Thermal Evolution History and Its Genesis of the Ailao Shan-Red River Fault Zone in the Ailao Shan and Day Nui Con Voi Massif during Oligocene-Early Miocene
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摘要: 哀牢山-红河断裂带范围内样品热史演化的系统构建工作偏少；部分学者往往将样品的冷却年龄简单地归因于断裂带的事件年龄，而没有考虑热扰动因素，致使以往研究结论仍然存在分歧及不合理之处.利用断裂带中高温测年资料，构建了T-t变化曲线，结合压力-温度-深度(P-T-D) 变化趋势及地层恢复，对T-t变化的成因提出了较为合理的解释.中高温热史演化表明断裂带SE端(大象山段) 与NW端(哀牢山段) 皆经历2期冷却过程；在地层剥蚀或构造剥露作用诱导下，SE端、NW端于32~30 Ma、32~22 Ma分别经历第1期冷却过程，而其在26~24 Ma、22~20 Ma分别经历的第2期冷却过程中，由于断裂活动减弱这一因素，致使该期冷却速率明显增大(尤其是断裂带NW端).伴随着印支地块的顺时针旋转挤出，断裂带中南部左旋转换拉张构造活动向北迁移.在断裂带T-t演化的第1个阶段内，受断裂带转换拉张强度NW向减弱的影响，断裂带SE端正断活动所致的山体隆升效应明显强于NW端，致使SE端样品冷却过程较早，同时冷却速率明显偏大；而在第2个阶段，伴随着青藏高原进入中新世早期的隆升阶段，作为高原东南缘板块调节边界的哀牢山-红河断裂带其活动性由SE端开始减弱，使得冷却过程由SE端向NW端传递.Abstract: In spite of much research focused on thermal evolution history-tectonic activity of the Ailao Shan-Red River fault zone (ASRR) during Late Oligocene-Early Miocene, its thermal reconstruction is limited. Moreover, the related thermal disturbance factors are often ignored and the measured ages (cooling ages) are generally irrationally recognized as the timing of tectonic events in the existing studies. Combined with the pressure-temperature-depth paths (P-T-D) and paleogeomorphology reconstruction, the T-t paths of the ASRR are constructed to explore the genesis of T-t paths and the evolutionary characteristics of the fault zone systematically. The cooling process of the metamorphic massif can be divided into two phases: for Day Nui Con Voi is 32-30 Ma and 26-24 Ma, while for the Ailao Shan is 32-22 Ma and 22-20 Ma. In the first phase, the rapid cooling may have been caused by the strata denudation or tectonic denudation, followed by the more rapid cooling of the second phase, in which the intensity weakening of the fault has been more dominant, compared with the denudation and other factors. With the clockwise rotation and extrusion of the Indochina terrane relative to the South China block, the sinistral tensile transformation zone in the south propagated northwards. Additionally, the spatial differences in the tectonic activities induced the varied cooling processes for the southeastern and northwestern part. In phase Ⅰ, the tectonic uplift in the southeastern part presented earlier and stronger than the northwestern one, with the northwestward propagation and weakening of the sinistral tensile transformation. So the cooling process of the southeastern part was much earlier and more rapid, compared with the northwestern process. In phase Ⅱ, the activity of the ASRR which acted as the boundary of the plate extrusion became weak northwards, along with a new period of Tibet uplift in early Miocene. Then the change stimulated another rapid cooling process, showing the northwestward decreasing trend.
