2000 to 500 ppm, respectively). These observations may indicate crystallization of mineral phases with high partition coefficients for these highly incompatible elements (except Ti) (e.g., cassiterite and rutile) followed by fractionation of a fluid phase at a later stage of magma crystallization. The preservation of zoning may indicate rapid cooling post-crystallization of the parent magma.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-05-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.1900101","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"45238174","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
L. Pautov, M. A. Mirakov, F. Cámara, E. Sokolova, F. Hawthorne, Manuchekhr A. Schodibekov, V. Y. Karpenko
Badakhshanite-(Y), ideally Y2Mn4Al(Si2B7BeO24), is a tetrahedral sheet-structure mineral found in the Dorozhny (Road) miarolitic granitic pegmatite within the Kukurt pegmatite field 45 km E of Murghab, Eastern Pamir, Gorno-Badakhshan Autonomous Oblast, Tajikistan. Badakhshanite-(Y) occurs in medium- to coarse-grained non-graphic albite-microcline-quartz pegmatites in close association with smoky quartz, Sc-bearing spessartine, Sc-bearing tusionite, and schorl. It often grows together with Sc-bearing tusionite and occurs as single columnar crystals ranging from 50 to 400 μm in length, as inclusions in spessartine and tourmaline, and rarely as crystals in blebs along boundaries between garnet, tourmaline, and quartz. Badakhshanite-(Y) is yellow brown and has a white streak and a vitreous luster. It is brittle, with a conchoidal fracture, Mohs hardness of 6.5–7, and calculated density of 4.41 g/cm. In thin section it is transparent and pale yellow, non-pleochroic, biaxial (–), with α = 1.805(2), βcalc = 1.827, γ = 1.835(3) (λ = 590 nm); 2V (meas.) = –60(10)°. Dispersion is weak, r > v. Extinction is straight, elongation is negative. FTIR spectra show the absence of (OH) and H2O groups. Chemical analysis by electron microprobe using WDS (6 points), SIMS, and ICP-OES for B and Be gave SiO2 11.96, ThO2 0.12, Sm2O3 0.17, Gd2O3 0.30, Tb2O3 0.10, Dy2O3 0.73, Ho2O3 0.19, Er2O3 1.34, Tm2O3 0.54, Yb2O3 8.82, Lu2O3 2.32, Y2O3 16.60, Sc2O3 1.57, Al2O3 3.06, B2O3 22.06, FeO 0.94, MnO 23.33, CaO 0.58, BeO 2.84, total 97.57 wt.%.The empirical formula based on 24 O apfu is (Y1.21REE0.78Th0.01)Σ2(Mn3.47Y0.34Ca0.11Fe2+0.08)Σ4(Al0.63Sc0.24Fe2+0.06□0.07)Σ1[(Si2.10B6.69Be1.20)Σ9.99O24], where REE = (Yb0.47Lu0.12Dy0.04Er0.07Tm0.03 Ho0.01Gd0.02Sm0.01Tb0.01)Σ0.78. Badakhshanite-(Y) is orthorhombic, space group Pnma, a 12.852(1), b 4.5848(5), c 12.8539(8) Å, V 757.38(7) Å3, Z = 2. The crystal structure was refined to R1 = 4.31% based on 1431 unique [F > 4σF] reflections. In the crystal structure of badakhshanite-(Y), a layer of tetrahedra parallel to (010) is composed of four different tetrahedrally coordinated sites: Si, B(1), B(2), and T ( = 1.623 Å, = 1.485 Å, = 1.479 Å, = 1.557 Å), which form four-, five-, and eight-membered rings, having the composition (Si2B7BeO24). Between the sheets of tetrahedra, there are three cation sites: M(1), M(2), and M(3) ( = 2.346 Å, = 2.356 Å, = 2.016 Å) occupied by Y(REE), Mn2+(Y, Ca, Fe2+), and Al(Sc), respectively. The M(1,2) sites ideally give Y2Mn4apfu; the M(3) site ideally gives Al apfu. Badakhshanite-(Y) is an Al- and Be-analogue of perettiite-(Y).
