Seismic monitoring of typhoons based on seismology
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摘要: 台风是全球最具破坏力的气象灾害之一，由于台风过境时现场海洋观测资料相对匮乏，与目前对台风的监测、预报和防灾减灾的迫切需求尚不相匹配。近年来，利用地震学观测资料与技术手段，通过台风激发的地震背景噪声，对台风进行监测的新方法逐渐兴起。本文对近年来有关台风激发地震背景噪声机理、源区分布以及基于地震背景噪声的台风定位追踪、海浪参数反演等研究进展进行综述，分析已取得的研究成果及可能存在的问题，讨论并展望基于地震学的台风监测研究思路与热点。基于地震学的台风监测有望为传统台风观测与研究提供跨学科的观测资料与技术支持。Abstract: Typhoons are one of the most destructive meteorological disasters all over the world. However, because of the lack of in situ observations under such extreme weather conditions during the typhoon’s passage, typhoon monitoring and forecasting are still not able to meet the needs of typhoon prevention and mitigation. In recent years, a new method of typhoon monitoring based on seismological observations and techniques has emerged and developed, utilizing typhoon-generated seismic noise as a proxy. This paper reviews the recent progress in study of typhoon-induced microseisms, including the generation mechanisms, source location distribution, and its potential implications on typhoon monitoring and ocean wave parameter inversion. Future prospects on seismic monitoring of typhoons are provided and discussed. This newly emerging method may provide interdisciplinary support to traditional observation and investigation of typhoons.
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Keywords:
- typhoon /
- ambient seismic noise /
- microseisms /
- seismic array /
- beamforming
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图 6 利用NECESSArray台阵对西北太平洋台风“卢碧”激发P波地脉动源区聚束定位（引自Lin et al，2018a）
Figure 6. Bunching located source of Lupit-generated P-wave microseisms using the NECESSArray in northwestern Pacific （modified from Lin et al，2018a）
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图 1 西北太平洋1980—2021年台风年频次分布（数据源于Japan Meteorological Agency，2022）
Figure 1. Annual distribution of typhoons in the period of 1980−2021 over the northwestern Pacific （Data from Japan Meteorological Agency，2022）
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图 2 台风激发地震背景噪声能量谱示意图
图中标注出了不同频段的激发源对应的作用力，其中ER，EL，EP，ESV和ESH分别表示瑞雷波、勒夫波、P波、SV波和SH波的能量（修改自Nishida，2017）。
Figure 2. Schematic power spectrum of typhoon-generated seismic ambient noise
The excitation sources of different period bins are labeled，ER，EL，EP，ESV and ESH represent energy of Rayleigh，Love，P，SV and SH waves，respectively （modified from Nishida，2017）
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图 3 台风“伊欧凯”激发第二类地脉动源区数值模拟结果（引自Farra et al，2016）
热力图表征数值模拟第二类地脉动源区能量强度的空间分布；灰色线表示台风轨迹；红色等值线表示定位区域；红色叉表示定位源区峰值点
Figure 3. Numerical simulation results of secondary microseisms sources, generated by typhoon “Ioke” （from Farra et al，2016）
Thermodynamic diagram shows the spatial distribution of secondary microseisms power；the gray line represents the typhoon track；the red isoline shows the located area；the red crosses show peak point of the located source
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图 4 台风移动过程中前后不同时刻引起的海浪相互作用而激发第二类地脉动示意图
西南象限中灰色椭圆表示两个时刻产生的涌浪通过波-波相互作用而激发第二类地脉动的可能源区位置（修改自Lin et al，2017）
Figure 4. Schematic secondary microseisms generated by the interaction waves at different times during the moving process of typhoon
The gray ellipse in the southwestern quadrant represents the possible source of secondary microseisms generated by two swells through wave-wave interaction （modified from Lin et al，2017）
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图 5 频率域反投影聚束法原理示意图（修改自IRIS DMC，2011）
当震源位于特定搜索格点时，基于该格点至台阵走时的聚束能量最强
Figure 5. Schematic back projection bunching method in frequency domain （modified from IRIS DMC，2011）
The bunching energy based on the travel time from the grid to the array is the strongest when the source is located in a specific search grid
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图 7 基于YULB单地震台站观测数据反演估计的t2时刻涌浪源区可能位置（虚线圆）与ERA5再分析数据集中t1时刻总涌浪有效波高（左）和最大波周期（右）的对比（引自Lin et al，2018b）
Figure 7. Comparison of the possible position （dotted circle） of swell source at time t2 estimated from inversion of the observation data at the station YULB with the significant heights of total swells （left panels） and peak wave periods （right panels） at time t1 in ERA5 reanalysis data set （after Lin et al，2018b）
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图 8 基于地脉动的海浪波高反演结果与浮标观测结果对比
（a） 试验海域及地震台站、浮标分布图；（b） 浮标实测有效波高与反演所得有效波高估计值的对比（引自Ferretti et al，2018）
Figure 8. Comparison between inversion results of wave height based on microseisms and buoy observation
（a） Distribution of test sea，seismic stations and buoys；（b） Comparison between the measured significant wave heights of buoy and the estimated significant wave heights from inversion （after Ferretti et al，2018）
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