地球物理学报  2015, Vol. 58 Issue (12): 4360-4372   PDF    
长江中下游成矿带及邻区三维Moho面结构:来自人工源宽角地震资料的约束
张明辉1,2, 徐涛1,3, 吕庆田4,5, 白志明1, 武澄泷1,2, 武振波1,2, 滕吉文1    
1. 中国科学院地质与地球物理研究所, 岩石圈演化国家重点实验室, 北京 100029;
2. 中国科学院大学, 北京 100049;
3. 中国科学院青藏高原地球科学卓越创新中心, 北京 100101;
4. 中国地质科学院地球物理地球化学勘查研究所, 河北廊坊 065000;
5. 中国地质科学院地球深部探测中心, 北京 100037
摘要: 为深入理解长江中下游地区在中生代成矿的深部动力学过程,对跨越宁芜矿集区地质廊带内的非纵剖面反射/折射地震数据进行动校正和时深转换处理,获得了非纵方向的Moho面深度;联合纵测线和非纵测线上Moho面深度数据,获得了长江中下游成矿带及邻区的三维Moho面深度结构.结果显示宁芜矿集区下方的Moho面整体较浅,约32~34 km,华北块体合肥盆地内Moho面整体较深,约34~35 km.Moho面深度和区域布格重力异常变化趋势对应良好.宁芜矿集区下方Moho面呈上隆特征,支持长江中下游地区成矿模式中增厚岩石圈发生拆沉、软流圈的上隆及底侵作用等动力学过程.Moho面平行于成矿带走向的变化趋势,预示长江中下游成矿带地壳和上地幔在板块边界发生了NE-SW向的切向流动变形.郯庐断裂带两侧,Moho面深度变化较大,表明地表近陡立的郯庐断裂为深大断裂,深部可能切穿Moho面并延伸至上地幔.
关键词: 长江中下游成矿带     三维地壳结构     宽角地震资料     纵剖面     非纵剖面    
3D Moho depth beneath the middle-lower Yangtze metallogenic belt and its surrounding areas: Insight from the wide angle seismic data
ZHANG Ming-Hui1,2, XU Tao1,3, LV Qing-Tian4,5, BAI Zhi-Ming1, WU Cheng-Long1,2, WU Zhen-Bo1,2, TENG Ji-Wen1    
1. State key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China;
2. University of Chinese Academy of Sciences, Beijing 100049, China;
3. CAS Center for Excellence in Tibetan Plateau Earth Sciences, Beijing 100101, China;
4. Institute of Geophysical and Geochemical Exploration, Chinese Academy of Geological Sciences, Hebei province, Langfang 065000, China;
5. China Deep Exploration Center-SinoProbe Center, Chinese Academy of Geological Sciences, Beijing 100037, China
Abstract: To understand the formation and the tectonic processes of the Mesozoic Middle Lower Yangtze metallogenic belt(MLYMB), the SinoProbe-03-02 program conducted a 450 km long in-line controlled-source seismic experiment with a 400 km long off-line data collection across the Ning-wu ore-district. We deal with the off-line seismic data using normal moveout correction and time-depth conversion in order to obtain the off-line Moho depth. Using the Moho depth derived both from in-line and off-line seismic data, we construct a Moho depth map in the Middle-Lower Yangtze metallogenic belt and its surrounding areas. The results show that the Moho depth is about 32~34 km beneath the Ning-Wu ore-district, shallower than that beneath the Hefei basin in North China which is about 34~35 km. The variation tendency of Moho depth coincides with the Bouguer gravity anomaly well. The uplifting characteristic of Moho depth in Ning-Wu ore-district supports the model of lithosphere delamination, asthenosphere welling, and mantle-derived magmatic underplating during the formation of MLYMB. The variation of Moho beneath metallogenic belt parallels the strike of the MLYMB. It supports the tangential flow deformation in NE-SW direction in the plate boundary of the crust and mantle. On both sides of Tanlu fault zone, the depth of the Moho changes greatly, which indicates that the Tanlu fault may extend to the mantle.
Key words: Middle-lower Yangtze metallogenic belt     Moho depth     Wide angle seismic data     In-line     Off-line    
 1 引言

长江中下游成矿带位于中国东部扬子块体的北 缘,地处华北与扬子块体的拼合地带(Pan and Dong,1999; Mao et al.,2006).该成矿带形成于燕山期,在长期的岩浆作用、构造活动及成矿作用下,形成了丰富的Cu、Fe、Au等金属矿床组合,多金属矿床有 200多个,由七个矿集区组成,自东向西分别为宁镇、宁芜、铜陵、庐枞、安庆—贵池、九瑞、鄂东南矿集区(常印佛等,1991; Pan and Dong,1999; Mao et al.,2006).

