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作者简介:

赵越,男,1955年生。研究员,博士生导师,主要从事区域地质、大地构造及极地地质研究。E-mail:yuezhao2307@163.com。

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目录contents

    摘要

    一百年前中国地质学会成立,先驱者们竖立起中国地质科学的旗帜,也是中国科学的第一面旗帜,从此中国地质科学发展进入快车道。燕山运动、中国北方科研究,长身贝研究、北京猿人头盖骨的发现是中国地质科学快速进入国际赛道的标志。经历了近百年的研究,北京西山及北京北山、冀北和辽西典型地区积累的证据和资料表明,翁文灏提出的燕山运动A期(幕)发生在160±3 Ma前;晚侏罗世早—中期记录了以髫髻山组和蓝旗组为代表的区域强烈火山喷发和广泛的岩浆侵入(中间期/幕);晚侏罗世晚期区域发育逆冲推覆构造;燕山期构造发展至早白垩世早期135 Ma,冀北张家口组和辽西义县组之下的不整合为燕山运动B期结束的代表。燕山运动是东亚大陆构造体制从古特提斯及古亚洲洋构造域转变为环太平洋活动大陆边缘构造域的产物。这是中国东部和东亚区域中生代独特的重大的地质构造事件。

    Abstract

    The Geological Society of China was founded one hundred years ago. The pioneers erected the banner of Chinese geological science, which was also the first banner of Chinese science. Since then, the development of geological sciences in China has entered the fast lane. The Yanshan (Yenshan) Movement, the Fusulinida in northern China, the Productus researches and the discovery of the skull of Peking man were the symbols of the rapid entry of Chinese geological science into the international track. According to the evidence and data accumulated in the Western Hills of Beijing, the northern Hebei and western Liaoning regions, the A phase of Yanshan Movement, proposed by Wong (1929), occurred 160±3 Ma ago. In the earlier to Middle-Late Jurassic, the region represented by the Tiaojishan Formation and the Lanqi Formation was characterized by strong volcanic eruption and extensive magmatic intrusion (intermediary phase). Overthrusting structures were developed in the later Late Jurassic. The Yanshanian structures were developed till 135 Ma in earlier Cretaceous, and the unconformity beneath the Zhangjiakou Formation in northern Hebei and the Yixian Formation in western Liaoning Province is representative of the end of B phase of the Yanshan Movement. The Yanshan Movement is a result of the transformation of the East Asian continental tectonic regime from the suturing of Paleo-Tethys and Paleo-Asian oceans to the onset of subduction of the Paleo-Pacific Ocean along the eastern Asian continental in later Jurassic to earlier Cretaceous during ca.160~135 Ma. This is a unique and significant tectonic event in East China and East Asia during the Mesozoic.

  • 2022年中国地质学会迎来百年华诞。回望历史,奠基者们重现视野。章鸿钊、丁文江、翁文灏、李四光等带领创业者们砥砺前行,创建地质调查所,组建中国地质学会,竖立起中国地质科学的旗帜,同时也是中国科学的第一面旗帜(张九辰,2005; 王鸿祯,2007)。1926年翁文灏在第3届泛太平洋科学会议上提出了燕山运动(Yenshan Movement或Yanshan Movement)的概念(Wong,1926)。次年及其后,翁文灏连续著文论述燕山运动(Wong,19271929)。九十余年过去了,燕山运动已成为国内外广泛使用的学术术语和教学与研究的要点(任纪舜等,1990; 赵越等,1994; 崔盛芹,1999; Davis et al.,2001; Wang et al.,2005; 葛肖虹等,2014)。燕山运动塑造了中国东部现今的构造格局,也成为中国科学家对世界地质科学的重要贡献之一。值此中国地质学会成立百年之际,本文回顾历史,追溯燕山运动的提出和对其认识的演变,致敬并缅怀翁文灏先生和中国地质学会的奠基者们。

