新疆北部志留纪晚期—早泥盆世海相红层时空分布与研究展望^*

Spatiotemporal distribution and research prospects on marine red beds in the late Silurian-Early Devonian from northern Xinjiang,NW China

摘要

海相红层因其特殊的颜色、复杂的成因、多样的沉积类型以及蕴藏的古海洋、古气候甚至生物演化信息而备受关注。然而,目前对于海相红层的关注度和研究存在明显的时代、层位和区域差异,以前寒武纪、早古生代、早三叠世、侏罗纪—白垩纪的海相红层最受关注。志留纪晚期—早泥盆世是全球海陆分布、大气成分、生态系统发生转换的关键期,但该时期的海相红层却很少受到关注。新疆北部是中国志留纪晚期—早泥盆世地层发育较连续的地区之一,基于前人研究资料,并结合近年来笔者团队广泛的区域地质调查和新获取的以牙形石为主的化石材料和沉积相标志,初步查明了该地区海相红层的时空分布、岩性组合和生物组合特征,并与国内同期海相红层进行了对比。在此基础上,对志留纪晚期—早泥盆世的海相红层研究提出展望: 在建立高精度生物—年代地层格架的前提下,构建志留纪晚期—早泥盆世海相红层的全球数据库,查明该时期海相红层的时空分布规律与特点,并开展综合对比,探讨其与该时期重要生物—环境事件之间的联系,以更全面、更系统和更深入地认识和理解志留纪晚期—早泥盆世地球多圈层变革及其耦合关系的特质。

Abstract

Marine red beds(MRBs)have attracted considerable attention due to their distinctive coloration,complex formation mechanisms,diverse sedimentary types,and valuable information regarding palaeo-oceanography,palaeoclimate,and even biological evolution. However,there are obvious bias in geological time and regional research and knowledge on MRBs,with particular focus concentrated on Precambrian,Early Paleozoic,Early Triassic,and Jurassic-Cretaceous MRBs. The late Silurian to Early Devonian represents a critical interval of global palaeogeographical reorganization,atmospheric compositional changes,and ecosystem transformation,yet MRBs from this period have received limited attention. Northern Xinjiang is one of the regions with relatively continuous late Silurian to Early Devonian strata in China. Based on previous research data,combined with our extensive regional investigations in recent years,newly acquired fossils dominated by conodonts,and sedimentary facies markers,this paper preliminary identifies the spatiotemporal distribution,lithological and biological assemblage characteristics of MRBs in the study area,and then makes comparisons with other contemporaneous MRBs in China. On this basis,the prospects for the study of MRBs in the late Silurian-Early Devonian are proposed. On the premise of establishing a high-precision biochronostratigraphical framework,a global database of MRBs at the late Silurian-Early Devonian is established to identify the distribution and characteristics of MRBs at this interval,and to carry out comprehensive comparison,then to explore the relationships between MRBs and important bio-environmental events in the period. It will contribute to a more comprehensive,systematic and in-depth understanding of the characteristics of the Earth’s multi-geosphere transformation and their coupling relationships during the late Silurian-Early Devonian.

Graphical abstract

关键词

海相红层 / 沉积环境 / 牙形石 / 志留纪晚期 / 早泥盆世 / 中亚造山带

Key words

marine red beds / sedimentary environment / conodonts / late Silurian / Early Devonian / Central Asian Orogenic Belt

0 前言

海相红层通常是指具有红色色调的海相沉积岩,其在前寒武纪至现代的沉积物中均不乏记录(Hu et al., 2012;戎嘉余等,2012;胡修棉,2013;吕璇和刘志飞,2017;Song et al., 2017;熊梓翔等,2021;Kuang et al., 2022;Card and Montenari,2023;Li et al., 2023),并因特殊的颜色而受到关注。显生宙以来,随着后生动物的大量繁盛,地球各圈层间相互作用的逐渐增强,大气氧含量波动、海平面升降、物源供给区及其成分的变化均会在沉积物中有所体现。海相红层作为一类具有鲜明特征的沉积体,为古海洋、古气候甚至生物演化的研究提供了一个特殊的窗口,被认为是一个符合开展地球系统科学、跨圈层相互作用研究的重要对象(王成善和胡修棉,2005;胡修棉,2013)。根据沉积环境或水体深度的不同,海相红层通常被分为3类(Brett et al., 2012;戎嘉余等,2012): 第1类是出现在远洋—半远洋环境中的大洋红层,如白垩纪大洋红层(Hu et al., 2005,2012;Wang et al., 2009),其形成于深水环境中,通常记录的是大尺度的古海洋、古气候和古环境变化,很少受到季节性或区域性地质事件的影响(Wagreich et al., 2009;Song et al., 2017),一般具有全球性分布,因而最受关注(如Wang et al., 2004,2005,2011;王成善和胡修棉,2005;Wagreich and Krenmayr,2005;胡修棉和王成善,2007;Hu et al., 2009,2012;Khorassani et al., 2015;吕璇和刘志飞,2017;熊梓翔等,2021);第2类为陆棚海或陆表海远岸较深水相红层,在早古生代地层中较为常见(如Ziegler and McKerrow,1975;林宝玉等,2018;Luan et al., 2021);第3类为近岸浅水相红层,以中国扬子地区志留纪海相红层为代表(戎嘉余等,2012;Zhang et al., 2014a,2018; Liu et al., 2016)。后两类红层的形成可能更容易受到区域性古环境或物源输入的影响(Zhang et al., 2014a; Song et al., 2017),不过近年来的研究发现,这些红层可能也会反映一些全球性的地质事件(Luan et al., 2021;Li et al., 2023)。此外,有不少海相红层常与黑色页岩伴生(王成善和胡修棉,2005;戎嘉余等,2012),与黑色页岩在还原条件下有机碳多被保存下来进入沉积圈相反,在海相红层所对应的氧化条件下,有机碳基本被氧化并返回到生物圈和大气圈中(胡修棉,2013),因此这类海相红层不仅可以反映古海洋的变化,还对认识地史时期地球碳库变化、重建碳埋藏过程具有重要的意义。