针对该成矿带为什么会在如此狭窄的区域内发生如此大规模的金属聚集、深部的岩浆活动机制和动力学过程等焦点问题,在国土资源部“长江中下游成矿带及典型矿集区深部结构探测研究专项”(吕庆田等,20112014; Dong et al.,2013;et al.,2013a2013b2015)的支持下,启动了NW-SE向横穿成矿带的廊带式多学科深部探测工作,对区域构造模式和成岩、成矿的深部动力学过程提供了新的约束.宽频带地震资料的接收函数结果显示成矿带对应软流圈上隆带(史大年等,2012; Shi et al.,2013)、上地幔各向异性特征显示沿成矿带方向(NE-SW)存在软流圈物质的流动变形(Shi et al.,2013)、远震层析成像的速度结果证实了岩石圈的拆沉(Jiang et al.,2013; 江国明等,2014);深地震反射结果显示陆内俯冲或是岩石圈拆沉前增厚的主要机制(et al.,2013b; 梁峰等,2014);人工源宽角反射/折射地震结果显示宁芜矿集区的下地壳为低速异常,可能与高速下地壳在燕山期的拆沉作用有关(徐涛等,2014).通过多学科的系列工作及相 关成果(滕吉文等,1985; 王强等,2001; 张旗等,20012002; Dong et al.,2004; 吕庆田等,2004; Wang et al.,20042006; Zhang et al.,20052007; Bai and Wang,2006; Bai et al.,2007; 侯增谦等,2007; Ling et al.,2009; 杨振威等,2012; Shi et al.,2013; et al.,2013b; 梁锋等,2014; 张永谦等,2014; 强建科等,2014),吕庆田等(2014)总结提出燕山期的陆内俯冲、岩石圈拆沉、熔融和底侵作用,是造成长江中下游晚侏罗和早白垩大规模成岩和成矿作用的主导机制.

人工源深地震测深资料是获取地壳和上地幔顶部速度结构信息的重要途径.为了解Moho面及地 壳结构沿成矿带方向(NE-SW)的变化,在实施450 km 长的“利辛—宜兴”人工源宽角反射/折射纵剖面过程中(徐涛等,2014),同时开展了400 km长非纵剖面的地震数据采集工作(图 1),期望用最小的代价,获得成矿带三维深部结构,并探讨其对成矿带深部动力学过程的约束.

图 1 长江中下游成矿带人工源深地震测深观测系统
红色五角星为人工源炮点;蓝色三角形为纵测线接收器;黄色三角形为非纵测线接收器; 紫色菱形为长江中下游矿集区;穿过纵剖面的黑色方框为宁芜矿集区;TLF,郯庐断裂; SDF,寿县—定远断裂; CHF,滁河断裂; MSF,茅山东侧断裂; JNF,江南断裂; YCF,阳新—常州断裂; XGF,襄攀—广济断裂; XLF,信阳—六安断裂.
Fig. 1 Geophysical surveys in the Middle-Lower Yangtze metallogenic belt
Red stars denote active seismic sources; Blue triangles denote the receivers of in-line profile; Yellow triangles denote the receivers of off-line profile; Purple diamonds denote metallogenic districts. Black box crossing the in-line profile denotes Ning-Wu ore-district. TLF,Tanlu fault; SDF,Shouxian-Dingyuan Fault; CHF,Chuhe Fault; MSF,Maoshan Fault; JNF,Jiangnan Fault; YCF,Yangxin-Changzhou Fault; XGF,Xiangpan-Guangji Fault; XLF,Xinyang-Liuan Fault.
2 构造背景

