黔东北地区南华系两界河组CIA指数特征及意义
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摘要
化学蚀变指数(CIA)是判断源岩风化程度的化学指标。通过分析黔东北地区苗哨溪剖面两界河组的CIA特征,为讨论其古气候特征提供地球化学方面的依据。结果表明,两界河组CIA值介于55. 48～89. 33之间,均值为72. 49,除极个别数值为55. 48、89. 33之外,其它数值皆介于65～75之间,指示两界河组具有温暖湿润的古气候特征。通过综合分析两界河组岩石组合、沉积构造及古气候特征,认为两界河组为间冰期沉积。在此基础上,结合最新同位素年代学数据,认为其可与富禄组中上部进行对比。
There has been much debated recently concerning the issue whether or not the Nanhuan Liangjiehe Formation may be classified into the interglacial deposits. The values of chemical alteration index(CIA)for the Liangjiehe Formation in the Miaoshaoxi section,northeastern Guizhou may directly provide geochemical evidence for the approaches to the palaeoclimatological features in this region. The values of chemical alteration index presented in this study generally vary from 55. 48 to 89. 33,with an average of 72. 49. Except the values 55. 48 and 89. 33,all the other ones range between 65 and 75,indicating the warm and humid palaeoclimatic conditions during the deposition of the Liangjiehe Formation. The integration of rock assemblages,sedimentary structures and palaeoclimatological features show that the Liangjiehe Formation should be assigned to the interglacial deposits,and may be correlated to the middle and upper parts of the Fulu Formation.
There has been much debated recently concerning the issue whether or not the Nanhuan Liangjiehe Formation may be classified into the interglacial deposits. The values of chemical alteration index(CIA)for the Liangjiehe Formation in the Miaoshaoxi section,northeastern Guizhou may directly provide geochemical evidence for the approaches to the palaeoclimatological features in this region. The values of chemical alteration index presented in this study generally vary from 55. 48 to 89. 33,with an average of 72. 49. Except the values 55. 48 and 89. 33,all the other ones range between 65 and 75,indicating the warm and humid palaeoclimatic conditions during the deposition of the Liangjiehe Formation. The integration of rock assemblages,sedimentary structures and palaeoclimatological features show that the Liangjiehe Formation should be assigned to the interglacial deposits,and may be correlated to the middle and upper parts of the Fulu Formation.
引文
[1]马国干,王砚耕.鄂、湘、川、黔毗邻地区早震旦世冰川地质问题讨论[A].中国地质科学院宜昌地质矿产研究所文集(7)[C].中国地质学会,1983. 43-51.
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[12]齐靓,余文超.黔东南华纪铁丝坳期—大塘坡期古气候的演变:来自CIA的证据[J].地质科技情报,2015,34(6):47-57.
[13]冯连君,储雪蕾.化学蚀变指数(CIA)及其在新元古代碎屑岩中的应用[J].地学前缘,2003(4):539-544.
[14]王自强,尹崇玉.宜昌三斗坪地区南华系化学蚀变指数特征及南华系划分、对比的讨论[J].地质论评,2006,(5):577-585.
[15]王自强,尹崇玉,高林志,等.黔南—桂北地区南华系化学地层特征[J].地球学报,2009,30(4):465-474.
[16]周琦,杜远生,颜佳新,等.贵州松桃大塘坡地区南华纪早期冷泉碳酸盐岩地质地球化学特征[J].地球科学(中国地质大学学报),2007,(6):845-852.
[17]何明华.贵州东部及邻区震旦纪铁丝坳期和南沱期沉积相与环境演化及构造属性探讨[J].贵州地质,1998,(1):26-31+25.
[18]伍皓,江新胜,王剑,汪正江,等.湘西托口地区南华系沉积地层学研究及其地质意义[J].地层学杂志,2015,39(3):300-309.
[19]柏道远.湘西南震旦纪长安期沉积相变与构造环境分析[J].湖南地质,2001,(1):5-8.
[20]林树基,肖加飞,卢定彪等.湘黔桂交界区富禄组与富禄间冰期的再划分[J].地质通报,2010,29(Z1):195-204.
[21]彭学军,刘耀荣,吴能杰等.扬子陆块东南缘南华纪地层对比[J].地层学杂志,2004,(4):354-359.
[22]Heron D P L. The significance of ice-rafted debris in sturtian glacial successions[J]. Sedimentary Geology,2015,322,19-33.
[23]Balgord E A,Yonkee W A,Link P K,et al. Stratigraphic,geochronologic,and geochemical record of the Cryogenian Perry Canyon Formation,northern Utah:Implications for Rodinia rifting and snowball Earth glaciation[J]. Geological Society of America Bulletin,2013,125(9-10):1442-1467.