  • 1 燕山运动的提出与演变

  • 1926年10月30日~11月11日,第3届泛太平洋科学会议在日本东京举行。翁文灏、竺可桢等12位中国科学家以中国科学社名义代表中国参会(刘亮,2015)。这是中国科学家第一次组团参加国际科学会议,是中国现代科学里程碑式的事件。作为中国科学社社长和地质调查所所长,翁文灏作了“中国东部地壳运动”的报告(Wong,1926),还代章鸿钊、李四光分别宣读他们提交会议的论文“中国温泉之分布”、“中国北部古生代含煤地层之时代及其分布”。在会上中国代表力争中国在国际科学界的代表席位,从而催生了其后成立的国立中央研究院(竺可桢,1927; 刘亮,2015)。翁文灏的“中国东部地壳运动”报告,用中国东部大地构造图作为附图,对中国东部中生代以来的地壳运动做了阐述,提出了燕山运动。次年2月,在中国地质学会第5届年会上,翁文灏作“中国东部中生代以来之地壳运动及火山活动”的会长演说,文章随后发表在《中国地质学会会志》第6卷第1期(Wong,1927)。翁文灏的文章对其第3届泛太平洋科学会议的论文作了修改、增补、扩充。

  • 翁文灏(Wong,1927)在文章中将中国东部中生代以来的地壳运动分为四大期:秦岭期、燕山期、南岭期、陇山期,重点论述了燕山期。翁文灏对中生代以来的地壳运动分期和构造幕时代的确定以地层,特别是煤系地层及其所含化石为基础和主要依据。燕山运动的时代被确定发生在北京西山九龙山组沉积之后,髫髻山组沉积之前,时代为晚侏罗世,白垩纪之前。作为北京西山地质志的作者之一,翁文灏注意到北京西山九龙山组与髫髻山组地层的倾角变化并不显著,但是从区域地层、构造、岩浆活动等要素的分析,确信髫髻山组沉积前区域重要变形和剥蚀的发生。由于北京西山更为详细的地层和地质构造的工作和证据,翁文灏将髫髻山组沉积前的构造运动命名为燕山运动。翁文灏还讨论了包括日本、朝鲜半岛和美国、加拿大等环太平洋地区中生代的构造变形。

  • 两年后翁文灏(Wong,1929)对阴山与秦岭之间华北为主要区域的燕山期逆冲构造进行专门论述。翁文灏系统分析了区域燕山晚期逆冲构造(图1),认识到这是燕山晚期变形的重要特征,并用燕山造山作用阐明燕山运动的重要意义。翁文灏根据北京西山、冀北、辽西和山东的地层记录将燕山运动划分为A期(幕),中间期(幕)和B期(幕)(图2、3)。A期时代发生在北京西山九龙山组沉积之后,髫髻山组沉积之前,区域出现宽广褶皱; 中间期发生强烈的火山喷发; B期出现剧烈褶皱和逆冲断层作用,时代发生在中白垩世,但是缺失地层约束(Wong,1929)。

  • 翁文灏提出中国东部燕山运动后,中国东部区域的造山运动逐渐成为热点议题。丁文江(Ting,1929)、章鸿钊(1936)、谢家荣(Hsien,1936)、李四光(Lee,1939)、李春昱(Lee,1950)、黄汲清(1954)赵宗溥(19591963)李廷栋(1982)崔盛芹等(1985)赵越(1990)任纪舜等(19901999)、Davisn et al.(1998,2001)、崔盛芹(1999)董树文等(2000,2015,2019)赵越等(2004a2004b)、王鸿祯等(Wang Hongzhen et al.,2005)、葛肖虹等(2014) 分别著文讨论燕山运动,但是燕山运动的时代、构造幕及阶段的划分以及构造背景和属性认识分歧较大(朱日祥等,20122019; 吴福元等,2014; 孟庆任,2017; 王瑜等,2018; Hao et al.,2019; 郑建平,2020; 林伟等,2021; 朱光等,2021)。主要原因是一方面研究者以传统的构造幕划分构造运动,确定其时代; 另一方面几十年间燕山运动构造幕确立的依据——地层时代不断发生变化,地层时代确定的精度不高。崔盛芹等(1985)主张以燕山地区地层对比为基础确定和划分燕山运动。然而历史的历程是:自丁文江(1929)后,研究者基本将中国东部侏罗纪—白垩纪时期发生的构造运动命名为燕山运动,或燕山旋回。李春昱(Lee,1950)曾主张应尊重翁文灏(Wong,1929)的初衷限定使用燕山运动,替代当时诸多意义不清的燕山运动划分意见。因四川境内主要造山运动发生在白垩纪红色砾岩沉积以后,他提出以四川运动代表中生代末期的造山运动,表示在时间上不同于翁文灏的燕山B期(Lee,1950)。