长江中下游地区位于下扬子板块的北缘,是大别—苏鲁超高压变质带的前陆,北部以北西向的襄樊—广济断裂和北东向的郯-庐断裂带为界,南部以江南断裂为界与江南古陆为邻,总体上呈南西狭窄、北东宽阔的“V”字型地带(图 1).扬子块体呈现“一盖多底”的地壳结构特征,盖层的基底由震旦系-三叠系海相碎屑岩及海陆交互相沉积岩石、侏罗系-白垩系陆相碎屑岩和火山岩组成;而长江中下游地区的陆壳基底由晚太古-早元古代和中元古代变质岩系组成,呈“双层结构”(常印佛等,19911996).成矿带内出露的地层有零星分布的前震旦纪变质基底和震旦纪碎屑岩、白云岩和硅质岩,广泛发育有寒武纪至早三叠世的碎屑岩和碳酸盐岩及侏罗纪-白垩纪陆相火山岩夹碎屑岩(常印佛等,1991).

长江中下游地区的岩浆作用和成矿作用主要发生于145~120 Ma(Chen et al.,2001; Sun et al.,2003; Mao et al.,2006; 周涛发等,20082012),是中国东部中生代大规模成岩成矿作用的典型代表.其形成的岩浆岩主要有高碱钙碱性系列、橄榄安粗岩系列和碱性(A型)花岗岩系列(周涛发等,20082012).周涛发等(20082012)总结了四种长江中下游成矿带中生代铜铁金多金属矿床成矿系统的基本类型:与高钾钙碱性岩系有关的矽卡岩-斑岩型成矿系统;与橄榄安粗岩系有关的“玢岩铁矿型”成矿系统;与A型花岗岩有关的氧化物-铜-金(铀)矿床成矿系统及与岩浆活动不明显的Ti,Au,Sb,Pb,Zn低温成矿系统.该区的岩浆活动在时空上表现出明显的分区性,主要分布在断隆区(如铜陵地区等)、断凹区(如庐纵盆地、宁芜盆地等)和隆凹过渡区(如鄂东南地区等)等不同的构造单元内,铜陵矿集区等地主要为高钾钙碱性岩石组合,宁芜和庐枞矿集区为高纳钙碱性侵入岩、橄榄安粗岩系火山岩组合,宁芜地区为碱性火山岩组合,以鄂东南为代表的隆凹过渡区以钙碱性-碱钙性岩浆岩为主等(常印佛等,1991; 周涛发等,2008),而其成矿具有较明显的阶段性和分带性(周涛发等,2008).自西向东,该区的成矿时代有变小的趋势(常印佛等,1991; 周涛发等,2008).长江中下游地区不同矿集区的成矿时代大致分为145~137 Ma、135~127 Ma、 126~123 Ma等三个阶段,其中145~137 Ma的岩浆活动主要发生在断隆区,是铜金矿化的主要时期,135~127 Ma的岩浆活动主要发生在断凹区,是铁矿化的主要时期(常印佛等,1991; 周涛发等,20082012).

3 地震资料采集与处理 3.1 地震数据采集

广角反射/折射深部地震探测剖面约850 km,其中纵剖面长450 km,非纵剖面长400 km; 沿纵探测剖面设计6个人工源爆破激发点(总数达 13.2 吨TNT),采用多深井组合激发方式,炮点间距 60~90 km; 地震观测采用三分量数字地震仪,共450台(纵测线250台,非纵测线200台),道间距为1.5~2.0 km,记录来自地壳上地幔顶部不同深度范围、不同属性的深层地震波信息.

纵测线(图 1)为NW-SE走向,起始于宜兴附近,然后跨过江南断裂(JNF)、茅山东侧断裂(MSF)、滁河断裂(CHF)和郯庐断裂(TLF),终止于利辛附近.自东向西依次穿过的构造单元有扬子块体,长江中下游成矿带内的宁芜盆地、滁河盆地,然后进入华北块体.非纵测线(图 1)呈NE-SW走向,与纵测线近乎垂直,长约400 km,穿过滁河断裂,与纵测线的交点在Sp03炮附近.

