中国东部陆缘中、新生代洋板块深地质作用追踪

doi:10.13745/j.esf.sf.2025.8.62

地学前缘 ›› 2025, Vol. 32 ›› Issue (6): 9-28.DOI: 10.13745/j.esf.sf.2025.8.62

中国东部陆缘中、新生代洋板块深地质作用追踪

肖庆辉¹(), 刘勇¹^,^*(), 李廷栋¹, 潘桂棠², 陆松年³, 丁孝忠¹, 张克信⁴, 庞建峰¹, 邱瑞照⁵, 赵国春⁶, 张恒¹, 程扬¹, 范玉须¹, 付利¹

1.中国地质科学院地质研究所, 北京 100037
2.中国地质调查局成都地质调查中心, 四川成都 610081
3.中国地质调查局天津地质调查中心, 天津 300170
4.中国地质大学(武汉) 地球科学学院, 湖北武汉 430074
5.中国地质调查局发展研究中心, 北京 100037
6.中国地质大学(北京) 地球科学与资源学院, 北京 100083

收稿日期:2025-06-12 修回日期:2025-08-13 出版日期:2025-11-25 发布日期:2025-11-12
通信作者: 刘勇
作者简介:肖庆辉(1939—),男,研究员,博士生导师,构造地质学专业,从事大地构造学和中国岩石圈三维结构研究。E-mail: qinghuixiao@126.com
基金资助:
内蒙古自治区岩浆活动成矿与找矿重点实验室开放课题(编号2024KF001);中国地质调查局地质调查项目“中国区域地质志和系列图件编制”(DD20221645)

Tracing the deep geological processes of the Mesozoic-Cenozoic oceanic plate on the continental margin of the East Asian continent in China

XIAO Qinghui¹(), LIU Yong¹^,^*(), LI Tingdong¹, PAN Guitang², LU Songnian³, DING Xiaozhong¹, ZHANG Kexin⁴, PANG Jianfeng¹, QIU Ruizhao⁵, ZHAO Guochun⁶, ZHANG Heng¹, CHENG Yang¹, FAN Yuxu¹, FU Li¹

1. Institute of Geology,Chinese Academy of Geological Sciences, Beijing 100037, China
2. Chengdu Geological Survey Center, China Geological Survey, Chengdu 610081, China
3. Tianjin Geological Survey Center, China Geological Survey, Tianjin 300170, China
4. School of Earth Sciences, China University of Geosciences (Wuhan), Wuhan 430074, China
5. Development and Research Center, China Geological Survey, Beijing 100037, China
6. School of Earth Sciences and Resources, China University of Geosciences (Beijing), Beijing 100083, China

Received:2025-06-12 Revised:2025-08-13 Online:2025-11-25 Published:2025-11-12
Contact: LIU Yong

摘要/Abstract

摘要：

中国东亚大陆中、新生代陆缘构造成因至今没有统一认识,分歧仍然很大。本文依据洋板块地质思维重新研究中国东亚大陆中、新生代陆缘构造成因后发现:中国东亚大陆中、新生代陆缘洋板块俯冲作用不仅普遍存在,而且一直俯冲到400~660 km深的地幔过渡带,并在那里滞留堆积构成具有造壳成陆功能的新的热动力学系统,或称第二大陆动力学系统,有人称之为第二大陆。它控制了中国中、新生代大陆的形成与演变。另一个发现是在中国大陆俯冲增生杂岩带内发现很多洋岛、海山、洋底高原等大洋遗迹,它们与表征洋板块俯冲作用的岛弧等共存在同一个俯冲带上,表明中国大陆的形成与演变普遍经受过曾存在过的五大古洋(古亚洲洋、特提斯洋、古太平洋、鄂霍茨克洋、华南洋)洋板块俯冲作用制约。第三个发现是,在内蒙古西拉木伦地区俯冲增生杂岩带中发现了与3种不同成因体制——“地幔柱”型、洋中脊型和岛弧型有关的洋岛、海山,表明古大洋演化过程中的构造背景多样而复杂,包括岛弧、热点、地幔柱、弧后盆地及洋中脊等各种构造背景。岛弧环境明显与板块俯冲有关,而热点、海山明显与地幔柱有关。这说明古大洋在演化过程中,洋内俯冲作用和软流圈地幔(柱)上涌两种完全对立的构造体制同时共存并相互作用。据此,我们提出东亚中、新生代造山带可能是东亚中、新生代造山带之下的地幔过渡带或所谓第二大陆引发的洋内俯冲+板内软流圈地幔(柱)上涌复合作用而形成的系统。因此,岛弧型洋岛、海山的发现为中国洋板块地质建立东亚中、新生代造山带洋内俯冲+板内软流圈地幔(柱)上涌同时共存的理论模型提供了重要科学依据。东亚中新生代造山带之下的地幔过渡带或所谓第二大陆的存在使中国大陆形成与演化、成矿作用潜力评价和战略找矿预测都可能要被重新认识。

