片麻岩热导率和热扩散系数的高温高压实验研究

熊自励; 张宝华; 刘红梅

doi:10.11858/gywlxb.20251076

片麻岩热导率和热扩散系数的高温高压实验研究

doi: 10.11858/gywlxb.20251076

熊自励^1,,
张宝华²,
刘红梅^{3, 4, 5}

1.
韩山师范学院地理科学与旅游学院, 广东潮州　521041
2.
浙江大学地球科学学院, 地球与行星物质科学研究中心, 浙江杭州　310058
3.
中国科学院广州地球化学研究所深地过程与战略矿产资源全国重点实验室, 广东广州　510640
4.
中国科学院广州地球化学研究所广东省矿物物理与材料研究开发重点实验室, 广东广州　510640
5.
广东省战略金属与绿色利用基础学科研究中心, 广东广州　510640

基金项目: 广东省科技计划项目（2023B1212060048，2024B0303390002）；韩山师范学院博士启动项目（QD2024105）

详细信息

作者简介:
熊自励（1993－），男，博士，讲师，主要从事矿物物理实验研究. E-mail：20230059@hstc.edu.cn

中图分类号: O736; P574.1; O521.2
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出版历程
- 收稿日期: 2025-04-18
- 修回日期: 2025-05-23
- 网络出版日期: 2025-05-27
- 刊出日期: 2025-10-05

High-Temperature and High-Pressure Experimental Study on the Thermal Conductivity and Thermal Diffusivity of Gneiss

XIONG Zili^1
,,
ZHANG Baohua²,
LIU Hongmei^{3, 4, 5}

1.
School of Geographic Science and Tourism, Hanshan Normal University, Chaozhou 521041, Guangdong, China
2.
Research Center for Earth and Planetary Material Sciences, School of Earth Sciences, Zhejiang University, Hangzhou 310058, Zhejiang, China
3.
State Key Laboratory of Deep Earth Processes and Resources, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou 510640, Guangdong, China
4.
Guangdong Provincial Key Laboratory of Mineral Physics and Materials, Guangzhou Institute of Geochemistry, Chinese Academy of Sciences, Guangzhou 510640, Guangdong, China
5.
Guangdong Research Center for Strategic Metals and Green Utilization, Guangzhou 510640, Guangdong, China

摘要

摘要: 片麻岩作为大陆地壳古老基底的代表岩石类型，研究其热输运特性对于揭示岩石圈热结构及构造演化具有重要意义。采用瞬态平面热源法，首次在高温（300～1073 K）、高压（1.0～3.0 GPa）条件下同时测量青藏高原东南缘云南大理前寒武纪变质基底片麻岩的热导率和热扩散系数。实验结果表明：热导率和热扩散系数均随着温度升高而降低，揭示了片麻岩的传热机制为声子导热，其中，声子散射是导致热导率和热扩散系数降低的主要机制；温度超过 950 K 时，声子散射的饱和效应使得片麻岩的热导率和热扩散系数不再降低而趋于稳定。经验公式拟合结果表明，压力对片麻岩热输运性质有明显的促进作用，呈线性正相关。此外，根据实验结果推测大陆的中-下地壳可能具有一致的热传导能力，热导率为(2.0±0.3) W/(m·K)。基于实验数据构建的岩石圈热结构模型显示，研究区莫霍面（44 km）的温度为1030～1210 K，岩石圈厚度为65～95 km，呈现出明显的梯度变化。结合脆-韧性转换带温度-深度关系，限定了该区域强震震源深度在11～23 km区间，为青藏高原东南缘构造变形机制及地震危险性评估提供了新的热动力学约束。
- 高温高压 /
- 片麻岩 /
- 热导率 /
- 岩石圈热结构 /
- 热扩散系数
Abstract: As a representative rock type of the ancient continental crustal basement, gneiss plays a crucial role in understanding the thermal structure and tectonic evolution of the lithosphere due to its thermal transport properties. In this study, the thermal conductivity (κ) and thermal diffusivity (D) of precambrian metamorphic basement gneiss from Dali, Yunnan, located at the southeastern margin of the Tibetan Plateau, were simultaneously measured for the first time under high-temperature (300–1073 K) and high-pressure (1.0–3.0 GPa) conditions using the transient plane source technique. Experimental results demonstrate that both κ and D decrease with increasing temperature, indicating that the heat transfer mechanism of gneiss is phonon thermal conduction, where phonon scattering is the primary mechanism leading to the decrease in κ and D. When the temperature exceeds 950 K, the saturation effect of phonon scattering causes κ and D of gneiss to no longer decrease but tend to stabilize. Empirical fitting reveals a significant positive linear correlation between pressure and the thermal transport properties of gneiss, suggesting that pressure enhances thermal transport. Based on these results, we infer that the middle to lower continental crust may exhibit relatively uniform thermal conductivity ((2.0±0.3) W/(m·K)). A lithospheric thermal structure model derived from the experimental data indicates that the Moho temperature range of 1030–1210 K at 44 km depth and the lithospheric thickness range of 65–95 km in the study area, demonstrating a pronounced thermal gradient. Furthermore, by integrating the temperature-depth relationship of the brittle-ductile transition zone, the focal depths of large earthquakes in this region are constrained to 11–23 km. These findings provide novel thermodynamic constraints for understanding tectonic deformation mechanisms and seismic hazard assessment in the southeastern Tibetan Plateau.
- high temperature and high pressure /
- gneiss /
- thermal conductivity /
- lithospheric thermal structure /
- thermal diffusivity

