柴达木盆地中新世古气候、古环境特征与湖盆生态环境演化

徐鸿彬; 伊帆; 伊海生; 唐闻强; 石宇翔; 陈云; 田康志

doi:10.19509/j.cnki.dzkq.tb20250389

柴达木盆地中新世古气候、古环境特征与湖盆生态环境演化

doi: 10.19509/j.cnki.dzkq.tb20250389

徐鸿彬^1a,,
伊帆^1b, ,,
伊海生^1c,
唐闻强^1c,
石宇翔²,
陈云³,
田康志^1c

1a.
成都理工大学：地球与行星科学学院
1b.
成都理工大学：地理与规划学院
1c.
成都理工大学：沉积地质研究院，成都 610059
2.
湖北省地质调查院，武汉 430034
3.
中国地质科学院，北京 100037

基金项目: 国家自然科学基金项目（41902107；42172121）

详细信息

作者简介:
徐鸿彬：E-mail：1246190255@qq.com

通讯作者:
E-mail：yifan12@cdut.edu.cn

计量
- 文章访问数: 429
- PDF下载量: 41
- 被引次数: 0
出版历程
- 收稿日期: 2025-08-27
- 录用日期: 2026-01-07
- 修回日期: 2025-12-12
- 网络出版日期: 2026-01-07

Miocene paleoclimate, paleoenvironmental characteristics, and lake basin ecological environment evolution in Qaidam Basin

1a.
College of Earth and Planetary Sciences
1b.
College of Geography and Planning
1c.
Institute of Sedimentary Geology, Chengdu University of Technology, Chengdu 610059, China
2.
Hubei Geological Survey, Wuhan 430034, China
3.
Chinese Academy of Geological Sciences, Beijing 100037, China

More Information

Author Bio:
E-mail：1246190255@qq.com

Corresponding author: E-mail：yifan12@cdut.edu.cn

摘要

摘要:
柴达木盆地作为青藏高原东北部新生代规模最大的陆相山间盆地，其中新世所记录的连续完整的湖相沉积序列，为精准重建古环境与湖盆生态演化提供了优质载体。本研究旨在揭示中新世柴达木盆地气候−构造耦合过程对湖盆生态系统演化的控制机制，阐明气候变化与湖盆及流域生态环境演化的协同演变关系。本研究以柴达木盆地一里坪凹陷JS-2井作为研究对象，综合运用元素录井、岩石热解、饱和烃色谱分析等技术手段，从有机质类型、古气候和沉积环境角度，剖析中新世沉积期间湖盆生态环境的演化特征。研究结果表明，下油砂山组下段至上油砂山组沉积期，盆地气候呈现明显干湿波动变化，湖泊沉积环境逐渐贫氧，盐度与水体深度同步发生多次波动，有机质类型以水生植物和陆生高等植物为主。而狮子沟组沉积期，盆地气候持续干旱，湖盆萎缩，湖泊水体盐度分层，沉积环境为强还原状态，陆生有机质输入显著增强，草本植物进一步占据优势。中新世期间，构造演化、气候波动是柴达木盆地湖盆生态环境及植被群落演化的关键所在。下油砂山组下段沉积期干旱化源于全球气候变冷与东昆仑山的初次隆升阻挡了水汽的输入；下油砂山组上部沉积期由于全球变暖与冰盖阶段性的消融强化了季风携带的水汽向盆地输送，促使这一时期气候温暖湿润；上油砂山组沉积期至狮子沟组沉积期，盆地气候转为冷干，且整体呈现急剧干旱化；这一变化主要受全球变冷（南极永久冰盖形成）驱动，加之青藏高原及周缘山脉加速隆升，有效阻断了向柴达木盆地输送的水汽。气候波动通过驱动湖泊水体环境演变，调节流域生产力水平与生态空间格局，最终主导了植被群落的演替过程。
- 柴达木盆地 /
- 元素地球化学 /
- 正构烷烃 /
- 古气候 /
- 古环境
Abstract:
Objective
The Qaidam Basin is the largest Cenozoic continental intermountain basin on the northeastern Qinghai-Xizang Plateau. The continuous and complete lacustrine sedimentary sequence recorded in the Miocene provides a good carrier for the accurate reconstruction of the paleoenvironment and the ecological evolution process of the lake basin. This study aims to reveal the controlling mechanism of the climate–tectonic coupling process on the evolution of the lake basin ecosystem in the Qaidam Basin during the Miocene, and to clarify the synergistic evolution relationship between climate change and the evolution of the lake basin and watershed ecological environment.
Methods
In this study, the Well JS-2 in the Yiliping Sag of the Qaidam Basin was taken as the research object. By comprehensively applying technical methods including elemental logging, rock pyrolysis, and saturated hydrocarbon chromatography analysis, the evolutionary characteristics of the lake basin ecological environment during the Miocene sedimentary period were systematically analyzed from the perspectives of organic matter types, paleoclimate, and sedimentary environment.
Results
The results indicated that during the sedimentary period from the lower member of the Lower Youshashan Formation to the Upper Youshashan Formation, the climate of the basin exhibited obvious fluctuations between arid and humid conditions. Meanwhile, the lacustrine sedimentary environment gradually became hypoxic, with multiple synchronous fluctuations occurring in salinity and water depth, and the organic matter was dominated by aquatic plants and terrestrial higher plants. In contrast, during the sedimentary period of the Shizigou Formation, the basin climate was persistently arid, the lake basin shrank significantly, and the lake water column developed salinity stratification. The sedimentary environment was characterized by a strongly reducing state, the input of terrestrial organic matter increased remarkably, and herbaceous plants further became the dominant vegetation type.
Conclusion
During the Miocene, tectonic evolution and climatic fluctuations were the key drivers of changes in the lake basin ecological environment and vegetation communities in the Qaidam Basin. The aridity during the deposition of the lower member of the Lower Youshashan Formation results from global cooling and the initial uplift of the East Kunlun Mountains, which blocks moisture transport into the basin. During the deposition of the upper member of the Lower Youshashan Formation, global warming and the periodic melting of ice sheets enhance moisture transport by monsoons into the basin, resulting in a warm and humid climate during this period. From the deposition of the Upper Youshashan Formation to the Shizigou Formation, the basin climate shifts to cold and dry conditions, with pronounced aridification across the basin. This change was primarily driven by global cooling (marked by the establishment of a permanent Antarctic ice sheet) coupled with the accelerated uplift of the Qinghai-Xizang Plateau and its surrounding ranges, which effectively obstructs moisture transport into the Qaidam Basin. Based on geological fundamentals, climate fluctuations drive the transformation of the lake aquatic environment, regulate the basin's productivity and ecological space, and ultimately control the succession of vegetation communities.
- Qaidam Basin /
- elemental geochemistry /
- n-alkanes /
- paleoclimate /
- paleoenvironment

