吉蘭泰盆地MIS 3階段沉積環(huán)境及生態(tài)環(huán)境研究
發(fā)布時間：2019-05-24 10:56
【摘要】：中國西部地區(qū)存在著大量湖泊,這些分布于干旱-半干旱區(qū)的湖泊能夠敏感地記錄區(qū)域內(nèi)干濕變化、流域生態(tài)演化等豐富的氣候與環(huán)境信息。因此,通過研究不同時期的湖岸堤、湖積階地和高位湖相沉積物等地層地貌證據(jù),可以重建湖面波動歷史和湖泊演化過程,為恢復和理解區(qū)域古環(huán)境提供確切的證據(jù)。而近年來,中國西部地區(qū)部分古湖岸的OSL測年結果似乎在否定該區(qū)基于14C測年的深海氧同位素3階段(下文簡稱"3階段"或"MIS 3時段")高湖岸特征,部分古湖岸的測年結果卻又試圖強化西部地區(qū)3階段氣候環(huán)境不同于全球的區(qū)域特殊性�？梢妼τ谖覈鞑康貐^(qū)3階段時期是否曾普遍發(fā)育古湖泊,在學術界尚存在爭議。前人研究顯示,至少在早于距今60～50 ka之前的某個時段曾經(jīng)存在一個幾乎覆蓋整個吉蘭泰盆地、河套盆地及周邊烏蘭布和沙漠、庫布齊沙漠的"吉蘭泰-河套"古大湖。該古大湖的發(fā)現(xiàn)對深入理解河套地區(qū)晚第四紀黃河演化、區(qū)域氣候特征、烏蘭布和沙漠及庫布齊沙漠的形成演化都具有重要意義。假如該古大湖確實存在,那么本文所研究的吉蘭泰地區(qū)則正處于其西部湖盆之中。雖然前期14C測年結果支持該區(qū)MIS 3階段時期發(fā)育高湖岸,且最高湖岸線形成于早于距今6萬年之前的某個時段,距今5-6萬年之后至全新世期間形成了海拔高程分別為1060-1050、1044-1035 m的一系列湖岸線。但是,在位于現(xiàn)今吉蘭泰鹽湖東岸的烏蘭布和沙漠中的鉆孔中卻未發(fā)現(xiàn)MIS 3階段的沉積物,有研究據(jù)此推斷現(xiàn)今烏蘭布和沙漠覆蓋的地區(qū)于MIS 3時段可能處于風沙環(huán)境�？梢�,吉蘭泰盆地在MIS 3時段的自然環(huán)境狀況尚有待進一步研究。因此,本文在前人研究基礎上,對吉蘭泰鹽湖西岸早先認為可能形成于MIS 3階段的湖岸(海拔高程為1050-1060 m)重新開挖剖面并測定石英OSL年代,并在吉蘭泰盆地邊緣的磴口次級隆起區(qū)鉆取了 81 m深的巖芯,結合磴口次級隆起區(qū)的鉆孔地層序列與OSL測年,試圖揭示吉蘭泰盆地在MIS 3時段是否存在積水環(huán)境,并通過孢粉記錄分析,探討了 MIS 3時段吉蘭泰盆地的生態(tài)環(huán)境。本文得到以下初步認識:(1)早于距今76 ka之前的某個時段,吉蘭泰盆地應當處于深湖環(huán)境,但更可能是距今90 ka之前就存在一個湖水覆蓋吉蘭泰盆地和河套盆地大面積地區(qū)的"吉蘭泰-河套"大湖;在距今76～52 ka時段,吉蘭泰盆地湖水較之前有所降低,盆地的邊緣出現(xiàn)風沙堆積;吉蘭泰盆地的淺湖環(huán)境可能由距今52 ka一直持續(xù)至距今39 ka,其間湖水上漲,但該時段湖面的升高更多的是在青藏高原快速隆升的影響下吉蘭泰湖盆中心自南向北調(diào)整的結果;距今39～13 ka時段,吉蘭泰盆地雖然仍處于湖泊狀態(tài),且湖水在距今23 ka左右再次蔓延至磴口次級隆起區(qū),但此時段湖水主要局限于吉蘭泰盆地內(nèi)部,高湖岸一直處于1060-1050m左右,并且不斷波動,而磴口次級隆起區(qū)可能為出露水面的湖濱環(huán)境,而現(xiàn)今的烏蘭布和沙漠的大面積地區(qū)為風沙環(huán)境;而在13～8 ka時段,黃河從現(xiàn)今烏蘭布和沙漠的東南部注入形成面積較大的古屠申澤。(2)本文賀蘭山前古河道剖面的沉積序列及OSL測年結果表明,在距今57～32ka之間,賀蘭山西麓曾出現(xiàn)大規(guī)模的地表徑流,并為吉蘭泰盆地提供大量的水源,可見此時段,賀蘭山西麓大量降水成因的地表徑流,對于盆地內(nèi)湖面上升也有重要貢獻。(3)MIS 3階段,磴口次級隆起區(qū)鉆孔地層中的孢粉分析結果顯示,該區(qū)沉積的孢粉以藜科、蒿屬、禾本科、香蒲屬、莎草科占優(yōu)勢,且其建群種主要是藜科植物,考慮到這些孢粉的傳輸距離較短,因此認為這種孢粉組合可能暗示MIS 3時段磴口次級隆起區(qū)處于湖泊與荒漠草原共存的狀態(tài),周邊山地可能發(fā)育有云杉林與松林;而吉蘭泰盆地1060 m湖岸線剖面地層序列及孢粉分析結果顯示,此時段最大可能是盆地內(nèi)部發(fā)育淺水湖泊,盆地周邊以荒漠環(huán)境為主,植被發(fā)育可能較差。
[Abstract]:There are a large number of lakes in the western part of China. These lakes, which are distributed in arid and semi-arid areas, can be sensitive to the rich climate and environmental information in the area, such as the change of dry and dry, and the ecological evolution of the river basin. Therefore, by studying the formation and geomorphological evidence such as the lake bank, the lake-area terrace and the high-order lake-phase sediment in different times, the lake wave history and the lake evolution process can be reconstructed, and the exact evidence is provided for the restoration and understanding of the regional paleo-environment. In recent years, the annual results of the OSL in part of the ancient lake in the western part of China appear to have negative characteristics of the high lake shore of the deep-sea oxygen isotope 3 (hereinafter referred to as" "Phase 3" or "MIS 3 period" "), which is based on the 14C dating in the region, The results of the survey in part of the ancient lake have also tried to strengthen the regional particularities of the three-stage climate in the western region. It can be seen whether the ancient lake has been developed in the three-stage period in the western region of China, and there is still a dispute in the academic circles. Previous studies have shown that at least one period before the current of 60-50 ka, there existed a "Glantey-Hetao"-old Great Lakes covering the whole of the Grangtai basin, the Hetao basin and the surrounding Ulana and the desert and the Kubuqi Desert. The discovery of the Great Lakes is of great significance to the deep understanding of the evolution of the Yellow River in the late Quaternary of the Hetao area, the regional climate