Late Eocene-Early Oligocene clay mineral characteristics and paleoclimate significance in Lunpola Basin, Tibet
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摘要:
始新世—渐新世是新生代气候从“温室”向“冰室”转变的重要节点，也是青藏高原及邻区气候格局发生重大变革的关键时期。为了重建高原中部腹地始新世—渐新世的古气候演变特征，探讨古气候变化的控制因素，利用X射线衍射分析对高原中部伦坡拉盆地382道班剖面的黏土矿物特征进行了综合研究，结果显示，伦坡拉盆地在始新世—渐新世牛堡组二段沉积的黏土矿物主要以伊利石为主，伊/蒙混层次之，高岭石与绿泥石含量极少，蒙脱石仅出现在极少样品中。黏土矿物类型及组合特征指示伦坡拉盆地在该时期整体处于寒冷干旱的气候条件，但在长周期趋势下伊利石相对含量逐渐减少，伊/蒙混层逐渐增多，显示出青藏高原中部地区的气候系统在晚始新世—早渐新世时期存在向更加湿润的气候条件转变，这种气候系统的改变可能与南亚季风在晚始新世的演化所带来的更多水汽条件和青藏高原中部中央分水岭的形成有关，但在始新世与渐新世之交，伊利石含量陡然增多，而伊/蒙混层含量则减少，且两者频繁波动，这反映了该盆地在EOT时期受到全球降温的影响。
Abstract:The Eocene-Oligocene Transition (EOT) is an important node of the Cenozoic climate transition from "greenhouse" to "icehouse" worldwide, especially on the Qinghai-Tibet Plateau and adjacent regions. In order to reconstruct the paleoclimatic evolution and controlling factors during the Eocene-Oligocene in the central hinterland of the Tibetan Plateau, clay mineral characteristics of 382 Daoban section in Lunpola Basin were analyzed by X-ray diffraction. Results show that the clay minerals deposited during the Eocene-Oligocene within the Second member of the Niubao Formation comprised of illite, illite/smectite mixed layers (I/S), kaolinite, chlorite and montmorillonite. Generally, the illite is the most abundant clay mineral, followed by I/S, while the kaolinite and chlorite contents are very low, and montmorillonite only appears in a few samples. Characteristics of clay minerals indicate that the Lumpola Basin was in a prolonged cold-dry climate conditions during this period, but a long-term decline in illite and rise in I/S contents indicating that the climate system in the central Tibetan Plateau changed to a more humid climate during this period. Such change could be related to the paleogeographic backgrounds of central Tibet and the evolution of South Asia monsoon since the late Eocene. However, at the EOT, illite content steeply increased, while the I/S content decreased and both fluctuated frequently, which reflects the influence of global cooling in the central Tibetan Plateau.
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图 1 青藏高原沉积盆地分布及伦坡拉盆地位置图（据Xia et al., 2021和中国石油化工股份有限公司勘探南方分公司,2012①修改）
Figure 1.
图 2 研究区地质简图（a）与剖面特征、采样位置（b-c）（据曲永贵等, 2011; 王永胜等, 2012; 陈玉禄等, 2015; Fang et al., 2020修改）
Figure 2.
图 4 伦坡拉盆地典型剖面地层对比与382道班剖面孢粉特征（达玉剖面资料据Fang et al., 2020修改，标准极性柱采用GPTS，2012）
Figure 4.
图 5 黏土矿物转化过程示意图 (据孙庆峰等, 2011修改)
Figure 5.
图 7 青藏高原及周缘地区现代季风区（a; 据Lu et al., 2020修改，地形数据来源于奥维互动地图)和晚始新世古地貌与古气候带分布图（b; 据Fang et al., 2021修改）
Figure 7.
