Research progress on detection of carbon leakage by ocean bottom seismometer
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摘要: 海底碳封存是解决全球温室效应，提高碳汇的重要手段. 然而，海底碳封存会存在碳泄漏的风险，因此有必要对碳储层结构和海底碳泄漏进行监测. 其中，一种有效的监测手段是海底地震仪（OBS）多波多分量地震探测. 本文介绍了使用OBS探测技术对储层结构和海底地壳内流体的探测实例：主要包括二维、三维台阵OBS试验，使用的方法为走时反演、各向异性分析以及微地震方法. 使用OBS进行多波多分量地震探测有范围广、深度大、信噪比高、大偏移距的优点. 然而，目前二维和三维OBS探测建立的碳储层和碳泄漏模型分辨率还有待提高，可以通过使用密集台阵的方式来提高观测精度，或布设更优化的台阵来获得最佳分辨率. 随着碳中和目标的不断临近，各国碳封存的需求迫在眉睫. 因此，尽快发展OBS海底碳泄漏监测技术，保证碳封存方案的实施是尤为必要的.Abstract: Marine carbon geological storage is an important strategy to slow the global warming. However, Marine carbon geological storage may pose a risk of carbon leakage, so it is necessary to monitor the carbon storage structure and seafloor carbon leakage. One of the effective monitoring means is ocean bottom seismometers （OBS） multi-wave component seismic detection. This paper presents an example of reservoir structures and fluids within the seafloor crust using OBS detection technology. The content mainly includes two-dimensional and three-dimensional array OBS experiments, and the methods include traveltime inversion, anisotropy analysis and microseismic methods. OBS multi-component seismic detection has the advantages of wide range, large depth, high signal-to-noise ratio, and large offset. However, there is still room to improve the resolution of reservoir and leakage models established by 2D and 3D OBS inspections. The observation accuracy can be improved by using a dense array, or a more reasonable array method can be used to obtain the best resolution. As the goal of carbon neutrality draws nearer, the need for carbon sequestration in countries is imminent. Therefore, it is particularly necessary to develop OBS seabed carbon leakage monitoring technology as soon as possible to ensure the implementation of carbon sequestration programs.
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图 4 斯瓦尔巴特群岛西部陆缘天然气水合物探测主要结果
（a） N3目标区P波和S波二维速度结构剖面；（b−f） N1，N2，N3，S1及S2目标区的P波和S波一维速度结构（Chabert et al，2011）
Figure 4. Main results of natural gas hydrate detection in the western Marginal area of the Svalbard Islands
（a） Two-dimensional velocity structure profiles of P-wave and S-wave in N3 target area；（b−f） One-dimensional velocity structures of P-wave and S-wave in N1，N2，N3，S1 and S2 target areas （Chabert et al， 2011）
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图 1 墨西哥湾Holstein油田开发延时地震监测应用
（a） 2001年首次地震探测获得的含油气储层地震振幅切片，图中白线为起始的油水接触界面，红色区域为含油区，蓝色区域为 含水区；（b） 2006年第二次地震探测获得的含油气储层地震振幅切片，橙色线为新的油水接触界面（van Gestel et al，2008）。
Figure 1. Real-time delay seismic monitoring of Holstein oil field development in the Gulf of Mexico
（a） Seismic amplitude slice of oil and gas reservoir obtained by the first seismic detection in 2001，the white line in the figure is the initial oil-water contact interface，the red area is the oil-bearing area，and the blue area is the water-bearing area；（b） Seismic amplitude slice of oil and gas reservoir obtained by the second seismic detection in 2006，the orange line is the new oil-water contact interface （van Gestel et al，2008）
