陇西盆地东南隅新近纪沉积与环境演变
摘要
青藏高原隆升不仅导致了亚洲大陆内部强烈的新生代构造变形,而且还对周边地区的地貌格局和环境演化产生了重大影响,因此,青藏高原隆升及其环境效应成为国际全球变化研究的热点问题之一。但目前人们对于高原开始隆升的具体时间、何时达到现今的高度以及对周边地区环境演化过程的影响等的认识还存有较大分岐。
青藏高原内部及周边诸多盆地是在地壳变形和隆起过程中形成的,盆地沉积物是盆地水系范围内造山带岩石经风化、剥蚀、搬运和沉积的产物,它们不仅反映了盆地充填过程中周围造山带的动力学性质,而且记录了沉积物在各种地质作用过程中的气候和环境变化信息。陇西盆地东南隅位于青藏高原东北缘六盘山与西秦岭两个重要构造带交汇处,是青藏高原与黄土高原的交接部位,其南界西秦岭造山带是中国大陆南、北构造交汇、衔接和转换的关键部位,其东界六盘山是我国东西有重要气候与构造意义的分界线,因此,陇西盆地东南隅是中国大陆构造和环境变化的敏感地带。
本文通过对陇西盆地东南隅进行广泛野外考察和大量室内分析,综合各种指标分析结果与相关资料,主要获得了以下的发现与认识:
1、陇西盆地东南隅古近纪沉积以山麓洪积扇相红色粗碎屑岩为主,22Ma左右青藏高原构造活动使其变形,并形成地幔热源的钾霞橄黄长质火山岩喷发,新近纪地层不整合于古近系之上,表明至少22Ma左右印度板块与欧亚板块碰撞变形远程效应己达青藏高原东北缘。新近纪以来陇西盆地东南隅形成沉积盆地,盆地广泛接受稳定的细粒河湖相沉积物,古生物繁盛,表明22Ma左右的构造活动尚未造成高原大幅隆升。
2、自西秦岭山前凹陷向北至广阔盆地及北部华家岭洪泛平原带,新近纪沉积厚度迅速变薄(即由>1000m减薄为200-300m),沉积物粒径变细,沉积相发生明显的水平分异。在垂向上,15.6MaB.R以来陇西盆地东南隅沉积演化经历了如下主要阶段:15.6-9.23Ma洪泛平原和河流沉积,沉积以红色泥岩与钙质泥岩或钙质层(calcrate)韵律互层为主的“下红层”:9.23-7.1Ma盆地广泛接受湖侵,
The uplift of the Tibetan Plateau not only causes the intense Cenozoic tectonic deformation in Asia, but also has effect on the relief framework and environmental evolution in the surrounding area of the Tibetan Plateau. So, the Tibetan Plateau uplift and its environmental effects become one of the hot spots of the Past Global Change Research. However, there are great differences on the exact time of the Tibetan Plateau uplift, reaching modern height and the impact of environmental evolution process of the surrounding area.Many basins around the Tibetan Plateau formed during the process of the crustal deformation and uplift. And the sediments in a basin is generally a production of rocks bearing the process of weathering, denudation, transition and deposition in river system in orogenic belt. So, the sediments not only reflect the dynamic properties in filling process, but also record the climate and environmental change information in all kinds of geological processes. The southeast Longxi basin, which is located at the convergence of Liupan Mountains and west Qinling on the northeastern margin of the Tibetan Plateau, is the connection between the Tibetan Plateau and the Loess Plateau. And its northern boundary is west Qinling which is the key part in tectonic movement transition from northern to southern China. Its eastern boundary, the east Liupan Mountains, is the line that separates the climatic types and tectonic movements in eastern and western China. As a result, the southeast part of the Longxi Basin is quiet sensitive to climate changes and tectonic movements. So it is an ideal area for studying the process of the Tibetan Plateau uplift, the environmental effects and the process of aridification in northwest inland of China.Based on wide field investigation, data analysis, synthesized various kinds of indice and correlative data, we have mainly obtained the following findings:1. The Paleogene red coarse clastic rocks with the characters of piedmont alluvial
fan facies were deposited in southeast Longxi basin. At about 22Ma, the rocks were deformed by the tectonic activity in the Tibetan Plateau and the kamafugitic series lava was formed and unconformably overlaped on the Paleogene sandstone. It showed that the distance effect of collisional deformation between the Indo plate and Eurasia plate has already reached the northeastern margin of the Tibetan Plateau at least on 22Ma. Since the Neogene, a basin has been formed in Southeast Longxi Basin. The fact of the steady finegrain fluvial-lacustrine sediments and abundant fossils suggested that the tectonic activity did not cause rapidly uplift at that time.2. The thickness of the Neogene deposition decreased rapidly (from greater than 1000m to 200-300m) from west Qinling piedmont depression to the broad floodplain in the basin. The sediments become finer and the horizontal difference of sediments facies is obvious. The deposition evolution experienced the following stage since 15.6MaB.P.:15.6-9.23Ma, floodplain and fluvial deposition, the "lower red bedding" consists of red mudstone and calcareous mudstone or calcrate with alternate appearance;9.23-7.1Ma, the lake invasion took place in the basin broadly, the "zebra bed" consists of celadon marlite interbeded with red mudstone;Since 7.1Ma, the lake began to shrink in large scale and floodplain developed in vast area of the basin. 