Coupling Processes of Xunhua-Hualong Basin-Orogenic Belt Since Late Cretaceous: Evidence from Apatite Fission Track Geochronology and Source Analysis
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摘要: 循化-化隆盆地新生代沉积及盆地基底和周缘山系磷灰石裂变径迹年代学分析揭示了青藏高原东北缘晚白垩世以来经历过3期隆升剥露事件: (1)盆地基底及拉脊山和西秦岭北缘构造带磷灰石裂变径迹年龄分析普遍记录了晚白垩世-始新世中期相对快速的区域性的隆升剥露事件, 西秦岭北缘快速抬升的起始时间为84Ma, 受控于向北的逆冲抬升; 向北到循化-化隆盆地中部的拉目峡抬升的起始时间为69Ma; 更北的拉脊山一带快速抬升期主要为40~50Ma, 从而反映晚白垩世-始新世中期的快速抬升由南向北逐渐扩展.这一期构造隆升事件导致循化-化隆盆地和临夏盆地缺失了北部西宁-民和盆地古近纪所具有的西宁群沉积.隆升剥露结束于31Ma左右, 此时化隆-循化盆地向东与同时期的临夏盆地相连为一个统一的大型西秦岭山前盆地, 两者具有相同的构造、沉积演化史, 因此循化-化隆盆地他拉组底部地层年龄最老不会超过临夏盆地最老地层的古地磁年龄, 即29Ma.(2)渐新世晚期约26Ma拉脊山开始双向逆冲隆升, 并可能延续到中新世早期约21Ma, 隆升作用使循化-化隆盆地成为挟持于拉脊山逆冲带和西秦岭构造带之间的山前挤压型前陆盆地, 循化-化隆盆地开始大规模沉积巨厚的他拉组冲积扇相粗碎屑岩.(3)通过循化-化隆盆地咸水河组和临夏组的沉积相分析、古流方向和砾石成分分析, 揭示出拉脊山构造带在中新世8Ma左右发生的最大规模的双向逆冲隆升事件, 这次事件直接导致循化-化隆盆地由前陆挤压盆地转变为山间盆地, 形成现今青藏高原东北缘的盆山地貌基本格局.Abstract: Xunhua-Hualong basin Cenozoic sedimentary strata, basement and surrounding mountains analysis of apatite fission track geochronology reveals the Northeast margin of Qinghai-Tibet plateau experienced three periods of uplift and exhumation events since Late Cretaceous: (1) Basin basement, Laji mountain and West Qinling orogenic belt apatite fission track ages generally record a Late Cretaceous-Eocene relatively rapid regional uplift and exhumation event. Northern margin of West Qinling rapidly uplift at 84Ma, which was controlled by the uplift of the northward thrust; to the North Lamu Gorge in central of Xunhua-Hualong basin uplift at 69Ma; further north rapid uplift stages along Laji mountain is mainly between 40-50Ma, reflecting Paleocene-Eocene rapid uplift gradually extending from south to north. This tectonic uplift event resulted in Xunhua-Hualong basin and Linxia basin missing Paleogene Xining group sedimentary strata that deposits in northern Xining-Minhe basin. The first period of uplift and exhumation ended at about 31Ma, when Xunhua-Hualong basin connected with eastern Linxia basin to a large unified foreland basin of West Qinling, both experience the same tectonic and sedimentary evolution history, therefore Cenozoic oldest Tala group sedimentary strata age in Xunhua-Hualong basin won't exceed the oldest sedimentary strata with Paleomagnetic age of 29Ma in Linxia basin. (2) Late Oligocene about 26Ma Laji mountain began bi-directionally thrust-uplift and may have continued to Early Miocene about 21Ma, and uplifting made Xunhua-Hualong basin become piedmont extrusion foreland basin between Laji mountain and West Qinling, when Xunhua-Hualong basin began to deposit Tala group alluvial fan of thick coarse clastic rocks. By analyzing sedimentary facies, the ancient flow direction and gravel composition of Xianshuihe group and Linxia group sedimentary strata in Xunhua-Hualong basin, it is concluded that Laji mountains experienced the largest bi-directional thrust-uplift event in the Miocene about 8Ma, which led directly to the event of Xunhua-Hualong piedmont extrusion foreland basin turning into mountain basin, which formed basic pattern of basin-mountain landform in northeastern margin of Qinghai-Tibet plateau nowadays.
