侏罗纪高分辨率大气二氧化碳浓度变化:来自C₃植物有机碳同位素的证据^*

High-resolution Jurassic atmospheric CO₂ concentration variations: evidence from C₃ plant organic carbon isotopes

摘要

大气二氧化碳(pCO₂)浓度升高被广泛认为是全球变暖的主要驱动因素。重建地质时期的pCO₂浓度对预测未来全球气候变化具有重要意义。侏罗纪是地质历史上典型的温室气候期,前人通过模拟计算和地质记录等多种方法估算了该时期的pCO₂浓度。然而,目前根据不同指标重建的侏罗纪pCO₂分辨率较低且存在较大差异。本研究系统收集了侏罗纪1808个C₃植物有机碳同位素数据,采用pCO₂重建新指标(C₃陆生植物有机碳同位素)恢复了侏罗纪高分辨率pCO₂连续变化趋势。研究表明,侏罗纪pCO₂浓度范围在407×10^-6~7540×10^-6之间,与前人研究结果基本一致。此外,该时期pCO₂整体呈现逐渐下降的趋势,并在早侏罗世和晚侏罗世中存在3次大气CO₂浓度高值区间。与同期地质事件相比,显示出良好的对应关系,表明研究结果具有较高的准确性。尽管研究结果表明早侏罗世托阿尔期的大气pCO₂浓度显著高于其他替代指标,可能由于所收集的C₃陆生植物有机碳同位素数据受区域因素影响,但该研究依然能够准确地反映侏罗纪pCO₂浓度的变化趋势,并具有一定的科学意义。

Abstract

The increase in atmospheric carbon dioxide(pCO₂)concentration is widely recognized as the primary driver of global warming. Reconstructing pCO₂ levels during geological periods is crucial for improving predictions of future climate change. The Jurassic period represents a typical greenhouse climate interval in Earth’s history. Previous studies have estimated Jurassic pCO₂ concentrations using various approaches,including climate simulations and geological proxies. However,existing reconstructions are characterized by low temporal resolution and significant discrepancies among different proxy records. In this study,we systematically compiled 1808 C₃ plant organic carbon isotope data points from the Jurassic period and applied a novel pCO₂ proxy—based on C₃ terrestrial plant organic carbon isotopes—to reconstruct a high-resolution,continuous record of atmospheric pCO₂ variation throughout the period. Our results indicate that pCO₂ levels ranged from 407×10^-6 to 7540×10^-6,which is broadly consistent with prior estimates. Furthermore,pCO₂ exhibited an overall decreasing trend punctuated by three distinct intervals of elevated concentrations,occurring in the Early and Late Jurassic. These fluctuations correlate strongly with coeval geological events,supporting the reliability of the reconstruction. Although the reconstructed pCO₂ values during the Early Jurassic Toarcian stage are higher than those derived from other proxies—likely due to regional influences on the isotopic composition of terrestrial C₃ plants—the dataset still accurately captures the long-term variation trend of pCO₂,underscoring its scientific value.

Graphical abstract

关键词

古气候 / 侏罗纪 / C₃陆生植物有机碳同位素 / 全球变暖 / pCO₂

Key words

palaeoclimate / Jurassic / organic carbon isotopes of C₃ terrestrial plant / global warming / pCO₂

人类活动排放的大量温室气体(如CO₂)已显著改变全球气候,导致地球系统处于前所未有的温暖状态(Tierney et al., 2020)。在当前全球变暖背景下,基于地质载体记录、同位素地球化学及模拟计算的气候重建具有重要意义。侏罗纪是地质历史上典型的稳定温室气候期,表现为高CO₂浓度、高全球表面温度和高全球海平面,因此,重建侏罗纪的大气CO₂浓度对于预测未来气候变化趋势至关重要。目前,重建大气CO₂浓度的方法包括地球化学模拟和替代性指标,其中成壤碳酸盐碳同位素方法应用最广泛(王尹等,2012)。然而,地球化学模拟方法分辨率相对较低,而获取连续的替代性指标相对困难,且重建结果存在差异。因此,迫切需要更加精确的方法来重建高分辨率的pCO₂,以更好地反映侏罗纪的气候特征。

