The Tectonic Evolution of the Central Anticline in Western Hubei of China during Mesozoic: Evidences from Apatite Fission Track
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摘要: 鄂西中央背斜带位于扬子陆块扬子碳酸盐台地构造区和川中（鄂西）前陆盆地构造区，构造形迹保存完整，对于研究区域构造演化具有重要的区域优势.根据详细的野外地质调查，结合磷灰石裂变径迹模拟将本区侏罗纪以来的构造活动分为5个主要期次：（1）187.4~180.1 Ma之间的早侏罗世时期，本区地层发生隆升，导致了九里岗组与桐竹园组之间的平行不整合；（2）180.1~115.6 Ma的侏罗纪中晚期至早白垩世，发生区域沉降，并接受陆相碎屑沉积；（3）115.6~78.8 Ma的白垩纪晚期，再次缓慢隆升并遭受剥蚀；（4）78.8~63.6 Ma的白垩纪末至古近纪初，再次发生构造沉降，沉积了白垩系跑马岗组；（5）之后，本区总体处于大幅度构造隆升状态，但2.6 Ma后的第四纪开始有小幅沉降.根据以上构造演化历史，结合平衡剖面技术定量重建了本区区域挤压-伸展过程.Abstract: The central anticline of the western Hubei is located in the tectonic zone of the Yangtze block and the central Sichuan (western Hubei) foreland basin, which possesses important advantages for the study of regional tectonic evolution. In this paper, according to the detailed field geological survey and evidences form apatite fission track simulation, five stages of tectonic activities have been identified:(1) tectonic uplift at 187.4 Ma-180.1 Ma that resulted in the parallel unconformity between the Jiuligang Formation and the Tongzhuyuan Formation. (2) tectonic subsidence and deposition of terrestrial sediments at 180.1 Ma-115.6 Ma. (3) slowl tectonic uplift once again associated with land erosion during 115.6 Ma-78.8 Ma. (4) subsidence again and the deposition of Cretaceous Paomagang Formation during the period of 78.8 Ma-63.6 Ma. (5) followed by great uplift until a small subsidence at 2.6 Ma of the Quaternary. Based on the tectonic evolution and the application of balanced profile technology, the regional tectonic pattern of extrusion-stretching process was established.
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Key words:
- tectonic evolution /
- fission track /
- balanced cross-section /
- Mesozoic /
- western Hubei /
- geochronology
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图 3 研究区野外照
a.斜歪褶皱特征(点1)(镜头方向NW)；b.小型平卧褶皱构造(点2)(镜头方向NW)；c.背斜核部发育的小型北西倾向逆断层(点3)；d.近直立岩层(点4)；e.背斜核部“Z”型褶皱(点5)；f.背斜南东翼斜歪褶皱(点6)
Fig. 3. Field photos of the study area
图 6 样品317裂变径迹单颗粒年龄分布图
Fig. 6. The measured results of fission track dating the sample 317
图 7 样品模拟结果
1.好的热史范围；2.可以接受的热史范围；3.最佳热史路径
Fig. 7. Time-temperature thermal history modele
图 8 样品320裂变径迹单颗粒年龄分布
Fig. 8. The measured results of fission track dating the sample 320
图 9 研究区平衡剖面构造演化
Fig. 9. Balanced cross-section of the study area showing the process of tectonic evolution
表 1 磷灰石裂变径迹测定结果
Table 1. Results of Apatite fission track
样品编号 构造位置 层位 颗粒数
(个)ρs(105/cm2)
(Ns)ρi (105/cm2)
(Ni)ρd(105/cm2)
(N)P(χ2)
(%)中值年龄(Ma)
(±1σ)Pooled年龄(Ma)
(±1σ)L(μm)
(N)317 庆阳坝背斜 S1s 35 3.905(499) 16.66(2 129) 10.197(6 313) 4.30 48±4.0 49±3 12.1±2.1(100) 318 金子山复向斜 T2b2 34 4.482(493) 15.428(1 697) 9.815(6 313) 88.40 58±4.0 58±3 13.1±1.6(107) 319 金子山复向斜 J1t 33 7.366(685) 19.131(1 779) 9.243(6 313) 98.60 73±5.0 73±5 12.5±2.3(102) 320 恩施盆地 K2p2 35 4.155(892) 9.167(1 968) 8.481(6 313) 2.80 77±5.0 78±5 12.1±2.0(100) HC-38 桑植石门复向斜 S 25 6.963(477) 13.124(899) 45.00 92±7.0 11.4±2.3(105) JL-1 石柱复向斜 J2 18 5.437(193) 14.535(516) 5.71 76.7±8.8 11.2±2.4(68) WD-44 华蓥山背斜 J3 28 1.618(153) 5.699(539) 58.70 47.8±7.1 11.5±1.7(59) 注：ρs和ρi分别表示矿物中自发裂变径迹密度和云母外探测记录的矿物中诱发裂变径迹密度；Ns和Ni分别表示所测径迹数量；P(χ2)为检验概率，当P(χ2)＞5%时，通常认为所测单颗粒年龄属于同组年龄，否则，属于不同组年龄组；中值年龄为裂变径迹测定年龄，当单颗粒年龄为0时，用Pooled年龄值；L为平均径迹长度；N为所测径迹条数.HC-38样品数据李双建等(2008)；JL-1、WD-44样品数据梅廉夫等(2010). 
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