  • 图1 宣化以南(黄羊山)构造的重新解释(据Wong,1929修改,中文为作者所加)

  • Fig.1 A re-interpretation of the structure south of Hsuan Hua (Huangyangshan, Xuanhua) (modified after Wong, 1929, and the Chinese words were added by authors)

  • Hl—震旦系灰岩; Jc—侏罗系煤层; Js—侏罗系砂岩

  • Hl—Sinian limestone; Jc—Jurassic coal series; Js—Jurassic sandstone

  • 图2 翁文灏的“燕山运动”(据Wong,1929修改,中文为作者所加)

  • Fig.2 The “Yanshan Movement” identified by Wong (modified after Wong, 1929, and the Chinese words were added by authors)

  • 图3 翁文灏燕山运动的期次划分(据Wong,1929

  • Fig.3 The phases of Yanshan Movement proposed by Wong (after Wong, 1929)

  • 2 北京西山与燕山地区燕山期变形

  • 北京西山是燕山运动的命名地(Wong,1927)。北京西山与燕山地区燕山期变形过程和时限是深入认识翁文灏提出的燕山运动的基础。近年来,很多研究者们在燕山以及北京西山等地区开展了构造变形(张长厚等,20112012; Li et al.,2016)、沉积盆地(Liu et al.,2015; Shi et al.,2019; Liu et al.,2021)、火成岩(李伍平等,20012012; 马强等,2009; Zhang et al.,2014)等诸多方面的工作,进一步深化了翁文灏先生提出的燕山运动的区域变形、岩浆作用、盆地演化和时代及其构造背景的认识。

  • 北京西山侏罗纪地层从下向上为杏石口组、南大岭组、窑坡组、龙门组、九龙山组、髫髻山组(图4),窑坡组和龙门组又称门头沟煤系。过去这套煤系地层和所含植物化石被认为是早侏罗世或早—中侏罗世。参考有海相地层约束的英国约克郡植物群(Harris,1979)的研究,陈芬等(1984)将北京西山侏罗纪植物群和区域这一时期含煤地层主体时代划归中侏罗世。此后,由于同位素年代学研究的进步,北京西山侏罗纪地层的时代有了可靠的年代约束。杏石口组的时代为早侏罗世(Yang et al,2006)。南大岭组时代主体为中侏罗世(Gao et al.,2018)。窑坡组、龙门组和九龙山组的时代为中侏罗世中—晚期。髫髻山组的底部时代为157±3 Ma,属于晚侏罗世(赵越等,2004a; Gao et al.,2018),而上部时代为早白垩世(袁洪林等,2005)。因此,北京西山髫髻山组时代实际分别与冀北髫髻山组+后城组和辽西蓝旗组+土城子组相当。北京西山并不缺少侏罗纪晚期—早白垩世早期沉积。北京西山东岭台组火山岩时代大致与冀北张家口组火山岩相当,年龄为约137~130 Ma(袁洪林等,2005; 张宏等,2005)。

  • 图4 燕山地区燕山期地层对比图

  • Fig.4 Stratigraphic columns of Jurassic to Early Cretaceous volcanic and sedimentary rocks across the Yanshan belt

  • 年龄数据来自:(1)—袁洪林等,2005;(2)—李伍平等,2001;(3)—于海飞等,2016;(4)—Fu et al.,2018;(5)—赵越等,2004a;(6)—Hao et al.,2019;(7)—Davis et al.,2001;(8)—Gao et al.,2018;(9)—赵越等,2006;(10)—牛宝贵等,2003;(11)—张宏等,2005;(12)—Cope,2003;(13)—刘健等,2006;(14)—Hao et al.,2020;(15)—Cope et al.,2007;(16)—Li et al.,2016;(17)—张运强等,2014;(18)—Liu et al.,2012;(19)—Liu et al.,2021;(20)—Swisher et al.,2002;(21)—马强等,2009;(22)—Chang et al.,2009;(23)—Gao et al.,2019;(24)—Chang et al.,2014;(25)—Yang et al.,2008

