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摘要:
深海黏土广泛分布在水深超过碳酸盐补偿深度(CCD)以下的大洋盆地中，其沉积速率十分缓慢，只有少量的生物组分(主要是生物磷灰石)被保存，通常具有较高的稀土元素含量；海洋沉积物常用的磁性地层与生物地层相结合的定年手段通常不能有效使用。因此，深海黏土沉积年龄框架的建立一直存在巨大的困难和挑战，严重阻碍了对沉积环境演化和稀土超常富集机制等方面的深入研究。本文回顾总结了20世纪以来逐步发展应用的多种深海黏土定年方法，主要包括磁性地层、鱼牙87Sr/86Sr定年、鱼牙U-Pb定年、10Be测年、230Thex测年、187Os/188Os定年、鱼鳞石生物地层、恒定Co通量模型以及常用的地层对比方法。这些方法各具优缺点，单一使用以上任何一种定年方法几乎都难以获得完整可靠的年龄框架。因此，综合运用多种定年方法，对获得的年龄框架进行系统对比和验证，将会更为有效地提高深海黏土年龄框架的可靠性。
Abstract:Pelagic clay, which is extensively distributed in the ocean basins below the carbonate compensation depth, exhibits slow sedimentation rate and contains only a small amount of preserved biogenic components (primarily biogenic apatite). The commonly used dating methods that combine magnetic stratigraphy with biostratigraphy in marine sediments cannot be effectively applicable. As a result, the establishment of a age framework for pelagic clay has been hindered by enormous difficulties and challenges, which seriously limits the researchers in geoscience to thoroughly investigate the evolution of sedimentation environment and the mechanisms of hyper-enrichment in rare earth elements in pelagic clay. In this article, we reviewed various dating methods for pelagic clay used since the last century, including mainly: magnetostratigraphy, fish teeth 87Sr/86Sr dating, fish teeth U-Pb dating, 10Be dating, 230Thex dating, 187Os/188Os dating, ichthyolith biostratigraphy, constant Co-flux model, and commonly used stratigraphic correlation methods. Each method has own advantages and disadvantages, and it is often difficult to acquire a complete and reliable age framework using any of the above methods alone. Consequently, systematic comparsion and validation for age framework obtained by intergrating multiple dating methods will be more efficient in improving the relability of an age framework for dating pelagic clay.
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Key words:
- pelagic clay /
- dating method /
- magnetostratigraphy /
- fish teeth/ichthyolith /
- integrated chronology
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表 1 部分深海黏土沉积物定年研究总结
Table 1. Summary of some pelagic clay dating studies
区域和站位 位置 定年方法 年龄范围和或深度 平均沉积速率
/(mm/ka)备注 参考文献 北太平洋
GPC330.33˚N、
157.82˚W鱼鳞石生物地层 上新世—古新世 0.2～0.3 误差约±1～5 Ma [5] 磁性地层 布容极性期
更新世2.2
1.7[7] 鱼牙87Sr/86Sr 用以上两种方法来进行验证 [8] 10Be 0～6 m
6～10 m约1.2
约0.5以1.387 Ma为半衰期重新
进行计算[6] 恒定Co通量模型 晚古新世—中中新世 0.2 显著低于更新世时期的沉积速率 [3] 铱元素异常 异常高值指示K-Pg边界(约65 Ma) [3] 北太平洋
PC0132.5˚N、
141.2˚W鱼牙87Sr/86Sr 0～10.7 m (0～24 Ma) 0.45 误差±1～3 Ma [12] 东赤道太平洋
PC078.8˚N、
135.4˚W鱼牙87Sr/86Sr 0～15 m (0～19 Ma)
0～4 m (深海黏土)
4～16 m (硅质黏土)
0.3
2.0误差<±2 Ma [13] 东赤道太平洋
GC19019.78˚N、
154.97˚W鱼牙87Sr/86Sr 21～32 Ma 2.3 误差约±0.8～3 Ma [14] 西太平洋
WPPC1902-0818.29˚N、
149.84˚E磁性地层 0～6 m (0～2.59 Ma) 2.3 棕黄色深海黏土 [15] 西太平洋
core C20.22˚N、
161.48˚E230Thex
自生10Be/9Be
磁性地层0～3.1 m (0～11.6 Ma)
0～1.2 Ma
1.2～11.6 Ma
1.67
0.125多种测年方法获得的沉积
速率一致[16] 西太平洋
GC1816.90˚N、
162.18˚E自生10Be/9Be
磁性地层
轨道调谐1.8～5.4 m
(11～15.4 Ma)0.1～2.5 [17] 西太平洋
WP4123°N、
158°E鱼牙U-Pb定年 2.2～6.5 Ma 1.4 误差±1～2 Ma [18] 西太平洋
PC1122.98˚N、
154.02˚E187Os/188Os
磁性地层9～12 m 0.43～1.02 假设187Os/188Os识别的E2-E3边界位于磁性地层内某一极性时期 [19-20] 南太平洋
U136522.85˚S、
165.65˚W磁性地层
Co通量模型0～6 m
10～18 m约1
＜0.2[21-22] 
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