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Journal of Tropical Oceanography >

2018 , Vol. 37 >Issue 1: 64 - 71

DOI: https://doi.org/10.11978/2017022

Orginal Article

The discovery of deep-water corals from cold seep area in the northern South China Sea and their characteristics

  • CHEN Zhong , 1 ,
  • MO Aibin 1, 2 ,
  • ZHAO Meixia 1 ,
  • ZHONG Yi 1, 2 ,
  • YAN Wen 1, 2
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  • 1. CAS Key Laboratory of Ocean and Marginal Sea Geology, South China Sea Institute of Oceanology, Guangzhou 510301, China
  • 2. University of Chinese Academy of Sciences, Beijing 100049, China
Corresponding author: CHEN Zhong. E-mail:

Received date: 2017-02-26

  Request revised date: 2017-05-10

  Online published: 2018-02-02

Supported by

National Natural Science Foundation (41376057, 41676056)

Copyright

热带海洋学报编辑部
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Abstract

Cold-water corals, also known as deep-water corals, are newly found ecological resources with high biological diversity and attract scientific research on environmental changes. In this study, we investigated cold-water corals retrieved from the cold seep area in the northern South China Sea. We identified two species (Crispatotrochus sp.1, Crispatotrochus sp.2) and four genera [Balanophyllia (Balanophyllia), Balanophyllia (Eupsammia), Lochmaeotrochus, and Enallopsammia]. Stable carbon and oxygen isotopic analyses revealed that the δ13C and δ18O of cold-water corals were -7.36‰ ~ -1.15‰ and -1.38‰ ~ 3.67‰, respectively. The δ13C and δ18O results were close to the carbon and oxygen isotopic values of cold-water corals in other parts of the world, but were quite different from those of warm-water corals, cold-seep carbonate rocks and low-temperature hydrothermal carbonate rocks. This research discovered cold-water corals in a cold seep region of the northern South China Sea. This discovery is important for the studies on environmental effects of deep-water currents and of cold springs in the region.

Key words： deep-water corals; hydrocarbon seepage; C-O isotope; bottom current; northern South China Sea

Cite this article

CHEN Zhong , MO Aibin , ZHAO Meixia , ZHONG Yi , YAN Wen . The discovery of deep-water corals from cold seep area in the northern South China Sea and their characteristics[J]. Journal of Tropical Oceanography, 2018 , 37(1) : 64 -71 . DOI: 10.11978/2017022

冷水珊瑚也称为深水珊瑚, 主要分布在大陆架、大陆坡、海山与深海盆地附近(Roberts, 2009; Davies et al, 2011), 通常位于海面以下30~1000m的海底, 最深可达6328m (Keller, 1976), 盐度32‰~38.8‰, 水温4~12℃, 最低可达-1.1℃(Wheeler et al, 2007)。冷水珊瑚不与单细胞藻类虫黄藻共生, 主要以水中的浮游生物和从浅水层沉降下去的有机质为食(Roberts et al, 2006), 或以与海底浅层甲烷流体有关的细菌、微小生物为食(Hovland et al, 2003), 因此, 可以生长在缺光或无光的深海冷水环境中。在特定的水动力条件下可形成具有多种形态特征的冷水珊瑚礁(泥丘), 为鱼、虾、蟹、管虫等提供了良好的生境条件, 使得暗淡无光的深海环境充满生机。目前发现的最大冷水珊瑚礁是挪威海岸的苏拉珊瑚礁, 礁体长度超过13km、宽达300m、高达35m (Freiwald et al, 1999)。
冷水珊瑚是深海生态系统的重要组成部分, 其在生物多样性、生态资源和科研价值方面的重要性引起了广泛关注。科研人员利用冷水珊瑚的地球化学和同位素指标, 如δ18O、Ba/Ca、Mg/Ca和Sr/Ca以及Sr-Nd-Pb等, 重建海水古海温(Mitsuguchi et al, 1996; Sinclair et al, 2006), 揭示深海的碳循环(Burke et al, 2012; Hines et al, 2015)、水团通风状况和演化历史(Montero-Serrano et al, 2011; Copard et al, 2012), 研究人类活动对大洋海水变暖和酸化(Guinotte et al, 2006; Turley et al, 2007)的影响等。同时, 由于冷水珊瑚生长较为缓慢, 一旦受到破坏, 需要成百上千年的时间才能恢复到原来的状况, 目前世界各国非常重视对冷水珊瑚及其生境的保护(Davies et al, 2007)。
我国近海分布冷水珊瑚, 国外学者对南海冷水珊瑚的研究较早, 1890年Bassett-Smith曾报道在南海的南沙群岛(郑和群礁)和中沙群岛采集到冷水珊瑚(Bassett-Smith, 1890)。直到20世纪70年代末, 我国学者才开启南海北部大陆架冷水石珊瑚研究(邹仁林 等, 1983), 随后在南海北部大陆架75504站(19°30′N, 113°00′E)(邹仁林, 1984a)、西沙群岛永乐群岛(邹仁林, 1984b)以及其他多处海域发现不同种属的冷水珊瑚(邹仁林, 1988), 但是早期的工作主要集中在鉴定珊瑚种属和生态分析方面(邹仁林, 1988), 而对这些冷水珊瑚的形成环境和机理研究甚少, 更谈不上采取保护措施了。
本文报道了在东沙西南海域冷泉区用抓斗采样器采获的珊瑚碎屑的种属形貌特征及其碳氧同位素组成, 证实南海深海环境存在和发育冷水珊瑚,其生态系统值得进一步关注、调查和研究。

