THE EVOLUTION OF RIVER SEDIMENTARY ENVIRONMENT IN THE MAONIUPING REE DEPOSIT
YANG Wei-he1, SHI Ze-ming1,2, NI Shi-jun1,2
1. College of Applied Nuclear Technology and Automation Engineering, Chengdu University of Technology, Chengdu 610059, China;
2. Sichuan Key Laboratory of Applied Techniques in Geosciences, Chengdu University of Technology, Chengdu 610059, China
Based on a systematic study of sedimentary profile from downstream of the Maoniuping REE deposit, the authors investigated the environmental impact of mine development on fluvial deposits. The results show that the sediment profile can be divided into four stages: 0~10 cm,10~30 cm,30~40 cm and 40~50 cm. The authors determined the depositional age of the sediment profiles by 210Pb. The average deposition rate of the river is 0.45 cm/a since 1910. According to the rate of sediment profiles, the deposition can be divided to four stages: The first stage is 1910~1940, whose deposition thickness is about 5 cm and whose average deposition rate is 0.168 cm/a. At this stage the content of K, Na, U, S, Mo, Mn, Pb and F decreased gradually. The second stage is 1940~1990, whose deposition thickness is about 22 cm and whose average deposition rate is 0.44 cm/a. At this stage the shallow 12 cm showed the characteristics of high pH, N, P and organic matter but low K, Na, U, S, Mo, Mn, Pb and F, whereas the deep 10 cm presented the characteristics of high K, Na, U, S, Mo, Mn, Pb and F. The third stage is 1990~1999, whose deposition thickness is about 8 cm and whose average deposition rate is 0.889 cm/a. At this stage there existed the characteristics of high pH, N, P and organic matter but low K, Na, U, S, Mo, Mn, Pb and F. The fourth stage is from 1999 up till now, whose deposition thickness is about 10 cm and whose average deposition rate is 0.909 cm/a. This stage presents the characteristics of low pH, N, P and organic matter but high K, Na, U, S, Mo, Mn, Pb and F.
杨伟河, 施泽明, 倪师军. 牦牛坪稀土矿区河流沉积环境演化[J]. 物探与化探, 2013, 37(3): 389-393.
YANG Wei-he, SHI Ze-ming, NI Shi-jun. THE EVOLUTION OF RIVER SEDIMENTARY ENVIRONMENT IN THE MAONIUPING REE DEPOSIT. Geophysical and Geochemical Exploration, 2013, 37(3): 389-393.
[1] 谢玉玲,徐九华,陈伟,等.四川冕宁牦牛坪稀土矿床与岩浆碳酸岩有关的成矿流体特征[J].矿物岩石地球化学通报,2005,24(增刊):265-266.[2] 侯增谦,田世红,谢玉玲,等.川西冕宁—德昌喜马拉雅期稀土元素成矿带:矿床地质特征与区域成矿模型[J].矿床地质,2008,27(2):145-176.[3] 蒲广平.牦牛坪稀土矿的特点及其开发利用[J].矿产保护与利用,1994(5):17-20.[4] 蒲广平.牦牛坪稀土矿床成矿模式及找矿方向探讨[J].四川地质学报,1993,13(5):46-57.[5] 蒋明全.牦牛坪稀土矿床地质构造特征及其控矿意义[J].矿床地质,1992,11(4):351-358.[6] 施泽民,叶幼兰.四川牦牛坪稀土矿区的氟碳铈矿[J].矿物岩石,1993,13(3):42-47.[7] XU Cheng,HUANG Zhilong,QI Liang.Genetic relation of ore-forming fluids and carbonatite-syenite complex in Maoniuping REE deposit, Sichuan province, China: A Review[J].Journal of the Graduate School of the Chinese Academy of Sciences, 2004, 21(4):557-561.[8] 滕达.四川省冕宁县牦牛坪稀土尾矿区植物修复研究.成都:成都理工大学,2009.[9] 许向宁.长江上游安宁河流域主要生态环境地质问题及其效应[J].山地学报,2004,22(5):572-577.[10] Shigern M,Futoshi N,Tohrn A.Using dendrogeomorphology and 137Cs and 210Pb radiochronology to estimate recent changes in sedimentation rates in Kushiro Mire,northern Japan,resulting from land use change and river channelization[J].Catena,2006,65:25-40.[11] 吴澄宇,袁忠信,白鸽.四川冕宁氟碳铈矿晶体的成分变化及其意义[J].中国稀土学报,1996,14(1):1-5.[12] 许成,黄智龙,刘丛强,等.四川牦牛坪稀土矿床碳酸岩地球化学[J].中国科学:D辑,2002,32(8):635-643.[13] 周家云,郑荣才,沈冰,等.四川冕宁木洛稀土矿床含矿岩体地球化学特征及其构造意义[J].矿物岩石,2007,27(1):83-89.[14] 阳正熙,Anthony E J,蒲广平.四川冕宁牦牛坪稀土矿床地质特征[J].矿物岩石,2000,20(2):28-34.[15] 陈振楼,许世远,柳林,等.上海滨岸潮滩沉积物重金属元素的空间分布与积累[J].地理学报,2000,55(6):641-651.[16] Cundy A B,Croudace I W,Cearreta A,et al.Reconstructing Historical Trends in Metal Input in Heavily-Disturbed,Contaminated Estuaries: Studies from Bilbao,Southampton Water and Sicily[J].Applied Geochemistry,2003,18(2): 311-325.[17] 陈静生,王飞越,陈江麟.论小于63 μm粒级作为水体颗粒物重金属研究介质的合理性及有关粒级转换模型研究[J].环境科学学报,1994,14(4):419-425.
