[논문]표면파 탐사 II: 수동 탐사법을 중심으로

조성오; 정인석; 김빛나래; 장한나; 장성형; 남명진

doi:10.7582/gge.2022.25.1.14

표면파 탐사 II: 수동 탐사법을 중심으로
Surface Wave Method II: Focused on Passive Method 원문보기

지구물리와 물리탐사 = Geophysics and geophysical exploration, v.25 no.1, 2022년, pp.14 - 25

조성오 (국립문화재연구원) , 정인석 (세종대학교 에너지자원공학과) , 김빛나래 (세종대학교 에너지자원공학과) , 장한나 (세종대학교 에너지자원공학과) , 장성형 (한국지질자원연구원) , , 남명진 (세종대학교 에너지자원공학과)

초록
AI-Helper

수동 표면파 탐사는 인공 송신원 없이 생활잡음 또는 자연 발생 소음 등을 송신원으로 이용해 탄성파 신호를 측정한다. 수동 송신원은 낮은 진동수 대역에서 발생하기 때문에 수동 표면파 탐사는 일반적인 능동 탐사법 보다 더 깊은 심도의 지질 정보를 확보할 수 있어 심부 부지 평가 분야에 많이 활용되고 있다. 수동 표면파 탐사 자료는 능동 표면파 탐사 자료 해석과 마찬가지로 자료 획득 후 진동수 분산곡선을 구하여 1차원으로 가정한 속도구조를 해석한다. 하지만 수동 표면파 탐사 자료는 송신원이 무작위로 발생한다는 특성 때문에 여러 수신기에서 측정된 신호들의 공간자기상관을(spatial autocorrelation) 이용해 수신 자료들의 일관성(coherence) 곡선을 구하고 이로부터 분산곡선을 구하게 된다. 이 기술보고에서는 수동 표면파 탐사 이론, 탐사 방법, 자료처리 기법을 살펴보고 실제 적용 사례를 분석한다.

Abstract ▼ AI-Helper

The passive surface wave method measures seismic signals from ambient noises or vibrations of natural phenomena without using an artificial source. Since passive sources are usually in lower frequencies than artificial ones being able to ensure the information on deeper geological structures, the passive surface wave method can investigate deeper geological structures. In the passive method, frequency dispersion curves are obtained after data acquisition, and the dispersion curves are analyzed by assuming 1D-layered earth, which is like the method of active surface wave survey. However, when computing dispersion curves, the passive method first obtains and analyzes coherence curves of received signals from a set of receivers based on spatial autocorrelation. In this review, we explain how passive surface wave methods measure signals, and make data processing and interpretation, before analyzing field application cases.

주제어

표/그림 (12)

그림 Fig. 1. Schematic diagram of two receivers located in a straight line. It is arranged at a certain separation distance in the same direction as the traveling direction of the plane wave.
그림 Fig. 2. (a) Signals measured at both receivers in Fig. 1 and (b) 2 Hz, (c) 25 Hz, (d) 50 Hz, (e) 75 Hz, (f) 100 Hz signal schematic diagrams obtained through Fourier transform.
그림 Fig. 3. A schematic diagram of the receivers arranged on a plane with a certain distance from the center receiver.
그림 Fig. 4. When the center receiver-receiver pair is arranged along the traveling direction of the plane wave (a), the calculated coherence curve (b), when the traveling direction of the plane wave and the center receiver-receiver pair are arranged in parallel (c), the calculated coherence curve (d), when a center receiver-receiver pair is arranged at any position between (a) and (c) ~ (e), the calculated coherence curve (f).
그림 Fig. 6. Principle of reflected-wave interferometry.
그림 Fig. 5. (a) The receivers arranged along a concentric circle with respect to the center receiver and (b) the coherence curve of waves traveling in one direction.
그림 Fig. 7. Schematic diagram of reconstruction of surface waves generated by (a) correlation-type interferometry and (b) convolution-type interferometry, respectively.
그림 Fig. 8. (a) The passive seismic method array shape and (b) The L-shape array detail.
표 Table 1. The natural and composition of the seismic noise-field (Setiawan et al., 2016)
그림 Fig. 9. Passive data processing with f-k beamforming technique. (a) Raw data in the time-distance domain, (b) data in the time-distance domain filtered around frequency f, (c) schematic representation of plane wave propagation through the array, (d) energy repartition in the plane of wavenumbers at frequency f, (e) dispersion image. Colours range from orange (low amplitude) to green, blue and purple (high amplitude) (Foti et al., 2018).
그림 Fig. 10. SWV profiles from SPAC microtremor surveys in the Melbourne area. (Roberts et al., 2004).
그림 Fig. 11. Comparison between the SASW (Blue) and SPAC(Black) results for 3 sites in Tangshan city (Kayen et al., 2008).

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