Progress of Tectonic Uplift Process in Northern Foothill of Qinling Mountains Based on Constraints of Low-Temperature Thermochronology
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摘要: 秦岭北麓的构造抬升过程对理解区域地质与生态演化具有重要意义.随着地质勘探技术的进步和区域地质研究的深入，秦岭北麓的构造抬升过程逐渐揭示出更多的细节.根据已报道的低温热年代学数据，该区域晚白垩世以来至少发生了3次主要的冷却-隆升事件：晚白垩世（95~75 Ma）的缓慢冷却，冷却速率约2.8 °C/Ma，剥露速率约0.12 km/Ma；始新世-渐新世（47~27 Ma）的快速冷却，冷却速率约6.1 ˚C/Ma，剥露速率约0.24 km/Ma以及晚新生代（10 Ma）以来的持续冷却，冷却速率约 2.1 ˚C/Ma，剥露速率约0.083 km/Ma，剥露抬升的方向呈现出从西南向东北逐渐迁移的趋势.这一迁移趋势与青藏高原东北缘约10~8 Ma的构造扩展密切相关，特别是毗邻的渭河盆地自晚中新世约7.3 Ma以来持续快速沉积、沉降，与秦岭北麓的隆升形成鲜明的构造响应，进一步印证了青藏高原东北缘扩展背景下区域构造活动的联动性与协同演化特征.这些结果表明，新生代以来秦岭北麓构造抬升及相邻渭河盆地沉积演化，均受到青藏高原东北向扩展的影响.这些结果不仅为区域构造动力学研究提供了关键的热年代学约束，也为进一步探讨秦岭北麓地区的地质演化及其与其他区域的构造关系提供依据.Abstract: The tectonic uplift of the northern foothill of the Qinling Mountains is of great significance for understanding its geological and ecological evolution. With the advancement of geological exploration techniques and the deepening of regional geological studies, more details of the tectonic uplift processes of the northern foothill of the Qinling Mountains have been gradually revealed. According to published low-temperature thermochronological data, at least three major cooling and exhumation episodes are revealed since the Late Cretaceous: a slow cooling during the Late Cretaceous (95-75 Ma), with a cooling rate of 2.8 °C/Ma and an exhumation rate of 0.12 km/Ma, a rapid cooling during the Eocene-Oligocene (47-27 Ma), with a cooling rate of 6.1 ˚C/Ma and an exhumation rate of 0.24 km/Ma, and a continuing slow cooling since the Late Miocene(10 Ma), with a cooling rate of 2.1 ˚C/Ma and an exhumation rate of only 0.083 km/Ma, with the cooling and exhumation migrating towards the northeast. This migration trend is closely related to the tectonic expansion of the northeast margin of the Tibetan Plateau at about 10-8 Ma. Meanwhile, the adjacent Weihe Basin has been undergoing rapid sedimentation and subsidence since the Late Miocene (7.3 Ma), forming a distinctive tectonic response to the uplift of the northern foothill of the Qinling Mountains, which further confirms the linkage and synergistic evolution of the regional tectonic activities in the context of the northeastern margin of the Qinghai-Tibetan Plateau. These results indicate that the tectonic uplift of the northern foothill of the Qinling Mountains and the sedimentary evolution of the neighboring Weihe Basin since the Cenozoic have been influenced by the northeastern expansion of the Qinghai-Tibetan Plateau. These results not only provide key thermochronological constraints for the study of regional tectonic dynamics, but also provide a basis for further discussion of the geological evolution of the northern Qinling Mountains and its tectonic relationship with other regions.
