An introduction to the Tectonophysics special issue on arc-continent collision processes
An introduction to the Tectonophysics special issue on arc-continent collision processes
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DOI：
10.1016/j.tecto.2009.11.008
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发表时间：
2009-12
期刊：
影响因子：
2.9
通讯作者：
Dennis Brown;Chi‐Yue Huang
中科院分区：
文献类型：
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作者：
Dennis Brown;Chi‐Yue Huang
地球科学基础研究的关键领域之一是沿着构成地球岩石圈的构造板块的边界发生的和今天正在发生的过程。特别重要的是沿会聚板块边界的构造增生和侵蚀过程。当洋内火山弧与大陆-或弧-大陆碰撞边缘碰撞时，导致大陆地壳生长和破坏的主要增生机制之一就发生了（Dewey, 2005； Brown等，2006；Huang等，2006；Zagorevski等，2007）。弧-陆碰撞通常被认为是地质时期大陆地壳生长过程中最重要的过程（Rudnick and Fountain, 1995），也可能在大陆地壳通过俯冲再循环回到地幔中发挥重要作用（Clift and Vannucchi, 2004; Clift et al., in press）。这是乌拉尔山脉（Brown et al., 1998; Brown and Spadea, 1999; Brown et al., 2006）、阿巴拉契亚山脉（van Staal, 1994; Zagorevski et al., 2007）和Variscides （Draut et al., 2002; Dewey, 2005）等古老山带形成的重要过程之一。火山弧和大陆边缘之间的碰撞今天继续沿着构造活跃的板块边界，如西南太平洋或加勒比海（Huang et al., 2006; Harris, 2006; Iturralde-Vinent et al., 2008）。约束良好的化石弧-大陆碰撞造山带提供了第三和第四个维度（深度和时间），这在目前活跃的例子中通常是缺失的，在这些例子中可以观察到俯冲、隆升和侵蚀等构造过程以及地形的形成。对活动造山带和化石弧形大陆造山带的综合研究为了解板块构造在今天是如何运作的，以及它在过去可能是如何运作的提供了关键数据。它还提供了大陆地壳在地质时期是如何生长和被破坏的信息。因此，了解弧-大陆碰撞过程中发生的地质过程，对于我们理解碰撞造山带是如何演化的，以及大陆地壳是如何生长或被破坏的，是非常重要的。此外，弧-陆碰撞带以矿物的形式产生了世界上大部分主要的经济财富（Herrington等人，2005），因此，了解这些构造事件期间发生的过程对于建模这些矿产财富是如何形成和保存的非常重要。弧-陆碰撞造山运动通常是短暂的，持续时间从5世纪到20世纪（Dewey, 2005; Brown et al., 2006），尽管也会发生更长的事件（Gordon et al., 1997）。弧-大陆碰撞造山运动的持续时间取决于碰撞的倾角，
One of the key areas of basic research in the Earth Sciences is processes that occurred, and are occurring today along the boundaries of the tectonic plates that make up the Earth's lithosphere. Of particular importance are the processes of tectonic accretion and erosion along convergent plate boundaries. One of the principal mechanisms of accretion, which leads to continental crustal growth and destruction, occurs when intraoceanic volcanic arcs collide with the margin of a continent—or arc–continent collision (Dewey, 2005; Brown et al., 2006; Huang et al., 2006; Zagorevski et al., 2007). Arc–continent collision is generally thought to have been the most important process involved in the growth of the continental crust over geological time (Rudnick and Fountain, 1995), and may also play an important role in its recycling back into the mantle via subduction (Clift and Vannucchi, 2004; Clift et al., in press). This was one of the important processes in the formation of old mountain belts such as the Urals (Brown et al., 1998; Brown and Spadea, 1999; Brown et al., 2006), the Appalachians (van Staal, 1994; Zagorevski et al., 2007), and the Variscides (Draut et al., 2002; Dewey, 2005). The collision between volcanic arcs and continental margins continues today along tectonically active plate boundaries such as those in the SW Pacific or the Caribbean (Huang et al., 2006; Harris, 2006; Iturralde-Vinent et al., 2008). The well-constrained fossil arc–continent collision orogens supply the third and fourth dimensions (depth and time) that are generally missing from currently active examples where tectonic processes such as subduction, uplift and erosion, and the formation of topography can be observed. The integration of research between active and fossil arc–continent orogens provides key data for the understanding of how plate tectonics works today, and how it might have worked in the past. It also provides information on how the continental crust has grown and been destroyed over geological time. Understanding the geological processes that take place during arc–continent collision is therefore of importance for our understanding of how collisional orogens evolve and how the continental crust grows or is destroyed. Furthermore, zones of arc–continent collision are producers of much of the world's primary economic wealth in the form of minerals (Herrington et al., 2005), so understanding the processes that take place during these tectonic events is of importance in modeling how this mineral wealth is formed and preserved.Arc–continent collision orogeny is generally short-lived, lasting from c. 5 to 20 My (Dewey, 2005; Brown et al., 2006), although much longer events do occur (Gordon et al., 1997). The duration of an arc–continent collision orogeny depends on the obliquity of the collision,