黄河源区晚新生代沉积与环境演化研究
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摘要
全球变化是国际当前研究的前沿课题。-65Ma以来,印度板块与欧亚板块的碰撞及其汇聚形成了全球海拔最高的独特地域单元-青藏高原。青藏高原是全球现今仍在活动中的板块碰撞区域之一,是研究岩石圈形成演化、探讨地壳运动机制的理想区域。青藏高原的隆起对其自身及毗邻地区自然环境的演化影响深刻,同时对全球变化的响应非常敏感,也强烈影响着全球变化。青藏高原晚新生代以来有过多次的古大湖期,湖泊沉积物中蕴涵着丰富的古环境变化信息,是研究高原环境变化的良好载体。
黄河源盆地位于青藏高原东北部,对高原隆升引起的气候变化的非常敏感,是研究高原环境变化的良好区域之一。然而,目前对这一地区晚新生代以来的湖相地层和环境变化还比较薄弱,在湖泊演化、高原隆升等方面尚需实际资料的进一步加强。
本论文以黄河源区湖相沉积地层为主要研究对象,以古气候环境演化为主线,进行了沉积地层、同位素年代、环境地球化学、孢粉与微古生物、构造地貌、盆地性质等方面的研究,总结了湖相地层沉积序列,恢复了黄河源盆地晚新生代以来的古环境、古气候变化,探讨了湖泊演化与高原隆升、环境演变的关系。取得的主要认识如下：
黄河源区晚新生代湖相地层其南界为巴颜喀拉山,北界为布青山,西界为雅拉达泽山,东侧则包括黄河干流达日县特合土乡以上的流域范围。这套地层开始沉积于223.9万年,由全新统黑河乡组(Qh1h)、上更新统大野马岭组(Qp31d)、中更新统鄂陵湖组(Qp21e)及下更新统野牛沟组(Qp11y)组成。
黄河源盆地受南北两条断裂控制,北缘为昆南断裂,南缘断裂为巴颜喀拉山山前断裂,两条断裂带在晚新生代均为挤压性质。盆内断裂主要有布青山山前断裂、玛多断裂、巴颜河前断裂、麻多—野牛沟断裂。黄河源盆地现今为一压陷盆地,这是由盆地南北断裂的性质决定的。盆地的形成演化可分为两个阶段,渐新世(35.4Ma-23.3Ma)黄河源盆地雏形形成,中新世黄河源盆地的基本形态形成。盆地基底岩石磁组构分析认为,黄河源盆地基底岩石中存在两条韧性剪切带,韧性剪切带控制现今湖盆的展布,两条韧性剪切带与两条湖泊分布带有很好的对应关系。
黄河源区整体海拔较高,但区域内地形坡度较缓。其中海拔4500-5000m的区域为黄河源盆地汇水区域,大于4500m的区域为黄河源盆地的集水区域。水系特征显示黄河源地区以黄河干流为中轴,两侧流域地貌发育呈现明显的南北分异现象,具有显著的不对称发育特征。三维DEM分析认为现今地貌形态是构造作用与地表过程共同作用的产物,现今盆地东西长,南北短。
黄河源盆地早更新世(223.9万年)以来的古植被、古环境演变经历四个阶段：第1阶段(223.9万年～90.1万年)为森林草原环境,当时气候温暖潮湿；第2阶段(90.1万年～35万年)为灌丛草原环境,气候变的干冷；第3阶段(35万年～2.8万年)为草甸草原环境,气候逐渐趋于寒冷；第4阶段(2.8万年～0.8万年)为荒漠草原环境,初期气候干冷,晚期气候干旱。黄河源地区早更新世(223.9万年)以来古湖泊发育经历了三次扩张三次萎缩过程,第一次扩张萎缩发生在早更新世,大致为223.9万年～76.4万年,湖泊沉积物主要为粗粒的砂砾石层,湖泊范围不大；第二次湖泊发育大致为70.7万年～21.1万年,为中更新世时期,这次湖泊发育达第四纪以来最大范围；第三次湖泊发育大致为20.5万年～8.10万年,这一时期湖泊扩张很快,但未达到中更新世最大范围即开始萎缩。进入全新世湖泊虽有波动,但仍以萎缩为主。
论文最后探讨了青藏高原湖泊演化、气候环境变迁与高原隆升的关系,认为高原内部的环境演化总体规律受高原隆升强烈控制,而全球尺度的气候变化在青藏高原上的表现则受全球变化因素影响。
The Qinghai-Tibet Plateau, the world's highest unique geographical unit formed during India-Eurasia collision since～65 Ma, is a hot spot of global change study--an international forefront of current research topics. It is considered to be one of the still active regions in the continental collision zone, and then an ideal field lab to study the formation and evolution of the lithosphere, and the mechanism of crust movements. The uplift of the plateau since the late Cenozoic has influenced the evolution and differentiation of natural environment for its own and adjacent areas profoundly, and has been also a sensitive response of and strong influence on global change. Lacustrine sediments from several phase ancient Great Lake in the Qinghai-Tibet Plateau since the Late Cenozoic, containing abundant information on palaeoclimate change, are good carriers for the study of plateau environmental change.