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图 1 哀牢山-红河断裂带大地构造背景(a)，哀牢山-红河断裂带及附近区域地质简图(b) 和哀牢山-红河断裂带地质构造图(c)
1.第四纪；2.第三纪；3.元古界变质岩群；4.第三纪花岗岩体；5.中生代火成岩体(?)；Ⅰ.华南陆块，Ⅱ.印支地块，Ⅲ.掸泰地块，Ⅳ.西缅地块；A.楚雄盆地，B.思茅盆地，JBS.金沙-奔子栏缝合线，YZS.雅鲁藏布江缝合线，MS.密支那缝合线，IS.印缅缝合线，CMS.昌宁-孟连缝合线，US.程逸缝合线，SS.马江缝合线，SF.实皆断裂，XSH-XJF.鲜水河-小江断裂，DBPF.奠边府断裂；图b据Leloup et al.(2001b)，Gilley et al.(2003)，Cao et al.(2011b)和Lin et al.(2012)
Fig. 1. The tectonic setting of the ASRR (a), simplified geological map showing the ASRR and surrounding areas (b), and map showing the main geological structure of the ASRR (c)
图 2 哀牢山-红河断裂带高温年龄(T封闭＞700 ℃) 样品分布及年龄值
(1)~(8) 代表分别引自Gilley et al.(2003)、Garnier et al.(2005)、李宝龙等(2009)、Searle et al.(2010)、Lin et al.(2012)、Tang et al.(2013)、王冬兵等(2013)、廖震等(2014)片岩、片麻岩、大理岩及花岗岩中锆石及独居石U-Pb年龄值
Fig. 2. The localities and ages (closure temperature > 700 ℃) of the samples in the ASRR
图 3 哀牢山-红河断裂带中温年龄(700 ℃＞T封闭＞200 ℃) 样品分布及年龄值
a~e代表分别引自Harrison et al.(1996)、Wang et al.(1998, 2000)、张进江等(2006)、李宝龙等(2009)片麻岩、角闪岩、花岗岩、混合岩、糜棱岩中角闪石、白云母及黑云母40Ar/39Ar年龄值
Fig. 3. The localities and ages (closure temperature is between 200 ℃ and 700 ℃) of the samples in the ASRR
图 4 哀牢山-红河断裂带自NW-SE样品年龄变化趋势
样品冷却年龄变化趋势(红线) 为线性拟合结果
Fig. 4. The change trends of dating data of the samples which are located in the ASRR from NW to SE
图 5 哀牢山-红河断裂带哀牢山-大象山段典型点位T-t (300 ℃＜T＜800 ℃) 变化曲线
Fig. 5. T-t paths (300 ℃ < T < 800 ℃) of several typical samples from the ASRR
图 6 据哀牢山北端YU20、YU21、YU24及YU86样品构建的P-T-D曲线
Ky.蓝晶石，Sill.夕线石，And.红柱石；底图据Leloup et al.(1995, 2001a)，Gilley et al.(2003)和宋志杰(2008)；红色线为Leloup et al.(1995, 2001a) 据YU20、YU21样品构建的变质作用演变曲线，紫色虚线为笔者根据Gilley et al.(2003)YU86样品构建的变质作用演变曲线
Fig. 6. P-T-D deformation paths for sample YU20, YU21, YU24 and YU86 from the northern Ailao Shan
图 7 红河县旧哈龙一带中新统沉积-构造剖面(a) 和地层恢复模式示意图(b)
图a据王二七等(2006)，测线位置LL'如图 1c中所示；图b中d1为现今哀牢山在红河县附近的山体宽度，取值19.3 km (据张进江等，2006)，其中60°和80°为山体东西两侧的倾斜角度(据Searle et al., 2010)，S0为堆积在哀牢山体东侧的中新世地层，S1和h1为中新世之后地层覆盖在现今山体之上的横截面积和高度，d2为中新世之后地层恢复的古山体宽度，S2和h2分别为中新世地层覆盖在山体之上的横截面积和高度
Fig. 7. Structural-sedimentary cross section of the Miocene strata in Jiuhalong area of Honghe county (a), and sketch map of the strata reconstruction (b)
图 8 哀牢山-红河断裂带哀牢山-大象山段典型点位T-t变化与印度板块运动速度及方向、青藏高原隆升期次、E-W向扩展及富钾碱性岩浆活动时间的对比
富钾碱性岩浆活动的年龄数据来源于Wang et al.(2001a)和Lu et al.(2012)
Fig. 8. The contrast between the T-t paths (300 ℃ < T < 800 ℃) determined from several samples in the (SE/NW) ASRR and the variation of the velocity and direction of movement of the Indian plate, the tectonic uplift and E-W extension of the Tibetan Plateau, and the ages of regional potassic alkaline rocks near the ASRR
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