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| 1 | Chemical and Isotopic Characteristics of the Water and Suspended Particulate Materials in the Yangtze River and Their Geological and Environmental Implications显示文摘The chemical and isotopic characteristics of the water and suspended particulate materials(SPM) in the Yangtze River were investigated on the samples collected from 25 hydrological monitoring stations in the mainsteam and 13 hydrological monitoring stations in the major tributaries during 2003 to 2007. The water samples show a large variation in both δD( 30‰ to 112‰) and δ18O( 3.8‰ to 15.4‰) values. Both δD and δ18O values show a decrease from the river head to the Jinsha Jiang section and then increase downstream to the river mouth. It is found that the oxygen and hydrogen isotopic compositions of the Yangtze water are controlled by meteoric precipitation, evaporation, ice(and snow) melting and dam building. The Yangtze SPM concentrations show a large variation and are well corresponded to the spatial and temporal changes of flow speed, runoff and SPM supply, which are affected by the slope of the river bed, local precipitation rate, weathering intensity, erosion condition and anthropogenic activity. The Yangtze SPM consists of clay minerals, clastic silicate and carbonate minerals, heavy minerals, iron hydroxide and organic compounds. From the upper to lower reaches, the clay and clastic silicate components in SPM increase gradually, but the carbonate components decrease gradually, which may reflect changes of climate and weathering intensity in the drainage area. Compared to those of the upper crust rocks, the Yangtze SPM has lower contents of SiO2, CaO, K2 O and Na2 O and higher contents of TFe2 O3 and trace metals of Co, Ni, Cu, Zn, Pb and Cd. The ΣREE in the Yangtze SPM is also slightly higher than that of the upper crust. From the upper to lower reaches, the CaO and MgO contents in SPM decrease gradually, but the SiO2 content increases gradually, corresponding to the increase of clay minerals and decrease of the carbonates. The δ30SiSPM values( 1.1‰ to 0.3‰) of the Yangtze SPM are similar to those of the average shale, but lower than those of the granite rocks( 0.3‰ to 0.3‰), reflecting the effect of silicon isotope fractionation in silicate weathering process. The δ30SiSPM values of the Yangtze SPM show a decreasing trend from the upper to the middle and lower reaches, responding to the variation of the clay content. The major anions of the river water are HCO 3, SO 4 2, Cl, NO 3, SiO 4 4 and F and the major cations include Ca2+, Na+, Mg2+, K+ and Sr2+. The good correlation between HCO3-content and the content of Ca2+may suggest that carbonate dissolution is the dominate contributor to the total dissolved solid(TDS) of the Yangtze River. Very good correlations are also found among contents of Cl, SO4 2, Na+, Mg2+, K+and Sr2+, indicating the important contribution of evaporite dissolution to the TDS of the Yangtze River. High TDS contents are generally found in the head water, reflecting a strong effect of evaporation in the Qinghai-Tibet Plateau. A small increase of the TDS is generally observed in the river mouth, indicating the influence of tidal intrusion. The F and NO3 contents show a clear increase trend from the upstream to downstream, reflecting the contribution of pesticides and fertilizers in the Chuan Jiang section and the middle and lower reaches. The DSi shows a decrease trend from the upstream to downstream, reflecting the effect of rice and grass growth along the Chuan Jiang section and the middle and lower reaches. The dissolved Cu, Zn and Cd in the Yangtze water are all higher than those in world large rivers, reflecting the effect of intensive mining activity along the Yangtze drainage area. The Yangtze water generally shows similar REE distribution pattern to the global shale. The δ30SiDiss values of the dissolved silicon vary from 0.5‰ to 3.7‰, which is the highest among those of the rivers studied. The δ30SiDiss values of the water in the Yangtze mainsteam show an increase trend from the upper stream to downstream. Its DSi and δ30SiDiss are influenced by multiple processes, such as weathering process, phytolith growth in plants, evaporation, phytolith dissolution, growth of fresh water diatom, adsorption and desorption of aqueous monosilicic acid on iron oxide, precipitation of silcretes and formation of clays coatings in aquifers, and human activity. The δ34SSO4 values of the