尽管海相红层几乎在各个地质时期都有分布,但对这些红层时空分布特征的研究程度却存在明显差异,以前寒武纪、早古生代、早三叠世、侏罗纪—白垩纪海相红层的工作积累较多(如Ziegler and McKerrow,1975;Hu et al., 2009,2012;胡修棉,2013;Song et al., 2017;Li et al., 2019;Tang et al., 2020;Kuang et al., 2022;Li et al., 2023及他们的参考文献),晚古生代海相红层目前只有少量的记录(Franke and Paul,1980;Mamet et al., 1997;Boulvain et al., 2001;Van Der Kooij et al., 2007;Bábek et al., 2018,2021;林宝玉等,2019;Card and Montenari,2023)。中国显生宙海相红层在20世纪中后期开展的1︰20万区域地质调查中就已被陆续识别出来,但广泛且深入的研究是从20世纪末—21世纪初才开始的(陈旭和戎嘉余,1996;王成源,1998;王成善等,1999;万晓樵等,2005;王成善和胡修棉,2005)。中国海相红层研究存在明显的层位、区域差异,研究的时代主要集中在寒武纪—奥陶纪、志留纪早期和白垩纪,又以扬子、华北和塔里木三大克拉通和青藏高原及周边地区的海相红层最受关注(王成源,1998,2011;万晓樵等,2005;王成善和胡修棉,2005;陈永权等,2008;戎嘉余等,2012;Zhang et al., 2014a,2018,2019;武振杰等,2015;Liu et al., 2016,2020,2021;林宝玉等,2018;薄婧方等,2019;李明等,2019a,2019b;Li et al., 2019,2023;Luan et al., 2021;李明和林宝玉,2022;刘牧等,2024)。中国志留纪晚期—早泥盆世的海相地层发育较差,多为浅水相沉积,虽然已在华南识别出了较稳定的红层分布(如罗德洛统红层或志留纪第3套红层),但红层的类型单一,以近岸浅水碎屑沉积为主(张小乐,2015;王怿等,2023),而该时期其他块体(尤其是志留系—泥盆系较发育的广大造山带地区)是否存在更多类型的海相红层尚不完全明确。

笔者基于对新疆北部志留纪晚期—早泥盆世区域地层的调查与研究,系统归纳总结了海相红层的时空分布、岩性组合特征及沉积环境,在此基础上与国内同期海相红层进行对比,并对该时期海相红层的深入研究提出展望。

1 区域地质背景与地层概况

本研究所指的新疆北部包括准噶尔盆地周缘及北天山地区,其中阿尔泰地区的古生代地层普遍发生不同程度的变质,古生物化石稀少,地层划分精度较差,不在本研究范围之内。研究区在古生代位于显生宙巨型增生型造山带——中亚造山带的西段南部,由一系列岛弧带和增生杂岩拼合而成,是古亚洲洋演化的产物(Xiao et al., 2010;图 1-A,1-B)。区内古生代地层以泥盆系—石炭系最为发育,早古生代地层分布较为零星,寒武纪沉积地层仅分布在北天山西段的科古琴山和果子沟一带(陈旭等,1998),但在准噶尔盆地周缘多个地区发现了寒武纪的蛇绿混杂岩(Jian et al., 2005;张元元和郭召杰,2010;Xu et al., 2013;Ren et al., 2014;Zhao and He,2014;冯晓强等,2016),反映了该地区在寒武纪可能处于大洋环境中。奥陶纪地层除了北天山西段和沙尔布尔提山一带之外,大多发生了不同程度的变质。本研究关注的志留纪晚期—早泥盆世地层主要由火山碎屑岩组成,夹有少量钙质碎屑岩、正常碎屑岩、碳酸盐岩、火山岩和硅质岩等(蔡土赐,1999)。按照地层区划,可分为西准噶尔、东准噶尔和北天山3个地层分区(王怿等,2021)(图 1-C)。