  • Age data are from: (1) —Yuan Honglin et al., 2005; (2) —Li Wuping et al., 2001; (3) —Yu Haifei et al., 2016; (4) —Fu et al., 2018; (5) —Zhao Yue et al., 2004a; (6) —Hao et al., 2019; (7) —Davis et al., 2001; (8) —Gao et al., 2018; (9) —Zhao Yue et al., 2006; (10) —Niu Baogui et al., 2003; (11) —Zhang Hong et al., 2005; (12) —Cope, 2003; (13) —Liu Jian et al., 2006; (14) —Hao et al., 2020; (15) —Cope et al., 2007; (16) —Li et al., 2016; (17) —Zhang Yunqiang et al., 2014; (18) —Liu et al., 2012; (19) —Liu et al., 2021; (20) —Swisher et al., 2002; (21) —Ma Qiang et al., 2009; (22) —Chang et al., 2009; (23) —Gao et al., 2019; (24) —Chang et al., 2014; (25) —Yang et al., 2008

  • 冀北杏石口组的时代为早侏罗世(Liu et al.,2012),南大岭组、下花园组为中侏罗世,九龙山组为中侏罗世末期—晚侏罗世初期(张运强等,2014),髫髻山组火山岩底部年龄164~159 Ma(刘健等,2006; Li et al.,2016),土城子组为晚侏罗世—早白垩世。在冀北承德鸡冠山,褶皱的土城子组(后城组)被未经变形的张家口组火山岩角度不整合覆盖(图5)。张家口组底部火山岩锆石U-Pb年龄135±1 Ma(赵越等,2004a)。

  • 辽西的侏罗纪盆地以牛营子地区和北票地区为代表。牛营子地区中侏罗世郭家店组含煤地层和砾岩层被蓝旗组火山岩角度不整合覆盖,底部火山岩时代为158±1 Ma(赵越等,2004a); 而北票盆地兴隆沟组为早侏罗世,北票组含煤地层为早侏罗世晚期至中侏罗世早期,海房沟组时代为中侏罗世中—晚期至晚侏罗世初期,其上被蓝旗组火山岩角度不整合覆盖,年龄为161 Ma,159±4 Ma(马强等,2009; Chang et al.,2009)。综上所述,北京西山和冀北髫髻山组及辽西蓝旗组底部火山岩年龄为160±3 Ma。这是翁文灏燕山运动A期(Wong,1929)的时代,与翁文灏最初限定的燕山运动的时代基本一致。

  • 图5 冀北承德鸡冠山上侏罗统—下白垩统后城组(J3-K1h)与下白垩统张家口组(K1zh)之间的角度不整合接触(张家口组底部年龄来自赵越等,2004a

  • Fig.5 The unconformity between the Upper Jurassic to Lower Cretaceous Houcheng Formation and Lower Cretaceous Zhangjiakou Formation (U-Pb age of Zhangjiakou Formation is from Zhao Yue et al., 2004a)

  • 北京西山盆地燕山期的演化从早侏罗世开始,盆地北缘177 Ma的花岗斑岩岩床侵入说明盆地还没有变形(Gao et al.,2018)。南大岭组是一套溢流玄武岩-安山玄武岩,锆石U-Pb年龄介于175±1~168±2 Ma之间,加权平均年龄为172±1 Ma,可作为南大岭组时代属于中侏罗世的参考值(Gao et al.,2018)。南大岭组火山岩是北京西山原型盆地的铸模(赵越等,2002)。窑坡组为一套沼泽-湖泊相沉积。从龙门组沉积开始,盆地周缘开始逐渐快速变形; 九龙山组沉积期北京西山盆地开始分化,原型盆地中心褶皱隆起,盆地中心向北迁移(李海龙等,2014); 髫髻山组-土城子组沉积期盆地演化结束(赵越等,2002)。盆地北缘被下白垩统东岭台组火山岩不整合覆盖。伴随北京西山盆地演化,盆地南缘南大寨断裂先逆冲,后在白垩纪伸展期后部发生新生反向正断(Wang et al.,2011)。而北京北山千家店盆地,原来认为是土城子期的盆地被证实是燕山运动A期(160 Ma)开始发育的盆地(Fu et al.,2018)。盆地开始接收北侧东西向古北口大断裂方向的物源,以髫髻山期火山沉积岩为主; 156 Ma后盆地西缘北北东向千家店断裂向东逆冲,盆地随后消亡(Fu et al.,2018)。区域上135 Ma张家口组火山岩不整合覆盖在变形的髫髻山组和土城子组地层之上(牛宝贵等,2003; 赵越等,2004b)。