{"title":"Badakhshanite-(Y), Y2Mn4Al(Si2B7BeO24), a new mineral species of the perettiite group from a granite miarolic pegmatite in Eastern Pamir, the Gorno Badakhshan Autonomous Oblast, Tajikistan","authors":"L. Pautov, M. A. Mirakov, F. Cámara, E. Sokolova, F. Hawthorne, Manuchekhr A. Schodibekov, V. Y. Karpenko","doi":"10.3749/canmin.2000003","DOIUrl":"https://doi.org/10.3749/canmin.2000003","url":null,"abstract":"\u0000 Badakhshanite-(Y), ideally Y2Mn4Al(Si2B7BeO24), is a tetrahedral sheet-structure mineral found in the Dorozhny (Road) miarolitic granitic pegmatite within the Kukurt pegmatite field 45 km E of Murghab, Eastern Pamir, Gorno-Badakhshan Autonomous Oblast, Tajikistan. Badakhshanite-(Y) occurs in medium- to coarse-grained non-graphic albite-microcline-quartz pegmatites in close association with smoky quartz, Sc-bearing spessartine, Sc-bearing tusionite, and schorl. It often grows together with Sc-bearing tusionite and occurs as single columnar crystals ranging from 50 to 400 μm in length, as inclusions in spessartine and tourmaline, and rarely as crystals in blebs along boundaries between garnet, tourmaline, and quartz. Badakhshanite-(Y) is yellow brown and has a white streak and a vitreous luster. It is brittle, with a conchoidal fracture, Mohs hardness of 6.5–7, and calculated density of 4.41 g/cm. In thin section it is transparent and pale yellow, non-pleochroic, biaxial (–), with α = 1.805(2), βcalc = 1.827, γ = 1.835(3) (λ = 590 nm); 2V (meas.) = –60(10)°. Dispersion is weak, r > v. Extinction is straight, elongation is negative. FTIR spectra show the absence of (OH) and H2O groups. Chemical analysis by electron microprobe using WDS (6 points), SIMS, and ICP-OES for B and Be gave SiO2 11.96, ThO2 0.12, Sm2O3 0.17, Gd2O3 0.30, Tb2O3 0.10, Dy2O3 0.73, Ho2O3 0.19, Er2O3 1.34, Tm2O3 0.54, Yb2O3 8.82, Lu2O3 2.32, Y2O3 16.60, Sc2O3 1.57, Al2O3 3.06, B2O3 22.06, FeO 0.94, MnO 23.33, CaO 0.58, BeO 2.84, total 97.57 wt.%.The empirical formula based on 24 O apfu is (Y1.21REE0.78Th0.01)Σ2(Mn3.47Y0.34Ca0.11Fe2+0.08)Σ4(Al0.63Sc0.24Fe2+0.06□0.07)Σ1[(Si2.10B6.69Be1.20)Σ9.99O24], where REE = (Yb0.47Lu0.12Dy0.04Er0.07Tm0.03 Ho0.01Gd0.02Sm0.01Tb0.01)Σ0.78. Badakhshanite-(Y) is orthorhombic, space group Pnma, a 12.852(1), b 4.5848(5), c 12.8539(8) Å, V 757.38(7) Å3, Z = 2. The crystal structure was refined to R1 = 4.31% based on 1431 unique [F > 4σF] reflections. In the crystal structure of badakhshanite-(Y), a layer of tetrahedra parallel to (010) is composed of four different tetrahedrally coordinated sites: Si, B(1), B(2), and T (<Si–O> = 1.623 Å, <B(1)–O> = 1.485 Å, <B(2)–O> = 1.479 Å, <T–O> = 1.557 Å), which form four-, five-, and eight-membered rings, having the composition (Si2B7BeO24). Between the sheets of tetrahedra, there are three cation sites: M(1), M(2), and M(3) (<M(1)–O> = 2.346 Å, <M(2)–O> = 2.356 Å, <M(3)–O> = 2.016 Å) occupied by Y(REE), Mn2+(Y, Ca, Fe2+), and Al(Sc), respectively. The M(1,2) sites ideally give Y2Mn4apfu; the M(3) site ideally gives Al apfu. Badakhshanite-(Y) is an Al- and Be-analogue of perettiite-(Y).","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-05-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.2000003","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"41308869","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Several models have been proposed to explain the origin of a chromitite stringer located at the contact between the Mafic and Ultramafic Sequences in the Unki Mine area of the Shurugwi Subchamber of the Great Dyke, Zimbabwe. A petrographic and geochemical study of this chromitite stringer was undertaken with the aim of constraining its origin. Forty-three chromite compositions were obtained