characteristics, the Ulan Buh and the formation and evolution of the desert and the Kubuqi Desert. If the Great Lakes do exist, the area of the Gillertai area studied in this paper is in the lake basin of the west. Although the early 14C dating results support the development of the high lake shore in the MIS 3 stage of this area, and the highest lake shore line is formed earlier than 60,000 years ago, a series of lake shore lines with elevation elevation of 1060-1050 and 1044-1035m are formed in the period from 5 to 60,000 years from now to the Holocene. However, in the drilling of the Ulaanb and the desert located in the east coast of the current Glantey Salt Lake, there are no deposits in the MIS stage, and it is concluded that the area covered by the Ulaanb and the desert may be in a sandstorm environment during the period of MIS 3. It can be seen that the natural environment in the period of MIS 3 is still to be studied. Therefore, on the basis of the previous research, this paper re-excavated the cross-section of the lake shore (1050-1060m with the elevation of 1050-1060m) in the MIS 3 stage and the quartz-OSL's in the west bank of the Gillantai Salt Lake, and drilled the 81-m-deep core in the secondary uplift area at the edge of the Gillantai basin. Based on the drilling formation sequence and the OSL dating of the secondary raised area of the MIS, an attempt was made to reveal the existence of the accumulated water environment in the MIS 3 period in the Grangtai basin, and through the analysis of the spore-pollen records, the ecological environment of the Jilin-Lantai basin in the 3-time period of the MIS was discussed. The following preliminary recognition is made in this paper: (1) The Gillantai basin should be in the deep lake environment before the 76 ka, but it is more likely that there is a large "Glantey-Hetao" of the lake in the area of the Jilantai basin and the Hetao basin before the 90ka. in that period from 76 to 52 ka, the lake water in the Gillantai basin is lower, and the edge of the basin is sand-laden; the shallow lake environment in the Gillantai basin may last from 52 ka to 39 ka this year, with the lake water rising, But the increase of the surface of the lake is the result of the rapid uplift of the Qinghai-Tibet Plateau and the result of the adjustment from the south to the north of the center of the Grangtai lake basin. The Gillantai basin is still in the lake state for the period from 39 to 13 ka, and the lake water again spread to the secondary raised area of the lake at about 23 ka. But at this time, the lake water is mainly confined to the interior of the Gillantai basin, and the high lake shore is at about 1060-1050m and is constantly fluctuating, while the secondary uplift area of the basin is likely to be the lakeside environment of the exposed water surface, and the large area of the current Ulaanbu and the desert is a sand and sand environment; and in the period of 13 to 8 ka, The Yellow River is injected from the southeast of Ulaan and the desert to form a large area of ancient Tu-Sze. (2) The sedimentary sequence of the section of the ancient river channel of Helan Mountain in this paper and the results of the measurement of the OSL show that a large-scale surface runoff has occurred at the western foot of the Helan Mountain, and a large amount of water source is provided for the Gillantai basin, and the surface runoff of a large number of precipitation causes at the western foot of the Helan Mountain is visible at this time. There is also an important contribution to the rise of the lake in the basin. (3) The results of the pollen and pollen analysis in the drilling formation at the stage of MIS 3 and in the secondary