  • 冀北下板城地区,早—中侏罗世火山-煤系-粗碎屑沉积被髫髻山组火山岩不整合覆盖。髫髻山组火山岩底部年龄164~159 Ma(Davis et al.,2001; 刘健等,2006; Li et al.,2016)。髫髻山期火山喷发结束后,土城子组沉积早期区域发生逆冲断裂作用(Davis et al.,1998; Liu et al.,2015; 图6、7)。而后晚侏罗世—早白垩世早期的火山-沉积地层被未变形的135 Ma张家口组火山岩不整合覆盖。

  • 辽西北票地区早—中侏罗世火山-煤系-粗碎屑沉积被蓝旗组火山岩不整合覆盖。蓝旗组底部火山岩年龄为161~159 Ma(马强等,2009; Chang et al.,2009)。晚侏罗世区域发生逆冲推覆构造,承德下板城为典型地区(图6、7)。冀北下花园黄羊山逆冲推覆构造被确认(图3; Wu et al.,2021),但是南天门式的推覆构造(Wong,1929)未被证实。区域更早的大规模逆冲推覆作用发生在晚三叠世(Hu et al.,2010; Liu et al.,2021)。与燕山地区其他区域相同,自早白垩世中期始伸展构造逐渐发育,火山喷发和岩浆侵入达到高峰。下白垩统义县组火山岩角度不整合覆盖在蓝旗组和土城子组火山-沉积地层之上。土城子组底部火山岩物源来自遭受剥蚀的三道营断裂上盘曾经覆盖的髫髻山组火山岩(图7)。

  • 北京西山及北山、冀北和辽西典型盆地和地点的分析说明:① 燕山运动A期发生在160±3 Ma前,这一时期区域强烈的变形导致更早的大-中盆地开始分化,迁移,消亡; 诸多小盆地新生。② 晚侏罗世早—中期记录了髫髻山组和蓝旗组为代表的区域强烈火山喷发和广泛的岩浆侵入(中间期),晚侏罗世晚期区域发育逆冲推覆构造。③ 北京西山东岭台组、冀北张家口组和辽西义县组之下的不整合为燕山运动B期的产物,时代为早白垩世早期135 Ma前,之后区域伸展构造开始发育。山东莱阳盆地的青山组后被证实是早白垩世中期之后的地层,与张家口组或义县组时代相当(张岳桥等,2008)。至此,翁文灏记录的燕山运动主要地质构造以及变形与岩浆过程得到确认,但是其构造背景和意义可能更为重要。

  • 图6 冀北承德盆地地质构造图及土城子组(后城组)古流向图(据Liu et al.,2015修改)

  • Fig.6 Geological sketch map showing the paleocurrents directions in Chengde County, northern Hebei Province (after Liu et al., 2015)

  • 1 —第四系; 2—下白垩统张家口组; 3—上侏罗统—下白垩统土城子组3段; 4—土城子组2段; 5—土城子组1段; 6—上侏罗统髫髻山组; 7—上侏罗统九龙山组; 8—中侏罗统下花园组; 9—中侏罗统南大岭组; 10—下侏罗统杏石口组; 11—中三叠统二马营组; 12—下三叠统刘家沟组; 13—奥陶系; 14—寒武系; 15—青白口系; 16—蓟县系; 17—长城系; 18—太古宇; 19—早白垩世花岗岩; 20—晚侏罗世花岗岩; 21—平行不整合; 22—角度不整合; 23—断层; 24—逆断层; 25—正断层; 26—走滑断层; 27—正常产状及倒转产状; 28—铁路; 29—河流; 30—古流向及测量个数; 31—锆石U-Pb测年数据; 32—40Ar/39Ar法测年数据; 33—火山岩; 34—砾岩; 35—含砾砂岩; 36—砂岩; 37—粉砂岩; 38—泥岩; 39—白云岩; 40—角度不整合; 41—平行不整合; 42—逆断层; 43—正断层; 44—走滑断层; 45—地层产状。断层名称:SMF.—双庙断层; SDYF.—三道营断层; JYQF.—吉余庆断层; CCF.—承德县断层。数据来源:Davis et al.,2001; Cope,2003; 赵越等,2004a; 牛宝贵等,2003; Davis,2005; 刘健等,2006