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图 1 点苍山变质杂岩带地质构造图（修改自文献[35]）

Figure 1. Tectonic map of the metamorphic complex belt in the Diancangshan area (modified from Ref. [35])

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图 2 黑云母长英质片麻岩正交偏光显微照片(a)和SEM背散射图像(b)（qtz：石英；fsp：长石；pl：斜长石；K-fsp：钾长石；bi：黑云母；ilm：钛铁矿；zi：锆石）

Figure 2. Photomicrograph under cross-polarized light (a) and backscattered SEM image (b) of biotite-bearing felsic gneiss (qtz: quartz; fsp: feldspar; pl: plagioclase; K-fsp: K-feldspar; bi: biotite; ilm: ilmenite; zi: zircon)

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图 3 样品组装示意图（修改自文献[10]）

Figure 3. Schematic diagram of sample assembly (modified from Ref. [10])

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图 4 瞬态平面热源法测量原理示意图（修改自文献[10]）

Figure 4. Schematic diagram of the measurement principle of the transient plane source method (modified from Ref. [10])

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图 5 (a) 3.0 GPa、373 K条件下样品测量时示波器记录图像（CH1 和 CH2 分别监测脉冲加热器电压和热电偶电动势变化），(b) 样品的温度响应曲线拟合结果（从热电偶输出的电压-时间数据转换而来）

Figure 5. (a) Oscilloscope diagram recorded during sample measurement at 3.0 GPa and 373 K (CH1 and CH2 monitor the voltage of the pulse heater and the thermoelectric voltage of the thermocouple, respectively.); (b) fitted temperature response curve of the sample (converted from the voltage-time data output by the thermocouple)

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图 6 温度和压力对片麻岩热输运性质的影响（(a)和(b)中的实线分别为式(6)和式(7)的拟合结果，(c)和(d)中的实线分别为式(8)和式(9)的拟合结果）

Figure 6. Effects of temperature and pressure on the thermal transport properties of gneiss (The solid lines in (a) and (b) represent the fitting results using Eq. (6) and Eq. (7), respectively; those in (c) and (d) represent the fitting results using Eq. (8) and Eq. (9), respectively.)

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图 7 1.0 GPa下片麻岩热输运性质与其他结果的对比

Figure 7. Comparison of the thermal transport properties of gneiss at 1.0 GPa with previously reported results

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图 8 采用不同地表热流密度时云南大理地区岩石圈的温度-深度剖面（地幔绝热线：T=1473+0.5z^[58]）

Figure 8. Lithospheric temperature-depth profile with different surface heat flow densities of the Dali region, Yunnan (Mantle adiabatic curve: T =1473+0.5z^[58])

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表 1 苍山群片麻岩在不同温度和压力下的κ和$D $

Table 1. κ and $D $ of the Cangshan group gneiss under varying temperature and pressure conditions

1.0 GPa			2.0 GPa			3.0 GPa
T/K	κ/(W·m⁻¹·K⁻¹)	D/(mm²·s⁻¹)	T/K	κ/(W·m⁻¹ ·K⁻¹)	D/(mm²·s⁻¹)	T/K	κ/(W·m⁻¹ ·K⁻¹)	D/(mm²·s⁻¹)
300	4.898(45)	1.571(20)	300	5.302(41)	1.671(18)	300	5.817(46)	1.814(21)
323	4.549(26)	1.442(11)	323	4.917(28)	1.597(13)	323	5.111(36)	1.656(15)
373	3.853(19)	1.383(8)	373	4.295(22)	1.449(10)	373	4.718(24)	1.617(10)
423	3.281(12)	1.253(6)	423	3.861(17)	1.336(9)	423	4.102(19)	1.491(8)
473	3.148(12)	1.245(7)	473	3.314(14)	1.321(7)	473	3.479(15)	1.368(7)
523	2.564(9)	1.120(5)	523	2.987(12)	1.215(7)	523	3.428(15)	1.344(8)
573	2.492(9)	1.122(6)	573	2.613(10)	1.218(5)	573	3.189(16)	1.285(9)
623	2.137(8)	1.043(5)	623	2.706(11)	1.100(7)	623	2.893(11)	1.281(7)
673	2.290(9)	1.008(6)	673	2.437(11)	1.093(7)	673	2.922(13)	1.167(8)
723	1.989(9)	0.936(6)	723	2.199(11)	1.012(6)	723	2.644(12)	1.122(7)
773	1.926(11)	0.954(7)	773	2.263(12)	1.006(7)	773	2.501(11)	1.076(7)
823	1.865(10)	0.876(6)	823	2.246(13)	0.988(8)	823	2.579(13)	1.090(8)
873	1.925(11)	0.875(7)	873	2.004(14)	0.976(9)	873	2.359(12)	1.051(7)
923	1.898(13)	0.864(9)	923	2.158(14)	0.929(8)	923	2.228(15)	1.075(9)
973	1.958(13)	0.874(8)	973	2.097(16)	0.964(10)	973	2.518(18)	1.050(10)
1023	1.966(14)	0.875(9)	1023	2.133(15)	0.929(9)	1023	2.309(14)	1.022(7)
1073	1.910(14)	0.879(9)	1073	2.154(160	0.926(10)	1073	2.474(19)	1.036(11)