关键词: 中国东亚, 中、新生代, 第二大陆, 洋内俯冲+软流圈地幔(柱)上涌复合系统

Abstract:

There remains no unified understanding regarding the causes of Mesozoic-Cenozoic continental margin tectonics in the East Asian continent of China, with significant differences persisting. Based on the geological framework of oceanic plates, this paper re-examines these causes. Our findings reveal that: (1) Subduction of oceanic plates along the Mesozoic-Cenozoic continental margin of East Asia was not only widespread but also continuously extended into the mantle transition zone (400-660 km depth), where they accumulated. This formed a novel thermodynamical system with crust formation and continent building functions, termed ‘second continental dynamics’ or the ‘second continent’. This system controlled the formation and evolution of the Mesozoic-Cenozoic continent in China. (2) Numerous oceanic islands, seamounts, and oceanic plateaus have been identified within subduction-accretionary complex zones in the Chinese mainland. Their coexistence with the opposing tectonic regime of oceanic plate subduction within the same subduction zone indicates that the formation and evolution of the Chinese mainland were fundamentally constrained by the subduction of five ancient oceanic plates (Paleo-Asian Ocean, Tethys Ocean, Paleo-Pacific Ocean, Okhotsk Ocean, and South China Ocean). (3) Within the Xar Moron subduction-accretionary complex zone in Inner Mongolia, three genetically distinct regimes of oceanic islands and seamounts have been discovered: ‘mantle plume’ type, mid-ocean ridge type, and island arc type. This demonstrates that the tectonic backgrounds during the evolution of these ancient oceans were diverse and complex, forming in environments including island arcs, hotspots, mantle plumes, back-arc basins, and mid-ocean ridges. The island arc environment is clearly linked to plate subduction, while hotspots and seamounts are associated with mantle plumes. This indicates that two opposing tectonic regimes- intra-oceanic subduction and intra-plate asthenospheric mantle upwelling - coexisted during ancient ocean evolution. Based on these findings, we propose that the Mesozoic-Cenozoic orogenic belts in East Asia formed through the composite evolution of an intra-oceanic subduction + intra-plate asthenospheric mantle upwelling system. This system was triggered by the mantle transition zone (the ‘second continent’) beneath these belts, rather than solely by mantle plumes. Consequently, the discovery of island arc-type oceanic islands and seamounts provides crucial scientific evidence for establishing the theoretical model of coexisting intra-oceanic subduction and intra-plate asthenospheric mantle upwelling within the Mesozoic-Cenozoic orogenic belts of East Asia, within the context of oceanic plate geology in China. It is therefore essential to re-evaluate the influence of the mantle transition zone (the ‘second continent’) beneath these orogenic belts on the formation and evolution of the Chinese mainland, its metallogenic potential, and its implications for strategic ore-prospecting predictions.