  • 1 —Quaternary sediments; 2—Lower Cretaceous Zhangjiakou Formation; 3—upper part of the Upper Jurassic-Lower Cretaceous Tuchengzi Formation; 4—middle part of Tuchengzi Formation; 5—lower part of Tuchengzi Formation; 6—Upper Jurassic Tiaojishan Formation; 7—Upper Jurassic Jiulongshan Formation; 8—Middle Jurassic Xiahuayuan Formation; 9—Middle Jurassic Nandaling Formation; 10—Lower Jurassic Xingshikou Formation; 11—Middle Triassic Ermaying Formation; 12—Lower Triassic Liujiagou Formation; 13—Ordovician sedimentary rocks; 14—Cambrian sedimentary rocks; 15—Qingbaikou System; 16—Jixianian System; 17—Changchengian System; 18—Archean metamorphic rocks; 19—Early Cretaceous granite; 20—Late Jurassic granite; 21—disconformity; 22—unconformity; 23—fault; 24—thrust fault; 25—normal fault; 26—strike-slip fault; 27—attitude and inverted attitude; 28—railway; 29—river; 30—paleocurrent data; 31—U-Pb zircon ages; 32—40Ar/39Ar ages; 33—volcanic rocks; 34—conglomerates; 35—pebbly sandstones; 36—sandstones; 37—siltstones; 38—mudstones; 39—dolomite; 40—unconformity; 41—disconformity; 42—thrust fault; 43—normal fault; 44—strike-slip fault; 45—attitude. Faults: SMF.—Shuangmiao fault; SDYF.—Sandaoying fault; JYQF.—Jiyuqing fault; CCF.—Chengde County fault. Age data are from: Davis et al., 2001; Cope, 2003; Zhao Yue et al., 2004a; Niu Baogui et al., 2003; Davis, 2005; Liu Jian et al., 2006

  • 图7 晚侏罗世承德盆地北区岩相柱状图(据刘健等,2013修改)

  • Fig.7 Late Jurassic lithofacies column in southern Chengde Basin (after Liu Jian et al., 2013)

  • (a)—土城子组野外照片;(b)—岩相柱状图;(c)—砾石成分统计图; 1—粉砂质泥岩; 2—泥岩; 3—砂岩; 4—含砾砂岩; 5—砾岩; 6—晶屑凝灰岩; 7—集块岩; 8—火山角砾岩及火山岩; 9—碳酸盐岩; 10—硅质岩; 11—花岗岩; 12—火山岩; 13—平行层理; 14—槽状交错层理; 15—板状交错层理; 16—叠瓦状砾石; 17—砂岩透镜体; 18—角度不整合; 19—观测点及统计砾石数量

  • (a) —Field photographs from Tuchengzi Formation; (b) —Late Jurassic lithofacies column; (c) —gravel composition; 1—silty mudstone; 2—mudstone; 3—sandstone; 4—pebbly sandstone; 5—conglomerate; 6—crystal tuff; 7—agglomerate lava; 8—volcanic breccia and volcanic rocks; 9—carbonate rock; 10—siliceous rocks; 11—granite; 12—volcanic rocks; 13—parallel bedding; 14—through cross-bedding; 15—tabular cross-bedding; 16—imbricate gravel; 17—sandstone lens; 18—angular unconformity; 19—observation point and gravel statistical quantity

  • 3 东亚区域燕山期变形的构造背景

  • 燕山运动的构造背景及其意义需要从更广阔的时空与更精准的构造过程节点的把握,更深刻的运动-动力分析阐明。翁文灏从环太平洋带分析了燕山运动的构造背景(Wong,19271929)。九十多年来,研究者们探索认识燕山运动的构造背景和动力过程一直没有停歇(Lee,1950; 黄汲清,1954; 赵宗溥,19591963; 李廷栋,1982; 崔盛芹等,1985; 任纪舜等,19901999; 赵越等,19942004a; Davis et al.,19982001; 崔盛芹,1999; Zorin,1999; 郑亚东等,2000; 董树文等,20002019; 朱日祥等,20122019; 吴福元等,2014; 张宏仁,2016; 孟庆任,2017; 王瑜等,2018; Hao et al.,2020; 林伟等,2021; 朱光等,2021)。