HTML全文

图 1 柴达木盆地地质构造图(a)（据文献[25]修改）、160测线位置示意图及地震剖面图(b)（据文献[26]修改）与柴达木盆地新生代地层年代表(c)（据文献[27]修改）

地层符号沿用青海油田公司的惯例，不再具有年龄指示意义

Figure 1. Geological tectonic map of Qaidam Basin (a), seismic profile map of survey line 160 (b), and Cenozoic stratigraphic chronology of Qaidam Basin (c)

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图 2 柴达木盆地JS-2井烃源岩HI与T_max交汇图(a)和S₁与w(TOC)交汇图(b)

R_o. 镜质体反射率；Ⅰ，Ⅱ₁，Ⅱ₂，Ⅲ为干酪根类型

Figure 2. Cross plots of HI versus T_max (a) and S₁ versus w(TOC) (b) of source rocks in Well JS-2, Qaidam Basin

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图 3 柴达木盆地JS-2井正构烷烃分布特征

Figure 3. Distribution characteristics of n-alkanes in Well JS-2, Qaidam Basin

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图 4 柴达木盆地JS-2井烃源岩元素比值剖面图

注：红线为各阶段平均值；蓝线为平滑曲线；剖面平滑采用滑动平均（相邻平均法），窗口为10个数据点

Figure 4. Element ratio profiles of source rocks in Well JS-2, Qaidam Basin

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图 5 柴达木盆地JS-2井烃源岩Pr/n-C₁₇与Ph/n-C₁₈交汇图(a)和Pr/Ph与∑n-C₂₁⁻/∑n-C₂₂⁺交汇图(b)

Figure 5. Cross plots of Pr/n-C₁₇ versus Ph/n-C₁₈ (a) and Pr/Ph versus ∑n-C₂₁⁻/∑n-C₂₂⁺ (b) of source rocks in JS-2 well, Qaidam Basin

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图 6 柴达木盆地JS-2井烃源岩样品w（TOC）及正构烷烃参数随深度变化图（红线为各阶段平均值）