7.1-3.6Ma, "upper red bedding" came into being and consisted mainly of red argillaceous beddings and siltstone beddings, moreover, gypsum-salt deposition has been found at the top of "upper red bedding" in some area;About 3.6Ma, affected by the Tibetan Plateau uplift, the south part near the west Qinling in the basin downfaulted and became lake again;3.6Ma-1.4Ma, "upper green bedding" came into being and consists of celadon mudstone interbeded with offwhite marlite;About 1.4Ma, affected by the intense uplift of the Tibetan Plateau, the development history of the lake in the study area ended. After that, the study area began to experience uplift ,denudation, river terraces development and eolian loess deposition.3. At the end of Paleogene, the climate was dry and huge bedding red calcareous cementation sandstone deposited. The climate bacame humid in Miocene obviously. Finegrain fluvial-lacustrine sediments under low energy circumstance were deposited in Linxia Basin in Miocene. The vegetation changed from woodland steppe at the end
of Paleogene to forest in Miocene, which indicated a humid climate. The finegrain fluvial-lacustrine sediments were also deposited in southeast Longxi Basin in Neogene. Large mammals, such as rhinoceros, elephant, deer and antelope, lived in the study area, which showed the climate was humid during this period. But the alternating environment between dry and humid occurred under the humid background. 15.6-9.23Ma, the climate is humid and fluvial process bloomed. 9.23-7.1 Ma, the climate was more humid and the lake expanded. 7.1-3.6Ma, the lake shrunk and climate became dry relatively. Since the climate continued to become drier, gypsum-salt deposition was developed in some areas;After 1.4Ma, the climate became dry and the lake deposition was finished, eolian deposition developed, then, the modern environmental framework came into being.4.Based on the grainsize, geochemistry and microstructure analysis of the sediments deposited during 22-6.2Ma in Guojia, Qin'an, Guo et al (2002) suggested that this set of red beds was eolian loess series. And they deduced that the inner Asian began to dry since 22Ma and this status related to the Tibetan Plateau uplift. But their conclusion is not consistent with other deposition records in the basin at the same period. The detailed contrast and analysis on the QA-I Neogene sediments and Lamashan and Yaodian Neogene lacustrine sediments have been carried out and showed:(1) The comparing analysis on the grainsize characters among QA-I Neogene sediments, Tianshui Neogene fluvial-lacustrine sediments and Quaternary eolian loess showed that the characters of Guojia Neogene sediments is more similar to that of Tianshui Neogene fluvial-lacustrine sediments. Moreover, the frequency and cumulation percentage curves of both sections are more similar, but there is difference between QA-I Neogene sediments and Quaternary eolian loess;In the grainsize scatter figures, two types can be divided obviously: one is QA-I Neogene sediments and Tianshui Neogene lacustrine sediments, the other is Quaternary eolian loess.(2) The geochemistry characters demonstrate that the calcium carbonate content of the yellow-brown "loess" of QA-I Neogene sediments samples may reach 15.76-46.34% or even higher, the silicon dioxide content may reach 29.54-52.26%.