Key words: East Asian continent in China, Mesozoic-Cenozoic, the second continent, the coexistence of intra-oceanic subduction + intra-plate asthenospheric mantle upwelling

中图分类号:

P542
P612

肖庆辉, 刘勇, 李廷栋, 潘桂棠, 陆松年, 丁孝忠, 张克信, 庞建峰, 邱瑞照, 赵国春, 张恒, 程扬, 范玉须, 付利. 中国东部陆缘中、新生代洋板块深地质作用追踪[J]. 地学前缘, 2025, 32(6): 9-28.

XIAO Qinghui, LIU Yong, LI Tingdong, PAN Guitang, LU Songnian, DING Xiaozhong, ZHANG Kexin, PANG Jianfeng, QIU Ruizhao, ZHAO Guochun, ZHANG Heng, CHENG Yang, FAN Yuxu, FU Li. Tracing the deep geological processes of the Mesozoic-Cenozoic oceanic plate on the continental margin of the East Asian continent in China[J]. Earth Science Frontiers, 2025, 32(6): 9-28.

图/表 31

图1 不同的大陆生长曲线(据文献[8]修改)

Fig.1 Growth curves of different continents. Modified after [8].

图2 普遍存在的大陆和洋区弧俯冲作用(据文献[12]修改) 中国大陆内已发现上百条俯冲增生杂岩带。图中数字为中国大陆内已发现的俯冲增生杂岩带编号。1—乌拉利亚语;2~6—中亚(2—贝加尔湖-穆亚;3—叶尼塞-外贝加尔-北蒙古; 4—阿勒泰-萨延-西北蒙古;5—额齐斯-宰山;6—天山);7—南内蒙古;8—蒙古-鄂霍次克;9—锡霍特-阿林; 10—上霍扬斯克;11—鄂霍次克-楚科奇;12—南阿努伊;13—西堪察加半岛;14—帕米尔-兴都库什;15—昆仑-秦岭; 16—西藏-喜马拉雅山;17—华南。

Fig.2 Ubiquitous subduction in continental and oceanic arcs. Modified after [12]. 1—Uralian; 2-6—Central Asian (2—Baikal-Muya; 3—Yenisey-Transbaikalia-North Mongolia; 4— Altay-Sayan-NW Mongolia; 5—Irtysh-Zaysan; 6—Tienshan); 7—South Inner Mongolia; 8—Mongol-Okhotsk; 9—Sikhote-Alin; 10—Verkhoyansk; 11—Okhotsk-Chukotka; 12—South Anuy; 13—West Kamchatka; 14—Pamir-Hindukush; 15—Kunlun-Qinling; 16—Tibet-Himalaya; 17—South China.

图3 西太平洋区域的洋内弧的分布(据文献[8]修改) 世界上超过三分之二的洋内弧产生在西太平洋。圈内的数字代表表1所示洋内弧。

Fig.3 Distribution of intra-oceanic arcs in the western Pacific. Modified after [8].

图4 菲律宾海板块内的五条洋内弧向日本本州岛和东亚大陆之下发生俯冲作用(据文献[8]修改)

Fig.4 Subduction of five intra-oceanic arcs within the Philippine Sea Plate beneath Japan’s Honshu and East Asian continent. Modified after [8].

图5 菲律宾海板块内的五条洋内弧向日本本州岛和东亚大陆之下发生俯冲作用,而东亚大陆之下大地幔楔则向东日本本州岛流动(据文献[13]修改)

Fig.5 Subduction of five intra-oceanic arcs beneath Honshu and East Asia, with eastward flow of the large mantle wedge. Modified after [13].

表1 西太平洋区域的洋内弧 (据文献[8]修改)

Table 1 Intra-oceanic arcs in the western Pacific. Modified after [8].

