Supplemental Material: Geochronology, petrogenesis, and magmatic oxidation state of the Mangling intrusive complex, Northern Qinling Belt, Central China: Implications for magma fertility and tectonic setting
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<p>Supplemental Text: Analytical Methods. Figure S1: Cathodoluminescence images of representative zircons for U-Pb dating and Lu-Hf isotope analyses for the Mangling intrusive complex. Figure S2: Chondrite-normalized REE patterns of analyzed zircons for the Mangling intrusive complex. Figure S3: Field photographs showing relationships of the granitic rocks of the Mangling intrusive complex. Figure S4: Harker diagrams of selected major and trace elements against SiO2 for the Mangling intrusive complex. Table S1: Zircon U-Pb dating results for the dioritic and granitic rocks of the Mangling intrusive complex. Table S2: Whole-rock major- (wt%), trace- (ppm), and rare earth (ppm) element compositions for the dioritic and granitic rocks of the Mangling intrusive complex. Table S3: Zircon trace element compositions (ppm) for the dioritic and granitic rocks of the Mangling intrusive complex. Table S4: Zircon Lu-Hf isotopic data for the dioritic and granitic rocks of the Mangling intrusive complex. Table S5: Summary of geochronological data for the Mangling intrusive complex. Table S6: Zircon trace element compositions (ppm) for the mineralized granitic rocks of porphyry molybdenum deposits in Central and NE China.</p>Keywords:
Petrogenesis
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Peninsular Malaysia, known as the world's famous producer of tin, has been drawn great attention to evolutionary relationship between the tin mineralization and the granitic magma activity during the Permain-Triassic period. This paper reports on Late Triassic (~217-215 Ma) highly fractionated granitoids of the Gerik pluton in Malaysia Main Range province to elucidate processes of magma differentiation and melt-crystal-fluid interaction. The Gerik pluton consists of two types of granitoids, the low silica series (LSS) and the high silica series (HSS), which both of them have similar source origin but experience different evolutionary routes. The LSS represent the products without obvious fluid fingerprints in the early stage, which is evidenced by their nearly constant twin-element behaviour (Nb/Ta, Zr/Hf and Y/Ho) and smooth REE pattern. However, with further melt differentiation and emplacement, the HSS predominantly exhibit characteristics of melt-fluid interaction during the late stage of magma evolution, as shown by their mineralogy features (e.g., zircon, tourmaline), non-charge-and-radius-controlled (non-CHARAC) twin-element behaviour, REE tetrad effect and especially large variation of initial Sr isotope (87Sr/86Sri: 0.7058 to 0.7282). Based on comparison between the two types of granitoids in the Gerik pluton, we suggest that the magmatic fluid with unradiogenic Sr isotope may result from deep magma reservoir, which subsequently rise to the shallow part of the crust due to saturation and participate in the interaction with the high evolved granitic melt. Meanwhile, the magmatic fluid may also bring in plenty of fluid-mobile Sn, which finally presents the most abundant hydrothermal vein-type deposits in Peninsular Malaysia.
Petrogenesis
Igneous differentiation
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Petrogenesis
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Rare-earth element
Amphibole
Incompatible element
Alkaline earth metal
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Geochronology
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Glass fragments in tephra erupted at Mt. Etna from May to December 1995 have been analyzed by laser ablation ICPMS. The trace element compositional variability of ashes deposited during this interval reveals the presence of discrete magma batches with different crystallization degrees in the shallow plumbing system. From May to October a highly crystalline magma is predominant within the conduit with only minor sporadic input of fresh and more primitive magma batches. After October new and less evolved magma batches become more prevalent and become progressively homogenized within more evolved resident magma. In December ashes closely match the chemistry of the volcanics subsequently erupted till February 1996. This study demonstrates that the trace element characterization of ashes has important implications for volcanic monitoring and is a useful tool for the forecasting of paroxysmal events at Mt. Etna.
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Magma chamber
Laser Ablation
Volcanic glass
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Abstract Cu and Fe skarns are the world's most abundant and largest skarn type deposits, especially in China, and Au‐rich skarn deposits have received much attention in the past two decades and yet there are few papers focused on schematic mineral deposit models of Cu–Fe–Au skarn systems. Three types of Au‐rich deposits are recognized in the Edongnan region, Middle–Lower Yangtze River metallogenic belt: ∼140 Ma Cu–Au and Au–Cu skarn deposits and distal Au–Tl deposits. 137–148 Ma Cu–Fe and 130–133 Ma Fe skarn deposits are recognized in the Edongnan region. The Cu–Fe skarn deposits have a greater contribution of mantle components than the Fe skarn deposits, and the hydrothermal fluids responsible for formation of the Fe skarn deposits involved a greater contribution from evaporitic sedimentary rocks compared to Cu–Fe skarn deposits. The carbonate‐hosted Au–Tl deposits in the Edongnan region are interpreted as distal products of Cu–Au skarn mineralization. A new schematic mineral deposit model of the Cu–Fe–Au skarn system is proposed to illustrate the relationship between the Cu–Fe–Au skarn mineralization, the evaporitic sedimentary rocks, and distal Au–Tl deposits. This model has important implications for the exploration for carbonate–hosted Au–Tl deposits in the more distal parts of Cu–Au skarn systems, and Fe skarn deposits with the occurrence of gypsum‐bearing host sedimentary rocks in the MLYRB, and possibly elsewhere.
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Metasomatism
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Skarn deposits occur throughout the world and have been mined for a variety of elements. This paper describes the basic stages of skarn formation and the main causes of variation from the general evolutionary model. Seven major classes of skarn deposits (Fe, W, Au, Cu, Zn, Mo and Sn) are briefly described, and relevant geological and geochemical features of important examples are summarized in a comprehensive table. The important geochemical and geophysical parameters of skarn deposits are discussed, followed by a summary of important petrologic and tectonic constraints on skarn formation. Finally, exploration models are presented for several major skarn types, with a plea for field mapping as a fundamental basis for future studies.
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