西准噶尔的志留纪晚期—早泥盆世地层主要分布于2个区域。第1处位于西准噶尔西南部的玛依拉山一带,包括玛依拉山群( S_{2-3}M)和马拉苏组(D₁ml)(蔡土赐,1999),但二者未见直接接触,且马拉苏组中的化石面貌偏向于早泥盆世中晚期,反映该地区可能缺失连续的志留纪—泥盆纪沉积。第2处位于沙尔布尔提山的芒克鲁地区,该地区志留纪晚期—早泥盆世的地层发育较好,地层连续,是研究中国北方志留系—泥盆系界线的重点地区,自下而上包括克克雄库都克组(S₃kk)、乌吐布拉克组(S₄D₁w)、曼格尔组(D₁m)和芒克鲁组(D₁mk),近年来根据牙形石的证据将志留系—泥盆系界线定在乌吐布拉克组上部(Ma et al., 2023;Yin et al., 2025)。

东准噶尔的志留纪晚期—早泥盆世地层较西准噶尔地区更加广泛,主要集中在3个区域。第1处为富蕴南部向东南至阿尔曼太山、库普一带,该地区的下泥盆统分布广泛,被称为托让格库都克组(D₁t)。曾有多位学者提及在富蕴以南的扎河坝、加波萨尔、奥什克山发现了包含Tuvaella rackovskii和T. gigantea的志留纪晚期图瓦贝动物群,并认为其层位与南部卡拉麦里山的白山包组相当(王务严,1979,1990;张川和张梓歆,1981;林宝玉等,1984;赵治信等,2000)。遗憾的是,这些地点均未见相关的剖面描述,对其岩性特征及分布情况亦不明确,之后也未见相关的深入研究工作。第2处为卡拉麦里山南坡,断续分布着包括白山包组(S₃b)、红柳沟组(S₄D₁h)和卡拉麦里组( D_{1-2}k)的志留纪晚期—早泥盆世地层。第3处为考克塞尔盖山至三塘湖一带,由考克塞尔盖组(S₄D₁k)、塔黑尔巴斯套组(D₁t)和卓木巴斯套组(D₁z)组成,其中考克塞尔盖山的考克塞尔盖组中的珊瑚等底栖生物化石表明,其时代为志留纪晚期(王务严,1979,1990;新疆维吾尔自治区区域地层表编写组,1981;蔡土赐,1984;林宝玉等,1984;肖世禄等,1992;王宝瑜,2000),而最近在该组近底部新发现的牙形石显示,其时代为洛赫考夫期最早期(Yin et al., 2024)。该地区很可能缺失志留纪晚期的沉积,泥盆纪最早期的沉积角度不整合覆盖在奥陶纪变质岩地层或志留纪花岗岩之上。不过向东南到三塘湖一带,考克塞尔盖组底部的细碎屑岩中含有普里道利世的笔石化石(Ni et al., 1998;Yin et al., 2025),反映出考克塞尔盖组在区域上存在穿时性。

北天山的志留纪晚期—泥盆纪早期地层出露不佳。在东段巴里坤与哈密地区,仅发育早泥盆世地层(大南湖组),时代为早泥盆世晚期(孟勇等,2013;张孟等,2018),缺少志留纪晚期的沉积记录。在西段的博罗霍洛山,情况恰好相反,出露多处志留纪晚期的地层(库茹尔组和博罗霍洛山组)(王务严,1990),但之上未见早泥盆世的沉积。

2 海相红层的时空分布

基于前人资料,通过广泛的地质调查,目前在研究区内多个地点和层位中识别出了海相红层(图 1-C;图 2)。需要说明的是,尽管研究区处在造山带地区,但这些红层不同于造山带内常见的产自蛇绿混杂岩内部或与之相关的紫红色硅质岩(Zong et al., 2015,2016),或与火山喷发相关的红色调海相火山岩(龚一鸣和纵瑞文,2015)。

2.1 玛依拉山群海相红层

玛依拉山群在玛依拉山一带广泛分布,厚度巨大,可达数千米,从底至顶多个层位均有海相红层发育,岩性主要为紫红色、灰紫色细粒火山碎屑沉积岩、正常碎屑岩和硅质粉砂岩(图 3-A;图 4-D),厚度从一两米至百余米不等。