近年来,科学家通过研究C₃陆生植物中碳同位素分馏(ΔC),提出了一种新的pCO₂重建指标(C₃陆生植物有机碳同位素)(Cui and Schubert,2016)。Dong 等(2021)利用C₃陆生植物有机碳同位素重建了423-252 Ma期间的高分辨率pCO₂浓度,结果与成壤碳酸盐碳同位素及植物叶片气孔参数的重建结果一致。Nordt等(2022)基于此方法,重建了早侏罗世和早白垩世(Nordt et al., 2024)的高分辨率pCO₂曲线,表明在早侏罗世温室气候条件下仍存在局部薄冰盖,其中阿普特期结果显示pCO₂浓度持续低于840×10^-6,进一步验证了南极洲冰盖的存在。基于C₃陆生植物有机碳同位素重建pCO₂浓度的方法,本研究系统收集了公开发表的侏罗纪C₃陆生植物的稳定碳同位素( {\delta }^{13} C_{plant})、箭石碳同位素( {\delta }^{13} C_{carb})和箭石氧同位素(δ¹⁸O)(Nordt et al., 2022;Richey et al., 2023),并计算出1条侏罗纪高分辨率的单一指标大气二氧化碳浓度变化曲线。研究回顾了相关文献,讨论了现有方法的可行性,并探讨了未来可能的改进方向。通过对不同方法的比较与评估,为侏罗纪pCO₂的准确重建提供了更多参考。

1 材料和方法

1.1 数据来源

Schubert 和 Jahren (2012)的实验发现,pCO₂与净碳同位素分馏(ΔC)之间存在显著相关性(公式1)。通过分析植物化石有机碳同位素组成,间接推断出当时的大气CO₂浓度。本研究系统收集了1808个侏罗纪C₃陆生植物有机碳同位素( {\delta }^{13} C_{plant})、1152个箭石化石碳同位素( {\delta }^{13} C_{carb})以及1231个箭石氧同位素( {\delta }^{18} O_{carb})数据。该研究收集的侏罗纪δ¹³C数据中,不同碳源的数量存在差异,但它们在相同时间段内表现出显著的协变关系。其中,C₃陆生植物δ¹³C数据主要来自7种类型,包括生物标志物、全岩、配子体、木质体、叶片、古土壤和孢子囊(Richey et al., 2023)。碳同位素浓度的范围为-31.9‰~-18.5‰,平均值为-24.6‰。同位素数据的丰度随时间变化,早侏罗世普林斯巴期(约182—185 Ma)的数据最为丰富,从早侏罗世到晚侏罗世呈现先增加后降低的趋势。在数据收集过程中,发现晚侏罗世的数据相对缺乏(图 1)。

1.2 pCO₂的计算

C₃陆生植物中的原始 δ¹³C值会受到成岩作用或化学作用等多种因素的干扰(Lukens et al., 2019),从而影响pCO₂的计算。然而,如果能够确保收集到足够多的有机碳同位素数据,就可以在一定程度上减少误差(Cui and Schubert,2016)。本研究所采用的方法基于Cui 等(2020),其中, {\delta }^{13} C_{plant}代表C₃陆生植物的 δ¹³C值(图 2-A), {\delta }^{13} C_{carb}为箭石化石的 δ¹³C值(图 2-B),而 {\delta }^{13} C_{C{O}_2}则根据净碳同位素分馏法获得(图 2-C)。

