基于岩浆凝固的地壳动力学研究

霍睿智; 贺端威

doi:10.11858/gywlxb.20180599

基于岩浆凝固的地壳动力学研究

doi: 10.11858/gywlxb.20180599

霍睿智^{1, 2,},
贺端威^{1, 2,*, ,}

1.
四川大学原子与分子物理研究所, 四川成都 610065
2.
四川大学高能量密度物理教育部重点实验室, 四川成都 610065

基金项目:

中国工程物理院中子物理学重点实验室课题 2014AB01

国家自然科学基金 51472171

国家自然科学基金 11427810

详细信息

作者简介:
霍睿智(1993-), 女, 硕士, 主要从事地壳动力学研究.E-mail:2323155992@qq.com

通讯作者:
贺端威(1969-), 男, 博士, 教授, 主要从事大腔体静高压技术、超硬材料及高压下的弹塑性研究.E-mail:duanweihe@scu.edu.cn

中图分类号: P65;P553
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出版历程
- 收稿日期: 2018-07-14
- 修回日期: 2018-07-16

Crustal Dynamics Based on Magma Solidification

HUO Ruizhi^{1, 2
,},
HE Duanwei^{1, 2,*
, ,}

1.
Institute of Atomic and Molecular Physics, Sichuan University, Chengdu 610065, China
2.
Key Laboratory of High Energy Density Physics and Technology of Ministry of Education, Sichuan University, Chengdu 610065, China

摘要

摘要: 地球在形成之初处于熔融状态，随着时间的推移，地球表面的岩浆不断冷却、凝固，发展成现在的圈层结构，并且地球物质的冷却及液-固转变依然在持续。通过对地震发生后地球日长变化进行统计分析，发现总体上地震后地球自转速率加快。分析认为，这一现象是由于地幔部分岩浆冷却凝固使地壳岩石圈下部体积塌缩所致。由此，建立了一个地壳动力学模型，以解释地壳各板块间的相互作用和相对运动，并且认为地震等地质活动的动力学成因主要是地球内部熔体持续凝固所导致的地壳下部体积收缩、压力减小，在重力作用下，构成地壳的各板块之间的相互作用加剧，原有力学结构失稳，发生大规模岩层错位、断裂，从而引起地震、火山爆发等剧烈的地质活动。通过建立热学模型和力学模型，验证了上述观点。
- 地壳动力学 /
- 岩浆凝固 /
- 地震机制 /
- 日长
Abstract: The earth was in a molten state at the beginning of its formation.Over time, the magma on the earth's surface began to cool down and solidify, and the earth has gradually become such a trap structure.However, the cooling and liquid-solid transformation process of the earth materials continues until today.This paper presents a statistical analysis of the change of earth's length-of-day after earthquakes, and it is found that the earth's rotation speed is generally accelerated after great earthquakes.We believe that this phenomenon is caused by the cooling and solidification of the magma in the part of the mantle, which causes significant volume collapse of the lower crustal lithosphere.Thus, we set up a crustal dynamic model to explain the interaction and relative motion of tectonic plates.We believe that the dynamic genesis of earthquake and other geological activities are due to the continuous solidification of the melt in the interior of the earth which could lead to a volume shrinkage and pressure drop in the lower part of the earth's crust.The effect of gravity enhances the interaction among tectonic plates, the original mechanical structure becomes unstable, and eventually the massive rock fracture occurs, which can cause severe geological events such as earthquakes, and volcanic eruptions.This conclusion has been further validated based on the thermal and mechanical model proposed in this paper.
- crustal dynamics /
- magma solidification /
- earthquake mechanism /
- length of day

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图 1 1963~2016年7.5级以上地震的震源深度分布

Figure 1. Focal depth distribution of earthquakes above magnitude 7.5 from 1963 to 2016

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表 1 6次大地震及其对LOD变化的影响

Table 1. The influences of six great earthquakes on the changes in length-of-day (ΔLOD)

No.	Aera	Date	Latitude/(°)	Longitude/(°)	Depth/km	Moment magnitude	ΔLOD	Ref.
1	Bio-Bio, Chile	1960-05-22	-38.143	-73.407	25	9.5	-8.4	[14]
2	Southern Alaska	1964-03-28	60.908	147.339	25	9.2	6.8	[14]
3	Offshore Valparaiso, Chile	1985-03-03	-33.135	71.871	33	8.0	-0.1	[19]
4	Michoacan, Mexico	1985-09-19	18.190	102.533	27.9	8.0	-0.085	[14]
5	Off the west coast of northern Sumatra	2004-12-26	3.295	-95.982	30	9.1	-0.48	[20]
6	Near the east coast of Honshu, Japan	2011-03-11	38.296	142.373	29	9.1	-5.81	[21]
	Average						-1.3	This work

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表 2 全球不同类型岩浆岩的主要化学成分

Table 2. Main chemical compositions for different types of magmatic rocks on Earth

