|
|
|
题名
|
作者
|
年代
|
出处
|
被引量
|
| 1 | Magnetostratigraphy and paleoenvironmental record of Tertiary deposits of Lanzhou Basin显示文摘The Tertiary deposits of the Yongdeng section, the Lanzhou Basin were studied by means of magnetostrati-graphy. The magnetostratigraphic sequences from Paleocene to Miocene were established, and the time scale for the corresponding stratigraphy and mammalian faunas was also established by referring to their correlation to the GPTS of BKSA95 (The geomagnetic polarity time scale which was thoroughly revised and updated by Berggreen et al. in 1995). In the end the paleoenvironmental records and their relationship with the uplifting of the Tibetan Plateau were discussed. The results are as follows. The top boundary of the Xiliugou Formation is dated to be 51 Ma, i.e. Eocene. TheYehucheng Formation covers the time span of 51-31.5 Ma, i.e. from late Early Eocene to early Early Oligocene. The Xianshuihe Formation covers the time span of 31.5-15 Ma, i.e. from Early Oligocene to Middle Miocene. The lower member of the Xianshuihe Formation spans from 31.5 to 20.0 Ma, i.e. from Early Oligocene to early Early | YUE Leping F.Heller QIU Zhanxiang ZHANG Li XIE Guangpu QIU Zhuding ZHANG Yunxiang | 2001 | Chinese Science Bulletin2001，46，9： | 28 |
| 2 | Assessment on heavy metals pollution of agricultural soil in Guanzhong District显示文摘The monitored soil samples were collected from Heihui irrigated area, Jiaokou irrigated area, Qianhe river valley and Jinghe river valley (hereafter Heihui, Jiaokou, Qianhe and Jinghe for short respectively) of Guanzhong District. According to the Environment Quality Standard for Soil (GB15618-1995II), we evaluated the pollution status of heavy metals (Cd, As, Cr and Pb) that could seriously endanger soil environment and human health by using single-factor index and synthetic pollution index methods. The results indicate that the synthetic pollution indices P of soil heavy metals are less than 0.7 in Heihui, Jiaokou, Qianhe and Jinghe of Guanzhong, the single-factor indices Pi of soil heavy metals of most soil samples are less than 0.7, so the soil environmental quality is in a good condition in Guanzhong on the whole; the enrichment degree of soil heavy metals is in the order of Heihui, Jinghe, Qianhe and Jiaokou; the contaminated degree of soil heavy metals has the feature of Cd > As > Cr > Pb; heavy metals contents in the cultivated horizon soil are generally higher than those in its underlayer soil, heavy metals contents of soil have the characteristic of enriching towards the cultivated horizon; Cd exceeds standard in the soil samples HS07a, b and HS08a, b at the Yangtao orchard in Heihui and in the soil sample QHS01a at the suburban vegetable plot in Qianhe, which was mainly caused by the long-term irrational use of chemical fertilizer and pesticide. | ZHENG Guozhang YUE Leping LI Zhipei CHEN Chao | 2006 | Journal of Geographical Sciences2006，16，1： | 21 |
| 3 | Taxonomy,age and environment status of the Yuanmou hominoids显示文摘The taxonomy, age and environment status of the Yuanmou hominoids had been contro-versial since their discovery. We launched new ex-cavations and investigations in the Yuanmou Basin and analyzed both old and newly collected data. We conclude that all hominoids from the Yuanmou Basin and the so-called Pliocene hominids can be attributed into a single species, and its valid nomination is Lufengpithecus hudienensis. It is different from Lufengpithecus lufengensis and Lufengpithecus kei-yuanensis. Based on the faunal comparison and pa-leomagnetic correlation, the strata yielding the Yuanmou hominoids are older than those of Lufeng hominoids and younger than those of the Kaiyuan hominoids. The age of the Yuanmou hominoids is Late Miocene. The environments of the Yuanmou hominoids were subtropical, hilly, with some dense forestry and partial transitional bushes and seasonal climate. | QI Guoqin DONG Wei ZHENG Liang ZHAO Lingxia GAO Feng YUE Leping ZHANG Yunxiang | 2006 | Chinese Science Bulletin2006，51，6： | 9 |
| 4 | Evolution of the Ordos Plateau and environmental effects显示文摘Based on the analysis of temporary-spatial distribution, geomorphic position, contact relationship with underlying strata and grain size of red clay, we studied the formation and environmental background of red clay. During late Miocene-Pliocene, the Ordos Block finished the transformation from the basin to the plateau, which had an obvious environmental effect on the topography, indicated by the formation of highland undergoing wind erosion and lowland receiving red clay deposits. The red clay materials were sourced from dusts carried by wind energy and covered on the initial topography. Unlike Quaternary loess dust covering the overall the Loess Plateau, red clay deposited on the highland would be