箭石化石的氧同位素(δ¹⁸O)是古温度重建中常用的替代性指标,研究利用箭石化石的 δ¹⁸O 来计算古温度,其中, {\delta }^{18} O_{sw}表示海水的氧同位素组成,假定为-1.2‰(Dera et al., 2011;Dong et al., 2021)(公式(1)至公式(5))。为了处理数据,使用Acycle对数据库中的数据点进行平滑处理(平滑窗口设5.4 Ma),并通过重新采样对时间尺度进行对齐。重建的pCO₂值及拟合结果详见附件。

(1)ΔC=δ¹³ {\mathrm{C}}_{\mathrm{C}{\mathrm{O}}_2}- \frac{{\delta }^{13}{C}_p}{1+\frac{{\delta }^{13}{C}_p}{1000}}

(2)Δ(Δ¹³C)= \frac{({\delta }^{13}{C}_{\mathrm{C}{\mathrm{O}}_2\left(t\right)}-{\delta }^{13}{C}_{plant\left(t\right)})}{\left(1+\frac{{\delta }^{13}{C}_{plant\left(t\right)}}{1000}\right)}- \frac{({\delta }^{13}{C}_{C{O}_{2(t=0)}}-{\delta }^{13}{C}_{plant(t=0)})}{\left(1+\frac{{\delta }^{13}{C}_{plant(t=0)}}{1000}\right)}

(3)δ¹³ C_{C{O}_2}= \frac{\left[\right({\delta }^{13}{C}_{carb}+{\epsilon }_{DIC-CaC{O}_3}+2.8)+1000]}{\left(\frac{{\epsilon }_{DIC-C{O}_2}}{1000+1}\right)}-1000

(4)pCO_2(t)= \frac{\begin{array}{r}\Delta \left({\Delta }^{13}C\right)\times A^2+\Delta \left({\Delta }^{13}C\right)\times A\times B\times pC{O}_{2(t=0)}+2\times \Delta \left({\Delta }^{13}C\right)\times A\times B\times C\\ +\\ \Delta \left({\Delta }^{13}C\right)\times B^2\times C\times pC{O}_{2(t=0)}+\Delta \left({\Delta }^{13}C\right)\times B^2\times C^2+A^2\times B\times pC{O}_{2(t=0)}\end{array}}{A^2\times B-\Delta \left({\Delta }^{13}C\right)\times A\times B-\Delta \left({\Delta }^{13}C\right)\times B^2\times pC{O}_{2(t=0)}-\Delta \left({\Delta }^{13}C\right)\times B^2\times C}

(5)T(℃)=17.0-4.52(δ¹⁸O_cc-δ¹⁸O_sw)+0.03(δ¹⁸O_cc-δ¹⁸O_sw)²

2 结果

基于C₃陆生植物有机碳同位素计算的方法,重建的侏罗纪pCO₂浓度范围为407×10^-6~7540×10^-6,并呈现3次显著的pCO₂高值区间(图 3-A)。该研究收集的侏罗纪不同替代指标重建的282个pCO₂记录(见附件)显示出较为平缓的趋势,但从早侏罗世到晚侏罗世仍可以观察到pCO₂整体下降的趋势(图 3-B)。尽管两者的总体趋势基本一致,但在卡洛夫期和托阿尔期,两者大气CO₂浓度存在较大差异。通过研究发现,前人在卡洛夫期利用地质载体重建大气CO₂浓度的相关研究较少,导致该时期的大气CO₂浓度记录不足,无法准确反映当时的CO₂浓度。而托阿尔期的差异可能源于C₃陆生植物有机碳同位素数据受区域性影响因素较大,该时期陆生植物对不同栖息地环境的适应具有很大的差异,进而影响了当时pCO₂的重建结果。