序号	名称	俯冲或增生弧	序号	名称	俯冲或增生弧
1	Shirshov-Bowers	不清楚	21	North Borneo-Sulu-Zamboanga	不清楚
2	Alaska-Aleutians	不清楚	22	Halmahera	增生
3	S. Kamchatka	不清楚	23	Sabgihe	增生
4	Kuriles	不清楚	24	Sulawesi East Arm	增生
5	Hidaka	不清楚	25	Sulawesi West Arm	增生
6	NE Japan	不清楚	26	Sula	不清楚
7	Izu-Bonin	部分增生	27	Banda	不清楚
8	East Mariana	不清楚	28	Sunda (Java-Flores)	不清楚
9	West Mariana	不清楚	29	Sunda (Sumatra)	不清楚
10	Sw Japan	不清楚	30	Bismarck	不清楚
11	Kyushu-Palao	俯冲	31	New Britain	不清楚
12	Amami	俯冲	32	Bewani-Torricelli	不清楚
13	Daito	俯冲	33	Central Papua New Guinea	不清楚
14	Okion-Daito	俯冲	34	Solomon	不清楚
15	Ryu-Kyu	不清楚	35	Vanuatu	不清楚
16	West Philippines	不清楚	36	Tofua (Tonga)	不清楚
17	Luzon	不清楚	37	Kermadec	不清楚
18	Negros	不清楚	38	New Zealand	不清楚
19	SE Mindanao	不清楚	39	Macquarie	不清楚
20	Palawan	不清楚

图6 洋板块俯冲增生形成新大陆的各构造单元示意图(据文献[14]修改)

Fig.6 Schematic diagram showing the tectonic elements of a new continent formed by oceanic plate subduction and accretion. Modified after [14].

图7 TTG和地幔岩密度剖面(据文献[15-16]修改)

Fig.7 TTG and mantle peridotite density profiles. Modified after [15-16].

图8 帕米尔—日本地震层析成像剖面图(据文献[17-18]修改) 在东亚地区发现大型罕见的热地幔楔低速带,由几个含水地幔软流上涌流构成。这些上涌流可以向下追踪到410~660 km深地幔过渡带或第二大陆,但是不跨过660 km或更深处。这就是第二大陆地幔软流上涌柱连体。

Fig.8 Seismic tomographic profile from the Pamir to Japan. Modified after [17-18].

图9 川滇地块—伊豆海沟地震层析成像剖面图(据文献[17]修改) 从图上可见太平洋板块以约45°倾角向下俯冲到地幔过渡带。

Fig.9 Seismic tomographic profile from the Chuan-Dian Block to the Izu Trench. Modified after [17].

图10 腾冲—马里亚纳海沟地震层析成象剖面图(据文献[17]修改)

Fig.10 Seismic tomographic profile from Tengchong to the Mariana Trench. Modified after [17].

图11 印度板块—羌塘地块地震层析成象剖面图(据文献[17]修改) 印度板块俯冲在西藏高原之下深度200~300 km处,角度低,近水平,印度板块俯冲的水平距离约为500 km,北缘到达柴达木地块。

Fig.11 Seismic tomographic profile from the India Plate to the Qiangtang Block. Modified after [17].

图12 印度板块—柴达木盆地地震层析成像剖面图(据文献[17]修改) 地幔过渡带和下地幔中可见印亚俯冲碰撞之前的晚中生代特提斯洋俯冲残留。

Fig.12 Seismic tomographic profile from the India Plate to the Qaidam Basin. Modified after [17].

图13 印度—准噶尔地震层析成像剖面图(据文献[17]修改) 印度板块低角度俯冲到西藏高原之下200~300 km处,在地幔过渡带中未见到印度板片俯冲停滞堆积成新的热动力层。

Fig.13 Seismic tomographic profile from the India Plate to the Junggar Basin. Modified after [17].

图14 印度—准噶尔地震层析成像剖面图(据文献[17]修改)

Fig.14 Seismic tomographic profile from the India Plate to the Junggar Basin. Modified after [17].