Yangtze water range from 1.7‰ to 9.0‰. The SO4 in the Yangtze water are mainly from the SO4 in meteoric water, the dissolved sulfate from evaporite, and oxidation of sulfide in rocks, coal and ore deposits. The sulfate reduction and precipitation process can also affect the sulfur isotope composition of the Yangtze water. The87Sr/86Sr ratios of the Yangtze water range from 0.70823 to 0.71590, with an average value of 0.71084. The87Sr/86Sr ratio and Sr concentration are primary controlled by mixing of various sources with different87Sr/86Sr ratios and Sr contents, including the limestone, evaporite and the silicate rocks. The atmospheric precipitation and anthropogenic inputs can also contribute some Sr to the river. The δ11B values of the dissolved B in the Yangtze water range from 2.0‰ to 18.3‰, which is affected by multifactors, such as silicate weathering, carbonate weathering, evaporite dissolution, atmospheric deposition, and anthropogenic inputs. | DING Tiping GAO Jianfei TIAN Shihong SHI Guoyu CHEN Feng WANG Chengyu LUO Xurong HAN Dan | 2014 | Acta Geologica Sinica(English Edition)2014，88，1： | 10 |
| 2 | S, C, O, H Isotope Data and Noble Gas Studies of the Maoniuping LREE Deposit, Sichuan Province, China: A Mantle Connection for Mineralization显示文摘Maoniuping REE 存款,定位了大约 22 km 到 Mlanning 的西南,四川省,是在中国的第二最大的轻 REE 存款,对 Bayan OboFe-Nfo-REE 存款 inihe 随后内部蒙古自治区域。构造地,它位于在 Panxi 裂缝之间的过渡地区和 Longmenshan-Jinpingshan orogenic 地区。它是在碱的复合岩石招待的 acarbonatite 静脉类型沉积物。bastnaesite 重晶石, bastnaesite 方解石,和 bastnaesite-microcline 矿脉是主要 REE 矿石矿脉的三种类型。在这些之中,第一条矿脉最广泛地被散布,它的 REE 矿化作用最强壮。在存款的矿石的 barltes 的 DELTA^(34 )S_(V-CDT ) 价值每千条 Inthe bastnaesite 重晶石矿脉在 bastnaesite 方解石矿脉和 +33 每千在 +5.0 的一个狭窄的范围变化到 +5.1 到 +5.9,显示出导出岩浆的硫的同位素的特征。分别地,O_(V降雪)在bastnaesite方解石矿脉珍视的TheDELTA^( 13 )C_( V-PDB )价值和DLETA^( 18 )每千每千并且从 +7.3 从 -3.9 到 -6.9 到 +9.7 它掉进“主要 carbonatites ”的范围,在 Maoniupingdeposit 的矿石显示出那碳和氧主要从深来源被导出。液包体的 DELTA^(13 )C_(V-PDB ) 价值每千从 -3.0 变化到 -5.6,与到在 bastnaesite 方解石矿脉的每千的 -4.0 的 -3.0 和到在 bastnaesite 重晶石矿脉的每千的 -5.6 的 -3.0,它显示出特征导出 ofmantle 的碳。detla^(18O_((H_2OV ) 液包体的 -SMOW)) 价值每千从 -57 to-88 ,与到 -86 的 -63 每千在到 -88 的 bastnaesite 方解石矿脉和 -57 每千在 bastnaesite 重晶石矿脉,它导出披风的氢的表演特征。TheDELTA^(18 )O_(H_2OV 降雪) 价值每千从 +7.4 变化到 +8.6 在。bastnaesite-calcitelode,和 +6.7 到 +7.8 每千在 bastnaesite 重晶石矿脉,几乎重叠范围 of+5.5 到 +9.5 每千为 magmatic。~ 4He 内容, R/Ra 比率是(13.95 to119.58 )X10^(-6)(cm^3/g )_(STP ) 并且 0.02 ~ 0.11,分别地并且 ^(40 )Ar/^(36 ) Ar 是 313 +- 1 to437 +- 2。就放射性元素的高内容引起的 4He 增加而言,导出 amantle 的液体可能在 fluorlte,方解石和 bastnaesitesamples 在包括存在。Maoniuping 存款和它的联系 carbonatite 碱的建筑群在 40.3to 被形成 12.2 妈根据 K-Ar 和 U-Pb 数据。所有这些数据建议披风液体的大数量通过一个差错系统涉及 Maoniuping REE 存款的 metallogenic 进程。 | TIAN Shihong DING Tiping MAO Jingwen LI Yanhe YUAN Zhongxin | 2006 | Acta Geologica Sinica(English Edition)2006，80，4： | 6 |
| 3 | Chemical and Isotopic Characters of the Water and Suspended Particulate Materials in the Yellow River and Their Geological and Environmental Implications显示文摘The chemical and isotopic characteristics of the water and suspended particulate materials(SPM)in the Yellow River were investigated on the samples collected from 29 hydrological monitoring stations in the mainstem and several major tributaries during 2004 to 2007.TheδD andδ^(18)O values of the Yellow River water vary in large ranges from-32‰to-91‰and from-3.1‰to-12.5‰,respectively.The characters of H and O isotope variations indicate that the major sources of the Yellow River water are meteoric water and snow melting water,and water cycle in the Yellow River basin is affected strongly by evaporation process and human activity.The average SPM content(9.635g/L)of the Yellow River is the highest among the world large rivers.Compared with the Yangtze River,the Yellow River SPM has much lower clay content and significantly higher contents of clastic silicates and carbonates.In comparison to the upper crust rocks,the Yellow River SPM contains less SiO_2,CaO,K_2O and Na_2O,but more TFe_2O_3,Co,Ni,Cu,Zn,Pb and Cd.The abnormal high Cd contents found in some sample may be related to local industrial activity.The REE contents and distribution pattern of the Yellow River SPM are very close to the average value of the global shale.The averageδ^(30)Si_(SPM)in the Yellow River(-0.11‰)is slightly higher than the average value(-0.22‰)of the Yangtze River SPM.The major factors controlling theδ^(30)Si_(SPM)of the Yellow River are the soil supply,the isotopic composition of the soil and the climate conditions.The TDS in the Yellow River are the