赫南特冰期古海洋环境转变及其成因机制研究现状

杨向荣，严德天，张利伟，张宝，徐翰文，刘文慧，郧嘉琳

中国地质大学(武汉)构造与油气资源教育部重点实验室，武汉　430070

0　引言

奥陶纪—志留纪转折期是一个重要的地质历史时期(图1)，研究发现这个时期全球板块构造形态、古气候条件、古海洋氧化还原条件、生物群类型等都发生了巨大的改变[1-5]，同时期在我国南方沉积了一套黑色页岩，并且该套页岩被作为我国页岩气勘探开采的重要层位[6-8]。因此人们逐渐认识到厘清赫南特冰期不仅对了解地球地质历史时期环境的演化及其与生物进化间的协同关系具有重要理论意义，更对华南页岩气开采具有重要指导意义。尽管学者对赫南特冰期的古海洋环境转变与冰期成因机制做了大量工作，但由于涉及内容的广泛性及学科交叉研究的复杂性，对两者之间的相互关系与及触发机制等许多问题仍未得到较好的解决。为此本文力图从地球科学的角度出发，综合国内外的研究成果，阐述奥陶纪—志留纪转折期古海洋元素地球化学循环与古气候转变，并对两者的协同演化关系做出简要的综述评论。

1　赫南特冰期

过去五亿年以来极地地区有三个时期形成了广泛分布的大陆冰川，其中一次就发生在晚奥陶世赫南特时期(约444百万年前)。反映该时期气温显著下降及冰盖形成的证据很多，比如δ13C发生了正漂、海平面的下降、凯迪期冰川沉积物与沉积旋回的出现、含有燧石和磷酸盐的碳酸盐岩以及全球海水中的δ18O值比无冰雪覆盖时期要高[1,9-14]。此外，全球的海洋水体循环程度与极地—赤道的温度梯度密切相关，其也可以揭示当时的气候变冷事件，因为温室气候条件不利于温度梯度的形成，进而导致海洋循环的减弱，相反温度下降会促进温度梯度的形成，导致强烈的海洋循环。因此Pohl采用FOAM重建了奥陶纪时期海洋表层水体以及海洋—大气的循环模式，发现赫南特冰期引发了11 ℃的气温变化，并导致了强烈的海洋水体循环[15]。通过古CO2含量计算模型[16]以及生物—非生物指标数据[17-19]显示该时期CO2的含量高达14～22倍现今的水平，而冰期就发生在这样的高CO2含量时期[20-21]。

2　赫南特冰期的影响

2.1　海洋碳循环

晚寒武世时期全球C循环被认为经历了强烈波动[22-23]，而这种波动是由不稳定的古海洋氧化还原条件以及间歇性的硫化水体扩张活动引发的[22-25]。到了早—中奥陶世δ13Ccarb值变得相对稳定[26-27]，反映了该时期较稳定的全球C循环[28]。到了晚奥陶世时期全球C同位素出现了两次波动即GICE和HICE事件，上奥陶统古登贝尔阶碳同位素正漂幅度较小(约+2‰～+4‰)，而在上奥陶统赫南特阶出现的δ13Ccarb正漂则更加强烈(约+3‰～+7‰)且持续时间更长(约1Myr)[23,29-30](图2)。晚奥陶世赫南特时期全球有机碳同位素δ13Corg(约-1‰)数据显示了较一致的趋势，即晚奥陶世凯迪期δ13Corg值保持较稳定的低值，随后在赫南特早期逐渐发生正漂，并在早志留世的鲁丹期δ13Corg值重新恢复到凯迪期水平，但是δ13Corg漂移事件存在一定的空间差异性，即其开始漂移的位置可以在凯迪阶—赫南特阶界限之下(在Dicellograptusmirus生物带)[31]，也可以在界限处[32]或者在界限之上(中M.extraordinarius-N.ojsuensis生物带)[33]。HICE事件的发生被很多研究认为是由于大量有机碳的埋藏[27,34]，另一种假设则认为HICE事件与暴露地表的碳酸盐岩风化作用有重要内在联系[1, 35]，但结合钙同位素等信息指示风化作用并不足以引发全球尺度的碳同位素波动[30,36]。两种模式的不同之处在于对赫南特阶冰期空气中CO2分压变化时间节点的确定。在生产力假设中大气CO2分压的下降及冰期的到来是由于海洋生产力的增强，导致富含12C同位素有机碳的大量埋藏并离开了海洋—大气系统，那么海相碳酸盐岩中C同位素开始升高处反映了海平面的变化、海洋表面温度的降低、冰川的扩张[2,37-38]。相反，碳酸盐岩风化假设认为空气中CO2分压的下降发生在海相碳酸盐岩中C同位素升高之前，这可能是由于强烈的硅酸盐风化或者构造作用引发的火成岩风化对CO2消耗量的增强[39]。最近对美国犹他州和内华达州的五个剖面进行的高精度δ13Ccarb研究发现，HICE时期δ13Ccarb最大值展现了明显的平面梯度，即从盆地中心(+7.5‰)向内陆架地区逐渐减少(+2.5‰)。这种梯度性可能是由于该时期海平面较低，海盆周围隆起地区被剥蚀得更严重，引发了区域性的不整合特征[35]。当然由于不同地质年代以及不同地质相带生活的生物存在一定差异性，因此缺乏较独立的生物地层单元同时能够控制浅水碳酸盐岩及深水泥页岩区，导致有机碳同位素δ13Corg与无机碳同位素δ13Ccarb间存在不一致性，引发学者思考对HICE的使用与解释的正确合理性[40]。

