新元古代成冰纪雪球地球与化学风化作用

陈欣阳; 李彪; 李超

doi:10.3799/dqkx.2025.006

新元古代成冰纪雪球地球与化学风化作用

doi: 10.3799/dqkx.2025.006

陈欣阳^{1, 2, 3, ,},
李彪^{2, 3},
李超^{1, 2, 3}

1.
成都理工大学油气藏地质及开发工程全国重点实验室, 四川成都 610059
2.
成都理工大学沉积地质研究院, 四川成都 610059
3.
成都理工大学沉积与生物地球化学国际研究中心, 四川成都 610059

基金项目:

国家重点研发计划项目 2022YFF0800100

国家自然科学基金项目 42425002

国家自然科学基金项目 42373070

国家自然科学基金项目 42130208

详细信息

作者简介:
陈欣阳（1987-），男，研究员，博士，主要从事非传统稳定同位素与风化作用研究.ORCID：0000-0002-7706-688X. E-mail：xinyangchen@cdut.edu.cn

中图分类号: P532
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- 被引次数: 0
出版历程
- 收稿日期: 2024-12-04
- 网络出版日期: 2025-03-19
- 刊出日期: 2025-03-25

Chemical Weathering during the Neoproterozoic Snowball Earth Events

Chen Xinyang^{1, 2, 3
,
,},
Li Biao^{2, 3},
Li Chao^{1, 2, 3}

1.
State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation, Chengdu University of Technology, Chengdu 610059, China
2.
Institute of Sedimentary Geology, Chengdu University of Technology, Chengdu 610059, China
3.
International Center for Sedimentary Geochemistry and Biogeochemistry Research, Chengdu University of Technology, Chengdu 610059, China

摘要

摘要: 新元古代成冰纪（约720~635 Ma）发生了两次全球范围的雪球地球事件（斯图特冰期和马里诺冰期），是地球生命系统和环境演化的重要转折期.越来越多的证据显示雪球地球时期的气候和海洋氧化还原状态存在显著的时空波动，然而这一特征背后的碳循环‒海陆系统交互以及冰期气候波动的驱动机制还很不清楚.作为链接雪球地球发育、海洋化学和生物演化最为关键过程之一的大陆风化作用目前仍旧没有被有效刻画是其中的一个重要原因.本文综述了现有风化指标及其在成冰纪化学风化强度方面的研究现状，在此基础上，统计了全球28个成冰纪剖面（含钻孔）867件碎屑岩样品的主量元素数据，利用ln（Al₂O₃/Na₂O）这一高效风化指标定量重建了从拉伸纪晚期到埃迪卡拉纪早期全球平均化学风化强度的演化趋势，发现了多次化学风化的强弱波动，表明冰期的启动和结束均与化学风化作用息息相关.此外，马里诺冰期的平均风化强度显著高于斯图特冰期，可能暗示马里诺冰期存在一定程度的水循环.未来的研究应进一步推动多指标的综合应用，以加深对成冰纪化学风化机制的理解，为全球环境演化的探索提供更多深入的视角和证据支持.
- 新元古代 /
- 成冰纪 /
- 化学风化指标 /
- 雪球地球 /
- 碳循环 /
- 气候变化
Abstract: Two global-scale Snowball Earth events occurred during the Cryogenian period of the Neoproterozoic era (ca. 720‒635 Ma), representing a crucial transition period for the Earth's biological systems and environmental evolution. An increasing amount of evidence indicates that there are spatio-temporal fluctuations in the climate and marine redox state during the Snowball glaciation. However, the driving mechanisms of the carbon cycle-land-ocean system interaction and glacial climate fluctuations during this period remain largely unclear. Continental weathering is a key process linking snowball development, ocean chemistry, and biological evolution, but existing research has been unable to effectively characterize continental weathering during the Snowball period. This paper summarizes the current status of proxies for chemical weathering intensity during the Cryogenian period, and statistically analyzes the major-element data of 867 clastic rock samples from 28 Cryogenian sections (including drill cores) worldwide. Using the index of ln(Al₂O₃/Na₂O), the evolutionary trend of the global average chemical weathering intensity from the Late Tonian period to the Early Ediacaran period is quantitatively reconstructed. Three fluctuations in chemical weathering intensity are discovered, indicating that the onset and termination of glaciation are closely related to chemical weathering. In addition, the average weathering intensity during the Marinoan glaciation is significantly higher than that during the Sturtian glaciation, possibly suggesting the existence of a certain degree of hydrological circulation during the Marinoan glaciation. Future research can further apply the comprehensive application of multiple proxies to deepen the understanding of the chemical weathering mechanisms during the Cryogenian period, and provide more in-depth perspectives and evidence to support the exploration of global environmental evolution.
- Neoproterozoic /
- Cryogenian /
- chemical weathering intensity /
- Snowball Earth /
- carbon cycle /
- climate change

HTML全文

图 1 全球新元古代成冰纪马里诺冰期的CIA记录对比

数据来自冯连君等（2004）、王自强等（2006）、Rieu et al.（2007）、刘兵等（2007）、赵小明等（2011）、蔡雄飞等（2017）、李王鹏等（2022）

Fig. 1. Comparison of the global CIA records in the Cryogenian glaical deposits

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图 2 新元古代成冰纪海水Sr同位素演化曲线（据Cox et al.，2016）

Fig. 2. The Sr isotope record of the Neoproterozoic seawater from marine carbonates (Cox et al., 2016)

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图 3 Lipp et al.(2020)提出的指示源岩成分指数(ψ)与化学风化指数(ω)示意图（a）以及ln（Al₂O₃/Na₂O）与化学风化指数（ω）协变图（b）