1 样品背景与珊瑚鉴定

发现冷水珊瑚的3个站位分别为08CF10站(116°28′30.48"E, 20°11′8.28"N, 水深863m)、08CF14A站(116°36′1"E, 20°14′11.34"N, 水深578m)和08CF14B站(116°36′6.3"E, 20°13′54.06"N, 水深621m)(图1a)。推测其底层水温度为5~7℃、盐度为34.5‰ (李薇 等, 1998), 这3个站位位于太平洋深水洋流经吕宋海峡侵入南海后向西输送的途经海域(邵磊 等, 2007; Qu et al, 2009; Liu et al, 2015)(图1b), 同时也处于南海北部天然气水合物异常区内(张树林, 2008)。在分布冷水珊瑚的海底发育大量泥底辟、气烟囱构造, 可能是海底含烃流体渗漏的通道(阎贫 等, 2014)。在冷水珊瑚站位北部海域, 分布与冷泉活动密切相关的冷泉碳酸盐岩(陈忠 等, 2006; 杨克红 等, 2009; Tong et al, 2013), 在站位东西两侧海域, 检测到水体甲烷含量的高异常(尹希杰 等, 2008), 指示海底下蕴含丰富的天然气水合物, 并存在浅部冷泉流体活动。
Fig. 1 The distribution of deep-water corals found in the northern South China Sea

图1 冷水珊瑚站位(a)及其位置(b)和地质环境(c)图
图c比例尺为1:13000;图c左侧为SWW,右侧为NEE

采获的冷水珊瑚样品清洗干净后冷藏保存。在室内, 先对样品进行肉眼观察, 然后根据显微镜和扫描电子显微镜观察结果, 鉴定出珊瑚种属。扫描电子显微镜观测和种属鉴定在中国科学院南海海洋研究所完成。为了与全球不同海区冷水珊瑚对比, 确定南海冷水珊瑚与暖水珊瑚、碳酸盐岩存在的差异, 进一步确定冷水珊瑚的地球化学特征, 选择鉴定出的6个特征种、属各1段较为完整的珊瑚骨骼, 粉碎后挑选新鲜碎块, 用玛瑙研钵研磨至小于200目(0.0750mm)粉末后, 进行碳、氧同位素组成测试, 可代表深水珊瑚的碳、氧同位素组成特征。测定在同济大学海洋地质国家重点实验室完成, 相对于V-PDB标准, δ13C的标准偏差为±0.04‰, δ18O的标准偏差为±0.07‰。

2 冷水珊瑚种属及形貌特征

2.1 冷水珊瑚种属

冷水珊瑚主要包括石珊瑚、软珊瑚(包括红珊瑚、柳珊瑚、竹珊瑚等)、黑珊瑚和柱星珊瑚等, 分属于刺细胞动物门的珊瑚虫纲(六射珊瑚亚纲和八放珊瑚亚纲)和水螅纲。某些种属珊瑚既可出现在深水海域, 为冷水珊瑚, 也可生长在热带浅海为暖水珊瑚。
珊瑚骨骼微细结构是鉴定珊瑚种属的重要依据, 通过对珊瑚样品的微细结构的显微镜和扫描电镜观察, 鉴定珊瑚种属。虽然研究的珊瑚骨骼部分石化, 且不完整, 但对比珊瑚图版及其骨骼微细结构描述, 可鉴定出至少2个种和4个属的冷水珊瑚(图2、图3)。2个种分别是Crispatotrochus sp.1和Crispatotrochus sp.2, 4个属分别为Balanophyllia (Balanophyllia)、Balanophyllia (Eupsammia)、Lochmaeotrochus和Enallopsammia, 其中锥形珊瑚属Balanophyllia在南海已有报道(Bassett-Smith, 1890; 邹仁林 等, 1983; 邹仁林, 1988); 而Lochmaeotrochus和Enallopsammia是南海冷泉区新发现的冷水珊瑚属。
Fig. 2 Morphology of cold-water corals found

图2 冷水珊瑚样品外部形貌图

Fig. 3 Scanning Electron Microscopeimages showing the internal structures of cold-water corals found