图2　奥陶纪—志留纪转折期全球碳同位素记录Fig.2　The variation of carbon isotope during O-S transition

2.2　海洋水体硫循环

地球系统中S元素的地球化学循环可以解释海相沉积物中硫同位素δ34S波动[41-46]，沉积物在硫化或铁化还原水体中通常会发生微生物硫酸盐还原作用(MSR)[47-49]，其可以引发海水硫酸盐中70%的34S发生分馏[50-52]，MSR作用也被广泛用于解释奥陶纪—志留纪转折期S同位素波动特征。同δ13Corg变化趋势一样，δ34Spyrite在凯迪期阶保持稳定，而在赫南特期发生显著的正漂事件，随后在早志留世鲁丹期重新恢复到冰期之前的水平[3,31,33-34](图3)。S同位素与C同位素的耦合作用对解释该时期古海洋—古气候变化具有重要意义，Youngetal.[53]从阿巴拉契亚盆地记录的中—晚奥陶世C-S同位素信息中发现了两次重要波动，即δ34SCAS出现显著(12‰)负偏的同时δ34Spyrite(+10‰)和δ13Ccarb(+2‰)发生了正漂，这种演化关系反映了赫南特时期全球黄铁矿埋藏速率以及海水硫酸盐与沉积黄铁矿间的S同位素分异程度降低。引发这些变化的原因很多，一是海洋系统逐渐富氧化，削弱了微生物硫酸盐还原作用(MSR)，进而降低了黄铁矿的沉淀量[31,34,54]。此外富黄铁矿沉积物风化作用的增强也是一个可能的因素，但目前还缺少相关的沉积学与地球化学证据能够支持这一假设。

2.3　海洋水体Os、Sr循环

海水的Os同位素组成反映了两种来源Os的相对强弱，一是地壳碎屑物质中高放射性Os(187Os/188Os风尘=1.05，187Os/188Os大陆地壳或河流=1.05)，另一个是来源于大洋地幔圈或地核的低放射性Os(187Os/188Os地幔或地核=0.13)[55-58]。Os元素在海洋中一般存在约10～40个千年，相较海洋混合的时间更长，因此使用Re-Os体系以及初始Os同位素(Osi)组成可以分析古海洋Os循环[58-62]，进而反映海洋沉积物来源变化[63-64]。有学者对苏格兰Dob′s Linn剖面(GSSP)做了Os同位素测定，并用来分析赫南特期古气候变化[65](图3)，发现Complanatushe和anceps生物带早期Osi值从0.28增高到1.08，这种具放射性来源的Osi(1.08)较整个显生宙甚至是现今海洋来说都是偏高的(～1.06)[63,66-68]。初始Os同位素(Osi)的变化趋势反映了晚奥陶世凯迪期风化作用具有增强的趋势，这很可能会促使大气CO2分压降低，进而引发冰期的形成。而后在赫南特阶底部的Extraordinarius带开始降低为低放射性来源，这被解释为赫南特阶大陆冰盖的形成降低了化学风化作用的强度[65-66]。