from the studied chromitite stringer, which is characterized by a chromium number between 59.9 and 62.8 and a magnesium number which ranges from 37.8 to 46.4. The chromites at the contact zone in the Unki Mine commonly contains inclusions of sulfides, orthopyroxene, plagioclase, and/or amphiboles. The chromites likely formed early in the crystallization history of the Mafic Sequence, as they are commonly partially rimmed by sulfides and they occur as inclusions in plagioclase crystals. Unlike chromites from underlying Ultramafic Sequence chromitite layers, chromites at the contact zone contain low Cr2O3 contents which range from 39.4 to 42.6 wt.%. Furthermore, these chromites are enriched in Fe compared to most Great Dyke chromitites, which is interpreted to be a consequence of subsolidus exchange of Mg into orthopyroxene and Fe into the chromite. The absence of zoning in the chromites at this contact zone, and their low Mn, Fe contents, is consistent with attainment of equilibrium because the altered chromites often contain Cr-bearing magnetite rims. Two possible models for the formation of this chromitite stringer are mixing of relatively primitive and evolved magmas (i.e., ultramafic and anorthositic magma), possibly of different oxygen fugacities, and chemical diffusion across the contact between the Mafic and the Ultramafic sequences which resulted in melting at and below this boundary. The latter would have caused preferential loss of orthopyroxene from the underlying P1 Pyroxenite Layer, accompanied by re-precipitation of chromite at this contact.
{"title":"Geochemistry of the chromitite stringer at the contact of the mafic sequence and the ultramafic sequence in the Unki Mine area, Shurugwi Subchamber of the Great Dyke, Zimbabwe","authors":"J. Chaumba, C. Musa","doi":"10.3749/canmin.1900052","DOIUrl":"https://doi.org/10.3749/canmin.1900052","url":null,"abstract":"\u0000 Several models have been proposed to explain the origin of a chromitite stringer located at the contact between the Mafic and Ultramafic Sequences in the Unki Mine area of the Shurugwi Subchamber of the Great Dyke, Zimbabwe. A petrographic and geochemical study of this chromitite stringer was undertaken with the aim of constraining its origin. Forty-three chromite compositions were obtained from the studied chromitite stringer, which is characterized by a chromium number between 59.9 and 62.8 and a magnesium number which ranges from 37.8 to 46.4. The chromites at the contact zone in the Unki Mine commonly contains inclusions of sulfides, orthopyroxene, plagioclase, and/or amphiboles. The chromites likely formed early in the crystallization history of the Mafic Sequence, as they are commonly partially rimmed by sulfides and they occur as inclusions in plagioclase crystals. Unlike chromites from underlying Ultramafic Sequence chromitite layers, chromites at the contact zone contain low Cr2O3 contents which range from 39.4 to 42.6 wt.%. Furthermore, these chromites are enriched in Fe compared to most Great Dyke chromitites, which is interpreted to be a consequence of subsolidus exchange of Mg into orthopyroxene and Fe into the chromite. The absence of zoning in the chromites at this contact zone, and their low Mn, Fe contents, is consistent with attainment of equilibrium because the altered chromites often contain Cr-bearing magnetite rims. Two possible models for the formation of this chromitite stringer are mixing of relatively primitive and evolved magmas (i.e., ultramafic and anorthositic magma), possibly of different oxygen fugacities, and chemical diffusion across the contact between the Mafic and the Ultramafic sequences which resulted in melting at and below this boundary. The latter would have caused preferential loss of orthopyroxene from the underlying P1 Pyroxenite Layer, accompanied by re-precipitation of chromite at this contact.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-05-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.1900052","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"45442898","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