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图 2 挪威北海Valhall油田永久式海底电缆长期观测结果
（a） Valhall油田海底电缆分布示意及LoFS1与LoFS6，LoFS8，LoFS10地震观测振幅差异；（b） 第一次观测LoFS1与LoFS2，LoFS3， LoFS4和LoFS5地震观测双程走时差异（van Gestel et al，2008）
Figure 2. Long-term observation of permanent seabed cable in Valhall oil field in the North Sea of Norway
（a） Schematic diagram of subsea cable distribution of Valhall oilfield and amplitude difference of seismic observation of LoFS1 and LoFS6，LoFS8，LoFS10；（b） Double travel time difference of seismic observation of LoFS1 and LoFS2，LoFS3，LoFS4 and LoFS5 for the first obser vation LoFS1（van Gestel et al， 2008）
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图 3 在全球开展的海底碳储层及流体调查分布图
（a） 斯瓦尔巴特群岛西部陆缘麻坑构造电磁和OBS联合探测（Goswami et al，2015）；（b） 挪威Nyegga麻坑构造OBS探测（Plaza-Faverola et al，2008）；（c） STEMM-CCS计划，在北海分析了一个麻坑构造中独特的主动源地震各向异性（Bayrakci et al，2021）；（d） 尼日尔河三角洲天然气水合物微地震探测（Sultan et al，2011）；（e） 斯瓦尔巴特群岛西部陆缘天然气水合物探测（Chabert et al，2011）；（f） 2009年广州海洋地质调查局南海北部陆坡天然气水合物地震调查（沙志彬等，2014）
Figure 3. A global distribution map of seabed carbon reservoir and fluid surveys
（a） Electromagnetic and OBS joint exploration of pockmark structure on the western margin of Svalbard Islands （Goswami et al， 2015）；（b） OBS exploration of Nyegga pockmark structure in Norway （Plaza-Faverola et al，2008）；（c） STEMM-CCS project，analyzing the unique active source seismic anisotropy in a pockmark structure in the North Sea （Bayrakci et al，2021）；（d） Microseismic exploration of natural gas hydrate in Niger Delta （Sultan et al，2011）；（e） Natural gas hydrate exploration on the western margin of Svalbard Islands （Chabert et al，2011）；（f） Seismic survey of natural gas hydrate on the northern slope of the South China Sea by Guangzhou Marine Geological Survey Bureau in 2009 （Sha et al，2014）
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图 5 挪威Nyegga麻坑五个OBS台站的P波速度模型
浅绿色区域表示低速带区域，在所有模型中都存在最浅低速区，而最深的低速区只出现在3H，1Z和6H中（Plaza-Faverola et al，2010）
Figure 5. P-wave velocity models of five OBS stations in Nyegga pockmark，Norway
The light green area indicates the low-velocity zone， All models have the shallowest low-velocity zone （LVZ1），and the deepest low-velocity zone （LVZ2） only appears in 3H，1Z and 6H （Plaza-Faverola et al，2010）
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图 6 尼日尔河三角洲OBS试验中部分OBS台站记录到的脉冲信号（Sultan et al，2011）
Figure 6. Pulse signals recorded by some OBS stations during the OBS trial in the Niger River Delta （Sultan et al，2011）
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图 7 斯瓦尔巴特群岛西部陆缘麻坑构造电磁和OBS联合探测
（a） OBS8下方P波速度结构，黑色实线表示OBS下方的一维P波速度，虚线表示在N3目标区的一维P波速度结构（Chabert et al，2011），绿色实线表示陆地沉积物标准P波速度结构（Goswami et al，2015）；（b−c） OBS8和OBS5的地震记录，数据采用角频率分别为10，20，250和300 Hz的梯形带通滤波器进行滤波，红色圆圈为到时；（d） OBS8和OBS5的反演速度模型；（e） 地震反射数据与图（d） 叠加出的低速带
Figure 7. Electromagnetic and OBS joint exploration of pockmark structures at the western margin of Svalbard Island