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图 2 秦岭北麓及周边地区部分已发表的低温热年代学数据分布
数据来源于附表1，图中年龄峰值由DensityPlotter软件计算；Vermeesch，2012
Fig. 2. Some published distribution of low-temperature thermochronological data in the northern foothill of the Qinling Mountains and surrounding areas
图 5 秦岭地区低温热年代学数据年龄-海拔散点图
a.东秦岭地区低温热年代学AFT数据；b.西秦岭地区低温热年代学AFT数据；c.西秦岭地区低温热年代学AHe数据；R2.趋势线拟合程度的指标
Fig. 5. Age-altitude scatter plot of low-temperature thermochronological data
图 7 秦岭北麓与渭河盆地构造过程示意图
改自Liu et al. 2013；剖面位置参见图1剖面B-B’
Fig. 7. Schematic diagrams of the tectonic processes in the northern foothill of the Qinling Mountains and Weihe basins
图 8 秦岭北麓晚新生代隆升与青藏高原东北缘迁移耦合示意图
地壳、地幔厚度模型引用孟文等，2022；班公湖断裂（56~43 Ma；高天扬， 2023）；金沙江断裂（45~20 Ma45~20 Ma；Zhao et al.， 1993，2011；Kind et al.， 2002；Wang et al.， 2013）；鄂拉山断裂（15 Ma；Yuan et al.， 2011；Lu et al.， 2012；Zhang et al.， 2012）；龙首山断裂（10~5 Ma；Tao et al.， 2025）；秦岭北缘断裂（10~5 Ma；杨鹏等， 2018；Yu et al.， 2022）；渭河盆地沉积（7.3 Ma；Liu et al.， 2013；Yu et al.， 2013）
Fig. 8. Late Cenozoic uplift of the northern foothill of the Qinling Mountains coupled with the migration of the northeastern margin of the Tibetan Plateau
表 1 秦岭北麓及周边地区构造抬升期次汇总
Table 1. Summary of tectonic uplift periods in the northern foothill of the Qinling Mountains and surrounding areas
阶段 时期 区域 年代(Ma) 冷却速率(℃/Ma) 剥露速率(km/Ma) 抬升幅度(km) 引用文献 阶段一 白垩纪 华山 120~80 4* 0.16 6.4 李齐等(2001) 120~70 2.5 0.1* 5* 吴中海等(2003) 125~115 4 0.16 1.6 Wang et al.(2022) 太白山 100~80 3 0.12 2.4 万景林等(2005) 渭河盆地 140~110 1.4* 0.06 1.68 王晓悦(2021) 终南山 130~120 4 0.16 1.6 Wang et al.(2022) 熊耳山 94.1~74 5.6* 0.159* 3.18* 雷万杉等(2025) 阶段二 早新生代 华山 29.26~25.05 4.8 0.183* 0.8* 万景林等(2000) 48~45 4.5* 0.18* 0.54* 尹功明等(2001) 30.5~17.8 2.5 0.1* 1.27* 尹功明等(2001) 32~22 5 0.2* 2* 吴中海等(2003) 65~45 2.5 0.1 2 Wang et al.(2022) 太白山 40~20 2 0.08 1.6 万景林等(2005) 45~35 4 0.16 1.6 Liu et al.(2013) 56~49 7.1 0.28 2 Yu et al.(2022) 25~20 7.5 0.3 1.5 Yu et al.(2022) 渭北隆起 45~32 3.1 0.12 1.61 杨鹏等(2018) 终南山 50~40 6 0.24 2.4 Wang et al.(2022) 熊耳山 57~40 1.2* 0.034* 0.571* 雷万杉等(2025) 40~30 4.5* 0.129* 1.286* 雷万杉等(2025) 阶段三 晚新生代 华山 17.8~0 4.7 0.19* 3.34* 尹功明等(2001) 8~0 4.8 0.19* 1.52 吴中海等(2003) 太白山 10~0 5 0.2 2 Liu et al.(2013) 渭北隆起 7.3~0 2.7 0.12 0.8 杨鹏等(2018) 渭河盆地 20~0 3* 0.12 2.4 王晓悦(2021) 终南山 20~10 4 0.16 1.6 Wang et al.(2022) 熊耳山 30~0 0.17* 0.005* 0.143* 雷万杉等(2025) 天水盆地 23.7~14.1 8.5* 0.34* 3.3* 王修喜等(2006) 14.1~0 26.2 1.05* 14.8 王修喜等(2006) 注：*代表原始数据，未标注的为本文计算所得数据. 
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