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Key words:
- Xunhua-Hualong basin /
- source /
- fission-track /
- Laji mountain /
- West Qinling
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图 1 青藏高原东北缘构造分区(a)、研究区地质简图(b)和样品分布图(c)
1.第四系；2.新近系；3.古近系；4.白垩系；5.三叠系；6.二叠系；7.奥陶系；8.寒武系；9.元古太古界；10.三叠纪侵入岩；11.奥陶纪石英闪长岩；12.奥陶纪花岗闪长岩；13.主要逆冲断层；14.一般断层；15.裂变径迹采样位置；16.剖面位置
Fig. 1. Tectonic framework of northeast Qinghai-Tibet plateau (a), Geological sketch map (b) and sample locations of research area (c)
图 2 循化县渐新统-上新统地层序列(据张楗钰等，2010修改)
Fig. 2. Stratigraphic sequence of Oligocene-Pliocene in Xunhua
图 3 循化-化隆盆地他拉组时期砾石成分及古流向分布
Fig. 3. Distribution of gravel composition and paleocurrent direction during Tala formation in Xunhua-Hualong basin
图 4 循化-化隆盆地他拉组时期砾石层及砾石形态
a.循化县南T50-2，他拉组下部层位的复成分砾岩层；b.循化县南T50-3，他拉组上部含砾砂岩层，砾石层减少，砂岩层比例增大；c.积石镇剖面第4层，冲积扇相的扇根沉积，叠瓦状砾石；d.积石镇剖面第7层，紫红色砂岩层夹砾石层
Fig. 4. Map showing gravel layer and gravel shape during Tala formation in Xunhua-Hualong basin
图 5 循化-化隆盆地咸水河组和临夏组柳树段时期砾石成分及古流向分布
Fig. 5. Distribution of gravel composition and paleocurrent direction during Xianshuihe formation and Linxia Liushu segment in Xunhua-Hualong basin
图 6 砂岩样品的碎屑磷灰石裂变径迹年龄峰值分布
红线为实际年龄分布，蓝线为二项式拟合峰值年龄分布
Fig. 6. Peak fitting and distributions of sandstone detrital apatite fission track dating ages
图 7 尕楞口磷灰石裂变径迹年龄-高程曲线
Fig. 7. Profile of Galengkou apatite fission track age-elevation
图 10 循化-化隆盆地地层角度不整合接触关系及逆冲褶皱构造
a.西南缘隆务峡三叠系复理石建造向北逆冲于他拉组紫红色复成分砾岩层上；b.中部拉目峡紫红色他拉组角度不整合沉积于化隆岩群基底之上；c.循化县附近山顶紫红色他拉组角度不整合沉积于白垩纪河口群灰紫红色砂砾岩层之上；d.西秦岭构造带尕楞口的隆务河群砂板岩背斜褶皱(SW翼缓NE翼陡)
Fig. 10. Map showing stratigraphic angular unconformity and thrust fold in Xunhua-Hualong basin
图 11 青藏高原东北缘循化-化隆盆地新生代的形成演化与盆地周缘山系隆升过程
Fig. 11. Schematic diagram on cenozoic formation and evolution of Xunhua-Hualong basin and uplifting of surrounding mountains in Northeast Qinghai-Tibet plateau
表 1 循化-化隆盆地磷灰石裂变径迹样品及年龄测试结果
Table 1. Apatite fission track dating ages in Xunhua basin