uplift area of the reservoir show that the sporo-pollen in this area is dominant in the family, the genus Artemisia, the Gramineae, the Typha, and the Cyperaceae, and the group of them is mainly the Cycophytes, taking into account that the transmission distance of these sporopollen is short, Therefore, it is considered that this sporo-pollen assemblages may imply that the secondary uplift of MIS 3 is in the state of the coexistence of the lake and the desert steppe, and the surrounding mountains may be developed with the spruce forest and the pine forest, while the stratigraphic sequence and the sporo-pollen analysis results of the 1060m lake line in the Gillantai basin show that, At this time, the largest potential of the section is the development of shallow lake in the basin, and the surrounding of the basin is dominated by the desert environment, and the development of the vegetation may be poor.
【學位授予單位】：蘭州大學
【學位級別】：碩士
【學位授予年份】：2015
【分類號】：P512.2
本文編號：2484807
[Abstract]:There are a large number of lakes in the western part of China. These lakes, which are distributed in arid and semi-arid areas, can be sensitive to the rich climate and environmental information in the area, such as the change of dry and dry, and the ecological evolution of the river basin. Therefore, by studying the formation and geomorphological evidence such as the lake bank, the lake-area terrace and the high-order lake-phase sediment in different times, the lake wave history and the lake evolution process can be reconstructed, and the exact evidence is provided for the restoration and understanding of the regional paleo-environment. In recent years, the annual results of the OSL in part of the ancient lake in the western part of China appear to have negative characteristics of the high lake shore of the deep-sea oxygen isotope 3 (hereinafter referred to as" "Phase 3" or "MIS 3 period" "), which is based on the 14C dating in the region, The results of the survey in part of the ancient lake have also tried to strengthen the regional particularities of the three-stage climate in the western region. It can be seen whether the ancient lake has been developed in the three-stage period in the western region of China, and there is still a dispute in the academic circles. Previous studies have shown that at least one period before the current of 60-50 ka, there existed a "Glantey-Hetao"-old Great Lakes covering the whole of the Grangtai basin, the Hetao basin and the surrounding Ulana and the desert and the Kubuqi Desert. The discovery of the Great Lakes is of great significance to the deep understanding of the evolution of the Yellow River in the late Quaternary of the Hetao area, the regional climate characteristics, the Ulan Buh and the formation and evolution of the desert and the Kubuqi Desert. If the Great Lakes do exist, the area of the Gillertai area studied in this paper is in the lake basin of the west. Although the early 14C dating results support the development of the high lake shore in the MIS 3 stage of this area, and the highest lake shore line is formed earlier than 60,000 years ago, a series of lake shore lines with elevation elevation of 1060-1050 and 1044-1035m are formed in the period from 5 to 60,000 years from now to the Holocene. However, in the drilling of the Ulaanb and the desert located in the east coast of the current Glantey Salt Lake, there are no deposits in the MIS stage, and it is concluded that the area covered by the Ulaanb and the desert may be in a sandstorm environment during the period of MIS 3. It can be seen that the natural environment in the period of MIS 3 is still to be studied. Therefore, on the basis of the previous research, this paper re-excavated