冷水珊瑚测年与大洋中—深层水碳储库

doi:10.11867/j.issn.1001-8166.2019.12.1243

冷水珊瑚古环境应用研究的首要问题是建立精确的年龄模式。目前常用的珊瑚定年技术包括U/Th,AMS ¹⁴C和²¹⁰Pb测年，其中前两种方法尤为重要。不同冷水珊瑚属种适用不同的定年方法。高镁方解石质的竹节柳珊瑚可用AMS¹⁴C和²¹⁰Pb测试方法定年。竹节柳珊瑚具有清晰的生长纹层，厘定其年龄模式后，可以成为中—深层大洋环境演变的高分辨率记录载体。文石质石珊瑚同时适用于U/Th和AMS ¹⁴C测年方法，在古海洋研究中有特殊价值。由于u/Th测年可以提供样品的绝对年龄，因此进一步计算可获得中—深层大洋的碳储库年龄，这为探究轨道和千年时间尺度上大洋—大气碳交换这一重大学术问题提供了可靠资料。冷水珊瑚测年数据发现末次冰消期时，赤道大西洋和南大洋中层水的碳储库年龄在Heinrich Stadial 1事件结束前后突然大幅度减小，很可能表示深部大洋一部分无机碳转移进入了大气圈，或者代表Heinrich Stadial 1事件前后大西洋中层水分别主要受南半球和北半球潜沉水团的影响。

关键词: 冷水珊瑚, U/Th测年, 放射性碳测年, 南海, 末次冰消期, 碳循环

Establishing a precise chorology is a critical issue when employing cold-water coral as paleoenvironmental archives. Currently, U-Th, ¹⁴C and ²¹⁰Pb dating techniques are the most frequently used methods. The high-magnesium calcite skeleton of bamboo coral has clear growth bands, which is appropriate for ¹⁴C and ²¹⁰Pb dating methods and holds a great potential to be high-resolution archives of mid-to-deep ocean evolution. Aragonitic stony coral is appropriate for both U-Th and ¹⁴C dating methods, which is valuable in paleoceanographic research. Because the U-Th method can provide the absolute chronology of coral samples, it can further be used to calculate the ¹⁴C age of ocean carbon reservoirs. Therefore, U-Th and ¹⁴C dating results of stony coral are currently the most reliable data for exploring the evolution of ocean carbon reservoirs through the Last Glacial Maximum to the present. It has been found that the ¹⁴C ventilation ages of intermediate water masses of the equatorial Atlantic and Southern Ocean significantly decreased at the end of the Heinrich Stadial 1. This suggests a massive carbon transfer from deep oceans to the atmosphere, or the Atlantic intermediate depths were ventilated by the southern- and the northern-sourced water masses, respectively, before and after the Heinrich Stadial 1.

Key words: Cold-water corals, U-Th Dating, Radiocarbon Dating, South China Sea, Last Deglaciation, Carbon Cycle.

中图分类号:

P736.4+4

图1 冷水珊瑚不同属种的寿命(蓝色)以及不同定年技术的测年范围(褐色)^{[

1
]}

Fig.1 Lifespan of several types of cold-water coral (blue), and the relative age span of different dating techniques used in chronology studies (dark brown)^{[

1
]}

图2 南海西沙海区冷水珊瑚照片
（a）,(b)为竹节柳珊瑚骨骼样品;（c）,(d)为石珊瑚骨骼样品；其中竹节柳珊瑚样品包含碳酸盐骨骼(白色)和蛋白质结节(黑色)两个部分

Fig.2 Photos of cold-water coral from Xisha, South China Sea
（a）~(d) are bamboo and stony coral, respectively. Fossil of bamboo coral comprises of two components, the carbonate internodes（white） and the gorgonin nodes（black）

Table 1 U/Th和 ¹⁴C dating results of cold-water corals from Xisha, South China Sea

珊瑚编号	品种	经度/°E	纬度/°N	水深/m	取样位置	²³⁸U/(×10^-9,±2σ)	²³⁰Th年龄/(a BP,±2σ)	AMS ¹⁴C年龄/(a BP,±1σ)
SY067-9-3	竹节柳珊瑚	110.7107	16.5724	1 338	径向生长轴外缘	58.8±0.1	18 876±3 470	-
SY067-9-3	竹节柳珊瑚	110.7107	16.5724	1 338	径向生长轴中心	25.6±0.1	1 010±237	-
SY068-7-2	竹节柳珊瑚	111.0540	16.7546	693.9	径向生长轴外缘	68.3±0.2	3 081±275	-
					径向生长轴中心	64.5±0.1	2 359±201	-
					径向生长轴中心	47.8±0.1	9 387±3 148	-
SY075-16-2	石珊瑚	110.6298	15.3121	577	径向生长轴外缘	3 602.5±62.7	762±142	1 885±20
SY075-16-2	石珊瑚	110.6298	15.3121	577	径向生长轴中心	3 799.7±8.5	718±44	1 995±20
SY076-9	石珊瑚	110.7132	16.5726	1 294	径向生长轴外缘	3 830.7±5.5	6 154±94	5 025±35
SY076-9	石珊瑚	110.7132	16.5726	1 294	径向生长轴中心	5 098.1±9.3	8 823±287	5 695±35

Table 1 U/Th和 ¹⁴C dating results of cold-water corals from Xisha, South China Sea