transported to the lowlands by wind and fluvial process. As a result, there was no continuous 'Red Clay Plateau' in the Ordos region and red clay was only preserved in former lowlands. However, red clay was discontinuously distributed through the Loess Plateau and to some extent modified the initial topography. The differential uplift in interior plateau is indicated by the uplift of northern Baiyushan, central Ziwuling and southern Weibeibeishan. The Weibeibeishan Depression formed earlier and became the sedimentary center of red clay resulting in the thicker red clay deposits in Chaona, Lingtai and Xunyi. Since Quaternary the aridity in the northern plateau enhanced and accelerated loess accumulation caused the formation of the Loess Plateau. During the late Pleistocene the rapid uplift led to the enhancement of erosion. Especially after the cut-through of Sanme Lake by the Yellow River, the decline of base level caused the falling of ground water level and at the same time the increase of drainage density resulting in the enhancement of evaporation capacity, which enhanced the aridity tendency of aridity in the Loess Plateau region. | YUE LePing LI JianXing ZHENG GuoZhang LI ZhiPei | 2007 | Science China Earth Sciences2007，50，z2： | 8 |
| 5 | Pedogenesis affecting the Matuyama-Brunhes polarity transition recorded in Chinese loess?显示文摘A detailed record of the Matuyama-Brunhes (M-B) transition has been obtained from the loess unit 8 (L8) at Duanjiapo (34.2° N, 109.2° E), Shannxi Province of China. An investigation of the rock magnetic properties using hysteresis loops, thermomagnetic analyses identifies pseudo-single domain magnetite as the main carrier of the rema-nence, with a small contribution from maghemite and hema-tite. The paleo-direction records obtained reveal: ( i ) The M-B transition was recorded in the middle and lower part of L8, and comprises of five fast reversals. (ii) The duration of the M-B polarity transition related to the directional change is about 4800 a. (iii) The virtual geomagnetic pole (VGP) path during the transition is confined over Africa, peaked 90° away from the sampling site, in contrast with the results obtained from the Weinan loess section. The different VGPs are probably attributed to the pedogenesis. | QUO Bin ZHU Rixiang Florindo Fabio PAN Yongxin YUE Leping | 2001 | Chinese Science Bulletin2001，46，12： | 4 |
| 6 | Magnetostratigraphic dating of mammalian fossils in Junggar Basin,northwest China显示文摘The first detailed chronology for the late Oligocene to early Miocene continental record in northern Junggar Basin is presented,based on rock magnetic experiments and magnetostratigraphic investiga-tions of a 192 m thick mammal-bearing section in the Ulungur River area. Magnetites and hematites were identified as the main carriers for the characteristic remanent magnetization,and the resulting polarity sequence allows an unambiguous correlation to the geomagnetic polarity time scale (GPTS). Furthermore,the Tieersihabahe fauna layer occurs below the Paleocene/Neocene boundary,and the Suosuoquan fauna layer is just above the Neocene onset. Therefore,the age of the Tieersihabahe fauna and Suosuoquan fauna layers can be definitely estimated to be about 25.2 Ma and 22.5 Ma,respectively. | ZHANG Rui YUE LePing WANG JianQi | 2007 | Chinese Science Bulletin2007，52，11： | 3 |
| 7 | The ecological sequence of Hipparion fauna in the middle reaches of the Yellow River during Neogene显示文摘The faunal ecological type and sequence in the Tertiary red clay indicate that Hipparion fauna during the period 7.4-6.1 Ma in the middle reaches of the Yellow River is composed mainly of dorcadoides and mixed types. This represents semiarid veld environment with small fluctuation. The fossil assemblages characterized by the abundance of gaudryi types and even the occurrence of some Hominoid and Chalicotherium indicate an obviously warm and humid period since 5.3 Ma. The fossil assemblages during 3.4 Ma show the typical steppe fauna representing dry climate. It is indicated by the changes of ecological sequence that the cli-matic conditions in Pliocene are drier than that in late Mio-cene. The clay-skin content of red clay, which has a syn-chronous change with faunal features, is a rather good re-placing palaeoclimatic index. | ZHANG Yunxiang YUE Leping CAO Hongxia | 2002 | Chinese Science Bulletin2002，47，1： | 3 |