利用主成分分析法（PCA），以上地壳平均组成为基准，结合现代土壤剖面以及岩浆演化序列的主量元素变化，可以识别出由土壤剖面代表的风化趋势ω和岩浆演化序列代表的源岩成分趋势.而氧化铝和氧化钠比值的自然对数值和风化指标具有显著的线性相关性，表明ln（Al₂O₃/Na₂O）可以作为良好的风化强度指标

Fig. 3. Cross-plot of weathering proxy (ω) and protolith proxy (ψ) based on the study by Lipp et al. (2020) (a), cross-plot between weathering proxy (ω) and natural log ratio ln(Al₂O₃/Na₂O) (b)

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图 4 本文统计的867件样品的CIA（a）、CIW（b）、PIA(c)、WIP(d)风化指标的统计分布直方图

图中样品各指标总体较为接近正态分布，主要是因为间冰期的样品数据占主导，而间冰期的风化强度高于冰期.更高的风化强度主要出现在成冰纪前的拉伸纪晚期以及之后的埃迪卡拉纪早期

Fig. 4. The histograms of the calculated weathering proxies CIA(a), CIW(b), PIA(c) and WIP(d) for the 867 samples compiled in this study

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图 5 成冰纪碎屑岩的ACNK图解

全球该时期的数据较为一致，均呈现出从源岩为玄武岩/英云闪长岩/花岗岩，向伊利石/白云母方向演化，说明源岩的化学风化过程中Ca和Na的流失要快于K，指示了斜长石的优先风化.仅在塔里木阿克苏地区的苏盖尔布拉克组和叶城地区的雨塘组中5件样品数据表现出K的富集

Fig. 5. ACNK diagrams of the Cryogenian siliciclastic rocks

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图 6 成冰纪碎屑岩风化指标ln（Al₂O₃/Na₂O）（a）、指示源岩成分差异的指标ln（K₂O/MgO）（b）、指示沉积物再循环的指标ICV（c），以及SiO₂/Al₂O₃比值（d）的统计直方图

Fig. 6. Histograms of the compiled proxies ln(Al₂O₃/Na₂O) (a) for weathering intensity, ln(K₂O/MgO) (b) for protoliths, ICV (c) for compositional variability and sediment recycling, and SiO₂/Al₂O₃ (d) ratio of the compiled Cryogenian siliciclastic rocks

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图 7 CIA、CIW、PIA、和WIP与风化指标ln（Al₂O₃/Na₂O）之间的相关性图解

其中CIA、CIW以及PIA均与ln（Al₂O₃/Na₂O）存在较好的正相关关系，但是在风化程度较高的区域，CIA表现得更加发散，表明在强风化地区，由于化学动力学的差异，碱金属K、Na和碱土金属Ca、Mg可能出现差异性风化.而CIW和PIA在强风化区则趋向饱和，可能是由于Ca和Mg接近于完全流失，从而使得CIW和PIA对较强烈的化学风化不够敏感

Fig. 7. The cross-plots between traditional weathering proxies CIA, CIW, PIA, WIP and ln(Al₂O₃/Na₂O)

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图 8 新元古代成冰纪前后风化指标ln(Al₂O₃/Na₂O) 随时间的演化示意

图中每一个箱线图左边为统计样品的拟合正态分布曲线，中间为统计数据点分布，右边为箱线图，箱体上下边界分别对应数据的上下四分位数，箱体内水平横线和数字为中位数.上下须线连接的水平横线表示数据的最大值和最小值，须线之外的点为异常值.图右侧棕色五角形代表后太古宙澳大利亚页岩（Taylor and McLennan，1985）（PAAS），绿色三角形为平均上地壳（Rudnick and Gao，2014）（UCC），蓝色正方形为花岗闪长岩（Wedepohl，1995）（Grd）

Fig. 8. The box-whisker plot of ln(Al₂O₃/Na₂O) values from the Late Tonian to the Early Ediacaran

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图 9 新元古代成雪球地球事件及前后各时期化学风化的直方图

图中箭头为ln（Al₂O₃/Na₂O）中位值随时间的变化，显示出多次强弱波动

Fig. 9. The histograms of ln(Al₂O₃/Na₂O) values divided by different periods ranging from the Late Tonian, Sturtian ice age, interglacial, Marinoan glaciation, and Early Ediacaran

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表 1 常用主量元素风化指标及适用范围

Table 1. Common proxies for chemical weathering intensity based on major element compositions and their limitations

风化指标	计算公式	指标适用范围
WIP	100×(CaO^*/0.7+2Na₂O/0.35+2K₂O/0.25+MgO/0.9)	不适用于强风化情况，受石英含量的影响显著
CIA	Al₂O₃/(Al₂O₃+CaO^*+K₂O+Na₂O)×100	受源区影响较大，同时成岩作用也会对其产生影响
CIW	[Al₂O₃/(Al₂O₃+CaO^*+Na₂O)]×100	没有考虑钾长石中的Al元素，不适用于物源区母岩中钾长石富集的样品
PIA	100×(Al₂O₃-K₂O)/(Al₂O₃+CaO^*+Na₂O-K₂O)	仅适用于判断母岩中含有斜长石而不含钾长石的物源区风化程度
ICV	(Fe₂O₃+K₂O+Na₂O+CaO^*+MgO+TiO₂)/Al₂O₃	对CIA值计算的检查，表征矿物成分的成熟度
CIX	100×A1₂O₃/(A1₂O₃+Na₂O+K₂O)	该指标不用考虑CaO
注：式中氧化物均为摩尔含量；CaO^*为硅酸盐中CaO的摩尔含量.

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