将用C₃陆生植物有机碳同位素方法重建的侏罗纪高分辨率pCO₂曲线与同时期的海水温度、海平面高度、冰川体积、热带植物分布曲线、火山活动、构造运动(Zachos et al., 2001)进行对比,发现3次pCO₂高值区对应侏罗纪的3次高温区,分别位于早侏罗世和晚侏罗世。Nordt等(2022)通过对侏罗纪箭石的低氧同位素分析发现托阿尔期处于高温期,同时重建的高分辨率pCO₂曲线显示托阿尔期处于高pCO₂区,由此可知托阿尔期的高温模式极有可能受大气CO₂浓度影响。气候的变化总体上是由大气CO₂浓度驱动的(Veizer et al., 2000;Royer et al., 2001;Royer and Berner,2003),Royer(2006)认为,当大气CO₂浓度低于500×10^-6时,地球气候处于冰期或寒冷气候模式; 当大气CO₂浓度高于1000×10^-6时,地球处于温暖模式。计算曲线与海平面变化、冰川的形成与消融呈现出高度的对应关系。当pCO₂浓度处于高值区域时,全球进入温暖模式,冰川消融,海平面上升; 而当pCO₂浓度处于低值区域时,全球处于寒冷模式,冰川形成,海平面下降(Lü et al., 2025;Wang et al., 2025)(图 4)。

将曲线与热带植物分布曲线进行对比,发现当曲线处于pCO₂高值区时,热带植物向高纬度迁移; 当曲线处于低pCO₂时,热带植物向低纬度迁移。pCO₂在海洋和陆地气候变化中起到了重要作用,能够控制地球表面温度。当曲线处于高pCO₂时,海洋温度升高; 而当曲线处于低pCO₂时,海洋温度降低,大陆气候变化显示出同样的趋势(Ruebsam and Schwark,2021)。

综上所述,本研究重建的侏罗纪高分辨率大气CO₂浓度曲线与同期的海平面高度、冰川体积、热带植物分布以及火山活动、构造运动等地质事件表现出良好的对应关系,充分证明了该研究重建结果的可靠性与准确性。

3 讨论

基于上述侏罗纪重建pCO₂曲线与各地质事件的高度契合,明确了侏罗纪pCO₂的波动与地质事件存在紧密关联。在此基础上,研究进一步结合不同时期的构造背景与地质事件,系统剖析了造成侏罗纪 pCO₂升高的具体驱动机制,并分别对侏罗纪时期已识别的3次pCO₂的高值区域展开具体讨论。

3.1 三叠纪末期至早侏罗世

三叠纪末期,中大西洋裂谷的形成与中部大西洋岩浆省(CAMP)岩浆活动同步发生,显著改变了地球的大气成分、气候和环境(Zhou et al., 2022)。Bachan Payne(2016)通过碳循环箱型模型讨论了CAMP火山喷发对三叠纪—侏罗纪过渡期 δ¹³C和pCO₂的影响,结果表明CAMP火山喷发释放的大量CO₂导致了当时pCO₂浓度的升高。CAMP火山活动释放的CO₂促进了温室气候的形成,裂谷活动在CAMP岩浆活动之后仍持续,直到中侏罗世才逐渐停止(Schlische et al., 2013)。因此,三叠纪末至早侏罗世期间的高pCO₂值与这一时期的大规模岩浆活动密切相关。CAMP火山喷发不仅释放大量CO₂,还显著改变了大气成分,直接驱动了三叠纪—早侏罗世pCO₂的显著上升,增强了全球温室效应(Lü et al., 2022)。

3.2 早侏罗世托阿尔期

早侏罗世托阿尔期的大洋缺氧事件(T-OAE)表现为全球海水温度升高、海平面上升、植物种类增多并向高纬度迁移以及碳同位素的异常变化。近年来的研究进一步证实,大洋缺氧事件不仅发生在北方洋和特提斯洋区域,还扩展到太平洋和冈瓦纳地区,显示了事件的全球性。该事件期间最显著的特征是碳同位素的负漂移,表明轻碳突发性增加,导致pCO₂的升高(邓胜徽等,2012;Zhang et al., 2025)。卡鲁—费拉大火成岩省的大规模喷发释放了大量CO₂(Pa’lfy et al., 2000;Svensen et al., 2007;Lena et al., 2019;Ruhl et al., 2020),同时,玄武岩烘烤周围富含有机质的沉积物,进一步释放了CO₂(张拴宏等,2022),这些因素共同导致了早侏罗世托阿尔期pCO₂的升高。托阿尔期其他小规模火山活动,如北海地区和巴塔哥尼亚的火山活动对侏罗纪气候发展的影响尚不明确(Ruebsam and Schwark,2021)。