  • 中国东部进入中生代后最先发生的重大构造事件是华北陆块与华南陆块沿秦岭造山带的碰撞和大别-苏鲁超高压变质地体的形成折返(Ratschbacher et al.,2003; Liu et al.2006; Li et al.2010; Dong et al.,2016)。这一碰撞造山过程从晚三叠世开始进入峰期,经晚三叠世中—晚期至侏罗纪晚期(约160 Ma; Huang et al.,2018)逐渐结束。华北陆块与华南陆块拼合完成,形成了中国东部大陆雏形。华北陆块北部和中亚造山带南侧在晚三叠世也经历了强烈变形(Hu et al.,2010; Li et al.,2016; Xiao et al.,2018; Zhao et al.,2018),但是华北陆块-中亚造山带东南部与西伯利亚陆块沿蒙古-鄂霍茨克带的拼合发生在中、晚侏罗世—早白垩世,形成了东亚大陆(Zorin,1999; 郑亚东等,2000; Pei et al.,2011; Huang et al.,2018; 许文良等,2022)。华北地块-中亚造山带东南部与西伯利亚地块沿蒙古-鄂霍茨克带的拼合形成了东亚大陆,这是其东缘发展形成古太平洋大洋俯冲带的基础,之前并无确切的古太平洋大洋板块向中国东部大陆边缘下俯冲的证据。而古太平洋大洋板块开始向东亚大陆俯冲发生在晚侏罗世,确凿的证据是古太平洋大洋板块俯冲留下的最早的增生杂岩(Ichikawa et al.,1990; Kimura et al.,1991; Maruyama et al.,1997; Kojima et al.,2000)和俯冲产生的沿古太平洋大陆边缘延续的岩浆岩带(Zhang et al.,2014)。燕山地区和中国东部髫髻山期开始的大规模火山喷发和岩浆侵入正是这一背景下的产物。北京北山千家店盆地和北京西山盆地演化记录了这一转变过程(鲍亦冈等,1983; Fu et al.,2018),从开始南北向的挤压缩短的动力过程转变为北西西-南东东向的挤压缩短的动力过程,并伴有区域北北东向断裂在晚侏罗世开始的左行走滑位移。

  • 古地磁研究曾揭示华北陆块与扬子陆块碰撞与拼合过程和159 Ma前后地块运动的重要改变(Gilder et al.,1997; Huang et al.,2018)。而这一重要陆块运动变化的时代与燕山运动A幕的时代高度吻合。这些区域燕山期的地质构造及古地磁记录正是东亚大陆构造体制从蒙古-鄂霍茨克造域转变为环太平洋活动大陆边缘构造域的写照(赵越等,19942004a)。因此,翁文灏提出并撰文阐述的燕山运动是东亚大陆构造体制转折的产物,是中国东部和东亚中生代独特的大地构造记录,是中国科学家对世界地质科学的重要贡献之一。中国东部和东亚燕山期的构造记录是自然过程,有其特定的动力学背景和时限,不应当简单以侏罗纪—白垩纪概括。

  • 早白垩世早期以后(约135 Ma),古太平洋板块运动方向与东亚大陆小角度交汇,快速向北运动(Engebretson et al.,1985; Seton et al.,2012)。边界条件的运动与动力约束的重要改变和从古太平洋板块运动和能量角度分析,可以推定古太平洋板块俯冲发生板片回撤,角度变陡。由此形成目前观察到的这一时期中国东部区域广泛的伸展和大规模的岩浆作用,并伴随大规模的成矿和深部的动力岩浆过程与岩石圈的减薄(毛景文等,2005; Sun et al.,2007; 吴福元等,2008; Xu et al.,2009; Wang et al.,2011; 朱日祥等,20122019; 杨明桂等,2020; Liu et al.,2021; Mao et al.,2021)。但这已进入后燕山时期,不属于翁文灏燕山运动的范畴。