[24]Kellerhals P,Matter A. Facies analysis of a glaciomarine sequence,the Neoproterozoic Mirbat Sandstone Formation,Sultanate of Oman[J]. Eclogae Geologicae Helvetiae,2003,96(96):49-70.
[25]蔡娟娟,崔晓庄,兰中伍,等.华南扬子陆块成冰纪冰川作用的启动时限及其全球对比[J].古地理学报,2018,20(1):65-86.
[2]刘撰峰,王庆生,高兴基等.贵州锰矿地质[M].贵阳:贵州人民出版社,1989. 59-184.
[3]刘鸿允.中国震旦系[M].北京:科学出版社,1991. 1-388.
[4]罗亮,孙志明,马志鑫,等.黔东渝东南地区南华纪沉积序列与沉积环境演变[J].地质科技情报,2015,34(2):27-35.
[5]王砚耕,谢志强,王来兴,等.贵州东部及邻区铁丝坳组层序及沉积环境成因[J].中国区域地质,1986,(4):341-348.
[6]林树基,卢定彪,肖加飞,等.贵州南华纪冰期地层的主要特征[J].地层学杂志,2010,37(4):542-557.
[7]陈建书,戴传固,彭成龙,等.湘黔桂相邻区新元古代820~635Ma时期裂谷盆地充填序列与地层格架[J].中国地质,2016,43(3):899-920.
[8]张传恒,刘耀明,史晓颖,等.下江群沉积地质特征及其对华南新元古代构造演化的约束[J].地球学报,2009,30(4):495-504.
[9]尹赞勋,徐道一,浦庆余.中国地壳运动名称资料汇编[J].地质论评,1965,(S1):20-81+83.
[10]汪正江,王剑,江新胜,等.华南扬子地区新元古代地层划分对比研究新进展[J].地质论评,2015,61(1):1-22.
[11]林树基,肖加飞,卢定彪,等.湘黔桂交界区富禄组与富禄间冰期的再划分[J].地质通报,2010,29(Z1):195-204.
[12]齐靓,余文超.黔东南华纪铁丝坳期—大塘坡期古气候的演变:来自CIA的证据[J].地质科技情报,2015,34(6):47-57.
[13]冯连君,储雪蕾.化学蚀变指数(CIA)及其在新元古代碎屑岩中的应用[J].地学前缘,2003(4):539-544.
[14]王自强,尹崇玉.宜昌三斗坪地区南华系化学蚀变指数特征及南华系划分、对比的讨论[J].地质论评,2006,(5):577-585.
[15]王自强,尹崇玉,高林志,等.黔南—桂北地区南华系化学地层特征[J].地球学报,2009,30(4):465-474.
[16]周琦,杜远生,颜佳新,等.贵州松桃大塘坡地区南华纪早期冷泉碳酸盐岩地质地球化学特征[J].地球科学(中国地质大学学报),2007,(6):845-852.
[17]何明华.贵州东部及邻区震旦纪铁丝坳期和南沱期沉积相与环境演化及构造属性探讨[J].贵州地质,1998,(1):26-31+25.
[18]伍皓,江新胜,王剑,汪正江,等.湘西托口地区南华系沉积地层学研究及其地质意义[J].地层学杂志,2015,39(3):300-309.
[19]柏道远.湘西南震旦纪长安期沉积相变与构造环境分析[J].湖南地质,2001,(1):5-8.
[20]林树基,肖加飞,卢定彪等.湘黔桂交界区富禄组与富禄间冰期的再划分[J].地质通报,2010,29(Z1):195-204.
[21]彭学军,刘耀荣,吴能杰等.扬子陆块东南缘南华纪地层对比[J].地层学杂志,2004,(4):354-359.
[22]Heron D P L. The significance of ice-rafted debris in sturtian glacial successions[J]. Sedimentary Geology,2015,322,19-33.
[23]Balgord E A,Yonkee W A,Link P K,et al. Stratigraphic,geochronologic,and geochemical record of the Cryogenian Perry Canyon Formation,northern Utah:Implications for Rodinia rifting and snowball Earth glaciation[J]. Geological Society of America Bulletin,2013,125(9-10):1442-1467.
[24]Kellerhals P,Matter A. Facies analysis of a glaciomarine sequence,the Neoproterozoic Mirbat Sandstone Formation,Sultanate of Oman[J]. Eclogae Geologicae Helvetiae,2003,96(96):49-70.
[25]蔡娟娟,崔晓庄,兰中伍,等.华南扬子陆块成冰纪冰川作用的启动时限及其全球对比[J].古地理学报,2018,20(1):65-86.