古海洋中Sr同位素组成受陆源风化物质与地幔热液流体的影响[69-70]，至今很多关于古生代87Sr/86Sr比值研究被用来分析古海洋环境、古构造演化以及古陆风化作用[70-74]。其中上奥陶统沉积物中的87Sr/86Sr同位素曲线显示出非常大的波动范围[75](图4)，早—中奥陶世海水87Sr/86Sr值开始下降(0.709 0～0.708 8)，在晚奥陶世早期骤降为0.707 8，这也被认为是显生宙以来最大的一次波动[39]，随后在晚奥陶世—早志留世时期开始逐渐上升[69,75-76]。如同对新生代87Sr/86Sr值波动的解释一样[77-78]，大多数人认为奥陶纪晚期87Sr/86Sr值的剧烈上升是由于海平面降低、构造造山运动加强，进而引发的大陆风化作用增强[75,78-80]。

图3　奥陶纪—志留纪转折期地球化学元素记录Fig.3　The variation of geochemical proxies during O-S transition

图4　奥陶纪—志留纪转折期全球Sr同位素记录[75-76]Fig.4　The variation of strontium isotope during O-S transition[75-76]

2.4　海洋水体氧化还原环境

Mo元素的含量可以被用来判定全球古海洋氧化还原条件[81-85]，而如今使用Mo同位素进一步探讨古海洋水体氧化还原条件的演化[86-89]。赫南特冰期Mo同位素出现了明显的波动(图3)，从中国南方的王家湾剖面来看，冰期前后具有较高的δ98Mo值，反映了缺氧的海洋环境，而在赫南特时期的一次突降指示了一次水体氧化事件[87,89,90-92]。U同位素同样可以被用来评估古海洋水体的氧化还原特性[93-97]，晚奥陶世晚期与早志留世早期海水中的δ238U被认为大约在-0.60‰到-0.85‰之间，而该时期河流中的δ238U则与现今一致约为-0.3‰[98-100]。通过计算可以发现，缺氧水体中的U通量与其他来源的U通量分别占据该时期U含量的46%～63%和37%～54%，并且缺氧水体中的U通量是现今海洋中的4～9倍，反映冰期前后古海水的严重缺氧[92]。Fe组分分析是重建海洋水体环境的一种重要手段[101-103]，通常认为在晚奥陶世晚期和早志留早期全球海水的FeHR/FeT>0.38且Fepy/FeHR<0.8，指示了缺氧铁化的水体环境，而赫南特期的FeHR/FeT<0.38反映了氧化的海洋环境[104](图3)，不过同开阔海的强水体循环不同，在局限海下水体更易形成缺氧的硫化水体[105]。但与先前普遍认为的冰期海水逐渐富氧化不同，有研究发现Fe组分特征在整个晚奥陶世包括赫南特时期都指示了一种严重缺氧的环境[106]。

2.5　海洋生物灭绝

赫南特阶被认定为奥陶纪最末期不到2 Myr的一段地层[107-108]，研究认为N.extraordinarius-N.ojsuensis带为该阶的下部笔石带[109-110]，其底界与N.extraordinarius和N.ojsuensis的首现一致。而其后的研究表明这两种笔石的首现并不完全相同，在王家湾北剖面(GSSP)N.ojsuensis的首现位于N.extraordinarius首现层位之下4 cm处，这种先后顺序均可和美国内华达[111]、西伯利亚科累马[112-113]以及哈萨克斯坦南部[114-115]等剖面对比，故而该笔石带改名为N.extraordinarius带，并作为赫南特阶的底界。赫南特阶的顶界与志留系底界重合，因此赫南特阶就包括下部的N.extraordinarius带和上部的N.persculptus带。