图 3 冷水珊瑚内部结构扫描电子显微镜图
a和b: Crispatotrochus sp.1, 骨骼表面溶蚀, 珊瑚杯隔片多(>40); c: Crispatotrochus sp.2, 隔壁肋突出, 珊瑚杯小, 隔片少(<40); d和e: Balanophyllia (Balanophyllia), 见有隔壁肋, 轴柱海绵状; f: Balanophyllia (Eupsammia), 常弯曲, 有隔壁肋; 轴柱为海绵状; g和h: Lochmaeotrochus, 杯壁厚且横纹明显, 见表壁和鳞板; i和j: Enallopsammia, 枝状复体, 轴柱乳突状, 隔片规则排列

2.2 冷水珊瑚种属形貌特征

Crispatotrochus sp.1 (疑似Crispatotrochus gregarius Cairns, 2004)
单体, 珊瑚骨骼弯锥状, 固着; 隔壁肋突出; 珊瑚杯大, 隔片多(>40); 无围栅瓣, 轴柱束状。不与虫黄藻共生, 出现在更新世—现代(图3a、3b)。
Crispatotrochus sp.2
单体, 珊瑚骨骼弯锥状, 固着; 隔壁肋突出; 珊瑚杯小, 隔片少(<40); 无围栅瓣, 轴柱束状。不与虫黄藻共生, 出现在更新世—现代(图3c)。
Balanophyllia (Balanophyllia) Wood, 1844
单体, 珊瑚骨骼呈圆锥形, 较直, 单体相连, 有多环基底; 有隔壁肋; 轴柱为海绵状。不与虫黄藻共生, 出现在白垩纪—现代(图3d、3e)。
Balanophyllia (Eupsammia) Milne Edwards and Haime, 1848
单体, 珊瑚骨骼呈弯曲牛角状, 经常弯曲, 单体不相连, 单环基底; 有隔壁肋; 轴柱为海绵状。不与虫黄藻共生, 出现在白垩纪—现代(图f)。
Lochmaeotrochus Alcock, 1902
单体, 但一个连一个, 整体呈灌木丛状; 单体弯锥状到近圆柱筒状; 多环基底; 杯壁厚, 有表壁; 有鳞板, 横纹明显; 轴柱乳突状。不与虫黄藻共生, 仅出现在现代(图3g、3h)。
Enallopsammia Michelotti In Sismonda, 1871
枝状复体; 珊瑚杯壁薄, 外有隔壁肋, 隔片规则排列, 轴柱乳突状。不与虫黄藻共生, 出现在始新世—现代(图3i、3j)。

3 冷水珊瑚碳氧同位素组成

碳酸盐岩碳、氧同位素组成是重要的元素地球化学示踪手段之一, 是沉积和成岩流体信息的重要载体, 可以为认识地质历史时期的地质过程、地球表面的气候过程和海洋环境过程等提供定量依据。形成于不同环境的各类海相碳酸盐岩, 其δ13C和δ18O值亦不相同。自生碳酸盐矿物的碳同位素特征通常反映了其形成环境中溶解CO2的碳同位素组成特点, 因此可利用碳酸盐岩的碳、氧同位素组成来重建地质历史时期海洋的温盐环流特征, 识别地质灾害、判别天然气水合物碳来源(Tong et al, 2013)及揭示海底流体成因(Feng et al, 2015)。
冷水珊瑚是不同于浅水珊瑚的一类珊瑚。浅水珊瑚生活在温暖的浅海水域里, 一般有虫黄藻与之共生进行光合作用, 并将光能转化为浅水珊瑚所需的能量(Cesar et al, 2003), 而冷水珊瑚生活在黑暗的冷水中, 无共生虫黄藻为其提供能量来源, 但可以通过海底牵引底流、烃类渗漏流体作用、海底热液来源的物质获得微体有机物和碎屑(Hovland et al, 2003; Freiwald et al, 2004; Roberts et al, 2006)。由于物质来源和生命效应不同, 冷水珊瑚和浅水珊瑚的骨骼具有不同的碳、氧同位素组成等地球化学特征。因此, 珊瑚骨骼的碳氧同位素组成差异可用于对比不同成因和环境的珊瑚类型。
如图4所示, 测定的珊瑚碎屑的δ13C变化范围-7.36‰~-1.15‰, 平均值为-4.07‰, δ18O变化范围-1.38‰~3.67‰, 平均值为1.06‰, 与大西洋(Blamart et al, 2005)、日本海及周边海域(Shirai et al, 2005)及世界其他不同海域(Thiagarajan et al, 2011)的冷水珊瑚骨骼的碳氧同位素组成相似, 明显不同于西沙群岛中石岛珊瑚礁体碳酸盐岩碳氧同位素组成(张明书 等, 1989);与南海北部现代珊瑚骨骼碳氧同位素组成(柯婷 等, 2015)、表层碳酸盐碳氧同位素组成(李春园 等, 2013)也明显不同, 进一步表明采获的珊瑚碎屑是冷水珊瑚。
Fig. 4 Comparison of the carbon and oxygen isotope compositions of cold-water corals, coral reefs from northern South China Sea and worldwide