图15 印度—哈萨克斯坦地震层析成像剖面图(据文献[17]修改)

Fig.15 Seismic tomographic profile from India to Kazakhstan. Modified after [17].

图16 地幔过渡带或第二大陆中的各种岩石类型含有的放射性元素对比图(据文献[12]修改) 地幔过渡带或第二大陆的放射性元素含量高出周围的上地幔放射性元素含量的几百到1 000倍,因此它是上地幔中的热动力源,在上地幔加热、上涌和产生地幔柱中起着关键作用。

Fig.16 Comparison of radiogentic elements in various rock types from the mantle transition zone or “Second Continent”. Modified after [12].

图17 东亚大陆之下地幔过渡带结构及其造壳成陆功能的东西向剖面图(据文献[19-20]修改)

Fig.17 Mantle transition zone beneath East Asia: An east-west transect illustrating its structure and role in crustal growth and continent formation. Modified after [19-20].

图18 中国东部大陆陆缘洋板块向下俯冲到地幔过渡带中并停滞堆积的示意图(据文献[16]修改)

Fig.18 Schematic diagram illustrating the subduction, stagnation, and accumulation of an oceanic plate beneath eastern China to the mantle transition zone. Modified after [16].

图19 第二大陆俯冲堆积示意图(据文献[16]修改) 地表岩浆弧和沉积物构成的陆壳板块或TTG板块俯冲下去后堆积在660 km处地幔过渡带中,部分也可能堆积在核幔边界上。

Fig.19 Schematic diagram of subduction and accumulation in the “Second Continent”. Modified after [16].

图20 地幔过渡带产生含水地幔底辟功能模型示意图(据文献[21]修改)

Fig.20 Schematic model illustrating the generation of hydrated mantle diapirs from the mantle transition zone. Modified after [21].

图21 指示地幔过渡带或第二大陆热场触发周围地幔发生部分熔融且形成软流底辟上涌并在地幔加热熔融、上涌和地壳发生裂谷作用中起到与洋中脊类似的大陆动力学关键作用的示意图(据文献[29]修改)

Fig.21 A schematic mode of mantle dynamics analogous to mid-ocean ridges: From thermal anomalies in the transition zone to asthenspheric upwelling and continental rifting. Modified after [29].

图22 第二大陆的造壳成陆模型(据文献[21]修改)

Fig.22 Model of crustal growth and continent formation in the “Second Continent”. Modified after [21].

图23 东亚位于太平洋、印度洋四条双向俯冲带夹持的独特的三角带,四条双向俯冲带为其下地幔过渡带提供了大量的水并使其成为全球最富含水的地幔过渡带(据文献[27]修改)

Fig.23 East Asia as a unique triangular zone: Hydrating the mantle transition zone via bidirectional subduction. Modified after [27].

图24 北冰洋将消失、亚洲与美洲相连示意图(据文献[12]修改)

Fig.24 Diagram illustrating the future closure of the Arctic Ocean and the formation of a land bridge between Asia and America. Modified after [12].

图25 表示菲律宾海板块上的五条洋内弧向日本本州岛之下俯冲且没有任何增生的大地构造背景及其剖面(据文献[44]修改)

Fig.25 Tectonic setting and profile showing five intra-oceanic arcs on the Philippine Sea Plate subducting beneath Japan’s Honshu without accretion. Modified after [44].

图26 本州岛中部大陆地壳的厚度只有约30~35 km且没有任何增生的剖面(据文献[43]修改)

Fig.26 A crustal profile of 30-35 km thickness with no accretion in Central Honshu Island. Modified after [43].

图27 篮子模型——捕获沉积物的俯冲机制示意图(据文献[21]修改)

Fig.27 The Basket Model: A schematic diagram of a sediment-trapping subduction mechanism. Modified after [21].

图28 板块汇聚带因构造侵蚀作用受到强烈破坏的证据(据文献[43]修改)

Fig.28 Evidence of intense tectonic erosion in a plate convergence zone. Modified after [43].