该时期生物灭绝事件消除了海洋无脊椎生物中49%～61%的属以及约86%的种[116-118]，使其成为显生宙以来仅次于P-T的第二大生物灭绝事件，在这次灭绝事件中受到强烈波及的生物包括三叶虫、腕足类、笔石、牙形虫、无脊椎珊瑚、几丁虫。并且本次事件可划分为两个阶段，第一幕灭绝发生在赫南特冰期的起始阶段，对应于445 Ma前的N.extraordinarius-N.ojsuensis生物带，并在全球具有有广泛分布[119-122]，第一幕导致了N.extraordinarius带底部的全球范围内的笔石消亡，仅在扬子区是个例外，因此Mitchelletal.[123]认为当时扬子区是笔石的避难所。尽管扬子地区剖面表明此带的灭绝率也很高，但是不少笔石动物群的分子仍然穿越了大灭绝的主幕而延入赫南特阶[124]，并且这一灭绝事件发生的时间是穿时的，在浅水区发生得早而深水区则晚[117,124-126]。第二幕则发生在约444 Ma前N.persculptus生物带[4,119-121]。赫南特时期海洋水体以赫南特贝动物群的凉水腕足类为代表，它以命名属赫南特贝Hirnantia为代表、伴以一些其他独特分子和广布型分子[119]，赫南特贝动物群在扬子区从近岸至远岸的一系列产地，首现层位逐渐升高，动物群延续时限越来越短，而多样性却越来越高。纵向考察表明，近岸产地的赫南特贝动物群多样性由高向低演变，而远岸较深水产地的多样性演变则由低变高。随地点和层位而发生的环境因子变化(如水深、底质等)，赫南特贝动物群对应于不同的群落、亚群落或群集[127]。赫南特阶时期，海底缺氧范围逐渐收缩，进而削弱了反硝化作用，因此提供了足够的生物氮给喜寒的真核生物，烃类生物标志化合物中的原核生物比例在该时期逐渐降低[128]以及微型浮游生物(疑源类)的增长[129]证明了这个观点，然而这样的环境转变非常不利于喜好高营养成分、低氧含量的笔石生存，导致了它的大面积绝灭[129-131]。即使有学者提出了海底硫化缺氧的环境可能是导致生物灭绝的原因[131]，但是人们更愿意相信气候的转变是触发这两幕绝灭事件的诱因。值得注意的是气温的变冷是冰期的直接效果，而海底硫化缺氧环境位置的下移则与冰期海平面的下降有关，因此无论哪种机制都与赫南特冰期的出现息息相关。

3　赫南特冰期的成因机制

3.1　风化作用

地质历史时期大气CO2浓度的缓慢下降可以解释为构造造山运动形成隆起，进而大大增强了硅酸盐岩、玄武岩的风化作用[1]，依据海水中87Sr/86Sr的比值[39,75]以及CIA指数[132]，表明其风化速率在早—中奥陶世时期是较强的，但在晚奥陶世开始出现显著的降低。值得注意的是，在冰期开始之前的凯迪期Osi值明显增高[65]，这一趋势表明该时期风化作用的增强，并且可以被解释为构造运动的加强引发的大陆硅酸盐风化作用增强。研究发现由于硅酸盐岩风化强度的阶段变化，导致大气中的CO2分压在距今400～360 Ma以前的泥盆纪出现了明显的下降，最后导致全球气温下降以及极地的冰期形成[16]，因此一些学者就认为晚奥陶世时期岩石的风化作用逐渐增强是触发赫南特冰期形成的重要机制[65,133]。温暖潮湿的温室气候条件可以促使硅酸盐岩化学作用的加剧，另外当大陆板块运动经过赤道地带时，充足的降水量也可以增强风化作用[27]。而近年来发现植物可能是风化作用增强的重要诱因，植物再生长过程中需要吸收矿物质—包括磷酸盐、钾元素、钙元素、镁元素和铁元素，而陆生植物的出现可以加强岩石中重要的营养物质释放，尤其是陆生维管植物的出现大大增强了对含有营养物质的硅酸盐矿物的风化作用[134]，比如对钙元素的风化因子就达到2～10。Timothyetal.[135]分别观察了苔藓植物(即无维管植物)与非生物因素控制下的花岗岩和安山岩的风化强度，证实了无维管植物的确可以增强硅酸盐岩的风化作用(图5)，并且利用COPSE模型[17]对480 Ma以来的CO2水平以及全球气温变化进行了模拟，发现在陆生维管植物与无维管植物的影响下，在约458 Ma和444 Ma以前出现了两个极低值，分别对应了GICE以及HICE事件。

图5 奥陶纪—志留纪转折期风化作用强度(据Yan et al.[132]; Timothy et al.[135]改)其中红实线、绿实线、橙虚线分别代表依据早期植物的磷酸盐风化作用预测的全球温度、大气CO2分压、碳同位素变化趋势Fig.5　The intensity of weathering during O-S transition(based on Yan et al.[132]; Timothy et al.[135])Model results, predicted Ordovician variations in red solid line, global temperature, green solid line, atmospheric CO2, and orange dotted line, δ13C of marine carbonates, for: baseline model with Ordovician adding transient enhancement of phosphorus weathering by early plants