图 4 南海北部珊瑚、珊瑚礁及全球冷水珊瑚的碳氧同位素组成
1. 冷水珊瑚(本文); 2. 表层碳酸盐(李春园 等, 2013); 3. 石岛表层碳酸盐岩(张明书 等, 1989); 4. 海南岛南部三亚湾(柯婷 等, 2015); 5. 西琛1井碳酸盐岩(张明书 等, 1989); 6~10. 冷水珊瑚。其中: 6. 北东大西洋(Blamart et al, 2005); 7. 众多海域数据 (Thiagarajan et al, 2011); 8. 日本海及周边海域(Shirai et al, 2005); 9. 锥形海山(Tran et al, 2014); 10. 失落城 (Früh-Green et al, 2003)

由图4还可知, 珊瑚碎屑的碳氧同位素组成(δ13C: -7.36‰~-1.15‰, δ18O: -1.38‰~3.67‰)与马里亚纳橄榄岩化弧锥形海山处碳酸盐岩(δ13C: -2.24‰~-0.11‰, δ18O: 2.58‰~6.71‰)(Tran et al, 2014)不同, 明显不同于低温热液成因碳酸盐岩的碳氧同位素组成(δ13C: 1.4‰~2.4‰, δ18O: 1.7‰~ 4.5‰)(Früh-Green et al, 2003)。由于在该海底未发现海底火山活动和热液流体, 也没有发现海底扩张有关的蛇纹石化证据, 且海底温度与周围海域相同。因此, 推测南海北部冷泉区冷水珊瑚不是在低温热液沉积环境中形成的。
虽然科学家已揭示浅水珊瑚与冷水珊瑚形成环境的差异, 但对冷水珊瑚成因, 仍存在多种不确定性, 存在内因和外因两种观点。内因涉及流体渗流和微生物作用, 外因则强调海底牵引底流作用和古海洋循环。海底流体渗流作用包括地下水、烃类物质特别是甲烷渗漏, 对北大西洋挪威海域的碳酸盐泥丘(Hovland et al, 2003)、爱尔兰西部陆架斜坡上的泥丘启动和生长有至关重要的作用(Naeth et al, 2005), 而海底牵引底流(Huvenne et al, 2003; Wheeler et al, 2005)以及海底地貌(Masson et al, 2002; Wheeler et al, 2007)、陆源营养物质的供应情况(De Mol et al, 2002)是欧洲大陆西部边缘大量大型冷水珊瑚和冷水泥丘形成的控制因素。目前研究更倾向冷水珊瑚和生物礁是底流、海底流体渗漏以及地貌等多种因素综合作用的结果, 如加利西亚(西班牙)沿岸、大西洋西北部伊比利亚半岛边缘(Somoza et al, 2014)。

4 结语

南海北部冷泉区的冷水珊瑚发育在深水底流向西输送的途经海域(图1), 在海底及其周围存在冷泉流体渗漏的多种证据。观测结果表明, 跨越吕宋海峡进入南海的太平洋深层水(或部分)可能在冬季来自南边, 在夏季来自北边(田纪伟 等, 2012), 而从沉积物输运推测的地质时期来自北边太平洋深层水的等深线流, 可将台湾西南部的沉积物沿下陆坡等深线带至东北陆坡形成高速堆积体(Lüdmann et al, 2005; 邵磊 等, 2007)。在此深度, 强劲的水流既给珊瑚虫带来了食物, 也荡击和搬走了沉积碎屑, 不利于沉积物堆积, 但有利于珊瑚生长和礁体发育。冷水珊瑚海底发育泥底辟、气烟囱构造(Wang et al, 2006; 阎贫 等, 2014), 存在甲烷厌氧氧化作用、微生物作用和冷泉生态系统, 是珊瑚生长和珊瑚礁丘发育的有利条件。但没有发现冷泉碳酸盐岩, 采集到生物碳酸盐岩的δ13C为0.71‰~3.49‰, δ18O为-3.76‰~1.55‰, 与海水碳氧同位素组成相似, 表明该碳酸盐岩属于正常海水沉淀的产物(另文讨论)。鉴于冷水珊瑚及冷水丘启动和发育成因的多因素影响, 以及发现冷水珊瑚海区的底流、海底地质的复杂性, 目前对冷水珊瑚的成因, 需要深入研究后才能揭示。但在冷泉区发现冷水珊瑚, 拓展了南海北部海底洋流、冷泉流体的环境效应研究视域。

The authors have declared that no competing interests exist.

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