the cross-section of the lake shore (1050-1060m with the elevation of 1050-1060m) in the MIS 3 stage and the quartz-OSL's in the west bank of the Gillantai Salt Lake, and drilled the 81-m-deep core in the secondary uplift area at the edge of the Gillantai basin. Based on the drilling formation sequence and the OSL dating of the secondary raised area of the MIS, an attempt was made to reveal the existence of the accumulated water environment in the MIS 3 period in the Grangtai basin, and through the analysis of the spore-pollen records, the ecological environment of the Jilin-Lantai basin in the 3-time period of the MIS was discussed. The following preliminary recognition is made in this paper: (1) The Gillantai basin should be in the deep lake environment before the 76 ka, but it is more likely that there is a large "Glantey-Hetao" of the lake in the area of the Jilantai basin and the Hetao basin before the 90ka. in that period from 76 to 52 ka, the lake water in the Gillantai basin is lower, and the edge of the basin is sand-laden; the shallow lake environment in the Gillantai basin may last from 52 ka to 39 ka this year, with the lake water rising, But the increase of the surface of the lake is the result of the rapid uplift of the Qinghai-Tibet Plateau and the result of the adjustment from the south to the north of the center of the Grangtai lake basin. The Gillantai basin is still in the lake state for the period from 39 to 13 ka, and the lake water again spread to the secondary raised area of the lake at about 23 ka. But at this time, the lake water is mainly confined to the interior of the Gillantai basin, and the high lake shore is at about 1060-1050m and is constantly fluctuating, while the secondary uplift area of the basin is likely to be the lakeside environment of the exposed water surface, and the large area of the current Ulaanbu and the desert is a sand and sand environment; and in the period of 13 to 8 ka, The Yellow River is injected from the southeast of Ulaan and the desert to form a large area of ancient Tu-Sze. (2) The sedimentary sequence of the section of the ancient river channel of Helan Mountain in this paper and the results of the measurement of the OSL show that a large-scale surface runoff has occurred at the western foot of the Helan Mountain, and a large amount of water source is provided for the Gillantai basin, and the surface runoff of a large number of precipitation causes at the western foot of the Helan Mountain is visible at this time. There is also an important contribution to the rise of the lake in the basin. (3) The results of the pollen and pollen analysis in the drilling formation at the stage of MIS 3 and in the secondary uplift area of the reservoir show that the sporo-pollen in this area is dominant in the family, the genus Artemisia, the Gramineae, the Typha, and the Cyperaceae, and the group of them is mainly the Cycophytes, taking into account that the transmission distance of these sporopollen is short, Therefore, it is considered that this sporo-pollen assemblages may imply that the secondary uplift of MIS 3 is in the state of the coexistence of the lake and the desert steppe, and the surrounding mountains may be developed with the spruce forest and the pine forest, while the stratigraphic sequence and the sporo-pollen analysis results of the 1060m lake line in the Gillantai basin show that, At this time, the largest potential of the section is the development of shallow lake in the basin, and the surrounding of the basin is dominated by the desert environment, and the development of the vegetation may be poor.
【學位授予單位】：蘭州大學
【學位級別】：碩士
【學位授予年份】：2015
【分類號】：P512.2
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