3.2　火山作用

研究表明通过火山活动或者变质作用导致的大量的C输送到海洋—空气系统中是导致温室气候的一个重要触发机制，而风化作用的加强在很多时代也被认定为剧烈的火山活动所引发，即火山喷发出的大量CO2气体以及易风化的玄武岩都能促进大陆风化作用[136-138]。相较于火山系统，沿着大陆边缘的岩浆弧俯冲带由于将地壳中储存的碳酸盐矿物分解，因而被认为释放了更多的CO2气体到空气中，尽管对于当时这种方式释放的CO2量计算还存在困难，但现今的大陆火山弧释放的CO2量大约为150 tg C/年，而大洋中脊大约释放12～60 tg C/年，大洋板内火山释放1～30 tg C/年[139-141]，因此大陆火山弧可能在控制地球地质历史时期的气候转变过程中扮演了重要角色。罗迪尼亚超大陆在约900万年以前开始形成，在约750万年以前经历了延展隆升期，最终在约600万年前开始崩解[142-144]。罗迪尼亚超大陆的存在就反映了大陆弧火山的减少，而随后的崩解就带来了大陆弧火山的增加，大气中CO2含量在寒武纪达到顶峰，而后冈瓦纳大陆在中奥陶世开始形成，大陆弧火山的量再次降低，导致大气CO2含量出现降低[145]，并且McKenzieetal.[142]发现年轻碎屑锆石含量的波动与冰期旋回具有一致性。与之前的CO2触发机制不同，Buggischetal.[146]认为火山活动释放的SO2对晚奥陶世赫南特冰期的形成具有重要作用，由于SO2在对流层极易被氧化固定，而在平流层形成的气溶胶则会阻挡太阳热能，引发地球表面的温度急剧下降，这样来看晚奥陶世凯迪期火山活动的减弱或许是触发冰室气候的关键条件。

3.3　有机碳埋藏

赫南特冰期与有机碳埋藏速率的加强存在一定的联系，即冰期前海洋生物死亡促进了大量有机碳埋藏[31,147-148]，进而导致大气CO2分压下降[20,149]。Rosenauetal.[150]在古登贝尔阶GICE时期发现了较高的δ18O值，认为该时期δ18O值增加了1.5‰，随后降低为19.0‰，并在其附近波动，这些结果表明在GICE时期内存在短期的冷却事件，因此凯迪阶前(赫南特阶前)出现的古登贝尔C同位素正漂(GICE)就可能是赫南特冰期的一个前奏[11,27,148]，这个时期海平面明显上升，碳酸盐沉积从热带过渡到温带[148,151]，磷酸盐和硅质沉积增多[11,151]。桑迪阶与凯迪阶界限附近的GICE事件可能代表了全球范围内的有机碳埋藏的加强[12,27,39]，而晚凯迪期δ13Corg值的大幅度变化又反映了低于晚奥陶世冰盖形成的临界pCO2阈值[21,148-149]。同样的，GICE期后有机碳持续埋藏，CO2分压继续降低，最终引发了时间更长、强度更大的赫南特阶碳同位素波动HICE与冰期。在这样的模式中，中奥陶世到晚奥陶世存在一个气候逐渐降低的平台，代表了CO2分压在地质时间尺度上的累积降低，直到其突破所需的临界值后，触发了赫南特期出现短暂的气温陡降[133]，这就排除了该时期火山活动引发的气候突变[152]。