M. Ondrejka, P. Bačík, M. Putiš, P. Uher, T. Mikuš, J. Luptáková, Š. Ferenc, A. Smirnov
A unique assemblage of hedyphane-group minerals of the apatite supergroup associated with galena, cerussite, and calcite occurs in a Permian aplite dike crosscutting orthogneisses belonging to the pre-Alpine basement of the Veĺký Zelený Potok Valley in the Veporic Unit, Western Carpathians, Central Slovakia. The secondary Ca-Pb phosphates include phosphohedyphane Ca2Pb3(PO4)3Cl and (OH)-dominant “hydroxylphosphohedyphane” Ca2Pb3(PO4)3OH. Detailed EPMA and Raman spectroscopy of the hedyphane-group minerals reveal the presence of Pb, Ca, P, and Cl as major constituents; the systematic presence of (CO3)2– (up to 2.6 wt.% CO2calc; 0.65 apfu C) substituting for (PO4)3– (B-type) is the first reported carbonate-bearing phosphohedyphane in nature. There is also significant localized halogen deficiency (0.38–0.49 apfu Cl+F) which suggests the potential for a new mineral, “hydroxylphosphohedyphane”. The secondary assemblage described herein results from very low-temperature sulfide-carbonate reactions and further near-surface supergene alteration of primary magmatic or metamorphic phosphate minerals (mainly apatite) and hydrothermal galena in the alkaline CO2-rich groundwater.
{"title":"Carbonate-bearing phosphohedyphane–“Hydroxylphosphohedyphane” and cerussite: Supergene products of galena alteration in Permian aplite (Western Carpathians, Slovakia)","authors":"M. Ondrejka, P. Bačík, M. Putiš, P. Uher, T. Mikuš, J. Luptáková, Š. Ferenc, A. Smirnov","doi":"10.3749/canmin.1900082","DOIUrl":"https://doi.org/10.3749/canmin.1900082","url":null,"abstract":"\u0000 A unique assemblage of hedyphane-group minerals of the apatite supergroup associated with galena, cerussite, and calcite occurs in a Permian aplite dike crosscutting orthogneisses belonging to the pre-Alpine basement of the Veĺký Zelený Potok Valley in the Veporic Unit, Western Carpathians, Central Slovakia. The secondary Ca-Pb phosphates include phosphohedyphane Ca2Pb3(PO4)3Cl and (OH)-dominant “hydroxylphosphohedyphane” Ca2Pb3(PO4)3OH. Detailed EPMA and Raman spectroscopy of the hedyphane-group minerals reveal the presence of Pb, Ca, P, and Cl as major constituents; the systematic presence of (CO3)2– (up to 2.6 wt.% CO2calc; 0.65 apfu C) substituting for (PO4)3– (B-type) is the first reported carbonate-bearing phosphohedyphane in nature. There is also significant localized halogen deficiency (0.38–0.49 apfu Cl+F) which suggests the potential for a new mineral, “hydroxylphosphohedyphane”. The secondary assemblage described herein results from very low-temperature sulfide-carbonate reactions and further near-surface supergene alteration of primary magmatic or metamorphic phosphate minerals (mainly apatite) and hydrothermal galena in the alkaline CO2-rich groundwater.","PeriodicalId":9455,"journal":{"name":"Canadian Mineralogist","volume":null,"pages":null},"PeriodicalIF":0.9,"publicationDate":"2020-05-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"https://sci-hub-pdf.com/10.3749/canmin.1900082","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"44992551","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":4,"RegionCategory":"地球科学","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
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