highest among those of world large rivers.Fair correlations are observed among Cl^-,Na^+,K^+,and Mg^(2+)contents of the Yellow River water,indicating the effect of evaporation.The Ca^(2+)and Sr^(2+)concentrations show good correlation to the SO_4^(2-)concentration rather than HCO_3^-concentration,reflecting its origin from evaporates.The NO_3^-contents are affected by farmland fertilization.The Cu,Zn and Cd contents in dissolved load of the Yellow River water are all higher than those of average world large rivers,reflecting the effect of human activity.The dissolved load in the Yellow River water generally shows a REE distribution pattern parallel to those for the Yangtze River and the Xijiang River.Theδ^(30)Si values of the dissolved silicon vary in a range from 0.4‰to 2.9‰,averaging1.34‰.The major processes controlling the D_(Si)andδ^(30)Si_(Diss)of the Yellow River water are the weathering process of silicate rocks,growth of phytolith in plants,evaporation,dissolution of phytolith in soil,growth of fresh water diatom,adsorption and desorption of aqueous monosilicic acid on iron oxide and human activities.The averageδ^(30)Si_(Diss)value of the Yellow River is significantly lower than that of the Nile River,Yangtze River and Siberia rivers,but higher than those of other rivers,reflecting their differences in chemical weathering and biological activity.Theδ^(34)S_(SO4)values of the Yellow River water range from-3.8‰to 14.1‰,averaging 7.97‰.There is some correlation between SO_4^(2-)content andδ^(34)S_(SO4).The factors controlling theδ^(34)S_(SO4)of the Yellow River water are the SO_4 in the meteoric water,the SO_4 from gypsum or anhydrite in evaporite rocks,oxidation and dissolution of sulfides in the mineral deposits,magmatic rocks and sedimentary rocks,the sulfate reduction and precipitation process and the sulfate from fertilizer.The^(87)Sr/^(86)Sr ratios of all samplesrange from 0.71041 to 0.71237,averaging 0.71128.The variations in the^(87)Sr/^(86)Sr ratio and Sr concentration of river water are primarily caused by mixing of waters of various origins with different^(87)Sr/^(86)Sr ratios and Sr contents resulting from water-rock interaction with different rock types. | DING Tiping GAO Jianfei TIAN Shihong WANG Huaibai LI Ming WANG Chengyu LUO Xurong HANG Dan | 2016 | Acta Geologica Sinica(English Edition)2016，90，1： | 4 |
| 4 | An Experimental Calibration on the Sphalerite-Galena Sulfur Isotope Geothermometer显示文摘A new experimental calibration was undertaken in this study to get a more reliable sphalerite-galenasulfur isotope geothermometer. The experimental conditions selected in study were very similar to those of naturalhydrothermal solution. The high-precision SF6 method was used in sulfur isotope analyses. The obtained calibrationcurve for sulfur isotope fractionation between sphalerite and galena can be expressed with the equation 1000lnαSp-Gn=0.74×106T-2+0.08. | DING Tiping, ZHANG Chengxin, WAN Defang, LIU Zhijian and ZHANG Guilan Institute of Mineral Resources, Chinese Academy of Geological Sciences, 26 Baiwanzhuang Rd.,Beijing 100037 | 2003 | Acta Geologica Sinica(English Edition)2003，77，4： | 0 |
| 5 | Quartz-Ferberite Oxygen Isotope Geothermometer and Its Geological Applications显示文摘Experiments for oxygen isotope exchange between ferberite and water were carried out and the followingequation on oxygen isotope fractionation between ferberite and water against temperature was obtained:Combining this equation with the equation of Clayton et al. (1972) on oxygen isotope fractionation be-tween quartz and water, an equation on oxygen isotope fractionation between quartz and ferberite was ob-tained:The Bigeleison-Mayer function method was used to calculate the oxygen isotope fractionation betweenquartz and ferberite. The theoretical curve obtained agrees with the experimental calibration results quite wellin the temperature range of study.The above calibrated equation has been used in 5 world famous tungsten deposits to determine their tem-peratures of formation. The results show that the temperature range for an idividual deposit determined by thisgeothermometer agrees with those obtained from fluid inclusion determination and other isotopegeothermometers. | Ding Tiping Liu Yushan Wan Defang Liu Zhijian Li Jincheng Zhang Guilan Institute of Mineral Deposits, Chinese Academy of Geological Sciences, Beijing | 1992 | Acta Geologica Sinica(English Edition)1992，66，3： | 0 |
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