Advances of driving mechanisms of the Early Eocene Climatic Optimum (EECO): Constraints from the Linzizong volcanic rocks in southern Tibet
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摘要:
早始新世气候适宜期(Early Eocene Climatic Optimum, 简称EECO, 53~51Ma)是新生代最重要的碳循环和气候扰动事件之一, 深入了解其驱动机制对于我们更准确的预测和应对正在发生的全球变暖将具有重要的指导意义。本文根据最新研究结果, 对该事件的驱动机制作一综述, 主要包括以下几种观点: 1)雷克雅内斯洋中脊扩张; 2)伊豆-小笠原-马里亚纳海沟(IBM)一带弧前玄武岩大规模爆发; 3)北美西部和东南亚地区大陆裂谷发育; 4)风化作用减弱; 5)岩石有机碳及硫化物氧化作用; 6)银河系中星际暗物质的影响; 7)大陆弧火山作用及其相关的变质脱碳; 8)青藏高原南部林子宗火山岩大爆发。在系统综述其驱动机制的基础上, 粗略估算了青藏高原南部早始新世林子宗火山岩爆发期的碳释放量, 并探讨了其对EECO事件的驱动作用。
Abstract:Early Eocene Climatic Optimum (EECO, 53~51Ma) is one of the most important warming events of the past 65 million years and associated with carbon cycle and climate disturbance. Investigating its driving mechanism is important for understanding the potential impact of ongoing global warming and its relationship to carbon release. This paper summarized the research progress concerning the driving mechanism of the EECO, which includes the following viewpoints: 1) the spreading of the Reykjanes mid-ocean ridge; 2) the flare-up of forearc basalts along the Izu-Bonin-Mariana (IBM); 3) the development of continental rifts in western North America and Southeast Asia; 4) the reduce of the weathering effect; 5) the oxidation of rock organic carbon and sulfide minerals; 6) the impact of dark matter in the galaxies; 7) the continental arc volcanism and associated metamorphic decarbonization; 8) the development of the Linzizong volcanic rocks in the southern Tibetan Plateau. Based on the systematic review, we roughly estimated the carbon emission of Early Eocene Linzizong volcanic rocks in the southern Tibetan Plateau, and discussed its potential contribution to the EECO event.
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图 1
晚白垩世以来全球深海碳、氧同位素及冈底斯岩基和林子宗火山岩年代学格架图
Figure 1.
Global deep-sea carbon, oxygen isotopes and chronological framework of the Gangdese batholith and Linzizong volcanic rocks since Late Cretaceous
图 2
洋中脊扩张速率、海底生产速率及相对海平面高度变化曲线
Figure 2.
Curves of mid-ocean ridge expansion rate, seafloor production rate and relative sea level
图 3
侏罗纪以来大陆裂谷长度变化(a)与大气中CO2浓度变化(b)(据Brune et al., 2017修改)
Figure 3.
Variation of continental rift length (a) and atmospheric CO2 concentration (b) since Jurassic (modified after Brune et al., 2017)
图 4
古新世以来深海燧石发育状况和深海底栖有孔虫δ18O同位素变化曲线(据Muttoni and Kent, 2007修改)
Figure 4.
Global deep-sea chert occurrence and benthic foraminifer δ18O isotope variation curves since Paleocene (modified after Muttoni and Kent, 2007)
图 5
滤波后的地磁倒转频率(a)、δ18O值(b)和板块俯冲速率(c)变化曲线(据Chen et al., 2015修改)
Figure 5.
The variation curves of filtered geomagnetic reversal frequency (a), δ18O value (b), and subduction rates of tectonic plates (c) (modified after Chen et al., 2015)
图 6
俯冲带火山系统碳的来源及其释放途径示意图(据Mason et al., 2017修改)
Figure 6.
Schematic diagram of sources of carbon in a subduction zone volcanic system and its release pathways (modified after Mason et al., 2017)
图 7
新生代温度大气中CO2浓度变化与岩浆作用之间的关系(据Sternai et al., 2020修改)
Figure 7.