The Yellow River Basin located at the northeast of the plateau, is the Yellow River source region sensitive to the plateau uplift and environmental change. The lacustrine strata and environmental change since the Late Cenozoic in this region has not been investigated in detail due to the lack of strengthened actual data on plateau uplift and lake evolution. In this dissertation, the lacustrine sedimentary strata of Yellow River Basin are selected to be the main target of palaeoclimate and environmental study.
The sedimentary sequence of lacustrine strata, the palaeoenvironment and palaeoclimate of Yellow River Basin, and the relationship among lacustrine evolution, plateau uplift and environmental change since the Late Cenozoic, are summed up and restored in this dissertation, through the combined study of sedimentology, isotopic geochronology, environmental geochemistry, pollen analyses and micro-palaeontology, tectonic geomorphology, and structural geology of the basin system. The main progresses and achievements made by the research here are as follows:
1. The Late Cenozoic lacustrine strata in the Yellow River source region, surrounded by Bayankala Mt. in the south, Buqing Mt. in the north, Yaladaze Hill in the west, and the Tehetu area of Dari County in the east, composed by the Holocene Heihexiang Group (Qh1h), the Upper Pleistocene Dayemaling Group (Qp31d), the Middle Pleistocene Eling Lake Group (Qp21e) and the Lower Pleistocene Yeniugou Group (QpI1y),is suggested to be formed since 2,239 kaB.P..
2. The Yellow River Basin is a sag basin in the Late Cenozoic, controlled by the two compressional margin faults, i.e., the Kunnan fault in the north and the Bayankala mountain-front fault in the south, and several intrabasinal faults such as the Buqingshan mountain-front fault, the Maduo fault, the Bayan River fault, and the Maduo-Yeniugou fault. The formation and evolution of the basin can be divided into two phases:the initial phase in the Oligocene between 35.4 Ma to 23.3 Ma, and the finally formation phase in the Miocene.
3. Two ductile shear zones, which are controlling and corresponding to the distribution of two lake zones, are detected in the Yellow River source region through magnetic fabric analyses of the basement rocks.
4. The structural landform analysis shows that the basin area is regionally high with elevation of 4500～5000 m in the gentle dipping water shedding area, and higher in the catchment area of>4500 m. The drainage system of the basin is charactered by the significant asymmetry in growth, with the Yellow River as its axis and clearly differentiated northern and southern valley landforms. Three-dimension DEM analysis suggests that the present elliptical basin with a long axis in E-W is a structural basin resulting from combined tectonic and surface processes.
5. The Yellow River Basin has suffered from four stage changes in palaeovegetation and palaeoenvironment since the early Pleistocene (2,239 kaB.P.). The first stage (2,239～901 kaB.P.) was dominated by the forest-steppe environment with a warm and humid climate. The second stage (901-350 kaB.P.) was the shrub steppe environment with a cold and dry climate. The third stage (350 kaB.P.～28 kaB.P.) was the meadow steppe environment with gradually cooling climate. The fourth Stage (28kaB.P.-8 kaB.P.) was the desert steppe with dry and cold weather in the early time and later drought.
6. The development of the ancient great lakes in the Yellow River source region had went through three expanding and three shrinking processes since the Early Pleistocene (2,239 kaB.P.). The first expansion and shrinking period as a limited lake was in the early Pleistocene during 2,239 kaB.P.～764 kaB.P., with sediments mainly of coarse-grained sands and gravel layers. The second period was in the Middle Pleistocene during 211 kaB.P.～70.7 kaB.P.when the lake had reached the maximum extent in the Quaternary and then shrank. The third period was during approximately 205kaB.P.～81 kaB.P, with the quickly expanding first, and then the beginning of shrinking of the lake. The lake was shrinking in the Holocene with several fluctuations.