However, there are obvious differences in content between the QA-I Neogene sediments and typical Quaternary eolian loess (CaCO3, general lower than 20%;SiOo, general 55-65%). The content of the calcium carbonate and silicon dioxide in the QA-I Neogene sediments is similar to those in Tianshui Neogene fluvial-lacustrine sediments. Moreover, both of the two sections have the same REE distribution patterns, which have the characters that all are moderately rich in Ce family elements, with negative slopes and negative Eu anomaly.(3) There are much sediments produced by fluvial process in the "loess-paleosol " series of QA-I Section, such as the fine sandstones with horizontal beddings or ripple cross beddings in the mudstone sequence and the marlite with red mud block or gravel inside at the bottom of the section, those belts and thick lens composed mainly by marlite and well-grinded gravel at the top part on the middle of the section, the intraclastic texture and diatom observed by microscope at some segments of the section. Moreover, from Tianshui, which is at the south basin, to Qin'an, the horizontal difference of sediments facies is obvious. For example, the celadon marlite in the "zebra bedding" appears in both of Yangjiadazhuang and Jiaowan, which are 20km away from the QA-I Section, but has lighter color and thinner thickness than that in Tianshui. And we also found many well-buried fossils of big vertebrates, such as rhinoceros and elephant, in the neogene stratum near the QA-I Section in Qin'an. The fact suggested that the climate in that period was quiet mild. According to those theories of taphouomy, it is obvious that those big fossils were not able to be buried at QA-I with the local sediments rate (1.67cm/kyr) in Neogene.The results above indicated that although the appearance of QA-I Neogene section is similar to the Loess-paleosol series, it should be an alternative series which is composed of finegrain mudflat deposition on the margin of the basin, floodplain deposition and those products of pedogenensis in the air.5. The article also discussed the aridification problem in inner Asian. The study showed that the early Neogene climate should be warm and moist in inner Asian. This climate change may relate to the Asian palaeo-monsoon formation. And the palaeo-monsoon origin may relate to the expansion of the Asian marginal sea. Notably,
the fracture and expansion of South China Sea on a large scale at that time provided an important passway for the Asian palaeo-monsoon;About 8Ma, the climate was dry and the red clay deposited, this may relate to the uplift of the Tibetan Plateau;About 2.6Ma, the uplift of the Tibetan Plateau was rapidly and the Asian monsoon established steadily, the climate was dry and the typical eolian loess began to deposit.
青藏高原内部及周边诸多盆地是在地壳变形和隆起过程中形成的,盆地沉积物是盆地水系范围内造山带岩石经风化、剥蚀、搬运和沉积的产物,它们不仅反映了盆地充填过程中周围造山带的动力学性质,而且记录了沉积物在各种地质作用过程中的气候和环境变化信息。陇西盆地东南隅位于青藏高原东北缘六盘山与西秦岭两个重要构造带交汇处,是青藏高原与黄土高原的交接部位,其南界西秦岭造山带是中国大陆南、北构造交汇、衔接和转换的关键部位,其东界六盘山是我国东西有重要气候与构造意义的分界线,因此,陇西盆地东南隅是中国大陆构造和环境变化的敏感地带。
本文通过对陇西盆地东南隅进行广泛野外考察和大量室内分析,综合各种指标分析结果与相关资料,主要获得了以下的发现与认识:
1、陇西盆地东南隅古近纪沉积以山麓洪积扇相红色粗碎屑岩为主,22Ma左右青藏高原构造活动使其变形,并形成地幔热源的钾霞橄黄长质火山岩喷发,新近纪地层不整合于古近系之上,表明至少22Ma左右印度板块与欧亚板块碰撞变形远程效应己达青藏高原东北缘。新近纪以来陇西盆地东南隅形成沉积盆地,盆地广泛接受稳定的细粒河湖相沉积物,古生物繁盛,表明22Ma左右的构造活动尚未造成高原大幅隆升。
2、自西秦岭山前凹陷向北至广阔盆地及北部华家岭洪泛平原带,新近纪沉积厚度迅速变薄(即由>1000m减薄为200-300m),沉积物粒径变细,沉积相发生明显的水平分异。在垂向上,15.6MaB.R以来陇西盆地东南隅沉积演化经历了如下主要阶段:15.6-9.23Ma洪泛平原和河流沉积,沉积以红色泥岩与钙质泥岩或钙质层(calcrate)韵律互层为主的“下红层”:9.23-7.1Ma盆地广泛接受湖侵,
The uplift of the Tibetan Plateau not only causes the intense Cenozoic tectonic deformation in Asia, but also has effect on the relief framework and environmental evolution in the surrounding area of the Tibetan Plateau. So, the Tibetan Plateau uplift and its environmental effects become one of the hot spots of the Past Global Change Research. However, there are great differences on the exact time of the Tibetan Plateau uplift, reaching modern height and the impact of environmental evolution process of the surrounding area.Many basins around the Tibetan Plateau formed during the process of the crustal deformation and uplift. And the sediments in a basin is generally a production of rocks bearing the process of weathering, denudation, transition and deposition in river system in orogenic belt. So, the sediments not only reflect the dynamic properties