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表 2 苍山群片麻岩的κ和$D $的温度拟合系数

Table 2. Fitting coefficients for the temperature dependence of κ and $D $ in the Cangshan group gneiss

p/GPa	κ(T) = a₀+a₁/T + a₂/T²
p/GPa	a₀/(W·m⁻¹·K⁻¹)	a₁/(W·m⁻¹)	a₂/(W·m⁻¹·K)	R²
1.0	1.605(235)	−83(258)	331028(62124)	0.984
2.0	1.526(241)	264(275671)	63711(15)	0.985
3.0	1.731(257)	355(283)	257100(68077)	0.984

p/GPa	D(T) = b₀+b₁/T + b₂/T²
p/GPa	b₀/(mm²·s⁻¹)	b₁/(mm²·s⁻¹·K)	b₂/(mm²·s⁻¹·K²)	R²
1.0	0.541(60)	321(66)	−5482(16086)	0.980
2.0	0.613(49)	316(54)	180(12995)	0.988
3.0	0.695(63)	334(70)	−1831(16889)	0.981

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表 3 苍山群片麻岩的κ和$D $的压力拟合系数

Table 3. Fitting coefficients for the pressure dependence of κ and $D $ in the Cangshan group gneiss

T/K	κ(p) = κ₀+cp			D(p) = D₀+dp
T/K	κ₀/(W·m⁻¹·K⁻¹)	c/(W·m⁻¹·K⁻¹·GPa⁻¹)	R²	D₀/(mm²· s⁻¹)	d/(mm²·s⁻¹·GPa⁻¹)	R²
300	4.419(69)	0.459(32)	0.990	1.442(26)	0.121(12)	0.979
323	4.297(108)	0.281(50)	0.937	1.351(59)	0.106(27)	0.875
373	3.423(11)	0.432(5)	0.999	1.249(64)	0.116(29)	0.878
423	2.926(210)	0.410(97)	0.893	1.122(44)	0.119(20)	0.942
473	2.983(0)	0.165(0)	0.999	1.188(18)	0.061(8)	0.961
523	2.130(10)	0.431(5)	0.999	1.002(21)	0.112(10)	0.983
573	2.067(282)	0.348(130)	0.752	1.046(18)	0.081(8)	0.979
623	1.822(238)	0.378(110)	0.843	0.903(77)	0.119(35)	0.835
673	1.917(210)	0.316(97)	0.825	0.931(7)	0.079(3)	0.996
723	1.622(146)	0.327(67)	0.918	0.870(9)	0.068(4)	0.991
773	1.656(61)	0.287(28)	0.980	0.890(10)	0.061(4)	0.987
823	1.516(29)	0.356(13)	0.996	0.771(5)	0.106(2)	0.998
873	1.662(172)	0.216(79)	0.762	0.906(249)	0.043(115)
923	1.764(118)	0.165(55)	0.800	0.803(4)	0.111(2)	0.999
973	1.631(175)	0.279(81)	0.845	0.767(34)	0.124(16)	0.967
1023	1.793(5)	0.171(2)	0.999	0.929(157)	−0.002(72)
1073	1.615(47)	0.282(21)	0.987	0.725(15)	0.139(7)	0.994

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表 4 计算岩石圈温度-深度剖面时采用的参数

Table 4. Parameters used for calculating the lithospheric temperature-depth profile

Layering	Layer thickness/km	κ/(W·m⁻¹·K⁻¹)	R/(μW·m⁻³)	Ref.
Upper crust	12	κ(T, p) = (1.290504+148.932568/T+ 226651.47256/T²)(1+0.12553p)	1.68	This study
Lower crust	32	κ(T) = (1618.4−0.021T−14047/T ^0.5)[0.593+ 2.773exp(−T/171.77)]×3127×10⁻⁶	0.49	[7]
Lithospheric mantle		κ(T, p) = (1.7+1177.8/T+32300/T ²)(1+0.044p)	0.02	[15]

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