黄土高原0.8 Ma以来地面抬升的时空特征研究

doi:10.13249/j.cnki.sgs.2012.09.1131

摘要/Abstract

摘要：

根据黄土高原地区黄河阶地的形态特征和成因分析,认为其形成主要是地面抬升所致并且在黄河达到均衡状态下形成,可以推断黄土高原的地面抬升。根据对黄土高原地区黄河0.8 Ma阶地的研究并结合相关文献资料,选取兰州段、黑山峡段、晋陕峡谷段和三门峡段作为典型研究区域,得出黄土高原0.8 Ma以来的地面抬升存在显著的时空特征,即空间特征表现为地面抬升量有西大东小的规律,时间特征表现为地面抬升速率有后期加速趋势、特别是晚更新世以来。并认为黄土高原0.8 Ma以来的地面抬升与青藏高原的构造抬升有成因上的联系。

关键词: 黄土高原, 河流阶地, 0.8 Ma, 地面抬升, 时空特征

Abstract:

The river terrace is one of the direct geomorphic evidences of the surface uplift. By analyzing the characteristics of the Yellow River terraces in Loess Plateau, it is presented that the terraces are mainly tectonic genesis, and formed after the Yellow River reached a quasi-equilibrium state. It is reasonable to use the Yellow River terraces for representing the surface uplift of the Loess Plateau. In the Lanzhou Basin, two fourth terraces of the Yellow River are selected as the study sections, namely the Zaoshugou terrace and the Wuyishan terrace. At the Zaoshugou terrace, the altitude of gravel stratum is 80 m higher than the river level. The top of the gravel stratum is overlain by at least 64 m eolian loess, and the paleosol S₈ is at the bottom of the eolian loess. At the Wuyishan terrace, the altitude of gravel stratum is 140 m higher than the river level. The top of the gravel stratum is overlain by at least 100 m eolian loess, and the paleosol S₈ is at the bottom of the eolian loess. The optically stimulated luminescence (OSL) dating result indicates that the age of the upper part of paleosol S₁ at the Zaoshugou terrace is 70.4±7.6 ka. The results of paleomagnetic dating, optically stimulated luminescence dating and loess-paleosol sequence matching indicate that the two terraces have the same age, and both were formed at about 0.865Ma. Therefore this paper advances that there is the Yellow River terraces at 0.8Ma in the Lanzhou Basin, and the fourth terrace of the Yellow River may be a geomorphic response to the event of the surface uplift at 0.8Ma around the Qinghai-Tibetan Plateau. According to the research on the Yellow River terraces at 0.8Ma in the Loess Plateau and the correlative literature, this paper verifies that there was a large-scale surface uplift at about 0.8Ma in the Loess Plateau, and the surface uplift resulted in river incision and terrace formation. Lanzhou, Heishan Canyon, Shanxi-Shaanxi Canyon and Sanmenxia were also selected as the typical research areas in the Loess Plateau,and obvious spatial and temporal features of the surface uplift of the Loess Plateau since 0.8Ma was discovered, basing on the characteristic analysis of the sequences of the Yellow River terraces at this four sites. The rates of surface uplift are calculated by the rates of river incision and the amounts of surface uplift are calculated by the depth of river incision (height above river). The spatial feature is that the surface uplift of the western Loess Plateau is more intense than that of the eastern Loess Plateau, and the temporal feature is that the uplift speeds up gradually, especially since the late Pleistocene. This paper also proposes that the surface uplift of the Loess Plateau since 0.8 Ma is related to the surface uplift of the Qinghai-Xizang Plateau.

Key words: Loess Plateau, river terrace, 0.8 Ma, surface uplift, spatial and temporal features

中图分类号:

P931

胡春生, 潘保田, 苏怀. 黄土高原0.8 Ma以来地面抬升的时空特征研究[J]. 地理科学, 2012, 32(9): 1131-1135.

Chun-sheng HU, Bao-tian PAN, Huai SU. The Spatial and Temporal Features of Surface Uplift in Loess Plateau Since 0.8 Ma[J]. SCIENTIA GEOGRAPHICA SINICA, 2012, 32(9): 1131-1135.