图29 日本东北及其周边俯冲板片上面发育的地堑构造把海沟浊积岩增生杂岩运送到地幔深处(据文献[43]修改)

Fig.29 Graben structures on the subducting slab transporting trench turbidites and the accretionary complex into the deep mantle. Modified after [43].

图30 日本东北及其周边的四个断代地质构造单元划分及上面发育的地堑把浊积岩运送到深地幔中(据文献[12]修改) 构造侵蚀作用的意义是使地幔过渡带的TTG物质总量大增而使其具有造壳成陆的功能。

Fig.30 Tectonic framework of Northeast Japan: Four chronostratigraphic units and associated graben systems transporting turbidites to the deep mantle. Modified after [12].

参考文献 45

[1]	CHENG Y, XIAO Q H, LI T D, et al. Geochemistry and tectonic history of seamount remnants in the Xingshuwa Subduction Accretionary Complex of the Xar Moron area, eastern margin of the Central Asian Orogenic Belt[J]. Acta Geologica Sinica, 2021, 95(4): 1086-1098.
[2]	OSANAI Y, KOMATSU M, OWADA M. Metamorphism and granite genesis in the Hidaka metamorphic belt, Hokkaido, Japan[J]. Journal of Metamorphic Geology, 1991, 9: 111-124.
[3]	WHITE W M. Oceanic island basalts and mantle plumes: the geochemical perspective[J]. Annual Review of Earth and Planetary Sciences, 2010, 38(1): 133-160.
[4]	SAFONOVA I, MARUYAMA S. Asia: a frontier for a future supercontinent[J]. International Geology Review, 2014, 56: 1051e1071.
[5]	DEWEY J F, WINDLEY B F. Growth and differentiation of the continental crust[J]. Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences, 1981, 301(1461): 189-206.
[6]	FYFE W S. The evolution of the Earth’s crust: modern plate tectonics to ancient hot spot tectonics[J]. Chemical Geology, 1978, 23: 89-114.
[7]	ARMSTRONG R L. Radiogenic isotopes: the case for crustal recycling on anearsteady state nocontinental-growth Earth[J]. Philosophical Transactions of the Royal Society of London 1981, A301: 443-472.
[8]	YAMAMOTO S, SENSHU H, RINO S, et al. Granite subduction: arc subduction, tectonic erosion and sediment subduction[J]. Gondwana Research, 2009, 15(3/4): 443-453.
[9]	RINO S, KON Y, SATO W, et al. The Grenvillian and Pan-African orogens: world’s largest orogenies through geologic time, and their implications on the origin of superplume[J]. Gondwana Research, 2008, 14: 51-72.
[10]	RICHARDSON W P, OKAL E A, VAN DER LEE S. Rayleigh-wave tomography of the Ontong-Java Plateau[J]. Physics of the Earth and Planetary Interiors, 2000, 118(1/2): 29-51.
[11]	SENO T, MARUYAMA S. Paleogeographic reconstruction and origin of the Philippine Sea[J]. Tectonophysics, 1984, 102: 53-84.
[12]	SAFONOVA I Y, MARUYAMA S. Asia: a frontier for a future supercontinent Amasia[J]. International Geology Review, 2014, 56(9): 1051-1071.
[13]	MARUYAMA S, HASEGAWA A, SANTOSH M, et al. The dynamics of big mantle wedge, magma factory, and metamorphic-metasomatic factory in subduction zones[J]. Gondwana Research, 2009, 16: 414-430.
[14]	OMORI S, SENSU H, KAWAI K, et al. Pacific-type orogens: new concepts and variations inspace and time from present to past[J]. Journal of Geography, 2011, 120: 115-223(in Japanese with English abstract and captions).
[15]	KAWAII K, TSUCHIYA T, TSUCHIYA J, et al. Lost primordial continents[J]. Gondwana Research, 2009, 16: 581-586.
