Sedimentary record of environmental evolution since ca 2000 cal yr B P ago in Qehan Lake, Inner Mongolia
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摘要:
以内蒙古东部查干淖尔湖西湖深97cm的浅井剖面为对象, 根据取得的7个AMS14C测年数据建立其2070cal a BP以来的年代序列, 结合孢粉组合特征与粒度组成的综合分析, 重建该地区2070cal a BP以来气候环境变化过程。研究结果表明, 查干淖尔湖2070cal a BP以来气候环境变化具体可以分为3个阶段:2070~1150cal a BP, 孢粉总浓度较高, 以蒿属、藜科为主, 沉积物各粒级组分变幅较小且以粉砂为主, 水动力条件较弱, 湖水位较高, 气候温凉偏湿; 1150~825cal a BP, 孢粉总浓度显著降低, 耐旱的麻黄属达到最高值, 沉积物粗颗粒含量显著增加, 水动力条件增强, 湖水位降低, 气候冷干, 其中940~870cal a BP期间气候极端干旱; 825cal a BP以来, 总体温暖偏湿, 有冷干事件发生。太阳活动可能是导致查干淖尔湖过去2000a气候变化的主要驱动力。
Abstract:A 97cm long lacustrine section from Qehan Lake, situated in eastern Inner Mongolia, was used to reestablish the environ-ment and climate changes since the last 2070cal a BP. The chronological framework was built on seven AMS14C ages. On the basis of pollen-spore characteristics and grain size distribution, three environmental stages can be recognized. From 2070~1150cal a BP, this interval was featured by high total pollen concentration, with the dominance of Artemisia and Chenopodiaceae; lacustrine sediments were mainly composed of silt and each fraction presented quite low amplitudes of increases, indicating the weak hydrological condi-tions and high lake level; this period was characterized by a warm, cool and slightly humid climate. During the period of 1150~825cal a BP, the total pollen concentration significantly decreased and the pollen percentages of xerophyte, especially Ephedra, reached the maximum; the coarse particle content showed obviously increase, sugge sting strong hydrodynamic conditions and low lake level; so in this period, the climate was cold and dry, especially from 940cal a BP to 870cal a BP. Since 825cal a BP, the climate mainly tend-ed to become warm and slightly humid with the occurrence of cold and dry oscillations. Solar activities might have been the domi-nant force that drove the climate changes in Qehan Lake area since 2000 years ago.