Figure 6. Plot of TOC and n-alkane parameters versus depth for source rock samples in Well JS-2, Qaidam Basin

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图 7 柴达木盆地中新世湖盆生态演化图（构造事件统计据文献[61]修改）

Figure 7. Ecological evolution map of Miocene lake basin in Qaidam Basin

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表 1 柴达木盆地JS-2井烃源岩元素含量及相关参数

Table 1. Element content and related parameters of source rocks in Well JS-2, Qaidam Basin

层位	w(Al)/%	w(Ca)/%	w(Ti)/%	w(Mn)/%	w(Sr)/%	w(Si)/%	w(Fe)/%	Mn/Fe	Ti/Al	Ti/Ca	Ti/Sr	Si/Al
狮子沟组${\mathrm{N}}_2^3 $	$ \dfrac{0.22\sim 5.85}{3.26(351)} $	$ \dfrac{0.76\sim 11.22}{6.64(351)} $	$ \dfrac{0.05\sim 3.08}{0.48(351)} $	$ \dfrac{0.02\sim 0.08}{0.05(351)} $	$ \dfrac{0.02\sim 0.34}{0.06(351)} $	$ \dfrac{0.71\sim 16.44}{9.25(351)} $	$ \dfrac{0.17\sim 3.03}{2.06(351)} $	$ \dfrac{0.02\sim 0.04}{0.02(351)} $	$ \dfrac{0.05\sim 0.89}{0.17(351)} $	$ \dfrac{0.02\sim 0.42}{0.07(351)} $	$ \dfrac{0.68\sim 30.34}{7.30(351)} $	$ \dfrac{2.34\sim 4.13}{2.89(351)} $
上油砂山组${\mathrm{N}}_2^2 $	$ \dfrac{0.52\sim 6.79}{3.94(971)} $	$ \dfrac{1.83\sim 21.23}{7.59(971)} $	$ \dfrac{0.12\sim 3.74}{0.72(971)} $	$ \dfrac{0.03\sim 0.12}{0.06(971)} $	$ \dfrac{0.01\sim 0.42}{0.07(971)} $	$ \dfrac{1.79\sim 17.62}{11.32(971)} $	$ \dfrac{0.68\sim 3.25}{2.24(971)} $	$ \dfrac{0.02\sim 0.06}{0.03(971)} $	$ \dfrac{0.06\sim 1.41}{0.20(971)} $	$ \dfrac{0.02\sim 0.61}{0.10(971)} $	$ \dfrac{1.58\sim 54.82}{11.64(971)} $	$ \dfrac{2.41\sim 4.21}{2.90(971)} $
下油砂山组${\mathrm{N}}_2^1 $	$ \dfrac{0.86\sim 6.89}{4.20(980)} $	$ \dfrac{1.97\sim 20.00}{5.83(980)} $	$ \dfrac{0.35\sim 4.82}{1.14(980)} $	$ \dfrac{0.03\sim 0.12}{0.07(980)} $	$ \dfrac{0.01\sim 0.35}{0.05(980)} $	$ \dfrac{4.20\sim 23.96}{13.44(980)} $	$ \dfrac{0.55\sim 4.39}{2.36(980)} $	$ \dfrac{0.01\sim 0.09}{0.03(980)} $	$ \dfrac{0.09\sim 4.76}{0.33(980)} $	$ \dfrac{0.02\sim 1.82}{0.22(980)} $	$ \dfrac{1.86\sim 74.51}{23.76(980)} $	$ \dfrac{2.47\sim 6.10}{3.28(980)} $
注：$\dfrac{0.22\sim 5.85}{3.26(351)} $表示$ \dfrac{最小值\sim 最大值}{平均值(样品数量件)} $，元素比值均为质量分数比值；下同

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表 2 柴达木盆地JS-2井烃源岩总有机碳w（TOC）及岩石热解相关参数

Table 2. Total organic carbon w(TOC) and rock pyrolysis-related parameters of source rocks in Well JS-2, Qaidam Basin