玛依拉山群上亚群中下部含多门类化石,最早依据其中少量的笔石Saetograptus cf. chimaeva var. salweyi,Pristiograptus cf. colonus var. compactus、珊瑚、腕足类和苔藓虫将其时代定为志留纪中—晚期(新疆维吾尔自治区区域地层表编写组,1981),其中笔石是晚志留世早期(现为罗德洛世早期)Pristiograptus nilssoni(现为Neodiversograptus nilssoni)带的分子(林宝玉等,1984)。此后,在该地区1︰5万区域地质调查中新发现了一些珊瑚化石,时代与以往根据笔石等确定的时代基本一致(仲星等,2011),反映出玛依拉山群上亚群海相红层的时代至少为罗德洛世。

2.2 克克雄库都克组海相红层

见于和布克赛尔县乌图布拉克村以东的芒克鲁地区,主体为一套粒度较细的类复理石沉积,与下伏沙尔布尔组和上覆乌吐布拉克组之间的界线还存在很大争议(林宝玉等,1984;王务严,1990;新疆地质矿产局,1993;王宝瑜,1997;蔡土赐,1999),笔者暂采用原始命名时的界线(新疆地质局区域地质测量大队,1974;新疆维吾尔自治区区域地层表编写组,1981)。海相红层在芒克鲁剖面的克克雄库都克组多个层位有出现(新疆维吾尔自治区区域地层表编写组,1981),为紫红色薄—中层状粉—细粒沉凝灰岩和凝灰质粉砂岩,常与浅灰色、浅灰绿色的同种岩性不均匀互层,韵律层较为发育(图 3-B;图 4-E,4-F)。该套红层规模较大,厚度在几十米至百余米之间,区域上分布较为稳定,在命名剖面(芒克鲁剖面)及其东北约6 km处的芒克鲁Ⅱ号剖面(Zong and Gong,2020)均可见到。克克雄库都克组化石稀少,其中灰岩透镜体内的珊瑚、腕足类和三叶虫时限较长,陈旭等(1998)在该组内发现了罗德洛世的笔石Bohemograptus bohemicus。笔者等近年来在芒克鲁Ⅱ号剖面红层内的灰绿色凝灰质粉砂岩夹层中新发现的笔石,经陈旭教授鉴定为罗德洛世中期的Bohemograptus tenuis(图 5-A),因此克克雄库都克组红层的时代当前可定为罗德洛世。

2.3 曼格尔组海相红层

曼格尔组的分布范围与克克雄库都克组基本一致,但可能受到断层的影响,在命名剖面——芒克鲁剖面上的曼格尔组内未见到红层分布,仅在芒克鲁Ⅱ号剖面可观察到2层海相红层。

第1层出现在该组近底部的8-3层中,为灰紫色、红褐色的灰岩或砂屑灰岩(图 4-C),厚度仅几厘米至十几厘米,呈透镜状产出。8-3层内产牙形石Caudicriodus angustoides bidentatus和Zieglerodina planilingua(图 5-G,5-H)(Ma et al., 2023),前者是洛赫考夫期的分子(Savage,1976;王平,2006;Boncheva et al., 2007;Slavík et al., 2012;王成源,2019),后者常见于志留纪普里道利世至泥盆纪洛赫考夫期早期的地层中(Murphy et al., 2004;Corradini and Corriga,2012;Corriga et al., 2014;Corradini et al., 2020)。此外,该层还含有杯形海百合的板状浮胞化石(图 5-B,5-C)(Zong and Gong,2020),杯形海百合及其浮胞的时限极短,仅出现在志留纪—泥盆纪之交的地层中(Haude,1992)。在中国云南保山,产板状浮胞的地层中含笔石Monograptus cf. uniformis angustidens,M. microden和牙形石Caudicriodus woschmidti,其时代被限定为泥盆纪最早期(洛赫考夫期)(时言和龚大明,1992)。在摩洛哥东南部的Tafifilalt地区,根据牙形石的生物地层学研究,杯形海百合Camarocrinus,Marhoumacrinus及其板状浮胞出现在普里道利统顶部至洛赫考夫阶底部的Caudicriodus hesperius带中(Corriga et al., 2014;Haude et al., 2014)。综合以上的化石证据,可将8-3层中的海相红层限定在泥盆系的第1个牙形石带内。

第2层海相红层出现在曼格尔组中部15层顶部至16层中,主要为灰紫色砂屑灰岩、钙质砂岩(图 3-D),厚度5 m左右,横向延伸范围较第1层更广。该层红层含较丰富的珊瑚、腕足类等底栖生物,上、下层位的灰岩透镜体或薄夹层中产洛赫考夫期的牙形石Caudicriodus angustoides bidentatus(图 5-M)和Zieglerodina sp.,红层之上的第18层产Caudicriodus cf. ruthmawsonae(图 5-L)(尹家一,2024),而Caudicriodus ruthmawsonae仅出现在洛赫考夫期早期的地层中(Drygant and Szaniawski,2012)。因此,该层海相红层的时代仍应为洛赫考夫期早期。