3.4　其他地质事件

Herrmannetal.[153]认为晚奥陶世古地理和CO2浓度的协同作用，加上海平面的下降、极地海洋热传送的减少导致冰盖的形成，进而触发了全球气温降低。冰川海洋以及大陆沉积物在时空上的分布指示了冰期始于中奥陶世，同时沉积学和动物形态特征也表明了晚奥陶世温暖水体向寒冷水体的转变[154-157]，但是这种转变模式存在一定问题，因为根据古地理重建和古气候指标，当时的北美处于热带到亚热带的纬度范围。而晚奥陶世冈瓦纳大陆的向南移动和海平面的下降可能导致了南大洋的热传导减少，最终引发了冈瓦纳冰期的形成或者加强[153]。同时，诸如早期较弱的太阳光照强度[158]、由宇宙射线引发的云层反射率高低[159]也被用来解释气温骤降。值得注意的是全球的氮循环转变可能是触发冰期的重要机制之一，这是因为固氮作用速率以及相伴生的氧化氮的产量对气候环境显得尤为重要[160]，氧化氮(N2O)是一种强有力的温室气体，其引发温室气候的效力是同等量CO2的300倍，并且在大气中的持续时间也超过了100年[161-162]。因此当N2O这一产物大量减少时，就有助于全球气温变冷甚至是冰期的到来。即使赫南特冰期的结束被归结于大气CO2含量的上升[1]，但是也有可能海相氮循环在这一事件中扮演了重要的角色[161]，因为在全世界多个剖面的赫南特冰期结束位置都出现了δ15N的漂移[30,129]，这一信号反映了该时期反硝化作用的增强，进而导致更多的N2O被释放到大气中增强了温室效应，导致冰期的结束。

4　不同地质作用耦合关系

地球作为一个整体系统，地质历史时期发生的各种地质过程会相互作用、相互影响、相互制约。晚奥陶世火山活动较为频繁，火山喷发出大量的CO2气体，这一过程能引发强烈的大陆铝硅酸盐化学风化作用[65,128]。那么火山活动之后风化作用的增强就可以解释晚奥陶世时期大量陆壳放射性187Os、87Sr同位素向海水的运移，进而引发该时期187Os/188Os与87Sr/86Sr的升高[65,75-76]。但长时期强烈的风化作用便会大量消耗CO2，使得大气CO2分压持续降低，加上火山活动喷发的SO2在平流层形成的气溶胶会阻挡太阳热能[148]，可以引发全球气温降低。气温的降低能加剧海洋系统的循环，海洋表层与底层水体的循环会促进营养物质的循环，进而诱发高的生物生产力与有机碳埋藏，这一过程不仅能进一步降低大气CO2分压水平，促进气温的降低，并且有机碳的下沉过程还会大量消耗海水中的氧气，在陆棚处形成缺氧的底层水体[31,104]。赫南特时期生物的绝灭事件众多学者有不同的解释，比如有人认为该时期海洋硫化水体的偏移使得大量海洋生物不适应新的生活环境发生了灭绝[5]，而更多的学者则将其归咎于赫南特时期气温的骤降引发了显生宙以来第一次生物灭绝事件。

5　存在问题

对于这一地质转折期古气候条件的研究还存在很多争论：

利用碳同位素[19,163]及显生宙碳循环模型[163-166]等古气候条件恢复都显示晚奥陶世时期整体处于一个高CO2分压条件(>8 PAL)，但有趣的是依据前人设计的复杂环境模型表明只有当CO2分压下降到8 PAL时才会引发冰期的形成[20-21]，这种矛盾性的存在可能受限于计算得到的CO2分压曲线的精度，具体原因还有待考证。

Os，Sr同位素数据显示晚奥陶世时期放射性187Os、87Sr含量逐渐升高，这被很多人解释为风化作用的升高[65,75-76]，但陆源风化指数CIA值[132]与Osi指数在凯迪期表现出明显不同的变化趋势，加之上奥陶统五峰组发育多层钾质斑脱岩，反映了大规模的火山喷发活动[167]，那么晚奥陶世凯迪晚期海洋水体中放射性187Os含量增高[65]或许指示了火山作用的减弱，而非风化作用的增强，总之目前对该时期大陆风化作用与火山作用的耦合关系，尤其是火山活动对海洋环境的影响还较为缺乏，其机制值得深思。

研究发现早凯迪期的气温骤降(GICE)后有气温的回暖[146]，这就为有机碳埋藏的时间尺度与冰期开始的时间节点提出了新的异议。另外诸如对冰期持续的时间长短存在差异性；志留纪之初的气候是迅速变暖还是持续寒冷也有不同的解释和结论；生物演化、海洋环境与气候转变如何相互影响与制约有待研究。而如此多的争论存在的原因很多，比如缺乏独立的生物地层单元同时能够控制浅水碳酸盐岩及深水泥页岩区，缺少转折界限处高精度的地球化学信息与全球等时地层格架下的对比，以及风化作用、成岩作用和构造热事件对古海洋与古气候重建时的干扰，这也就需要我们今后更多的工作来克服这些局限性。

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