| 8 | Magnetic characteristics and their paleoclimatic significance of Fengzhou loess in the Qinling Mountains of China显示文摘The Fengzhou loess section is very typical in the Qinling Mountains. The section, about 82 m thick and underlain by the Neogene red clay, consists of 33 layers of loess and 33 layers of paleosol. The section covers Brunhes normal polarity zone and Matuyama reversed polarity zone, and the B/M boundary is located in the middle of L\-8. Matuyama reversed polarity zone records Jaramillo, Olduvai and Reunion normal polarity subchrons. The boundary between Matuyama reversed polarity zone and Gauss normal polarity zone (M/Ga) appears in the lithological boundary between loess and the Neogene red clay. Loess accumulation in Fengzhou started before 2.48 Ma. The magnetic susceptibility curve indicates 33 cold_dry and humid_warm cycles of paleoclimatic variation in the Qinling Mountains during the last 2.48 Ma. The above climatic fluctuation may be well compared with that of the oxygen isotopic records from deep_sea deposits. | Xiangyi Lei Leping Yue Jianqi Wang Li Zhang | 1998 | Chinese Science Bulletin1998，43，18： | 3 |
| 9 | A New Model for Correlation between the Marine Benthic Oxygen Isotope and Red Clay Magnetic Susceptibility on the Chinese Loess Plateau显示文摘Objective Aeolian sediments on the Chinese Loess Plateau contain some of the best continental archives of palaeoclimate change in the Late Cenozoic.The consensus that alternating MS in loess-paleosols in China was due to the strengthening and weakening of the East Asian palaeomonsoon provides an excellent climate record when correlated with global ice volume.Significantly,new basal dates from the red clay underlying the loess-paleosol sequence indicate that wind-blown dust began to accumulate on the Chinese Loess Plateau at least | GONG Hujun ZHANG Rui ZHANG Yunxiang YUE Leping | 2017 | Acta Geologica Sinica(English Edition)2017，91，3： | 1 |
| 10 | Chemical characteristics and pollution sources of petroleum hydrocarbons and PAHs in sediments from the Beiluohe River,Northern China显示文摘 | Li Zhang Kelin Shi Leping Yue | 2007 | Environmental Geology2007，53，2： | 1 |
| 11 | Petroleum hydrocarbon contamination in surface sediments of Bei- luohe Basins, China 显示文摘 | Helin Shi Li Zhang Leping Yue | 2008 | Bulletin of Environmental Contamination and Toxicology2008，81，4： | 1 |
| 12 | The Loess in the Qinling Mountains and Its Records of Palaeoenvironmental Changes显示文摘The Fengzhou loess section is very typical in the Qinling Mountains. The section, which is about 82 m thick and underlain by Neogene red clays, consists of 33 layers of loess and 33 layers of palaeosol. It covers the Brunhes normal polarity zone and Matuyama reversed polarity zone, and the B/ M boundary is located in the middle part of loess layer 8 (L8). The loess of the Matuyama reversed polarity zone records the Jaramillo, Olduvai and Reunion normal polarity subchrons. The boundary between the Matuyama reversed polarity zone and Gauss normal polarity zone (M / Ga) appears on the lithological boundary between loess and Neogene red clays. Loess accumulation in the Fengzhou section started before 2.48 Ma B.P. Based on the stratigraphical structure, the material composition and magnetic susceptibility curve of the Fengzhou loess section, the palaeoclimatic changes during the last 2.48 Ma in the Qinling Mountains are subdivided into 66 cold-dry and warm-humid stages, equivalent to 33 climatic cycles. | LEI Xiangyi YUE Leping | 1998 | Acta Geologica Sinica(English Edition)1998，72，4： | 1 |
| 13 | Paleogene-Neogene stratigraphic realm and tectonic-sedimentary evolution of the Qilian Mountains and their surrounding areas显示文摘The Cenozoic uplift of Qilian Mountains is critical to comprehend the uplift and extension of the Tibet Plateau as well as the formation of the first and second steps in China's topography. This study summarized dynamic stratigraphic realm comprehensively on the basis of stratigraphic correlation of different Cenozoic sedimentary basin regions of the Qilian Mountains and adjacent mountains. This facilitated the re-creation of the tectonic-sedimentary evolutionary process of the Qilian Mountains and their surrounding areas. The results indicate that during the Early Paleogene(Paleocene-Eocene), the Qilian Mountains were part of an uplift realm. During the Oligocene, Guide-Xining-Lanzhou-Linxia sag basin at the northern margin of the West Qinling Mountains came into being and was subjected to sedimentation. The Suli Basin located between the North and South Qilian paleo-uplifts began to form and undergo sedimentation. Intracontinental orogenic extrusion and basin detachment occurred at the Qilian Mountains during the Miocene, which caused successive uplifts of various mountains, including the Laji, South Qinghai,Jishi, Liupan, and South Shule Mountains. Until Pliocene, Qilian Mountains uplifted continuously and resulted in the shrink,extinction and being eroded of the basins, and aeolian red clay started to accumulate. | YANG LiRong LI JianXing YUE LePing WANG HongLiang GUO HuaiJun ZHU XiaoHui ZHU Tao DU Kai ZHANG Rui ZHANG YunXiang GONG HuJun | 2017 | Science China Earth Sciences2017，60，5： | 1 |
您所在的机构暂未开通此部分的功能，请联系管理员