2.4 托让格库都克组海相红层

见于富蕴县恰库尔图镇NNE方向约20 km处的加波萨尔地区。近年来,笔者对该剖面进行了实测,发现3层海相红层,但厚度均不大,在5~7 m之间,其中第1层为灰紫色钙质砂岩,第2层和第3层为紫红色生屑灰岩、泥灰岩或砂屑灰岩与泥质粉砂岩或钙质粉砂岩不均匀互层(图 3-C;图4-A,4-I,4-J)。该地区地形起伏较小,露头不佳,红层在区域上的分布情况不明。该剖面的第2层、第3层红层及之上的灰岩中含较丰富的三叶虫、珊瑚、腕足类、腹足类、海百合茎等化石。张太荣(1983)曾报道了该层位中的三叶虫Crassiproetus globosus,该种见于哈萨克斯坦早泥盆世晚期地层中。本次工作中,笔者在该剖面中新发现了多种三叶虫,包括Cordania属(图 5-D,5-E),该属主要见于早泥盆世地层中(周志强,1989)。

故从三叶虫化石来看,加波萨尔地区的托让格库都克组海相红层的时代应为早泥盆世埃姆斯期。

2.5 红柳沟组海相红层

红柳沟组广泛出露于卡拉麦里山南坡,从底至顶多个层位均有海相红层分布,主要由紫红色、红褐色或红绿相间的细粒碎屑岩、火山碎屑岩和硅质泥岩组成,下部含紫红色、红褐色泥质灰岩或钙质粉砂岩(林宝玉等,1984)(图 3-F,3-G;图 4-B,4-K,4-L)。该套红层厚度较大,可达百余米至数百米,区域上分布较为稳定,仅下部的钙质碎屑岩及泥质灰岩在区域上多呈透镜状产在细粒碎屑岩中,通常东南部较厚,向西北减薄甚至消失。该套红层还见于巴里坤东部的小柳沟一带,主要为红绿相间的细粒碎屑岩、硅质碎屑岩(中国地质大学(武汉)地质调查研究院,2017)。

红柳沟组化石较为稀少,主要产自下部的泥质灰岩或钙质粉砂岩中,根据其中的腕足类、珊瑚、三叶虫、头足类等化石,其曾长期被定为晚志留世(林宝玉等,1984,1998;王宝瑜和李恒海,1989;王务严,1990)。最近,笔者在该组下部灰岩夹层中采集的牙形石样品中,发现了泥盆纪最早期的Caudicriodus sp.和Latericriodus steinachensis(图 5-I,5-J,5-K),但红柳沟组上部的时代目前还缺少化石证据,而上覆的卡拉麦里组中的少量化石和碎屑锆石证据反映其时代为早泥盆世(埃姆斯期)至中泥盆世(蔡雄飞等,2015;白建科等,2018)。综合上述证据来看,红柳沟组海相红层的时代可能主要为早泥盆世早—中期。由于红柳沟组与下伏含图瓦贝动物群的白山包组呈整合接触(林宝玉等,1984),不排除该组底部包含了一部分志留纪晚期的沉积。

2.6 考克塞尔盖组海相红层

见于巴里坤县西北约150 km处考克塞尔盖山克安库都克剖面的考克塞尔盖组下部。该组总体为一套黄绿色、灰绿色的火山碎屑岩夹少量碳酸盐岩,角度不整合在奥陶系荒草坡群或志留纪的花岗岩之上,向上与塔黑尔巴斯套组呈整合接触。海相红层出现在剖面第5层(新疆地质局区域地质测量大队,1977),为玫瑰色、灰紫色结晶灰岩(图 3-E),其中含保存不佳的珊瑚和海百合茎化石,厚度不足5 m,横向上呈透镜状产出。红层上、下层位中均含丰富的珊瑚、腕足类等底栖生物化石,过去根据这些底栖生物长期认为考克塞尔盖组的时代为志留纪晚期(林宝玉等,1984;蔡土赐,1989;王务严,1990;肖世禄等,1992;王宝瑜,2000)。最近,在该剖面第2层的灰岩中(之下为底砾岩)发现了泥盆系第1个牙形石带——Caudicriodus hesperius带的带分子(图 5-F)(Yin et al., 2024),红层之上的第6层中含彗星虫类三叶虫(新疆地质局区域地质测量大队,1977),而在新疆北部该类三叶虫的时代上限被限定在牙形石Caudicriodus hesperius带内(Ma et al., 2023),因此考克塞尔盖组的海相红层时代应为洛赫考夫期,并极可能属于Caudicriodus hesperius带。