层位	w(TOC)/%	(S₁+S₂)/(mg·g⁻¹)	HI/(mg·g⁻¹)	T_max/(℃)
狮子沟组${\mathrm{N}}_2^3 $	$ \dfrac{0.30\sim 1.14}{0.53(7)} $	$ \dfrac{0.18\sim 2.91}{0.87(7)} $	$ \dfrac{53.57\sim 126.44}{98.75(7)} $	$ \dfrac{391.00\sim 410.00}{401.29(7)} $
上油砂山组${\mathrm{N}}_2^2 $	$ \dfrac{037\sim 0.83}{0.47(14)} $	$ \dfrac{0.20\sim 1.31}{0.40(14)} $	$ \dfrac{45.46\sim 135.27}{67.74(14)} $	$ \dfrac{371.00\sim 454.00}{411.64(14)} $
下油砂山组${\mathrm{N}}_2^1 $	$ \dfrac{0.32\sim 1.58}{0.68(29)} $	$ \dfrac{0.39\sim 11.47}{1.82(29)} $	$ \dfrac{64.90\sim 544.62}{175.69(29)} $	$ \dfrac{391.00\sim 444.00}{393.97(29)} $
注：w（TOC）为总有机碳质量分数；（S₁+S₂）为生烃潜量；HI为氢指数；T_max为热解最高峰温；下同

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表 3 柴达木盆地JS-2井烃源岩正构烷烃参数

Table 3. n-alkane parameters of source rocks in Well JS-2, Qaidam Basin

层位	ACL_21～33	TAR	CPI	OEP	Pr/n-C₁₇	Ph/n-C₁₈	Pr/Ph	Paq	∑n-C₂₁⁻/∑n-C₂₂⁺
狮子沟组${\mathrm{N}}_2^3 $	$ \dfrac{24.67\sim 27.90}{26.59(7)} $	$ \dfrac{0.25\sim 7.88}{3.86(7)} $	$ \dfrac{1.06\sim 2.99}{1.97(7)} $	$ \dfrac{0.89\sim 5.53}{2.11(7)} $	$ \dfrac{0.51\sim 0.75}{0.67(7)} $	$ \dfrac{0.50\sim 2.38}{1.29(7)} $	$ \dfrac{0.26\sim 0.99}{0.52(7)} $	$ \dfrac{0.32\sim 0.83}{0.52(7)} $	$ \dfrac{0.20\sim 1.62}{0.62(7)} $
上油砂山组${\mathrm{N}}_2^2 $	$ \dfrac{26.10\sim 27.70}{27.10(14)} $	$ \dfrac{0.73\sim 2.48}{1.38(14)} $	$ \dfrac{1.16\sim 2.43}{1.79(14)} $	$ \dfrac{0.85\sim 3.84}{1.72(14)} $	$ \dfrac{0.54\sim 0.95}{0.69(14)} $	$ \dfrac{0.60\sim 3.58}{1.04(14)} $	$ \dfrac{0.30\sim 1.12}{0.84(14)} $	$ \dfrac{0.38\sim 0.55}{0.44(14)} $	$ \dfrac{0.37\sim 0.96}{0.71(14)} $
下油砂山组${\mathrm{N}}_2^1 $	$ \dfrac{23.67\sim 27.05}{26.10(29)} $	$ \dfrac{0.15\sim 2.07}{1.07(29)} $	$ \dfrac{0.77\sim 1.71}{1.41(29)} $	$ \dfrac{0.89\sim 2.61}{1.17(29)} $	$ \dfrac{0.46\sim 1.76}{1.03(29)} $	$ \dfrac{0.44\sim 2.07}{0.96(29)} $	$ \dfrac{0.71\sim 1.38}{1.04(29)} $	$ \dfrac{0.48\sim 0.87}{0.58(29)} $	$ \dfrac{0.43\sim 1.65}{0.79(29)} $
注：ACL_21～33为平均碳链长度，ACL_21～33=(∑[n-C_i]×i)/(∑[n-C_i])(21≤i≤33)；TAR为陆生高等植物与水生植物的比值，TAR=(n-C₂₇+n-C₂₉+n-C₃₁)/(n-C₁₅+n-C₁₇+n-C₁₉)；CPI为碳优势指数，CPI=[∑(n-C₂₅-n-C₃₃)_odd/∑(n-C₂₄-n-C₃₂)_even+∑(n-C₂₅-n-C₃₃)_odd/∑(n-C₂₆-n-C₃₄)_even]/2；OEP为奇偶优势比，OEP=(n-C₂₃+6×n-C₂₅+n-C₂₇)/[4×(n-C₂₄+n-C₂₆)]；Paq为水生植物比例指数，Paq=(n-C₂₃+n-C₂₅)/(n-C₂₃+n-C₂₅+n-C₂₉+n-C₃₁)；Pr/Ph为姥鲛烷与植烷的比值；∑n-C₂₁⁻/∑n-C₂₂⁺为短链正构烷烃与长链正构烷烃比值

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