Evolution Characteristics and Rheological Significance of Dehydration Melting and Water-Fluxed Melting in Deep Continental Crust
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摘要: 深熔作用是链接地壳深部变质作用、构造变形以及岩浆活动的重要纽带，对大陆地壳演化及其流变学性质具有重要意义.根据是否有自由水的参与，深熔作用分为水致熔融和脱水熔融两种机制.脱水熔融主要通过云母、角闪石等含水矿物的分解来实现，其发生所需的温度一般大于650 ℃.在脱水熔融反应中会生成钾长石、石榴石等转熔矿物和部分熔体，该熔体呈水不饱和态，具有高Rb、高Rb/Sr比、高87Sr/86Sr，低Sr、Ba和Ca的特点.其产生的熔体含量主要受温压条件和全岩水含量的影响，在麻粒岩相条件下才有可能产生大量熔体.水致熔融是在含水流体参与下所发生的熔融反应，其最显著的特点就是所需温度较低，在角闪岩相条件下可以生成大量熔体.生成的熔体可以是水饱和或水不饱和，在高温条件下生成的水不饱和熔体具有向上迁移的能力.水致熔融生成熔体的地球化学特征与脱水熔融相反，Sr、Ca、Ba含量较高，Rb、Rb/Sr比较低.深熔作用不仅可以显著改变岩石的热力学和流变学性质，而且熔体的迁移可以促进地壳分异并形成广泛的淡色花岗岩，在陆壳的起源、改造和稳定中起着至关重要的作用.Abstract: Anatexis is significant for the evolution and rheological properties of the continental crust, linking metamorphism, tectonic deformation, and magmatic activities in deep crust. According to the presence or absence of free water, anatexis can be divided into water-fluxed melting and dehydration melting. Dehydration melting involves the breakdown of hydrous phases, such as muscovite, biotite or amphibole. Generally, dehydration melting reactions begin at ~650 ℃ and produce melt, peritectic garnet and K-feldspar. Melt resulting from dehydration melting is water unsaturated, characterized by high Rb, high Rb/Sr ratio, high 87Sr/86Sr ratio, and low Sr, Ba, Ca. Melt productivity of dehydration melting reaction is controlled by P-T condition and water content in rock, and it is only possible to produce a large amount of melt at granulite facies. Water-fluxed melting reactions involve the presence of free water. Its most significant feature is that the temperature required is relatively low, and can produce voluminous melting at amphibolite facies. The resulting melt is water-saturated or water unsaturated that can extract from the source. Melt derived from water-fluxed melting reactions has high Sr, Ba, Ca, low Rb/Sr ratio and low Rb. Anatexis has a profound impact on the thermodynamic and rheological properties of the rocks. At the same time, the movement of melt out of the lower continental crust promotes the chemical differentiation of the crust and forms a wide range of leucogranite, playing a crucial role in the origin, reworking, and stability of the continental crust.
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Key words:
- anatexis /
- water-fluxed melting /
- dehydration melting /
- rheological weakening /
- leucogranite /
- tectonics
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图 1 大陆地壳的深熔作用(修改自Sawyer et al., 2011)
图中显示当温度升高超过固相线时，深部地壳就会发生深熔作用并生成混合岩.熔体首先形成于颗粒边界，沿一条逐渐集中的路径（红色线）从残余固相中分离出来.当有H2O参与熔融时，会降低固相线的温度（蓝色线），使深熔作用更容易发生
Fig. 1. Anatexis of the continental crust (modified from Sawyer et al., 2011)
图 2 水致熔融和脱水熔融反应的对比总结图(修改自Weinberg and Hasalová, 2015)
Fig. 2. Summarizing diagram comparing H2O-present and absent melting reactions (modified from Weinberg and Hasalová, 2015)
图 3 实验得到的不同水致熔融反应(修改自Weinberg and Hasalová, 2015)
虚线2a~2e代表了Qtz+Or+Ab+H2O体系在不同水活度下发生熔融所需的温压条件，红色线代表了变泥质岩的水致熔融反应，绿色反应线代表了变基性岩的水致熔融反应
Fig. 3. Experimentally determined water-fluxed melting reactions (modified from Weinberg and Hasalová, 2015)
图 4 由脱水熔融形成的混合岩的宏观和显微特征