2.7 塔黑尔巴斯套组海相红层

塔黑尔巴斯套组多与考克塞尔盖组相伴出现,是一套以紫红色为主的碎屑岩及火山碎屑岩夹碳酸盐岩。考克塞尔盖山多个剖面的多个层位内均发育灰紫色、玫瑰色灰岩、砂屑灰岩,厚度从十几米到几十米不等,含丰富的珊瑚、腕足类和苔藓虫等化石(新疆地质局区域地质测量大队,1977)。塔黑尔巴斯套组目前尚未发现微体化石,所含的底栖生物延限较长,其中部分珊瑚、三叶虫等化石(曾亚参和肖世禄,1991)与西准噶尔地区的曼格尔组上部的化石面貌相近,再加上整合在该组之下的考克塞尔盖组发现了洛赫考夫期早期的牙形石化石(Yin et al., 2024),因此将塔黑尔巴斯套组的时代定为洛赫考夫期中晚期较为合适,顶部可能会延续到布拉格期。

2.8 博罗霍洛山组海相红层

见于北天山西段的博罗霍洛山一带。该组为一套以紫红色、灰紫色为主的碎屑岩地层(图 3-H;图 4-G,4-H),常夹有灰绿色同种岩性,或呈不均匀互层产出,厚度从几十米到400余米不等。该组化石稀少,曾根据其中少量的珊瑚化石将其与西准噶尔的克克雄库都克组进行对比(新疆地质矿产局第一区调大队,1987),时代可能为晚志留世早期(罗德洛世)。

3 海相红层的类型

根据上述地点海相红层的时空分布特征,新疆北部志留纪晚期—早泥盆世的海相红层主要出现在4个层位: 第1个为罗德洛统,包括玛依拉山群上部、克克雄库都克组和博罗霍洛山组的海相红层; 第2个为泥盆系洛赫考夫阶下部,包括曼格尔组中部及底部、红柳沟组下部和考克塞尔盖组下部的海相红层; 第3个为洛赫考夫阶中上部,并可能包含了一部分布拉格阶,包括塔黑尔巴斯套组和红柳沟组中上部的海相红层; 第4个为埃姆斯阶,仅包括富蕴南部加波萨尔的托让格库都克组海相红层(图 2)。研究区尽管发育连续的志留纪晚期—泥盆纪早期地层或普里道利世地层,但目前尚未发现确切的普里道利世海相红层。从岩性上看,这些海相红层包括了火山碎屑岩、(钙质)碎屑岩、硅质碎屑岩和碳酸盐岩。在较为细粒的沉凝灰岩或凝灰质粉砂岩及硅质碎屑岩中通常含有笔石或放射虫化石(图 4-F),灰岩、泥灰岩或砂屑灰岩中含大量的珊瑚、腕足类、三叶虫、海百合茎等底栖动物(图 4-A,4-B,4-C,4-I,4-J)以及少量游泳生活的头足类和牙形动物,粒度较粗的碎屑岩或钙质碎屑岩中化石稀少或不含化石。

海相红层通常根据其形成环境和水深进行分类。戎嘉余等(2012)将海相红层分为3类,分别是近岸浅水红层、陆棚海或陆表海远岸较深水红层和大洋深水红层。林宝玉等(2018,2019)通过对中国古生代海相红层的系统总结,进一步明确了上述3类红层的沉积水体深度,其中水深小于50 m称为浅水红层,50~200 m称为半深水红层,大于200 m称为深水红层。研究区玛依拉山群上部、克克雄库都克组和红柳沟组细粒火山碎屑岩和硅质碎屑岩较为发育,常可见明显的韵律层,红层内部或上、下层位中含有放射虫化石,前二者的灰绿色细粒火山碎屑岩中还含有浮游生活的笔石,故这些层位中的红层似可归为深水红层。李永铁(1995)通过对北天山西段博罗霍洛山组沉积学、岩石学和地球化学的分析,认为其属于浊流沉积的产物,亦可归为深水红层。新疆北部志留纪晚期—早泥盆世深水红层的普遍特征为: 主要由韵律层较发育的薄层细粒碎屑岩组成,常含有放射虫、笔石等浮游生物,而含底栖生物的灰岩或钙质碎屑岩几乎不发育或以透镜体/薄夹层的形式产出。曼格尔组底部、托让格库都克组和考克塞尔盖组下部的红层具有一定的相似性,主要由薄—中层状的灰岩、泥灰岩和(或)砂屑灰岩组成,富含珊瑚、腕足类、三叶虫、海百合茎等化石,部分层位中还含有头足类、牙形石等化石,这类海相红层可能形成于半深水环境。研究区这类红层的普遍特征为: 主要由单层厚度不大(薄—中层)的碳酸盐岩组成,红层内部底栖生物和游泳生物混生。曼格尔组中部和塔黑尔巴斯套组的红层主要由砂屑灰岩、(钙质)砂岩组成,砂屑灰岩中主要含复体珊瑚和腕足类化石,砂岩中化石较稀少甚至不含化石,常发育交错层理,反映其沉积环境较浅,可归入浅水红层。这类红层主要以粒度较粗的(钙质)碎屑岩或砂屑灰岩为主,化石较稀少(以复体珊瑚、厚壳型腕足类为主),浅水沉积相标志较发育,韵律性主要由中—远端风暴沉积所致。