[16]	KAWAII K, YAMAMOTO S, TSUCHIYA T, et al. The seond continent: existence of granitic continental materials around the bottom of the mantle transition zone[J]. Geoscience Frontiers, 2013, 4: 1-6.
[17]	HU A Q, WEI G J, ZHANG J B, et al. SHRIMP U-Pb ages for zircons of the amphibolites and tectonic evolution significance from the Wenquan domain in the West Tianshan Mountains, Xinjiang, China[J]. Acta Petrologica Sinica, 2008, 24(12): 2731-2740 (in Chinese with English abstract).
[18]	ZHAO W P, JIA Z K, WEN Z G, et al. The discovery of the blueschists from the Baerluke ophiolitic melange belt in Western Junggar, Xinjiang[J]. Northwest Geology, 2012, 45(2): 136-138 (in Chinese with English abstract).
[19]	TAIRA K, PICKERING T, WINDLEY B F, et al. Accretion of Japanese island arcs and implications for the origin of Archean greenstone belts[J]. Tectonics, 1992, 11: 1224-1244.
[20]	ZHAO G, SUN M, WILDE S A, et al. A Paleo-Mesoproterozoic supercontinent: assembly, growth and breakup[J]. Earth-Science Reviews, 2004, 67: 91-123.
[21]	SENSHU H, MARUYAMA S, RINO S, et al. Role of tonalite-trodhjemite-granite (TTG) crust subduction on the mechanism supercontinent breakup[J]. Gondwana Research, 2009, 15(3): 433-442.
[22]	KANEKO Y, MARUYAMA S, KADARUSMAN A, et al. On-going orogeny in the outer-arc of the Timor-Tanimbar region, eastern Indonesia[J]. Gondwana Research, 2007, 11: 218-233.
[23]	BRENAN J M, SHAW H F, PHINNEY D L, et al. Rutile-aqueous fluid partitioning of Nb, Ta, Hf, Zr, U and Th: implications for high field strength element depletions in island-arc basalts[J]. Earth and Planetary Science Letters, 1994, 128(3): 327-339.
[24]	PRYTULAK J, ELLIOTT, et al. TiO₂ enrichment in ocean island basalts[J]. Earth and Planetary Science Letters, 2007, 263(3): 388-403.
[25]	SAUNDERS A. Putting continents asunder[J]. Nature, 1988, 332(6166): 679.
[26]	McCULLOCH M T, GAMBLE J A. Geochemical and geodynamical constraints on subduction zone magmatism[J]. Earth and Planetary Science Letters, 1991, 102(3): 358-374.
[27]	MARUYAMA S, SANTOSH M, ZHAO D, et al. Superplume, supercontinent, and post-perovskite: mantle dynamics and anti-plate tectonics on the core-mantle boundary[J]. Gondwana Research, 2007, 11: 7-37.
[28]	SANTOSH M, MARUYAMA S, KOMIYA T, et al. Orogens in the evolving Earth: from surface continents to ‘lost continents’ at the core-mantle boundary[J]. Geological Society, London, Special Publications, 2010, 338: 77-116.
[29]	HONG K C, WANG S F, ZHANG S W, et al. Oligocene melting of subducted mélange and its mantle dynamics in northeast Asia[J]. Geology, 2024, 52: 539-544.
[30]	CRUZ U A M, MARSCHALL H R, GAETANI G A, et al. Generation of alkaline magmas in subduction zones by partial melting of mélange diapirs: an experimental study[J]. Geology, 2018, 46(4): 343-346.
[31]	GERYA T V, YUEN D A. Rayleigh-Taylor instabilities from hydration and melting propel ‘cold plumes’ at subduction zones(Article)[J]. Earth and Planetary Science Letters, 2003, 212(1): 47-62.