a，b.由脱水熔融形成的混合岩，浅色体与围岩之间具有尖锐的接触边界，存在清晰界定的暗色边缘；c.暗色体中存在石榴石暗色矿物；d.浅色体中存在石榴石；e.变泥质岩中黑云母脱水熔融的逆反应，形成了黑云母与矽线石的交织连晶结构；f.变基质岩中角闪石的脱水熔融，石榴石和辉石共生
Fig. 4. Outcrop and microscopic features of migmatites resulting from dehydration melting
图 5 脱水熔融和水致熔融生成熔体的地球化学特征
a. An-Ab-Or标准三元长石图；b. Rb vs. Sr；c. Sr vs. 87Sr/86Sr（t）；d. Ba vs. Rb/Sr；e. Sr vs. Rb/Sr；f. Nb vs. Ta；b，c中数据来源于Gao et al.（2017）
Fig. 5. Geochemical characteristics of melt resulting from dehydration melting and water-fluxed melting
图 6 副矿物溶解行为对生成熔体的微量元素影响
a. Zr vs. Hf；b. Th vs. U；修改自Gao et al.（2017）
Fig. 6. The effect of dissolution behavior of accessory minerals on the trace elements in the melt
图 7 NCKFMASH体系中泥质岩变质过程中温度与熔体产量的关系(a)和泥质岩和片麻岩在脱水熔融和水致熔融中的熔体产量(b)
a.修改自White et al.（2001）；b.修改自Weinberg and Hasalová（2015）
Fig. 7. The relationship between temperature and melt production of metapelite in NCKFMASH system (a); melt prodution of metapelite and gneiss in dehydration melting or water-fluxed melting (b)
图 8 由水致熔融形成的混合岩的宏观和显微特征
a. 深熔形成的浅色体呈网状，存在从孤立碎块状到脉状的短距离变化，可能暗示了流体的流入；b. 浅色体与围岩之间无暗色边界，呈弥散状；c. 淡色花岗岩中发育的熔体薄膜，分布于长石颗粒边界；d. 混合岩中发育的蠕英结构
Fig. 8. Outcrop and microscopic features of migmatites resulting from water-fluxed melting
图 9 等压升温下细晶花岗岩的演化
点B.系统在645 ℃开始熔融，生成熔体中的水含量为10 %；点C.785 ℃时达到4%H2O的液相线；点D.890 ℃时达到完全熔化，此时2% H2O的液相线.黑色实线：液相线；近水平虚线：熔体的最大水溶解度；修改自Weinberg and Hasalová（2015）
Fig. 9. Evolution of a haplogranite undergoing isobaric heating
图 10 大陆弧环境下流体控制的地壳熔融示意
大洋板块俯冲诱发了软流圈上涌和下地壳含水玄武岩岩浆底侵，温度升高发生了脱水熔融；含水矿物中的水向上运移，进一步诱发了水致熔融；修改自Xu et al.（2022）
Fig. 10. Schematic diagram illustrating the fluid-controlled crustal melting in a continental arc setting
图 11 典型超高压变质岩的P-T轨迹与主要脱水熔融反应
红色线代表了苏鲁造山带的P-T轨迹，苏鲁造山带在近等温降压过程中经历了脱水熔融作用.矿物缩写：Zo.黝帘石；Phe.多硅白云母；Pl.斜长石；Coe.柯石英；Qtz.石英；Grt.石榴石；Bt.黑云母；Cpx.单斜辉石；Tc.滑石；m.熔体；修改自 张泽明等（2020）
Fig. 11. P-T tracks and dehydration melting reactions of typical UHP metamorphic rocks
图 12 喜马拉雅造山带的流体循环模式简图
热板片逆冲于冷板片之上，温度的升高石冷板片发生脱水熔融，释放的含水流体向上运移，引发上部板片的水致熔融；脱水熔融产生的含水流体也可能向周围运移，并使围岩发生水致熔融.STD.藏南拆离带；MCT.主中央逆冲断层；修改自 雷凯（2020）
Fig. 12. Schematic diagram of fluid circulation patterns in the Himalayan orogenic belt
图 13 剪切带作为流体通道示意
如果流体高效流动，流体与岩石之间的相互作用较小，几乎不发生熔融；当剪切带为网络状时，或当流体运移减慢时，流体与岩石相互作用增加，为了与周围环境保持平衡，岩石发生大量熔融；修改自Weinberg and Hasalová（2015）
Fig. 13. Schematic diagram of shear zone as fluid channels
图 14 部分熔融岩石和岩浆的密度与熔体分数的关系
紫色阴影部分表示在封闭系统下熔体/固体两相系统的密度范围，浅灰色阴影表示与熔体连通性和固体连续性相对应的熔体分数范围；熔体连通性允许熔体迁移，而固体框架的破裂允许固相沉降；黑色粗箭头描绘了熔体/固相系统密度的演变：（ⅰ）在熔体迁移导致残余部分熔融岩石密度增加，（ⅱ）在固相沉降的情况下残余岩浆相对于部分熔融岩石的浮力增加；修改自Vanderhaeghe（2009）
Fig. 14. Density of partially-molten rocks and magmas as a function of melt fraction taking into account melt migration and solid settling
图 15 熔体分离、迁移和岩浆流动的机制
a. 沿断裂上升；b. 透入性运移；修改自Vanderhaeghe（2009)
Fig. 15. Mechanisms of melt segregation, melt migration, magma mobility and solid segregation
图 16 深熔作用中岩石的流变学强度与熔体比例的关系
变熔岩代表先前部分熔融的岩石，全熔岩和花岗岩代表了先前的岩浆.变熔岩/全熔岩过渡标志着由部分熔融岩向岩浆的过渡；修改自Vanderhaeghe（2009）
Fig. 16. The relationship between the rheological strength of rocks and the melt ratio during anatexis
图 17 岩石在部分熔融和结晶过程中的几何演化
熔体首先在颗粒边界聚集，随着熔体含量的增加，形成熔体网络，最后失去固相骨架；修改自Vanderhaeghe（2009）
Fig. 17. Geometric evolution of partially-molten rocks during partial melting and crystallization
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