3.2 非纵折合走时剖面

纵剖面折合走时记录的装配过程中,以炮点到每个接收器的距离为偏移距,在炮点的两侧分别定义为正或负方向.而非纵剖面的装配需要以纵剖面和非纵剖面的交点(图 1中Sp03炮点附近)作为坐标零点,该点到接收器的距离作为横坐标,接收器到该点两侧定义为正或负方向(本文中定义NE为正方向,SW为负方向).6炮计算得到的剖面如图 2所示.由于计算偏移距的参考点一致,因此6炮折合走时剖面的接收器的横坐标(桩号)都一样,为-200~210 km左右.需要注意的是,在图 2(a—f)纵坐标折合走时T-X/6.0的计算中,X为炮点到接收器的距离(即偏移距),而非图中的横坐标,这是非纵剖面和纵剖面成图的差异所在.

图 2 长江中下游成矿带折合走时非纵观测记录剖面
(a)—(f)分别表示六炮(Sp01-06)激发的非纵观测记录剖面,图中纵坐标折合走时中的X为炮点到接收器的距离,横坐标的距离为非纵测线和纵测线交叉点到各接收器的距离.
Fig. 2 The off-line profiles of Shots Sp01-06(a—f)in the Middle-Lower Yangtze metallogenic belt
(a)—(f)denote six off-line profiles; X in y-coordinate denotes the distance between a shot and a receiver. The x-coodinate denotes the distance between the cross point and a receiver.
3.3 非纵剖面数据动校正和时深转换

非纵剖面数据处理包括两个步骤(Cerveny,2001; 徐涛等,2004; Xu et al.,200620102014): 动校正和时深转换处理.

(1)动校正和时深转换

非纵剖面地震记录动校正过程与纵剖面记录处理过程类似,都需要基于已有平均地壳速度模型将观测反射到时数据校正为反射点的零偏移距自激自收到时数据.假定地壳平均速度为v,实际观测到时为tobs,接收器炮检距为x,则动校正后反射点的零偏移距自激自收到时t0表示为:

时深转换的反射点深度为:
值得注意的是,接收器R得到的Moho面深度最终要归位到炮点S和接收器R的中点M处(图 3).

图 3 非纵剖面数据动校正和时深转换示意图 Fig. 3 Illustration of moveout and time-depth conversion of off-line profile

上述处理过程中,选择合适的地壳平均速度比较关键.我们利用“利辛—宜兴”剖面的二维速度结构(徐涛等,2014)得到了该剖面的地壳平均速度结构,具体计算过程如下.

首先,将剖面某点下方的地壳介质在深度上以Δh(如1 km)为间隔划分为n个单元,每个单元的速度为vi(i=1,2,…,n).则每个单元的走时可近似表示为Δti= $\frac{\Delta h}{{{v}_{i}}}$.相应地,该点下方的地壳平均速度v

可以看出,某点下方的地壳平均速度((3)式)是该点下方水平薄层平均慢度的倒数.根据上述过程,便可得到纵剖面的地壳平均速度结构(图 4).

图 4 利辛—宜兴纵剖面平均速度
CHF,滁河断裂; MSF,茅山东侧断裂; JNF,江南断裂.
Fig. 4 Average velocity along the Lixin-Yixing in-line profile
CHF,Chuhe Fault; MSF,Maoshan Fault; JNF,Jiangnan Fault.

由于纵剖面基本上和主要的构造延伸及断裂走向垂直,因此动校正过程中,将三维地壳速度结构近似为垂直于纵剖面的2.5维速度结构,即速度结构沿垂直于纵剖面方向进行均匀延拓.这样的近似处理基本上符合三维速度结构真实情况.

非纵剖面某接收点R(图 3)的动校正速度,用纵剖面上的投影点O点与炮点S点之间的速度曲线(图 4),求取OS间的平均值来近似.

(2)非纵剖面Moho面深度

经过动校正和时深转换,获得6炮的深度剖面(图 5),再在深度剖面上进行人工拾取Moho面深度.可以看出,Sp02-05炮非纵剖面震相信噪比高,测线端点附近的炮点Sp01和Sp06炮信噪比稍低.