（a） P-wave velocity structure below OBS8，black solid line represents the one-dimensional P-wave velocity below OBS，dashed line represents the one-dimensional P-wave velocity structure in the N3 target area by Chabert et al （2011），green solid line represents the standard P-wave velocity structure of terrestrial sediments （Goswami et al，2015）；（b-c） Seismic records of OBS8 and OBS5 respectively，the data are filtered with a trapezoidal band-pass filter with angular frequencies of 10，20，250 and 300 Hz respectively，red circles indicate arrival times；（d） Inverted velocity models of OBS8 and OBS5；(e) A low velocity zone reflected by seismic reflection data superimposed on fig.(d)
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图 8 欧盟STEMM-CCS在挪威北海研究甲烷储层泄漏的各向异性试验
（a） OBS1和（b） OBS8径向分量和切向分量地震记录，左图红色箭头表示径向地震图上c波相位的到达时间，红线表示由于振铃而导致的事件观测幅度最高的时间，右图中红色箭头表示在90°间隔时的极性变化；（c） Scanner麻坑水平应力分布，蓝色箭头表示区域水平应力最大值（σ1）和最小值（σ3），黄色箭头表示由高孔隙流体压力引起的局部应力条件，红色虚线表示观察到的气体的方向；（d） 麻坑下方不同界面气体聚集（红色区域）分布（Bayrakci et al，2021）
Figure 8. EU STEMM-CCS anisotropy experiment on methane reservoir leakage in the North Sea of Norway
Radial and tangential component seismic records of OBS1 (a) and OBS8 (b)，the red arrow in the left figure indicate the arrival time of the c-wave phase on the radial seismic map，the red line indicates the time when the event observation amplitude is highest due to ringing，and the red arrow in the right figure indicate the polarity change at 90° intervals；（c） Scanner pockmark horizontal stress distribution map， blue arrow indicates regional maximum （σ1） and minimum （σ3） horizontal stress，yellow arrow indicates local stress conditions caused by high porosity fluid pressure，red dashed line indicates the direction of gas observed in the middle；（d） Gas accumulation distribution at different interfaces below the pockmark， indicated in red （Bayrakci et al，2021）
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图 9 中国南海北部大陆坡地震反射数据及纵横波速度结构反演效果图（沙志彬等，2014）
Figure 9. Inversion effect of seismic reflection data and P-wave and S-wave velocity structure on the northern continental slope of the South China Sea （Sha et al，2014）
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图 10 不同深度海底碳储层及泄漏特征示意图
Figure 10. Schematic diagram of seabed carbon reservoir and leakage characteristics at different depths
表 1 流体探测常用地震方法的特点
Table 1 Characteristics of commonly used seismic methods for fluid detection
研究方法 震源类型 特点和作用 二维/三维反射地震方法 人工震源 分辨率较高，探测地下结构性质和内部结构 延时地震 人工震源 评估地下流体随时间变化特征，推测流体运移特征 地震层析成像 人工震源和天然地震 分辨率较低，可确定地下构造及周边环境纵、横波速度结构 剪切波分裂 人工震源和天然地震 使用P/S转换波 地震衰减 人工震源和天然地震 地震衰减的各向异性，需使用不同频率的震源来区分地下结构的性质 微地震方法 天然地震 使用微地震作为被动震源，可以获得断裂构造的活动性和空间展布 
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表 2 使用OBS进行海底碳储层及泄漏探测实例
Table 2 Examples of submarine carbon reservoir and leakage detection using OBS
时间 探测区域 研究方法 来源 2008 北极地区，斯瓦尔巴特群岛
西部大陆边缘二维台阵与三维台阵结合：南部选择两个目标区分别布设四
台和三台OBS；北部则选择一条线上三个目标区，每个目标
区布设两台OBS，使用射线追踪对五个目标区进行正演模拟Plaza-Faverola等（2008） 2009 挪威中部边缘，Nyegga麻坑 布设二维台阵，两条测线分别沿线布设2台和3台OBS，
通过走时反演得到P波速度模型Chabert等（2011） 2011 尼日尔河三角洲东部边界 断层周围布设OBS以监测微地震活动性，微地震事件信号由
三分量检波器监测，水中较大振幅事件由水听器监测Sultan等（2011） 2012 中国南海北部大陆坡 使用20台OBS布设三维台阵，走时反演得到纵横波速度模型，
建立反射剖面和层位模型沙志彬等（2014） 2015 斯瓦尔巴特群岛西部
边缘Vestnesa脊布设两台OBS，使用走时反演方法得到P波速度模型 Goswami等（2015） 2021 挪威北海麻坑 布设三维台阵，横向剪切波分裂方法、地震衰减方法及微地震
方法研究麻坑构造下各向异性Bayrakci等（2021）
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