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Keywords:
- 2000a /
- pollen /
- grain size /
- climate change /
- Qehan Lake /
- Inner Mongolia
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蒙阴金伯利岩是大部分侵入到晚太古代变质变形的侵入岩，部分侵入早古生代沉积盖层，蒙阴金伯利岩侵位最高层位为奥陶纪马家沟群土峪组[1-4]。朱源等①对蒙阴地区金伯利岩采用Sm-Nd法测得年龄值在450~480Ma之间；1988年有学者用采自胜利Ⅰ号岩管的钙钛矿进行U-Pb法高灵敏度离子探针分析测定的年龄值为457±7Ma[5]；李秋立等[6-7]采用钙钛矿、斜锆石进行二次离子质谱分析，获得年龄数据为478.9~480.6Ma；王瑛等[8]用采自胜利Ⅰ号岩管的金云母、蛇纹石和石榴子石及全岩采用Rb-Sr法确定蒙阴金伯利岩岩浆侵位年龄为560±10Ma。有学者根据常马矿带金伯利岩与辉绿岩脉（全岩KKr法，113Ma）的切割关系认为，金伯利岩体侵入时间应为下白垩世[9]；杨斌等[10]根据金伯利岩带受构造控制，认为蒙阴金伯利岩带形成于中生代后期。
对于蒙阴金伯利岩带的形成时代，许多学者提出了不同的意见，通过不同同位素测年方法测得蒙阴金伯利岩侵位年龄最大为15.84亿年，最小为0.77亿年，测年数据差别较大，且与通过地质、控矿特征得出的侵位年龄差别也较大，到底是测年数据的误差所致，还是确有金伯利岩形成于中生代，从而显示金伯利岩是一个多期喷发而出现的年龄差异，现仍没有得出确切结论[11]。
坡里岩带岩浆活动可分为2期，早期为强碳酸盐化斑状富金云母金伯利岩，晚期为斑状金伯利岩（强烈蛇纹石化），岩带以早期岩性为主，晚期岩性较少。K24号岩脉岩性为强碳酸盐化斑状富金云母金伯利岩，为早期岩浆活动的产物，具有较好的代表性。在金伯利岩直接测年数据不能确定其形成时代的情况下，本文以蒙阴地区坡里岩带K24号脉侵入的辉绿岩为测年对象，通过测得辉绿岩侵位时代的年龄数据，获得坡里金伯利岩带的形成时代上限，结合蒙阴盆地白垩纪—古近纪官庄群底砾岩中含有已知岩带供给的金刚石及含铬镁铝榴石，确定其形成时代下限，从而确定坡里金伯利岩的形成时代。
1. 矿区地质概况
矿区大地构造位置处于华北板块（Ⅰ）、鲁西隆起区（Ⅱ）、鲁中隆起（Ⅲ）、马牧池-沂源断隆（Ⅳ）、马牧池凸起（Ⅴ）的中部[12]。
矿区内出露的地层主要为寒武纪馒头组、张夏组及第四系。矿区内构造以断裂为主，主要为北北西向、北东向断裂。坡里金伯利岩带严格受北东向断裂控制，金伯利岩多赋存于北东向断裂中，构成明显的赋矿断裂。矿区内岩浆岩主要出露有新太古代二长花岗岩、中元古代牛岚单元辉绿岩和古生代常马庄单元金伯利岩。
2. 坡里金伯利岩带特征
坡里岩带位于蒙阴县城东北约30km的岱崮镇野店—坡里―金星头一带，由25组岩脉组成，未发现有岩管，总走向北东35°~40°，长约18km，宽约0.6km。岩脉走向基本与岩带一致，多呈断续或侧列式排列（图 1）。岩脉明显受构造控制，主要是北东35°~45°的压扭性断裂，在成矿前为张扭性，成矿时为压扭性。金伯利岩脉规模也随断裂规模大小而变化，当侵位在较大的张扭性断裂时，岩体相应形成较宽而长的岩脉，宽可达1~2m，长数百米；若侵位在张扭性节理时，岩体则为细小岩脉，宽几厘米至十几厘米。岩性主要为斑状富金云母金伯利岩（碳酸盐化）、斑状金伯利岩（蛇纹石化强烈）。坡里金伯利岩带中只有10条岩脉（K2、K4、K5、K8、K10、K11、K12、K13、K17、K23）含有金刚石，且均达不到工业品位，其余岩脉不含金刚石，品位最大的为K23号岩脉，平均品位为4.86mg/m3。