图 5 长江中下游成矿带非纵剖面深度剖面
红色十字为拾取的Moho面深度;(a)—(f),Sp01-06炮.
Fig. 5 (a)—(f),Results of NMO correction of off-line profile and picked Moho depths
Red crosses denote picked Moho depths;(a)—(f),Shot Sp01-06
4 长江中下游成矿带及邻区Moho深度 4.1 Moho面深度

图 3所示,每个接收器R拾取的Moho面深度要归位到炮点和接收器的中点M处.将图 5中6条非纵剖面拾取的Moho面深度归位到相应的位置,并联合跨越宁芜矿集区的长450 km的纵剖面的Moho面深度结果(徐涛等,2014),通过插值及一定程度的平滑获得宁芜矿集区及其邻域的Moho面深度结构(图 6).图中只显示了信噪比较高的Moho面深度区域.

图 6 联合纵剖面和非纵剖面获得的Moho面深度 Fig. 6 Moho depth derived from the in-line and off-line seismic data

Moho面深度结构显示,扬子块体内部宁芜矿集区及华北块体合肥盆地内部,Moho面深度呈现较大的非均匀性.在郯庐断裂的两侧,Moho面深度呈现一定的差异.长江中下游成矿带中的宁芜矿集区内的Moho面存在隆起,深度约32~33 km,华北块体中的合肥盆地内Moho面深度约34~35 km.炮点Sp01和Sp06 附近Moho面深度均比较浅,由于受端点两侧射线覆盖的限制,误差稍大.

4.2 结果比较

图 7为卫星布格重力异常分布图.图中的布格重力异常值分布只选取了和Moho面深度范围一致的区域.从图中可以看出,研究区内的重力异常值范围为-30~20 mGal,且和Moho面深度有很好的相关性,如郯庐断裂东侧地区,布格异常值普遍较高,变化范围约为-10~20 mGal;郯庐断裂西侧,异常值相对东侧较低,变化范围约-30~5 mGal;宁芜 矿集区下方为正异常,异常值范围大约为0~10 mGal. 通常情况下,正的布格重力异常表示地壳物质亏损、Moho面较浅等基本特征,正值越大,Moho面深度越浅,其异常结果和Moho面深度有很好的相关性.比较Moho面深度和布格重力异常结果,可以看出整体特征吻合较好,差异较大的区域主要集中在Sp01和Sp06炮等边缘地区.由于这两炮的地震剖 面偏移距较大,信噪比较低,且射线覆盖密度非常 低,因此误差相对较大,与该区域的重力异常值特征吻合性差.

图 7 Moho面深度区域对应的布格重力异常分布 Fig. 7 Bouguer gravity anomaly in the study area

严加永等(2011)利用区域重力异常反演得到的Moho面深度显示,宁芜火山岩盆地下方的Moho面存在隆起.宽频资料的远震接收函数结果显示宁芜矿集区下方Moho面为隆起特征,郯庐断裂带两侧的Moho面深度存在差异,且西侧较东侧的Moho面要深(Shi et al.,2013).反射地震结果也显示Moho面在宁芜火山岩盆地下方较浅,在合肥盆地下方较深(吕庆田等,2014).这些结果都与我们的结果特征相一致,显示了结果的可靠性.

5 讨论

根据宽频地震、反射地震、折射地震、大地电磁等多学科地球物理深部探测结果,吕庆田等(2014)提出了长江中下游成矿带成矿地球动力学模型.模型认为发生在研究区的印支运动和燕山运动是两次独立的造山过程.印支运动在长江中下游地区并没有产生强烈的地壳变形(Zhu et al.,2009),但因古太平洋板块NW向低角度俯冲远程效应引起的燕山期造山运动(Chen et al.,2006),是决定研究区构造格局、并产生强烈岩浆活动的根源.燕山运动是一期快速造山过程,不仅造成长江中下游成矿带强烈的地壳变形,同时还发生了陆内俯冲或叠瓦,使岩石圈增厚.增厚的岩石圈在随后的区域应力减弱和自身不稳定性的双重因素作用下,发生拆沉和软流圈的上隆.拆沉岩石圈的熔融(包含下地壳的熔融)、底侵和软流圈上隆的热流作用,导致了长江中下游地区大规模的岩浆作用和成矿作用.