图/表 6

图1

图2

表1

表2

表3

图3

参考文献 27

[1]	朱照宇,丁仲礼.中国黄土高原第四纪古气候与新构造演化[M].北京:地质出版社, 1994.
[2]	赵景波. 黄土高原发展过程中的五大转折[J].水土保持学报, 2002,16(1): 132~135.
[3]	李荣全,邱维理,张亚力,等.对黄土高原的新认识[J].北京师范大学学报(自然科学版),2005,41(4):431~436.
[4]	杨东,方小敏,彭子成,等. 陇西六盘山黄土及最近1.8 Ma B.P.以来的构造运动与气候变化[J].地理科学,2006,26(2): 192~198.
[5]	潘保田,李吉均,李炳元.青藏高原地面抬升证据讨论[J].兰州大学学报(自然科学版),2000,36(3):100~111.
[6]	潘保田,邬光剑,王义祥,等.祁连山东段沙沟河阶地的年代与成因[J].科学通报,2000,45(24):2669~2675.
[7]	Li Jijun,Zhang Bao,Zhu Junjie,et al.Magneto-and pedo-stratigraphy of paleosol-loess sequences in the Lanzhou Basin:evidence for evolution of Huang He[J].Chinese Science Bulletin,1999,44(supplement): 119-128.
[8]	Maddy D.Uplift-driven valley incision and river terrace formation in southern England[J].Journal of Quaternary Science,1997,12(6):539-545.
[9]	Bridgland D,Schreve D C.Implication of new Quaternary uplift models for correlation between the Middle and Upper Thames terraces sequences,UK[J].Global and Planetary Change,2009,68(4):346-356.
[10]	Tabito Matsu’ura,Akira Furusawa,Hidetaka Saomoto.Late Quaternery uplift rate of the northeastern Japan arc inferred from fluvial terraces[J].Geomorphology,2008,95(3-4):384-397.
[11]	Claessens L,Veldkamp A,Broeke E M,et al.A Quaternary uplift record for the Auckland region,North Island,New Zealand,based on marine and fluvial terraces[J].Global and Planetary change,2009,68(4):383-394.
[12]	Arger J, Mitchell J, Westaway R.Neogene and quaternary volcanism of south-eastern Turkey[C]//Bozkurt E, Winchester J A,Piper J D A (Eds.).Tectonics and Magmatism of Turkey and the Surrounding Area.London:Geological Society of London Special Publication,2000:173,459-487.
[13]	Maddy D,Bridgland D R,Westaway R.Uplift-driven valley incision and climate-controlled river terrace development in the Thames Valley,UK[J].Quaternary International,2001,79(1):23-36.
[14]	Burbank D W.Rates of erosion and their implications for exhumation[J].Mineralogical Magazine, 2002,66(1):25-52.
[15]	潘保田. 黄河发育与青藏高原隆升问题[D].兰州:兰州大学,1991.
[16]	沈玉昌,龚国元.河流地貌学概论[M].北京:科学出版社,1986.
[17]	Ding Z L,Derbyshire E,Yang S L,et al.Stacked 2.6Ma grain size record from the Chinese loess based on five sections and correlation with the deep-sea δ18O record[J].Paleoceanography,2002,17(3):501-521.
[18]	邢成起,尹功明,丁国瑜,等.黄河黑山峡阶地的砾石Ca膜厚度与粗碎屑沉积地貌面形成年代的确定[J].科学通报,2002,47(3):167~172.
[19]	王均平. 黄河中游晚新生代地貌演化与黄河发育[D].兰州:兰州大学博士论文,2006.
[20]	潘保田,王均平,高红山,等.河南扣马黄河最高阶地古地磁年代及其对黄河贯通时代的指示[J].科学通报,2005,50(3):255~261.
[21]	苏怀,王均平,潘保田,等.黄河三门峡至扣马段的阶地序列及成因[J].地理学报,2009,63(7):745~750.
[22]	韩文峰. 黄河黑山峡大柳树松动岩体工程地质研究[M].兰州:甘肃科学技术出版社,1993.
[23]	雷祥义. 黄土高原地质灾害与人类活动[M].北京:地质出版社,2001.
[24]	崔之久,伍永秋,刘耕年.昆仑-黄河运动的发现及其性质[J].科学通报,1997,42(18):1986~1989.
[25]	李吉均,方小敏,马海洲,等.晚新生代黄河上游地貌演化与青藏高原隆升[J].中国科学(D)辑, 1996,26(4):316~322.
[26]	李吉均,方小敏,潘保田,等.新生代晚期青藏高原强烈隆起及其对周边环境的影响[J].第四纪研究,2001,21(5):381~391.
[27]	潘保田,高红山,李炳元,等.青藏高原层状地貌与高原抬升[J].第四纪研究,2004,24(1):50~58.

地点	阶地序	拔河高度(m)	年代 (Ma)	定年方法	数据来源
兰州	T4	80~140	0.865	古地磁	自测
黑山峡	T9	140	0.742	钙膜	[18]
河曲	T3	100	0.787	古地磁	[19]
吴堡	T5	130	0.787	古土壤	[19]
吴堡	T5	109	0.85	古土壤	[1]
禹门口	T5	127	0.85
韩城	T5	74	0.85
三门峡	T4	70	0.865	古地磁	[20]
三门峡	T4	50	0.86	古地磁	[21]

地点	阶地序	拔河(m)	年代(Ma)	定年方法	数据来源
兰州段	T4	140	0.865	古地磁	自测
	T3	70	0.141	TL	[7]
	T2	25	0.05	¹⁴C
	T1	10	0.01	¹⁴C
黑山峡段	T9	140	0.742	钙膜	[18]
	T8	120	0.495	钙膜
	T7	95	0.36	钙膜
	T6	85	0.285	钙膜
	T5	80	0.215	钙膜
	T4	73	0.139	钙膜
	T3	55	0.094	钙膜
	T2	30	0.018	钙膜
	T1	13	0.005	¹⁴C	[22]
晋陕峡谷段	T3	100	0.787	古地磁	[19]
	T2	60	0.336	古土壤
	T1	10	0.06	TL
	T5	130	0.787	古地磁
	T4	110	0.412	古土壤
	T3	70	0.245	古土壤
	T2	30	0.129	古土壤
	T1	10	0.06	TL
三门峡段	T4	70	0.865	古地磁	[20]
	T3	30	0.625	古地磁	[19]
	T2	12	0.129	TL	[21]
	T1	5	0.06	TL	[21]