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图 1 坡里金伯利岩带分布[13]βμ—牛岚单元辉绿岩？；δμ—中生代闪长玢岩；Ar3—新太古代花岗岩；Q—第四系；∈2—中寒武统；∈1—下寒武统Figure 1. Distribution of kimberlite belt in Poli3. 辉绿岩与金伯利岩的关系
蒙阴地区辉绿岩走向大部分为北东向，与金伯利岩带方向总体一致，金伯利岩与辉绿岩均受牛岚构造体系控制[14]，少数为北西向。与金伯利岩有穿切关系的仅为常马矿带红旗1号岩脉切穿了辉绿岩脉[15]、坡里岩带K24号岩脉侵入辉绿岩脉（图 2）。坡里岩带K24号岩脉走向与辉绿岩脉走向完全一致，为350°。新鲜辉绿岩呈暗绿色、灰绿色，风化后呈深褐黄色，辉绿结构，具球状构造。近矿辉绿岩受金伯利岩的烘烤作用发生褪色现象，呈黄褐色，褪色带20~50cm，同时辉石发生重结晶现象，结晶比原岩粗大，呈中粒。从穿切关系看，金伯利岩形成时代晚于其所切穿或侵入的辉绿岩形成时代。本区辉绿岩划分为2期，一期为中生代燕山期辉绿岩，因在其中可见中生代苍山序列花岗斑岩捕虏体，辉绿岩全岩K-Ar法测得的年龄值为100.8~116.4Ma[16]；另一期为中元古代牛岚单元辉绿岩。K24号岩脉侵入的为中生代还是中元古代的辉绿岩？若为中生代燕山期辉绿岩，则金伯利岩带形成时代应为燕山期或更晚。
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图 2 K24号岩脉与辉绿岩切穿关系∈2m—中寒武统馒头组；Ar3—新太古代二长花岗岩；βμ—牛岚单元辉绿岩？；Kb—金伯利岩Figure 2. Penetrating relationship of K24 dike and diabase4. 锆石年龄测定结果
重砂样品取自坡里K24号岩脉赋存的辉绿岩脉，该处辉绿岩岩脉与金伯利岩脉有明显的穿切关系。本次采用刻槽法进行取样，样品为半风化辉绿岩。辉绿岩重砂样品在山东省第七地质矿产勘查院采用常规方法进行粉碎，并用重选和电磁选方法进行分选，处理完的样品由河北省区域地质矿产调查所实验室在双目镜下进行挑选。本次在30kg重砂样品中人工选出14粒锆石，分离出的锆石颗粒细小，粒径小于0.2mm，白色，透明-半透明，大部分呈柱状或针状。锆石阴极发光显微照相由中国冶金地质总局山东测试中心的JXA8230电子探针显微分析仪的阴极发光系统（CL）图像分析，阴极发光图像如图 3所示。多数锆石具较宽的振荡结晶环带，晶形较好，颗粒较完整，为典型的岩浆成因锆石[17]；8、10、12号锆石不具振荡环带，显示无分带、弱分带、面形分带等特征，暗示锆石经过后期变质作用的改造[18]。
锆石的U-Pb年代学测试工作在中国冶金地质总局山东测试中心电感耦合等离子体质谱仪（LA-ICP-MS）上完成，根据锆石样品的透射光、反射光和阴极发光图像，离子探针测点选择颗粒表面光洁、无裂痕的位置。LA-ICP-MS激光剥蚀系统为美国Conherent公司生产的GeoLasPro 193nm ArF准分子系统，ICP-MS型号为ThermoFisher公司生产的iCAPQ。激光剥蚀采样过程以氦气作为载气，氮气为辅助气。测试条件见表 1。未知样品测试时采样方式为单点剥蚀、跳峰采集；单点采集时间模式为：20s气体空白+55s样品剥蚀+25s冲洗；每7个未知样品点插入1组标样（锆石标样91500/PL/GJ-1和成分标样NIST610）。采用GJ-1标准锆石（TIMS获得谐和年龄为600±5Ma[19]）为外标进行基体校正；成分标样采用NIST SRM 610，其中Zr为内标元素。同位素比值采用标准锆石91500进行校正。样品的同位素比值及元素含量计算采用ICPMSDATACAL数据处理程序，普通铅校正采用Anderson[20]提出的ComPbCorr#3.17校正程序，U-Pb谐和图、年龄分布频率图绘制和年龄加权平均值计算采用Isoplot/ Ex_ver3[21]程序完成。分析结果见图 4和表 2。
表 1 测试条件Table 1. Summary of test conditions技术指标 参数 激光电压/kV 23~29 激光能量/J·cm2) 10.2 载气流速(ml·min-1) 745 剥蚀次数/次 500 激光频率/Hz 9 束斑直径/μm 30/20 激光能量透过率/% 75 截取透镜(V) 140 雾化器(l/min) 0.760 U(cps) > 3×105 Th/U ≈1.0 ![]()