采样位置 样品号 高程(m) 颗数(N) ρd (106cm-2) (Nd) ρs (105cm-2) (Ns) ρi (105cm-2) (Ni) U (μg·g-1) P(χ2) (%) P1 (Ma±1σ) (%) P2 (Ma±1σ) (%) P3 (Ma±1σ) (%) 中值年龄(Ma±1σ) 岩性 拉目峡 T51-1 2705 15 3.449(3524) 19.0(705) 16.3(606) 58 45.3 69.0±4.8 砂岩 T51-2 2698 15 3.431(3520) 6.69(297) 7.82(326) 23 79.2 50.6±4.7 片麻岩 T51-3 2567 15 3.413(3516) 24.4(2007) 26.0(2138) 89 1.4 54.6±3.4 片麻岩 T51-4 2425 15 3.396(3511) 7.57(635) 10.2(854) 34 1.7 42.7±3.6 片麻岩 T51-5 2303 15 3.378(3507) 6.02(377) 7.12(446) 24 53.6 49.2±4.0 片麻岩 T51-6 2195 15 3.360(3503) 7.21(398) 10.6(587) 38 4.7 39.3±3.7 混合花岗岩 T51-7 2115 15 3.343(3498) 9.98(581) 18.4(1070) 67 0 31.0±2.9 片麻岩 西秦岭尕楞口 T51-9 2624 50 3.325(3494) 28.1(4982) 16.9(2989) 62 0 69.3±6.8(22.3) 97.0±8.0(57.2) 144.4±18.9(20.5) 97.0±5.9 砂岩 T51-10 2703 51 3.307(3490) 17.7(4862) 10.2(2817) 38 0 60.6±5.1(9.5) 95.1±6.3(9.5) 121.7±9.3(35.2) 98.5±5.8 砂岩 T51-11 2794 55 3.289(3486) 16.1(4681) 7.50(2178) 29 0 55.7±8.7(7.2) 112.7±12.6(56.2) 146.9±24.7(36.2) 118.8±6.9 砂岩 T51-12 2959 50 3.272(3481) 23.8(4332) 13.9(2531) 52 0 73.5±5.6(32.1) 109.6±6.5(67.9) 96.2±5.6 砂岩 T51-13 3097 15 3.254(3477) 34.3(2100) 26.0(1591) 97 0.1 73.9±4.0 花岗岩 T51-14 3205 50 3.236(3473) 11.3(2753) 7.15(1741) 27 53.7 88.0±4.6(100) 88.0±4.6 砂岩 拉脊山 T53-1 3670 15 3.219(3468) 28.5(1926) 15.2(1029) 58 24.5 103.4±5.9 花岗闪长岩 T53-4 3700 50 3.165(3456) 6.09(1048) 5.65(972) 22 28.5 50.1±6.4(51.6) 71.9±10.9(48.4) 59.9±4.0 砂岩 T53-5 3603 48 3.148(3451) 6.95(1185) 7.29(1243) 27 11.8 40.7±2.7(92) 81.2±15.0(8) 43.2±3.1 砂岩 T53-6 3480 15 3.112(3443) 2.87(199) 3.49(242) 14 95.6 44.2±4.6 花岗斑岩 T53-8 3227 51 3.077(3434) 6.44(1134) 6.96(1225) 28 91.6 49.1±2.9(100) 49.1±2.9 砂岩 T53-10 2935 50 3.041(3426) 9.14(1373) 11.6(1744) 46 0 25.8±4.5(23.6) 43.7±3.3(70.3) 81.9±13.2(6.1) 40.4±2.9 砂岩 注：N样品测试颗粒数；ρd铀标准玻璃径迹密度，Nd铀标准玻璃诱发径迹数；ρs自发径迹密度，Ns自发径迹数；ρi诱发径迹密度，Ni诱发径迹数；P(χ2)自由度为N-1时χ2值的概率. 
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