Finally, the relationship among the formation and evolution of the lakes, the climate change and the plateau uplift is discussed, and the overall evolutional law of the intra-plateau environment is considered to be strongly controlled by the uplifting of the plateau with the superposing of global climate change.
黄河源盆地位于青藏高原东北部,对高原隆升引起的气候变化的非常敏感,是研究高原环境变化的良好区域之一。然而,目前对这一地区晚新生代以来的湖相地层和环境变化还比较薄弱,在湖泊演化、高原隆升等方面尚需实际资料的进一步加强。
本论文以黄河源区湖相沉积地层为主要研究对象,以古气候环境演化为主线,进行了沉积地层、同位素年代、环境地球化学、孢粉与微古生物、构造地貌、盆地性质等方面的研究,总结了湖相地层沉积序列,恢复了黄河源盆地晚新生代以来的古环境、古气候变化,探讨了湖泊演化与高原隆升、环境演变的关系。取得的主要认识如下：
黄河源区晚新生代湖相地层其南界为巴颜喀拉山,北界为布青山,西界为雅拉达泽山,东侧则包括黄河干流达日县特合土乡以上的流域范围。这套地层开始沉积于223.9万年,由全新统黑河乡组(Qh1h)、上更新统大野马岭组(Qp31d)、中更新统鄂陵湖组(Qp21e)及下更新统野牛沟组(Qp11y)组成。
黄河源盆地受南北两条断裂控制,北缘为昆南断裂,南缘断裂为巴颜喀拉山山前断裂,两条断裂带在晚新生代均为挤压性质。盆内断裂主要有布青山山前断裂、玛多断裂、巴颜河前断裂、麻多—野牛沟断裂。黄河源盆地现今为一压陷盆地,这是由盆地南北断裂的性质决定的。盆地的形成演化可分为两个阶段,渐新世(35.4Ma-23.3Ma)黄河源盆地雏形形成,中新世黄河源盆地的基本形态形成。盆地基底岩石磁组构分析认为,黄河源盆地基底岩石中存在两条韧性剪切带,韧性剪切带控制现今湖盆的展布,两条韧性剪切带与两条湖泊分布带有很好的对应关系。
黄河源区整体海拔较高,但区域内地形坡度较缓。其中海拔4500-5000m的区域为黄河源盆地汇水区域,大于4500m的区域为黄河源盆地的集水区域。水系特征显示黄河源地区以黄河干流为中轴,两侧流域地貌发育呈现明显的南北分异现象,具有显著的不对称发育特征。三维DEM分析认为现今地貌形态是构造作用与地表过程共同作用的产物,现今盆地东西长,南北短。
黄河源盆地早更新世(223.9万年)以来的古植被、古环境演变经历四个阶段：第1阶段(223.9万年～90.1万年)为森林草原环境,当时气候温暖潮湿；第2阶段(90.1万年～35万年)为灌丛草原环境,气候变的干冷；第3阶段(35万年～2.8万年)为草甸草原环境,气候逐渐趋于寒冷；第4阶段(2.8万年～0.8万年)为荒漠草原环境,初期气候干冷,晚期气候干旱。黄河源地区早更新世(223.9万年)以来古湖泊发育经历了三次扩张三次萎缩过程,第一次扩张萎缩发生在早更新世,大致为223.9万年～76.4万年,湖泊沉积物主要为粗粒的砂砾石层,湖泊范围不大；第二次湖泊发育大致为70.7万年～21.1万年,为中更新世时期,这次湖泊发育达第四纪以来最大范围；第三次湖泊发育大致为20.5万年～8.10万年,这一时期湖泊扩张很快,但未达到中更新世最大范围即开始萎缩。进入全新世湖泊虽有波动,但仍以萎缩为主。
论文最后探讨了青藏高原湖泊演化、气候环境变迁与高原隆升的关系,认为高原内部的环境演化总体规律受高原隆升强烈控制,而全球尺度的气候变化在青藏高原上的表现则受全球变化因素影响。
The Qinghai-Tibet Plateau, the world's highest unique geographical unit formed during India-Eurasia collision since～65 Ma, is a hot spot of global change study--an international forefront of current research topics. It is considered to be one of the still active regions in the continental collision zone, and then an ideal field lab to study the formation and evolution of the lithosphere, and the mechanism of crust movements. The uplift of the plateau since the late Cenozoic has influenced the evolution and differentiation of natural environment for its own and adjacent areas profoundly, and has been also a sensitive response of and strong influence on global change. Lacustrine sediments from several phase ancient Great Lake in the Qinghai-Tibet Plateau since the Late Cenozoic, containing abundant information on palaeoclimate change, are good carriers for the study of plateau environmental change.