  • 4 结语

  • 北京西山及北京北山、冀北和辽西典型地区的研究说明:翁文灏提出的燕山运动A期发生在160±3 Ma前; 晚侏罗世早—中期记录了髫髻山组和蓝旗组为代表的区域强烈火山喷发和广泛的岩浆侵入(中间期); 晚侏罗世晚期区域发育逆冲推覆构造; 燕山期构造发展至早白垩世早期135 Ma前结束,冀北张家口组和辽西义县组之下的不整合为燕山运动B期的代表。燕山运动是东亚大陆构造体制从古特提斯构造域-古亚洲洋构造域转变为环太平洋活动大陆边缘构造域的产物。

  • 百年前中国地质学会成立,从此中国地质先驱者们开创了一段快速步入国际地质科学赛道的光辉岁月。他们的理想、他们的奋斗、他们的协作、他们的精神虽然早已隐匿于历史深处,然而从中国地质学会成立,地质调查所图书馆和陈列馆开馆,到燕山运动提出,中国北部之科(Lee,1927)和长身贝(Chao,1927)研究、北京猿人头盖骨发现······星光闪耀,引来国际学术期刊Nature(Gregory,1924)和国内外著名学者们的高度评价(胡适,1922; 李学通,2009)。当时的中国地质科学达到的高度代表了中国科学达到的高度。本文回眸燕山运动,向其创立者致以崇高敬意,也向中国地质调查所的创建者们和中国地质学会的奠基者们致以崇高敬意。翁文灏的燕山运动引领后人,特别是国内诸多著名学者从不同角度开展了相关研究(赵宗溥,1963; 越越等,1994,2004a; 张宏仁等,20132016; 黄迪颖,20152019; 董树文等,2019)。由于邀稿时限,本文只作主要议题简述,没有展开讨论,也没对翁文灏未完成的东南沿海和华南东部燕山期构造问题开展评述,待于后续论文中补充。

  • 致谢:诚挚感谢杨经绥主编和匿名评审专家的悉心评审与意见、建议,特别感谢其中一位匿名评审专家提供翁文灏先生学术生平与贡献的初稿。编辑部为本文提出了建议和提供资料,在此一并致谢。

  • 注释

  • ❶ 胡适.1922. 努力周报,一周专栏.1922年7月23日.

  • 中国地质早期与中国地质学会初创时期的翁文灏

  • 翁文灏是我国地质科学的先驱者。他早年留学比利时鲁汶大学,是我国从欧美获得地质学博士第一人。1912年回国,1913年进入丁文江和章鸿钊建立的农商部地质研究所,主讲矿物学、岩石学等课程,培养了中国第一代地质人才。1913~1920年他和章鸿钊、丁文江一道指导学生到北京西山、河北和江南等地实习,并把实习报告整理编纂成《农商部地质研究所师弟修业记》一书正式印行。1920年,在他们的指导下,地质调查所年轻骨干叶良辅等发表了《北京西山地质志》,该报告是我国第一部区域地质调查著作,同时也是翁文灏后来提出燕山运动的重要基础性工作。

  • 作为中国地质科学的开创者,他的科学生涯多半在考察的路上。他和同时代的一批先驱者,将这一传统深深植入当时的中国地质学界。1921年继丁文江出任地质调查所代所长和所长,带领全体同仁取得了一批具有重要国际影响的成果。他在极其艰苦的条件下开展地质调查和研究,先后组织了几次重要的野外调查工作,如1921年海原地震调查,开启了中国人对河西走廊地区科学考察的先河; 派学生谢家荣西行至玉门进行石油地质调查,写出了《甘肃玉门石油报告》。1928~1930年,他和丁文江一道组织了我国早期西南地区最大的野外调查活动。1920年发表《中国矿产区域论》,为中国区域成矿学研究之先导,并为以后的中国矿床学研究奠定了基础。

  • 翁文灏是中国地质学会早期26名创立会员之一,也是5名筹备委员之一,并在1922年的成立大会上当选为首届副会长,会长为章鸿钊,此后当选第3届(1924年)、第5届(1926年)、第9届(1931年)和第18届(1941年)会长。1922年他当选万国地质大会(国际地质大会)副会长,是我国科学家进入国际学术领导机构的第一人。1924年担任中国科学社社长。他于1919年主持创办《地质汇报》、《地质专报》等学术刊物; 编著出版第一部中国矿产资源报告《中国矿产志略》; 1925~1937年担任《中国地质学会志》的编辑主任。

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