[32]	MARSCHALLCA H R, SCHUMACHER J C. Arc magmas sourced from mélange diapirs in subduction zones[J]. Nature Geoscience, 2012, 5(12): 862-867.
[33]	CODILLO E A, Le ROUX V, KLEIN B, et al. The ascent of subduction zone mélanges: experimental constraints on mélange rock densities and solidus temperatures[J]. Earth and Planetary Science Letters, 2023, 621: 118-398.
[34]	HALL P S, KINCAID, et al. Diapiric flow at subduction zones: a recipe for rapid transport[J]. Science, 2001, 292(5526): 2472-2475.
[35]	REBAZACA A M, MALLIK A, STRAUB S M. Multiple episodes of rock-melt reaction at the slab-mantle interface: formation of high silica primary magmas in intermediate to hot subduction zones[J]. Journal of Petrology, 2023, 64(3): 1408-1424.
[36]	HASEGAWA A, NAKAJIMA J, KITA S, et al. Anomalous deepening of a belt of intraslab earthquakes in the Pacific slab crust under Kanto, central Japan: possible anomalous thermal shielding, dehydration reactions, and seismicity caused by shallower cold slab material[J]. Geophysical Research Letters, 2007, 34: L09305.
[37]	KLEIN, BENJAMIN Z, BEHN, et al. On the evolution and fate of sediment diapirs in subduction zones[J]. Geochemistry, Geophysics, Geosystems, 2021, 22(11): e2021GC009873.
[38]	RYDELEK P A, SACKS I S. Asthenospheric viscosity inferred from correlated land-sea earthquakes in Northeast Japan[J]. Nature, 1988, 336(6196): 234-237.
[39]	ZHAO W, MECHIE J, BROWN L D, et al. Crustal structure of central Tibet as derived from project INDEPTH wide-angle seismic data[J]. Geophysical Journal International, 2001, 145(2): 486-498.
[40]	DONG Y, XIONG S, WANG F, et al. Triggering of episodic back-arc extensions in the Northeast Asian continental margin by deep mantle flow[J]. Geology, 2023, 51(2): 193-198.
[41]	WADA I, HE J H, HASEGAWA A, et al. Mantle wedge flow pattern and thermal structure in Northeast Japan: effects of oblique subduction and 3-D slab geometry[J]. Earth and Planetary Science Letters, 2015, 426: 76-88.
[42]	WANG Z W, ZHAO D P. 3D anisotropic structure of the Japan subduction zone[J]. Science Advances, 2021, 7(4): eabc9620.
[43]	MARUYAMA S, SANTOSH M, ZHAO D, et al. Superplume, supercontinent, and post-perovskite: mantle dynamics and anti-plate tectonics on the core-mantle boundary[J]. Gondwana Research, 2007, 11: 7-37.
[44]	ISOZAKI Y, AOKI K, NAKAMA T, et al. New insight into a subduction-related orogen: a reappraisal of the geotectonic framework and evolution of the Japanese Islands[J]. Gondwana Research, 2010, 18(4): 709.
[45]	NAKAJIMA, TAKASHI. The Ryoke plutonometamorphic belt: crustal section of the Cretaceous Eurasian continental margin[J]. Lithos, 1994, 33(1): 51-66.

中国东部陆缘中、新生代洋板块深地质作用追踪

Tracing the deep geological processes of the Mesozoic-Cenozoic oceanic plate on the continental margin of the East Asian continent in China

RichHTML

PDF (PC)

可视化

摘要/Abstract

引用本文

使用本文

图/表 31

参考文献 45

相关文章 3

编辑推荐

Metrics

本文评价

[1]	万天丰. 论全球岩石圈板块构造的动力学机制[J]. 地学前缘, 2018, 25(2): 320-335.
[2]	任建业于建国张俊霞. 济阳坳陷深层构造及其对中新生代盆地发育的控制作用[J]. 地学前缘, 2009, 16(4): 117-137.
[3]	李文勇曾祥辉王信国安战锋. 北黄海盆地构造运动学解析[J]. 地学前缘, 2009, 16(4): 74-86.