3.3 晚侏罗世

晚侏罗世,全球构造运动异常活跃。中大西洋的打开促成了西非、中非和东非3大裂谷系的形成,非洲与南美洲板块的南部也出现了大型裂谷系。同时,环太平洋火山带的构造运动十分丰富,伴随着板块间或板块内碰撞的造山活动。东太平洋板块俯冲至美洲板块下,导致了落基山脉和安第斯山脉的形成。此外,东亚大陆构造活动产生了蒙古—鄂霍次克洋造山带(Lawver and Lawrence, 2002;Iturralde-Vinent,2003;Bachan and Payne,2016)。该造山带的东部碰撞持续至晚侏罗世甚至早白垩世,连续的板块碰撞诱发了东亚大陆内多条小型造山带的形成,包括阴山—燕山造山带、太行造山带、雪峰造山带等。此外,晚侏罗世期间,造山运动伴随着频繁的火山活动和地震(Yarmolyuk et al., 2000;Daoudene et al., 2013;Dong et al., 2015)。在北巴西、东北非洲和西非的牛津期沉积中记录了火山柱事件,而智利的沉积层则进一步证实了当时大规模的沉积活动。这些事件伴随着火流星、地震、野火和海啸等灾害,释放了大量CO₂和SO₂,进一步增强了温室效应(Wilson and Guiraud,1992;Maluski et al., 1995;Vergara et al., 1995;Baksi and Archibald,1997;Segev,2000;Tennant et al., 2017)。

晚侏罗世的造山运动和火山活动显著影响了全球大气的二氧化碳浓度和温度。频繁的火山喷发不仅释放大量火山灰,还将大量CO₂和SO₂注入大气层,导致了全球变暖。同时,造山运动促进了岩石风化,加速了碳循环(Parrish et al., 1982;Kutzbach and Gallimore,1989;Fluteau,2003),进一步影响了全球气候系统,造成了晚侏罗世的高大气CO₂浓度和高温气候。

4 结论

通过重建全球范围内高分辨率单一指标侏罗纪大气二氧化碳浓度曲线,并将其与侏罗纪的各类地质事件进行对比,揭示了侏罗纪时期古气候变化的关键驱动因素。与以往利用替代指标所建立的CO₂浓度曲线相比,作者重建的曲线更具参考价值,能够更准确地反映侏罗纪时期全球气候的动态变化。重建的pCO₂曲线整体呈现下降趋势,浓度范围为407×10^-6~7540×10^-6,最高值出现在早侏罗世托阿尔期。研究发现,侏罗纪期间多次火山活动持续时间存在差异,且伴随温室气体(以CO₂为主)的大量释放,这显著改变了大气中CO₂的浓度。尤其在早侏罗世和晚侏罗世的pCO₂高值阶段,火山活动与重建曲线呈现出良好的对应关系,表明火山活动是当时驱动pCO₂升高的主要因素之一。

通过对侏罗纪pCO₂曲线的重建及其与同时期地质事件的对比研究,进一步验证了火山活动通过释放温室气体对侏罗纪气候变化的驱动作用,同时也揭示了其他地质过程在区域或全球尺度上调控CO₂浓度的潜在影响。这些发现为深入理解古气候变化与地质过程的耦合机制,提供了重要的实证支撑与研究思路。

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基金资助

* 深地国家科技重大专项项目(2024ZD1001100)

国家自然科学基金项目(41772096)