增厚岩石圈发生拆沉、软流圈的上隆及底侵作 用等动力学过程,可能会导致宁芜矿集区下方Moho面呈上隆特征,这已经被二维的宽频地震接收函数结果所证实(史大年等,2012; Shi et al.,2013).纵测线的宽角折射地震结果显示矿集区下方Moho呈现整体上隆,局部凹陷的特征(徐涛等,2014).三维Moho面深度特征同样显示,宁芜矿集区下方Moho面整体偏浅,为32~34 km左右(图 6).布格重力异常结果显示,宁芜矿集区下方整体为正异常(图 7),约为0~10 mGal,通常情况下对应Moho面隆起特征.区域重力异常反演及反射地震结果等也显示了这样的特征.

从Moho面的深度结构可以看出,在郯庐断裂东侧,Moho深度的变化基本上平行于成矿带的NE-SW走向(图 6);布格重力异常结果(图 7)呈现同样的清晰特征.不仅如此,主要反映上地幔流变特征的SKS分裂特征也显示,成矿带附近快波偏振方向呈现NE-SW向(Shi et al.,2013).上述结果支持了在总体NW-SE挤压下,长江中下游成矿带地壳和上地幔由于受到华北克拉通的阻挡,在板块边界发生了切向(垂直挤压应力方向)流动变形,而上地壳仍然发生NW-SE向的褶皱或冲断变形(吕庆田等,2014).

郯庐断裂带在中国东部绵延数千公里,中生代以来,上地壳的走滑达500余公里(Zhu et al.,2009).早白垩世岩浆岩的岩石学和地球化学研究,反映它们既有壳源的信息,又有幔源的信息,指示走滑期的郯庐断裂带可能已切入了壳幔边界(牛漫兰等,2002).新生代中国东部最大规模的玄武岩喷发带的出现,反映郯庐断裂带此时已切入了上地幔,构成了幔源玄武岩喷发的通道(朱光等,2004a2004b).垂直反射地震剖面显示郯庐断裂下方 Moho存在一定的错断(吕庆田等,2014; et al.,2015). 宽频地震剖面接收函数结果(Shi et al.,2013)和宽角反射/折射地震剖面(徐涛等,2014)均显示Moho面在郯庐断裂下方深度最深,达36公里左右.宽角折射地震剖面的二维速度结构还显示,在整个地壳内郯庐断裂东西两侧的速度结构相差较大(徐涛等,2014).不仅如此,研究区内三维Moho面深度(图 6)以及布格重力异常结果(图 7)同样显示了郯庐断裂两侧的Moho面深度变化较大.因此,我们推测,地表近陡立的郯庐断裂,深部可能切穿到了Moho面深度.

6 结论

(1)联合纵测线和非纵测线宽角反射/折射地震数据,获得了长江中下游成矿带及邻区的Moho面结构.结果显示,宁芜矿集区下方Moho面呈上隆特征,支持长江中下游地区成矿模式中增厚岩石圈发生拆沉、软流圈的上隆及底侵作用等动力学过程.Moho面平行于成矿带走向的变化趋势,显示长江中下游成矿带地壳和上地幔在板块边界发生了NE-SW向的流动变形.郯庐断裂带两侧的Moho面深度变化较大,这表明地表近陡立的郯庐断裂,深部可能切穿到Moho面深度.我们期望通过联合纵剖面和非纵剖面的观测资料,利用最小的代价,实现长江中下游成矿带及邻区的三维地壳结构探测.

(2)本文获得的Moho面的深度结构信息,为进一步的三维速度结构反演提供了初始的Moho面深度约束,是得到精确三维速度结构成像的重要条件.

致谢 谨以此文纪念中国科学院地质与地球物理研究所张忠杰研究员(1964—2013).感谢中国地震局物探中心及中国科学院地质与地球物理研究所参加野外地震数据采集工作的所有人员;感谢王夫运研究员、史大年研究员、田小波研究员、刘宝峰副研究员的指导和帮助.

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