表 1 伦坡拉盆地382道班剖面黏土矿物含量测试结果（%）
Table 1. Test results of clay mineral content of 382 Daoban section in Lunpola Basin (%)
编号 岩性 黏土矿物含量 伊利石 高岭石 绿泥石 蒙脱石 伊/蒙混层 伊利石结晶度 编号 岩性 黏土矿物含量 伊利石 高岭石 绿泥石 蒙脱石 伊/蒙混层 伊利石结晶度 ZP-0 白云质泥岩 41.67 91 9 — — — 0.47 ZP-22-1 白云质泥岩 25.30 17 — — — 83 0.39 ZP-01 泥质白云岩 17.41 95 5 — — — 0.40 SL74 泥质白云岩 3.65 84 — — — 16 0.40 ZP-02 泥质白云岩 11.43 45 9 — — 46 0.35 SL70 白云质泥岩 16.88 79 — — — 22 0.47 ZP-03-1 白云质泥岩 27.71 83 2 — — 14 0.45 SL67 泥质白云岩 3.01 69 — — — 31 0.40 ZP-03 泥质白云岩 15.80 72 28 — — — 0.33 SL63 泥质白云岩 3.24 45 3 — — 52 0.32 ZP-04 泥质白云岩 17.42 81 6 — — — 0.43 SL57 白云质泥岩 24.80 63 — — — 37 0.48 ZP-05 泥质白云岩 16.29 50 2 — — 48 0.51 ZP-22 泥质白云岩 7.60 75 3 — — 23 0.44 ZP-06-1 白云质泥岩 21.58 82 5 — — 13 0.54 SL49 泥质白云岩 12.34 69 2 — — 29 0.44 ZP-06 泥质白云岩 21.61 87 1 — — — 0.49 ZP-23-2 白云质泥岩 22.84 20 — — — 80 0.41 ZP-07-1 白云质泥岩 34.07 80 — — — 20 0.51 ZP-23 泥质白云岩 7.56 21 — — — 79 0.38 ZP-07 泥质白云岩 22.89 80 2 — — 17 0.47 ZP-24-1 白云质泥岩 27.52 16 — — — 84 0.46 ZP-08-1 白云质泥岩 33.28 71 — — — 29 0.53 SL41 白云质泥岩 16.06 60 — — — 40 0.46 ZP-08 泥质白云岩 14.22 70 3 — — 27 0.34 ZP-25-1 白云质泥岩 64.43 24 1 — — 75 0.39 ZP-09 泥质白云岩 14.62 77 — — — 23 0.44 ZP-25 泥质白云岩 11.12 16 — — — 84 0.35 ZP-10-1 白云质泥岩 21.39 78 — — — 22 0.53 SL33 泥质白云岩 4.64 48 — — — 52 0.47 ZP-10 泥质白云岩 7.96 79 — — — 21 0.33 ZP-26-2 白云质泥岩 14.59 75 8 3 — 15 0.49 ZP-11 泥质白云岩 15.70 81 — — — 19 0.39 ZP-26 泥质白云岩 7.38 26 — — — 74 0.38 ZP-12-1 白云质泥岩 22.15 81 1 1 — 17 0.53 ZP-27-1 白云质泥岩 40.13 32 — 1 — 67 0.41 ZP-12-2 白云质泥岩 31.36 79 — — — 21 0.51 ZP-27 泥质白云岩 6.03 83 — — — 17 0.31 ZP-12 泥质白云岩 15.05 50 21 5 — 24 0.36 ZP-28-1 白云质泥岩 19.88 29 — 2 — 69 0.39 ZP-13-1 白云质泥岩 16.05 64 8 1 — 27 0.44 ZP-28 泥质白云岩 12.30 38 — — — 62 0.43 ZP-13 白云质泥岩 23.71 64 — — — 36 0.51 ZP-29-1 白云质泥岩 29.27 25 — — — 75 0.35 ZP-14 泥质白云岩 11.09 68 4 — — 28 0.45 ZP-29 泥质白云岩 19.98 36 — — — 64 0.37 ZP-15-2 白云质泥岩 26.57 55 4 — — 41 0.48 ZP-30-1 白云质泥岩 30.63 25 — — — 75 0.44 ZP-15 泥质白云岩 12.12 59 — — — 41 0.49 ZP-30 泥质白云岩 26.69 40 — — — 60 0.41 ZP-16 泥质白云岩 14.40 55 5 — — 40 0.39 ZP-31-1 白云质泥岩 22.38 33 — 4 — 63 0.40 ZP-17-1 白云质泥岩 26.46 43 1 — — 56 0.53 ZP-31 泥质白云岩 22.59 37 — 4 — 60 0.40 ZP-17 泥质白云岩 14.27 72 — — — 28 0.47 ZP-32-1 白云质泥岩 29.95 19 — 3 — 78 0.39 ZP-18 泥质白云岩 9.37 53 — — — 47 0.39 ZP-32 泥质白云岩 35.19 24 1 3 — 72 0.40 SL112 白云质泥岩 28.91 47 — — — 53 0.43 ZP-33-1 白云质泥岩 43.63 24 — 2 — 75 0.46 SL106 白云质泥岩 16.04 53 — — — 47 0.47 ZP-33 泥质白云岩 15.37 22 — 2 — 76 0.41 ZP-19-1 白云质泥岩 23.37 13 2 1 84 — 0.43 ZP-34-1 白云质泥岩 30.31 9 — 1 90 — 0.34 ZP-19 泥质白云岩 7.95 82 — — — 18 0.36 ZP-34 泥质白云岩 3.15 5 — — 95 — 0.37 SL99 白云质泥岩 24.63 29 — — — 71 0.53 ZP-35-1 白云质泥岩 19.53 19 — 2 79 — 0.40 SL91 白云质泥岩 27.53 43 — — — 57 0.43 ZP-35 泥质白云岩 36.78 24 — 3 — 73 0.43 ZP-20 泥质白云岩 14.74 17 — — — 83 0.43 ZP-36-1 泥质白云岩 34.35 30 — 4 — 66 0.40 SL85 泥质白云岩 3.88 89 — — — 11 0.34 ZP-36 白云质泥岩 58.01 32 — 5 — 63 0.34 ZP-21-1 白云质泥岩 23.78 71 — — — 29 0.46 ZP-37-1 泥质白云岩 26.06 46 — 3 — 51 0.41 SL80 泥质白云岩 8.53 100 — — — — 0.29 ZP-37 泥质白云岩 3.15 56 — 4 — 40 0.36 ZP-21 泥质白云岩 11.41 23 — — — 77 0.40 ZP-38-1 白云质泥岩 36.90 47 — — — 53 0.48 SL77 泥质白云岩 8.03 46 — — — 54 0.47 ZP-38 泥质白云岩 8.98 60 — — — 40 0.49 
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