珊瑚编号	品种	经度/°E	纬度/°N	水深/m	取样位置	²³⁸U/(×10^-9,±2σ)	²³⁰Th年龄/(a BP,±2σ)	AMS ¹⁴C年龄/(a BP,±1σ)
SY067-9-3	竹节柳珊瑚	110.7107	16.5724	1 338	径向生长轴外缘	58.8±0.1	18 876±3 470	-
SY067-9-3	竹节柳珊瑚	110.7107	16.5724	1 338	径向生长轴中心	25.6±0.1	1 010±237	-
SY068-7-2	竹节柳珊瑚	111.0540	16.7546	693.9	径向生长轴外缘	68.3±0.2	3 081±275	-
					径向生长轴中心	64.5±0.1	2 359±201	-
					径向生长轴中心	47.8±0.1	9 387±3 148	-
SY075-16-2	石珊瑚	110.6298	15.3121	577	径向生长轴外缘	3 602.5±62.7	762±142	1 885±20
SY075-16-2	石珊瑚	110.6298	15.3121	577	径向生长轴中心	3 799.7±8.5	718±44	1 995±20
SY076-9	石珊瑚	110.7132	16.5726	1 294	径向生长轴外缘	3 830.7±5.5	6 154±94	5 025±35
SY076-9	石珊瑚	110.7132	16.5726	1 294	径向生长轴中心	5 098.1±9.3	8 823±287	5 695±35

图3 冷水珊瑚记录的核爆信号^{[

19
,

20
,

21
,

22
,

23
]}
其中同一个竹节柳珊瑚样品的碳酸盐骨骼和蛋白质结节AMS ¹⁴C年龄出现较明显的偏差

Fig.3 Recognize the ¹⁴C bomb signal in cold-water coral samples^{[

19
,

20
,

21
,

22
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23
]}
Note the apparent offset between ¹⁴C ages of carbonate skeleton and gorgonin nodes belonging to a same bamboo coral sample

图4 0~25 ka BP期间大气CO₂浓度及大气Δ¹⁴C水平以及变化
(a)大气CO ₂浓度 ^{[

29
,

30
]}，在冰消期的Heinrich Stadial 1和新仙女木时期出现CO ₂浓度的上升；(b)重建的大气Δ ¹⁴C ^{[

17
]}和模拟的大气Δ ¹⁴C ^{[

32
]}波动历史比较；其中模拟大气Δ ¹⁴C水平来自模型BICYCLE的输出结果，假定海洋—大气碳交换速率不变，利用宇宙射线速率波动进行估算；可以看出，重建和模拟结果并不吻合，说明海洋—大气碳交换速率出现过巨大波动

Fig.4 Atmospheric CO₂and Δ¹⁴C changes between 25 and 0 ka BP
(a) Reconstructed atmospheric CO ₂concentrations ^{[

29
,

30
]}, which rose in two stages over the last deglaciation: A first 50×10 ^-6 rise during Heinrich Stadial 1 and a later 25×10 ^-6 rise during the Younger Dryas(YD) interval; (b) A comparison of reconstructed and simulated atmospheric Δ ¹⁴C changes ^{[

17
,

32
]}. The model output is from the BICYCLE model, which was forced by changing production rates of cosmic rays and a constant carbon exchange rate between the atmosphere and the ocean. The offset between the reconstruction and the simulation suggests a significant change in the carbon exchange rate between the atmosphere and the ocean in the past

图5 根据冷水珊瑚和有孔虫重建的2.5万年以来中深层海洋碳储库年龄变化
(a)冷水珊瑚和深海沉积物站位图，背景为工业革命之前的海水Δ ¹⁴C值 ^{[

57
]}；(b),(c)冷水珊瑚估算的赤道大西洋和德雷克海峡中—深层海水ΔΔ ¹⁴C值变化 ^{[

37
,

58
]}；(d),(e)有孔虫估算的南大洋深部水团ΔΔ ¹⁴C值变化 ^{[

36
,

59
]}；(f)重建的大气Δ ¹⁴C波动历史 ^{[

17
]}；ΔΔ ¹⁴C表示海水与大气Δ ¹⁴C值的差值；注意Heinrich Stadial 1事件结束时(约1.46万年前)，不同深度海水ΔΔ ¹⁴C值均出现大幅度下降

Fig.5 Changes of intermediate-deep ocean carbon reservoirs ages between 25 and 0 ka BP, derived from cold-water coral and foraminifera
(a) Geographic locations and water depths of coral samples and sediment cores, plotted against the pre-industrial distribution of seawater Δ ¹⁴C values ^{[

57
]}； (b),(c) Reconstructed intermediate-deep ocean ΔΔ ¹⁴C values in the equatorial tropical Atlantic and the Drake Strait, derived from cold-water coral samples ^{[

37
,

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]}； (d),(e) Reconstructed ΔΔ ¹⁴C values of the deep Southern Ocean, derived from foraminiferal samples ^{[

36
,

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]}； (f) Reconstructed atmospheric Δ ¹⁴C changes ^{[

17
]}； ΔΔ ¹⁴C indicates the Δ ¹⁴C value offset between the contemporary ocean and atmosphere； Note a significant decline of ΔΔ ¹⁴C values at different water depths occurred at the end of the Heinrich Stadial 1 (about 14.6 ka BP)

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Dating Methods of Cold-water Corals and Their Application in Reconstructing Carbon-reservoir Ages of Intermediate and Deep Oceans