图 4 辉绿岩U-Pb锆石年龄谐和图（a）和直方图（b）Figure 4. U-Pb zircon age concordia diagram (a) and age histogram (b) of diabase表 2 蒙阴坡里辉绿岩锆石U-Th-Pb测年分析结果Table 2. The results of the zircon U-Th-Pb dating analysis of the diabase in Poli of Mengyin样号 Pb Th U 207Pb/206Pb 207Pb/235U 206Pb/238U 208Pb/232Th 207Pb/206Pb 207Pb/235U 206Pb/238U 208Pb/232Th 谐和度 10-6 10-6 10-6 比值 1 σ 比值 1 σ 比值 1 σ 比值 1 σ 年龄/Ma 1 σ 年龄/Ma 1 σ 年龄/Ma 1 σ 年龄/Ma 1 σ 1 76.079 38.057 83.811 0.226 0.012 16.467 0.728 0.519 0.009 0.579 0.0393 3021 81 2904 42 2696 39 9238 503 92% 2 53.504 28.869 90.2661 0.163 0.004 10.896 0.282 0.484 0.0078 0.179 0.0079 2483 42 2514 24 2547 34 3332 136 98% 3 194.438 194.369 387.736 0.168 0.004 9.221 0.327 0.394 0.0114 0.122 0.0044 2543 37 2360 33 2142 53 2332 79 90% 4 268.238 309.890 531.286 0.163 0.017 8.227 0.408 0.363 0.0089 0.267 0.0429 2487 176 2256 45 1998 42 4791 685 87% 5 204.267 193.460 540.218 0.160 0.003 7.109 0.161 0.320 0.0058 0.108 0.0033 2461 35 2125 20 1791 28 2072 60 82% 6 167.254 183.344 517.917 0.174 0.003 6.323 0.135 0.262 0.0032 0.079 0.0022 2594 32 2022 19 1502 16 1536 41 70% 7 222.876 591.128 653.885 0.147 0.003 5.482 0.125 0.268 0.0034 0.058 0.0016 2314 35 1898 20 1532 17 1118 30 78% 8 442.952 1002.751 960.304 0.344 0.015 10.632 0.396 0.225 0.0047 0.189 0.0070 3670 69 2492 35 1308 25 3496 119 37% 10 74.758 146.663 280.781 0.091 0.002 2.892 0.081 0.231 0.0042 0.067 0.0020 1439 46 1380 21 1337 22 1303 39 96% 11 79.646 79.047 112.431 0.136 0.008 9.196 0.250 0.498 0.0072 0.212 0.0131 2176 98 2358 25 2604 31 3888 219 90% 12 363.162 154.543 279.508 0.377 0.009 32.198 0.927 0.614 0.0099 0.849 0.0286 3820 37 3556 28 3087 39 12420 312 85% 14 237.477 1733.793 2191.428 0.154 0.005 1.780 0.066 0.083 