The relationship between atmospheric CO2 concentration and magmatism in Cenozoic (modified after Sternai et al., 2020)
图 8
岛弧、大陆弧简图及750Ma以来全球大陆弧发育情况和碎屑锆石记录
Figure 8.
Sketch map of island arc, continental arc, global continental arc development and detrital zircon records since 750Ma
图 9
青藏高原地质简图(据Wu et al., 2010修改)
Figure 9.
Simplified geological map of the Tibet Plateau (modified after Wu et al., 2010)
表 1
早始新世青藏高原至苏门答腊地区不同构造域脱碳量估算
Table 1.
Estimation of decarbonization of different tectonic domains from Tibet Plateau to Sumatra region in Early Eocene
脱碳对象 年龄(Ma) 长度(km) 宽度(km) 面积(km2) 厚度(km) 体积(km3) 与Deccan玄武岩体积比 CO2 (mol) CO2 (g) 自身脱碳(Tg C/yr) 变质脱碳倍数 变质脱碳(Tg C/yr) 总的碳释放通量(Tg C/yr) 帕那组火山岩 ca.52~51 10505 2 21010 0.016 0.07×1017 2.94 0.08 3.6 0.29 0.37 2 21010 0.016 0.07×1017 2.94 0.08 8.6 0.69 0.77 7.8 81939 0.06 0.26×1017 11.48 0.31 3.6 1.13 1.44 7.8 81939 0.06 0.26×1017 11.48 0.31 8.6 2.69 3.0 青藏高原构造域早始新世火山岩 ca.52~51 1200 100 120000 2 2.4×105 0.18 0.76×1017 3.36×1018 0.92 3.6 3.30 4.22 2 2.4×105 0.18 0.76×1017 3.36×1018 0.92 8.6 7.89 8.81 4 4.8×105 0.37 1.53×1017 6.73×1018 1.83 3.6 6.60 8.43 4 4.8×105 0.37 1.53×1017 6.73×1018 1.83 8.6 15.78 17.61 6 7.2×105 0.55 2.29×1017 1.01×1019 2.75 3.6 9.91 12.66 6 7.2×105 0.55 2.29×1017 1.01×1019 2.75 8.6 23.66 26.41 8 9.6×105 0.74 3.06×1017 1.35×1019 3.67 3.6 13.21 16.88 8 9.6×105 0.74 3.06×1017 1.35×1019 3.67 8.6 31.55 35.22 青藏高原-苏门答腊构造域早始新世火山岩 ca.52~51 6000 100 600000 2 1.2×106 0.92 3.82×1017 1.68×1019 4.59 3.6 16.51 21.09 2 1.2×106 0.92 3.82×1017 1.68×1019 4.59 8.6 39.44 44.02 4 2.4×106 1.85 7.64×1017 3.36×1019 9.17 3.6 33.02 42.19 4 2.4×106 1.85 7.64×1017 3.36×1019 9.17 8.6 78.88 88.05 6 3.6×106 2.77 1.15×1018 5.04×1019 13.76 3.6 49.53 63.28 6 3.6×106 2.77 1.15×1018 5.04×1019 13.76 8.6 118.31 132.07 8 4.8×106 3.69 1.53×1018 6.73×1019 18.34 3.6 66.04 84.38 8 4.8×106 3.69 1.53×1018 6.73×1019 18.34 8.6 157.75 176.10 注：帕那组火山岩爆发时限采用的52~51Ma来自于作者对文献数据的汇总和未发表数据；Deccan玄武岩体积(1.3×106km3)来自于Jay and Widdowson (2008)，Deccan玄武岩脱碳量(4.14×1017mol CO2)来自于 Tobin et al. (2017) ；早始新世帕那组火山岩的最小和最大厚度分别来分别自于莫宣学等(2003)、杨德明等(2005①)；青藏高原-苏门答腊构造域早始新世火山岩宽度采用最小估计值100km，厚度使用2~8km的范围
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