Type of rock	Mass fraciton/%								Ref.
Type of rock	SiO₂	Al₂O₃	FeO	MgO	CaO	Na₂O	K₂O	Sum	Ref.
Alkali olivine basalts	46.7	15.1	11.7	7.7	9.9			98.2	[32]
Tholeiitic basatle (tholeiites and olivine Tholeiites) of the Hawailian Islands	49.36	13.94	8.53	8.44	10.3			99.03	[33]
Alkalic basalt	46.46	14.64	9.11	8.19	10.33			99.71	[33]
Picrite basalt of oceanite type	46.41	8.53	9.82	20.81	7.38			100.1	[33]
Hawaiite ('andesine andesite')	48.6	16.49	9.11	8.19	10.33			99.23	[33]
Primary tholeiite of the Izu-Hakone region	48.73	16.53	8.44	8.24	12.25			100.02	[34]
Olivine basalt of Niuafo'au	50.37	14.65	9.24	7.13	11.74			99.8	[35]
Tholeiitic picrite-basalt	46.4	8.5	9.8	20.8	7.4			99.7	[36]
Ankaramite	44.1	12.1	9.6	11.5	13			99.3	[36]
K-poor alkali olivine basalt	45.4	14.7	9.2	7.8	10.5			99.3	[36]
Hawaiite	47.9	15.9	7.6	4.8	8			99.1	[36]
Nephelinite	39.7	11.4	8.2	12.1	12.8			98.4	[36]
Olivine tholeiite	49.16	13.33	9.71	10.41	10.93			100.12	[37]
Tholeiite	53.8	13.9	9.3	4.1	7.9			100.7	[38]
Tholeiite andesite	59.31	13.77	6.48	2.27	5.58	3.91		97.97	[39]
Icelandite	61.76	15.36	5.84	1.76	5.04	4.37		100.0	[40]
High-alumina basalt	49.15	17.73	7.2	6.91	9.91			99.18	[38]
High-alumina andesite	58.65	17.43	3.48	3.28	6.26	3.82		99.1	[39]
Dacite	69.68	15.21	1.9	0.91	2.7	4.47		99.46	[40]
Rhyolite	73.23	14.03	1.7	0.35	1.32	3.94	4.08	99.56	[40]
Pantellerite	69.8	7.4	6.15	0.05	0.45	6.7	4.3	98.19	[41]
Commendite	75.23	11.99	1.25	0.02	0.27	4.79	4.67	99.42	[41]
Alkalic picrite-basalt	46.57	8.2	9.75	19.65	9.43			99.79	[42]
K-rich alkali olivine basalt	42.43	14.15	8.48	6.71	11.91			99.18	[43]
Trachybasalr	46.48	16.68	7.3	4.65	9.4			99.68	[43]
Trachyte	60.7	20.5	0.4	0.2	1.4	6.2	6.7	99.13	[43]
Tristanite	55.85	18.98	3.11	2.04	4.51	5.16		98.63	[44]
Benmorite	55.64	16.38	4.91	1.06	2.9	6.07	3.49	95.23	[44]
Phonolite	60.64	18.29	1.18	0.09	0.83	8.93	5.1	98.08	[45]
Wyomingite	54.09	9.94	1.48	6.99	4.71		11.38	97.3	[46]
Average	53.41	14.19	6.67	6.30	7.31			99.087

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表 3 不同熔融岩浆的化学成分及其在高温高压下的密度

Table 3. Chemical compositions of different molten magmas and their densities at high temperature and high pressure

Type of molten magma	Mass fraciton/%						Density/(g·cm^-3)	Ref.
Type of molten magma	SiO₂	Al₂O₃	FeO	MgO	CaO	Sum	Density/(g·cm^-3)	Ref.
Magma^*	53.41	14.19	6.67	6.3	7.31	99.1	2.88	This work
PHN1611	45.1	2.8	10.4	38.4	3.4	100	2.87^a, 2.94^b	[47]
Mid-ocean ridge basalt	51.81	15.95	9.97	7.86	11.69	100	2.88^c	[48]
Hydrous peridotite magma	45.9	3.8	8.5	32.5	3.6	99.2	2.77^d, 2.8^e, 2.83^f	[49]
Note:(1) The asterisk “*” represents the main chemical compositions of magma in this paper. (2) The letter “a” and “b” represent the values come from compression curves of PHN1611 melt at 31 kPa/2 360 ℃ and 31 kPa/2 030 ℃ respectively. (3) The letter “c” represents the value comes from compression curves of basaltic melts at 31 kPa/2 200 ℃. (4) The letter “d”, “e” and “f” represent the values come from isothermal compression curves of the peridotite melt at 31 kPa/1 973 K, 31 kPa/1 873 K and 31 kPa/1 773 K respectively.

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表 4 不同固态岩浆岩的化学成分及其在高温高压下的密度

Table 4. Chemical compositions of different solid magmatic rocks and their densities at high temperature and pressure

Type of magmatic rock	Mass fraciton/%						Density/(g·cm^-3)	Ref.
Type of magmatic rock	SiO₂	Al₂O₃	FeO	MgO	CaO	Sum	Density/(g·cm^-3)	Ref.
Average sediment	62.77	13.12	4.28	3	8.76	100	3.16^c	[50]
Mid-ocean ridge basalt	49.67	16.1	7.3	11.42	7.66	100	3.5^d	[50]
Hypothetical magmatic rock^a	56.22	14.61	5.79	7.21	8.21	100	3.3^e	This work
Magma^b	53.41	14.19	6.67	6.3	7.31	99.1	3.3^e	This work
Note:(1) The letter “a” represents an hypothetical magmatic rock which is a mixture of average sediment and mid-ocean ridge basalt in a ratio of one to one. (2) The letter “b” represents the main mineral composition content of the magma which is set in this paper. (3) The letters “c” and “d” represent the values come from density chart for average sediment and MORB at 3.1 GPa/1 000 ℃ respectively. (4) The letter “e” represents the value is the average of c and d.

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