0.0022 0.028 0.0016 2395 52 1038 24 515 13 549 27 32% 9 1.853 68.147 81.843 0.058 0.011 0.131 0.019 0.018 0.0009 0.005 0.0005 522 411 125 18 117 6 106 9 92% 13 7.779 225.29 325.240 0.051 0.003 0.129 0.007 0.019 0.0004 0.007 0.0003 256 142 123 6 121 3 132 6 98% 由表 2可知，8号、14号样品谐和度较低，本次分析不予采用；6号、7号样品谐和度低于80%，207Pb/ 206Pb＞207Pb/235U＞206Pb/238U，其结果仍可采用。1~7、10~12号样品206Pb/238U年龄大于1000Ma，因此选择207Pb/206Pb年龄值（分析过程中Pb同位素之间分馏小），其样品中Pb丢失，导致在谐和曲线图上偏离谐和曲线。9号、13号样品206Pb/238U年龄小于1000Ma，235U衰变呈207Pb的含量低，207Pb/206Pb值远低于其他样品，因此年龄值选择206Pb/238U年龄值。
由图 4可知，可采用的12件样品锆石年龄值很分散，2件样品位于117~121Ma，1件样品为1439Ma，7件样品位于2176~2594Ma，2件样品大于3000Ma。
基性火成岩作为锆石U-Pb定年已经得到较广泛的研究，但基性岩中的锆石成因仍较复杂。大多数学者认为，辉绿岩岩浆属于贫硅硅酸盐体系，大多数锆石捕获自岩浆上侵过程中的围岩，只有少数锆石是基性岩浆原生结晶的[22]。样品中年龄值大于2600Ma的锆石，是辉绿岩侵位过程中捕虏深部太古宙老变质岩的反映。测定年龄大于1439Ma的锆石为辉绿岩捕虏的元古宙侵入岩中的锆石。117~ 121Ma代表了辉绿岩的侵位年龄，形成于中生代燕山晚期。
5. 讨论
关于蒙阴金伯利岩的侵位时代，目前存在较大的争议，主要为古生代奥陶纪还是中生代白垩纪。就坡里金伯利岩带而言，本次从金伯利岩的直接测年数据及地质事实进行分析。
5.1 金伯利岩直接测年数据
由表 3可以看出，坡里岩带采用全岩K-Ar法获得的测年数据在233.8~379Ma之间，测年最大差值为145.2Ma，差别较大，因金伯利岩是多源混杂岩（包括捕虏晶、斑晶、基质矿物和蚀变矿物），其全岩测年结果是多源矿物年龄的平均值，带有混合特点，不宜代表金伯利岩的侵位年龄[23]。斑状金伯利岩中锆石U-Pb同位素年龄值为1452.8Ma，而坡里金伯利岩侵入并穿插了寒武纪馒头组砂页岩、寒武纪张夏组灰岩，说明金伯利岩的侵位时代应晚于早寒武世，锆石U-Pb同位素年龄值比实际情况至少老1000Ma，故其锆石测年结果与地质事实不符，锆石应来源于捕虏晶，不能代表金伯利岩的侵位年龄。
表 3 测年结果Table 3. Summary of dating results岩性 方法 年龄/Ma 测试单位 测年时间 斑状富金云母金伯利岩 企岩K-Ar 371.8 屮科院地球化学研究所 1968年 斑状富金云母金伯利岩 企岩K-Ar 233.8 成都地质学院 1988年 富金云母金伯利岩 企岩K-Ar 379 地矿部宜昌地研所 1988年 斑状富金云母金伯利岩 Sm-Nd法 479±32 地矿部宜昌地研所 1988年 斑状金伯利岩 锆石U-Pb 1452.8 地矿部宜昌地研所 1989年 5.2 侵入接触关系
坡里岩带K24号岩脉侵入于北西向辉绿岩中。该区辉绿岩大都从寒武纪—奥陶纪沉积盖层下穿过，但不穿入沉积盖层中，因此大多数学者[24-26]推测，该区辉绿岩为中元古代牛岚单元辉绿岩。本次对K24号金伯利岩脉及其侵入的辉绿岩进行野外调查，K24号金伯利岩脉赋存的辉绿岩脉北部自寒武纪馒头组下穿过，馒头组石店段灰岩与辉绿岩接触带上见有明显的大理石化，说明辉绿岩侵位于馒头组石店段以后，而非中元古代牛岚单元辉绿岩。本次辉绿岩锆石U-Pb年龄大于509Ma（馒头组石店段时代）的数据与地质事实不符，辉绿岩与馒头组石店段侵入接触关系从侧面印证了辉绿岩锆石U-Pb测年数据117~ 121Ma为辉绿岩的侵位年龄。而坡里岩带K24号岩脉侵入于中生代燕山晚期辉绿岩，因此K24号岩脉形成时代应为中生代燕山晚期或更晚。