in filling process, but also record the climate and environmental change information in all kinds of geological processes. The southeast Longxi basin, which is located at the convergence of Liupan Mountains and west Qinling on the northeastern margin of the Tibetan Plateau, is the connection between the Tibetan Plateau and the Loess Plateau. And its northern boundary is west Qinling which is the key part in tectonic movement transition from northern to southern China. Its eastern boundary, the east Liupan Mountains, is the line that separates the climatic types and tectonic movements in eastern and western China. As a result, the southeast part of the Longxi Basin is quiet sensitive to climate changes and tectonic movements. So it is an ideal area for studying the process of the Tibetan Plateau uplift, the environmental effects and the process of aridification in northwest inland of China.Based on wide field investigation, data analysis, synthesized various kinds of indice and correlative data, we have mainly obtained the following findings:1. The Paleogene red coarse clastic rocks with the characters of piedmont alluvial
fan facies were deposited in southeast Longxi basin. At about 22Ma, the rocks were deformed by the tectonic activity in the Tibetan Plateau and the kamafugitic series lava was formed and unconformably overlaped on the Paleogene sandstone. It showed that the distance effect of collisional deformation between the Indo plate and Eurasia plate has already reached the northeastern margin of the Tibetan Plateau at least on 22Ma. Since the Neogene, a basin has been formed in Southeast Longxi Basin. The fact of the steady finegrain fluvial-lacustrine sediments and abundant fossils suggested that the tectonic activity did not cause rapidly uplift at that time.2. The thickness of the Neogene deposition decreased rapidly (from greater than 1000m to 200-300m) from west Qinling piedmont depression to the broad floodplain in the basin. The sediments become finer and the horizontal difference of sediments facies is obvious. The deposition evolution experienced the following stage since 15.6MaB.P.:15.6-9.23Ma, floodplain and fluvial deposition, the "lower red bedding" consists of red mudstone and calcareous mudstone or calcrate with alternate appearance;9.23-7.1Ma, the lake invasion took place in the basin broadly, the "zebra bed" consists of celadon marlite interbeded with red mudstone;Since 7.1Ma, the lake began to shrink in large scale and floodplain developed in vast area of the basin. 7.1-3.6Ma, "upper red bedding" came into being and consisted mainly of red argillaceous beddings and siltstone beddings, moreover, gypsum-salt deposition has been found at the top of "upper red bedding" in some area;About 3.6Ma, affected by the Tibetan Plateau uplift, the south part near the west Qinling in the basin downfaulted and became lake again;3.6Ma-1.4Ma, "upper green bedding" came into being and consists of celadon mudstone interbeded with offwhite marlite;About 1.4Ma, affected by the intense uplift of the Tibetan Plateau, the development history of the lake in the study area ended. After that, the study area began to experience uplift ,denudation, river terraces development and eolian loess deposition.3. At the end of Paleogene, the climate was dry and huge bedding red calcareous cementation sandstone deposited. The climate bacame humid in Miocene obviously. Finegrain fluvial-lacustrine sediments under low energy circumstance were deposited in Linxia Basin in Miocene. The vegetation changed from woodland steppe at the end
of Paleogene to forest in Miocene, which indicated a humid climate. The finegrain fluvial-lacustrine sediments were also deposited in southeast Longxi Basin in Neogene. Large mammals, such as rhinoceros, elephant, deer and antelope, lived in the study area, which showed the climate was humid during this period. But the alternating environment between dry and humid occurred under the humid background. 15.6-9.23Ma, the climate is humid and fluvial process bloomed. 9.23-7.1 Ma, the climate was more humid and the lake expanded. 