4 讨论

4.1 与中国其他地区志留纪晚期—早泥盆世海相红层的对比

尽管中国志留纪晚期—早泥盆世海相地层发育较差,但新疆北部的这几套海相红层在中国多个地区同期地层中几乎都有发育。在地层划分精度略高的扬子台地或华南及其周缘地区,志留纪晚期地层中普遍发育海相红层。

扬子台地内部以小溪组为代表,含土著型鱼类、板足鲎类、线形植物等化石,缺少典型的海相动物化石(如有铰纲腕足类、三叶虫等),时代为罗德洛世晚期—普里道利世早期(王怿等,2023)。在扬子周缘的滇东地区,关底组上部发育紫红色、黄色、黄绿色粉砂岩和泥岩,见大型虫管状遗迹化石,时代为罗德洛世晚期(王怿等,2021)。四川西部雅安二郎山地区的岩子坪组下部为紫红色泥岩夹黄绿色泥岩、粉砂岩,川西北广元、北川一带的车家坝组为黄绿色夹紫红色含虫管的砂岩或粉砂岩,间夹灰岩,二者均含腕足类Retziella动物群(金淳泰等,1989;Chen et al., 2023),时代为罗德洛世晚期—普里道利世早期(王怿等,2023)。虽然新疆北部的克克雄库都克组、玛依拉山组和博罗霍洛山组形成时代与它们相近,但沉积环境完全不同,扬子地区及其周缘的志留纪晚期海相红层主要形成于近岸浅水环境中。

华南地区泥盆纪最早期的海相红层以广西的莲花山组为代表,为一套紫红色碎屑岩沉积,因其上覆的那高岭组中含中洛赫考夫期的牙形石,故其时代被推测为不晚于中洛赫考夫期(Lu et al., 2023),在时代上与新疆北部的塔黑尔巴斯套组海相红层相近。不同的是,它们虽都属于近岸浅水红层,但莲花山组中的化石类型以鱼类、舌形贝类(邝国敦,1984)和浅水相遗迹化石Skolithos(杨式溥,1983)为主,缺少珊瑚、有铰纲腕足类等典型的海相化石,说明莲花山组的沉积环境较新疆北部同期海相红层的水体更浅。华南埃姆斯期地层分布广泛(侯鸿飞和王士涛,1988;郄文昆等,2021),化石丰富,地层划分精度也较高,在广西崇左的郁江组和隆林含山的坡脚组中都存在红层,前者为紫红色页岩夹薄层灰岩,含腕足类和牙形石化石,后者为紫灰色粉砂质泥岩(鲜思远等,1980)。从岩石组合和化石面貌来看,郁江组的海相红层沉积环境与新疆北部的托让格库都克组较为接近。

云南西部保山地区志留纪晚期—早泥盆世的地层被称为牛屎坪组和向阳寺组,前者产多层紫红色生物碎屑灰岩、泥质灰岩,含板状浮胞化石(即过去所谓的“多房海林檎”,谭雪春等,1982),“多房海林檎”层中产有泥盆纪最早期的笔石和牙形石化石(时言和龚大明,1992)。因此,牛屎坪组中的海相红层至少有一部分可与新疆北部的曼格尔组底部海相红层进行对比,它们的岩性特征和生物组合也较相似,但近年来有学者发现牛屎坪组上部含陆源物质并可能有淡水注入(Zhang et al., 2014b),故二者的沉积环境是否相同还有待进一步研究。

内蒙古达尔罕茂明安联合旗巴特敖包地区的志留纪晚期—早泥盆世地层包括西别河组、查干合布组和阿鲁共组,3套地层中出现多层粉色、紫褐色、紫红色碎屑岩和灰岩,但3个组彼此之间未见直接接触,仅根据其中的化石证据确立了相对的上下层序关系(李文国等,1983),与新疆北部这几套海相红层的精确对比还存在一定困难。过去认为属于志留纪晚期的昆仑地层分区的温泉沟群和祁连地层分区的旱峡群,前者发育多层紫红色灰岩,后者主体是一套紫红色碎屑岩(林宝玉等,1984),近年来较新的地层划分对比研究已将其时代下压至兰多维列世晚期,仅前者可能会延续到罗德洛世(王怿等,2021)。

综合来看,志留纪晚期—早泥盆世的海相红层在中国多个地区均有分布,地层划分精度较高的地区可识别出多期次的海相红层沉积,但在造山带地区,尽管志留纪晚期—早泥盆世地层分布较广泛,然而由于研究程度较低,精确的生物—年代地层格架尚未建立,这些红层的确切时代还不够明确,导致无法开展深入的综合对比工作。