5.3 构造、金伯利岩、闪长玢岩先后顺序
坡里金伯利岩带严格受断裂构造控制，除K24号岩脉外（走向350°），其他金伯利岩脉均呈40°左右展布。在桑树峪村西有一条走向40°~45°的断层，K1金伯利岩脉赋存在该断裂中，且金伯利岩脉未见后期构造对其破坏现象，说明北东向断裂形成时代早于金伯利岩的侵位时代。该断裂在北端切入燕山中期闪长玢岩岩体中，说明该控矿断裂晚于燕山中期的闪长玢岩。构造、金伯利岩、闪长玢岩的先后顺序说明，金伯利岩应侵位于燕山中期之后。
5.4 金刚石砂矿储集层
山东省第七地质矿产勘查院在山东金刚石找矿工作中共发现了6个金刚石含矿层位，寒武纪李官组砾岩、石炭纪本溪组砾岩、晚侏罗世三台组砾岩、白垩纪—古近纪官庄群底砾岩、古近纪—新近纪白彦组砾岩、第四纪中更新世郯城砂矿及东汶河中下游地区含矿层。从砂矿储集层所含金刚石的颜色、晶体形态、粒级等特征与蒙阴已知金刚石原生矿中金刚石对比分析，前3个储集层中的金刚石与已知矿带金刚石差别较大，后3个储集层中的金刚石与已知矿带金刚石具有较高的一致性[27]。同时，在蒙阴盆地官庄群底砾岩中含有大量的已知矿带供给含铬镁铝榴石等金刚石指示矿物，因此蒙阴地区的金伯利岩形成于白垩纪—古近纪官庄群之前。
6. 结论
（1）本文从坡里K24号金伯利岩与辉绿岩侵入关系、辉绿岩锆石U-Pb定年及辉绿岩、灰岩接触蚀变及K1金伯利岩脉与控矿构造、闪长玢岩的先后顺序分析，坡里金伯利岩带形成时代晚于辉绿岩的形成时代（121Ma）。
（2）从金刚石砂矿储集层中的金刚石与已知矿带中金刚石对比分析，以及官庄群底砾岩中含有大量的已知矿带供给含铬镁铝榴石等金刚石指示矿物可知，蒙阴坡里金伯利岩形成于白垩纪—古近纪官庄群之前，坡里金伯利岩带侵位于121~79.1Ma之间，应为中生代燕山晚期。
致谢: 孢粉鉴定由中国地质科学院水文地质环境地质研究所童国榜老师完成，在此表示衷心的感谢。 -
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图 2 查干淖尔湖泊沉积年龄与深度的对应关系
Figure 2. The relationship between age and depth for lake sedimentation in Qehan Lake
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图 3 查干淖尔湖泊沉积物粒度组成及参数
Figure 3. Grain size composition and parameters of lake sediments in Qehan Lake
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图 5 查干淖尔2000a来主要孢粉与粒度曲线对比图
Figure 5. Comparison of main pollens and grain-sizes since the last two millennium years in Qehan Lake
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表 1 查干淖尔沉积物14C测年结果
Table 1 14C dating results of Qehan Lake sediments
样号 测试材料 深度
/cml4C年龄
/a BP去除碳库后
年龄/a BP日历年龄
(2σ中值cal a
BP)Cg-b09-0-1 全有机质 0~2 760±30 Cg-b09-27 全有机质 27 1630±30 876±30 782 Cg-b09-51 全有机质 51 1950±35 1196±35 1123 Cg-b09-75 全有机质 75 2115士25 1361±25 1291 Cg-b09-86 全有机质 86 2360士30 1606±30 1482 Cg-b09-93 全有机质 93 2665士25 1911±25 1858 Cg-b09-97 全有机质 97 2850士35 2096±35 2068 
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