The Yellow River Basin located at the northeast of the plateau, is the Yellow River source region sensitive to the plateau uplift and environmental change. The lacustrine strata and environmental change since the Late Cenozoic in this region has not been investigated in detail due to the lack of strengthened actual data on plateau uplift and lake evolution. In this dissertation, the lacustrine sedimentary strata of Yellow River Basin are selected to be the main target of palaeoclimate and environmental study.
The sedimentary sequence of lacustrine strata, the palaeoenvironment and palaeoclimate of Yellow River Basin, and the relationship among lacustrine evolution, plateau uplift and environmental change since the Late Cenozoic, are summed up and restored in this dissertation, through the combined study of sedimentology, isotopic geochronology, environmental geochemistry, pollen analyses and micro-palaeontology, tectonic geomorphology, and structural geology of the basin system. The main progresses and achievements made by the research here are as follows:
1. The Late Cenozoic lacustrine strata in the Yellow River source region, surrounded by Bayankala Mt. in the south, Buqing Mt. in the north, Yaladaze Hill in the west, and the Tehetu area of Dari County in the east, composed by the Holocene Heihexiang Group (Qh1h), the Upper Pleistocene Dayemaling Group (Qp31d), the Middle Pleistocene Eling Lake Group (Qp21e) and the Lower Pleistocene Yeniugou Group (QpI1y),is suggested to be formed since 2,239 kaB.P..
2. The Yellow River Basin is a sag basin in the Late Cenozoic, controlled by the two compressional margin faults, i.e., the Kunnan fault in the north and the Bayankala mountain-front fault in the south, and several intrabasinal faults such as the Buqingshan mountain-front fault, the Maduo fault, the Bayan River fault, and the Maduo-Yeniugou fault. The formation and evolution of the basin can be divided into two phases:the initial phase in the Oligocene between 35.4 Ma to 23.3 Ma, and the finally formation phase in the Miocene.
3. Two ductile shear zones, which are controlling and corresponding to the distribution of two lake zones, are detected in the Yellow River source region through magnetic fabric analyses of the basement rocks.
4. The structural landform analysis shows that the basin area is regionally high with elevation of 4500～5000 m in the gentle dipping water shedding area, and higher in the catchment area of>4500 m. The drainage system of the basin is charactered by the significant asymmetry in growth, with the Yellow River as its axis and clearly differentiated northern and southern valley landforms. Three-dimension DEM analysis suggests that the present elliptical basin with a long axis in E-W is a structural basin resulting from combined tectonic and surface processes.
5. The Yellow River Basin has suffered from four stage changes in palaeovegetation and palaeoenvironment since the early Pleistocene (2,239 kaB.P.). The first stage (2,239～901 kaB.P.) was dominated by the forest-steppe environment with a warm and humid climate. The second stage (901-350 kaB.P.) was the shrub steppe environment with a cold and dry climate. The third stage (350 kaB.P.～28 kaB.P.) was the meadow steppe environment with gradually cooling climate. The fourth Stage (28kaB.P.-8 kaB.P.) was the desert steppe with dry and cold weather in the early time and later drought.
6. The development of the ancient great lakes in the Yellow River source region had went through three expanding and three shrinking processes since the Early Pleistocene (2,239 kaB.P.). The first expansion and shrinking period as a limited lake was in the early Pleistocene during 2,239 kaB.P.～764 kaB.P., with sediments mainly of coarse-grained sands and gravel layers. The second period was in the Middle Pleistocene during 211 kaB.P.～70.7 kaB.P.when the lake had reached the maximum extent in the Quaternary and then shrank. The third period was during approximately 205kaB.P.～81 kaB.P, with the quickly expanding first, and then the beginning of shrinking of the lake. The lake was shrinking in the Holocene with several fluctuations.
Finally, the relationship among the formation and evolution of the lakes, the climate change and the plateau uplift is discussed, and the overall evolutional law of the intra-plateau environment is considered to be strongly controlled by the uplifting of the plateau with the superposing of global climate change.
引文
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