4.2 海相红层研究展望

精确的生物—年代地层格架是开展海相红层后续相关工作(如成因机制、形成背景)的基础。然而,在造山带地区,受地层物质组成(如普遍发育火山岩、火山碎屑岩)和后期构造—岩浆活动改造的影响,生物—年代地层的研究程度和地层分辨率远不及克拉通地区,如克拉通地区的海相红层根据红层内部或上、下层位中的古生物化石,甚至可以将红层的时限精确到具体的化石带(如: 林宝玉等,2018;李明和林宝玉,2022)。新疆北部志留纪晚期—早泥盆世的海相红层除了个别层位发现了具有明确时代意义的笔石和牙形石(陈旭等,1998;尹家一,2024;Yin et al.,2025)之外,大多数层位的时代均由珊瑚、腕足类这些底栖生物限定,地层划分精度较低,部分层位甚至缺少时代依据(蔡土赐,1999),这一现象在中国其他造山带地区同样存在。在广泛的区域或路线地质调查和大比例尺剖面实测基础上,海相红层内部及上、下层位中的多门类化石,尤其是微体化石如牙形石、放射虫、孢子等的处理分析,是将来查明中国志留纪晚期—早泥盆世海相红层时空分布的关键。

当前,除了少量层段(如白垩纪晚期的大洋红层,Hu et al., 2012)外,对海相红层的研究主要集中在时空分布、沉积环境、成因机制分析等方面,它们的古海洋、古气候意义以及与地史时期重要的生物—环境事件之间的内在联系还有待进一步探究(戎嘉余等,2012;胡修棉,2013)。志留纪晚期—早泥盆世是全球海陆分布、大气成分、生态系统发生转换的关键时期,加里东造山运动导致陆地面积增加(Dewey and Strachan,2003),为海相沉积提供了更多样的物源区和更丰富的沉积组分类型。以节肢动物为代表的无脊椎动物开始广泛登陆(Størmer 1977;Shear et al., 1996;Anderson and Trewin,2003;Wilson and Anderson,2004;Dunlop and Garwood,2018),早期维管植物在陆地上逐渐扩张,出现了陆地上的“寒武纪大爆发”(Bateman et al., 1998)。到早泥盆世中晚期维管植物出现了原始的根(Raven and Edwards,2001;Driese and Mora,2001;Gensel et al., 2001)、叶(Boyce and Knoll,2002;Hao et al., 2003)、木质部(Gerrienne et al., 2011)等组织器官,对陆地的改造作用增强,真正的古土壤开始出现,导致了陆地化学风化作用的加强(薛进庄等,2022)。维管植物的扩张还导致了大气O₂含量明显增高、CO₂含量降低,沉积物中有机碳埋藏量增加,出现全球性的δ¹³C正偏事件(Małkowski and Racki,2009;Husson et al., 2016)。同时,这一时期河流系统也发生了转变,出现了单一河道的曲流河和较为稳定的洪泛平原(Gibling and Davies,2012;Xue et al., 2016),趋于稳定的河流系统会给海洋提供更稳定的沉积物源。作为主要受氧化作用和含高价铁氧化物物源供给控制的海相红层,它们的形成和分布与这些事件是否相关或具有何种关系尚不清楚。将来,在精确的生物—年代地层框架的基础上,系统整合全球志留纪晚期—早泥盆世海相红层数据资料,查明各时期海相红层是区域性还是全球性分布,并明确各时期海相红层的致色因素或成因机制,将有望回答上述问题。通过海相红层这一载体,基于其与大气圈、岩石圈、生物圈之间内在联系的研究,也将会更全面、更系统、更深入地认识和理解志留纪晚期—早泥盆世地球多圈层变革和相互作用的特质。

5 结论

新疆北部志留纪晚期—早泥盆世的地层早在20世纪70年代前后开展的1︰20万区域地质调查工作中就已发现,并描述了部分层位中的海相红层。但是,由于红层内古生物化石(尤其是浮游生物化石)发现较少,缺少精确的时代约束,且红层分布零散、露头局限,故这些海相红层过去受关注度较低。笔者基于前人资料,以及近年来笔者在区域上的广泛调查与新获取的化石和沉积相材料,系统归纳总结了研究区内志留纪晚期—早泥盆世海相红层的时空分布,认为研究区内至少存在4个时期的海相红层: (1)志留纪罗德洛世的克克雄库都克组、玛依拉山群上部和博罗霍洛山组红层; (2)早泥盆世早洛赫考夫期的曼格尔组、红柳沟组下部和考克塞尔盖组下部红层; (3)早泥盆世中—晚洛赫考夫期(或包含一部分布拉格期)的塔黑尔巴斯套组和红柳沟组中上部红层; (4)早泥盆世埃姆斯期的托让格库都克组红层。其中罗德洛世红层均为深水红层,早泥盆世的红层除了红柳沟组之外,其余均为浅水或半深水红层。上述4个时期的海相红层在中国其他地区的同期地层中均可识别,但它们的沉积环境并不完全一致。

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基金资助

* 国家自然科学基金项目(42072041)

国家自然科学基金项目(42272014)