7.1-3.6Ma, the lake shrunk and climate became dry relatively. Since the climate continued to become drier, gypsum-salt deposition was developed in some areas;After 1.4Ma, the climate became dry and the lake deposition was finished, eolian deposition developed, then, the modern environmental framework came into being.4.Based on the grainsize, geochemistry and microstructure analysis of the sediments deposited during 22-6.2Ma in Guojia, Qin'an, Guo et al (2002) suggested that this set of red beds was eolian loess series. And they deduced that the inner Asian began to dry since 22Ma and this status related to the Tibetan Plateau uplift. But their conclusion is not consistent with other deposition records in the basin at the same period. The detailed contrast and analysis on the QA-I Neogene sediments and Lamashan and Yaodian Neogene lacustrine sediments have been carried out and showed:(1) The comparing analysis on the grainsize characters among QA-I Neogene sediments, Tianshui Neogene fluvial-lacustrine sediments and Quaternary eolian loess showed that the characters of Guojia Neogene sediments is more similar to that of Tianshui Neogene fluvial-lacustrine sediments. Moreover, the frequency and cumulation percentage curves of both sections are more similar, but there is difference between QA-I Neogene sediments and Quaternary eolian loess;In the grainsize scatter figures, two types can be divided obviously: one is QA-I Neogene sediments and Tianshui Neogene lacustrine sediments, the other is Quaternary eolian loess.(2) The geochemistry characters demonstrate that the calcium carbonate content of the yellow-brown "loess" of QA-I Neogene sediments samples may reach 15.76-46.34% or even higher, the silicon dioxide content may reach 29.54-52.26%.
However, there are obvious differences in content between the QA-I Neogene sediments and typical Quaternary eolian loess (CaCO3, general lower than 20%;SiOo, general 55-65%). The content of the calcium carbonate and silicon dioxide in the QA-I Neogene sediments is similar to those in Tianshui Neogene fluvial-lacustrine sediments. Moreover, both of the two sections have the same REE distribution patterns, which have the characters that all are moderately rich in Ce family elements, with negative slopes and negative Eu anomaly.(3) There are much sediments produced by fluvial process in the "loess-paleosol " series of QA-I Section, such as the fine sandstones with horizontal beddings or ripple cross beddings in the mudstone sequence and the marlite with red mud block or gravel inside at the bottom of the section, those belts and thick lens composed mainly by marlite and well-grinded gravel at the top part on the middle of the section, the intraclastic texture and diatom observed by microscope at some segments of the section. Moreover, from Tianshui, which is at the south basin, to Qin'an, the horizontal difference of sediments facies is obvious. For example, the celadon marlite in the "zebra bedding" appears in both of Yangjiadazhuang and Jiaowan, which are 20km away from the QA-I Section, but has lighter color and thinner thickness than that in Tianshui. And we also found many well-buried fossils of big vertebrates, such as rhinoceros and elephant, in the neogene stratum near the QA-I Section in Qin'an. The fact suggested that the climate in that period was quiet mild. According to those theories of taphouomy, it is obvious that those big fossils were not able to be buried at QA-I with the local sediments rate (1.67cm/kyr) in Neogene.The results above indicated that although the appearance of QA-I Neogene section is similar to the Loess-paleosol series, it should be an alternative series which is composed of finegrain mudflat deposition on the margin of the basin, floodplain deposition and those products of pedogenensis in the air.5. The article also discussed the aridification problem in inner Asian. The study showed that the early Neogene climate should be warm and moist in inner Asian. This climate change may relate to the Asian palaeo-monsoon formation. And the palaeo-monsoon origin may relate to the expansion of the Asian marginal sea. Notably,
the fracture and expansion of South China Sea on a large scale at that time provided an important passway for the Asian palaeo-monsoon;About 8Ma, the climate was dry and the red clay deposited, this may relate to the uplift of the Tibetan Plateau;About 2.6Ma, the uplift of the Tibetan Plateau was rapidly and the Asian monsoon established steadily, the climate was dry and the typical eolian loess began to deposit.
引文
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