University:
California State University, Northridge
Course:
GEOL 101 | Geology of Planet Earth
Academic year:

2012
Views:

466

Pages:

28
Author:

Adelyn Pacheco

Surface waves  Earthquakes generate both body waves (P, S) and surface waves  Surface waves are generated along any free surface in the medium  In the Earth, free surfaces exist at the surface and at the core-mantle boundary (CMB). Seismic Waves Traveling through the Oceanic Lithosphere  Surface waves helped us discover the anisotropic properties of olivine in the Earth's mantle lithosphere. Seismic Waves Traveling through the Oceanic Lithosphere  Which waves travel faster ? Why ?  Surface waves traveling parallel to the spreading axis ?  Or surface waves traveling perpendicular to the axis ? Surface waves and Anisotropy in the Oceanic Mantle Surface waves were used to first discover “seismic anisotropy” in the oceans along the Mendocino Fracture Zone by Harry Hess in 1964.  Love waves propagating in the same direction as Rayleigh waves traveled at different speeds!  This was key evidence for the study of anisotropic properties in minerals such as olivine.  Surface Waves in the Earth Love waves: Propagate perpendicular to the direction of travel along the horizontal plane (SH) Rayleigh waves: Also propagate perpendicular to the direction of travel but in the vertical plane (SV) Surface waves During an Earthquake   Because surface waves are the largest amplitude signal on a seismogram, they can amplify displacement where sediment is thick. In the Mexico City earthquake (1985) streets were observed to rise and fall as the surface waves passed, causing great damage from high amplitude displacements. X 10^2 Surface waves on the Seismogram Aleutian Islands P X 10^3 S Mw = 7.9 R Time (s) Surface waves are the largest amplitude signal on the wave train  Surfaces arrive after the P and S waves, because they travel along the surface layers of the Earth where velocities are lower.   Surfaces wave energy (amplitudes) decay with distance as 1 / r  Body wave energy decays as 1 / r2  So at a given distance, which will have more energy ? Propagation of Surface Waves   Rayleigh waves travel in the vertical (z) and radial (x) plane and exhibit a combination of SV and P energy Love waves travel in the horizontal (y) or transverse plane and exhibit SH energy only Propagation of Surface Waves  Rayleigh wave displacement occurs by retrograde elliptical motion  Love waves propagate side-to-side, trapped within a layer Fundamental and Multiple Surface Waves  Because surfaces wave amplitudes are slow to decay, they can travel around the globe many times The R1, R2 (Rayleigh), or G1, G2 (Love) travel paths are shown  Record section of vertical components from the IDA (International Deployment of Accelerometers) network.  Body wave arrivals are early and appear as steeper slopes  Class Notes  Love Waves  Rayleigh Waves Rayleigh Wave Particle Motion  P and Sv amplitudes are out of phase by /2  This results in elliptical motion (retrograde) Evanescent Waves Rayleigh wave amplitudes decay with depth in the Earth and are termed “evanescent”  (Also see Fig 8.3 in your text book) Surface Wave Dispersion Phase velocity (C) travels at a different (slower) speed than the Group velocity (U) envelope.  Surface Wave Dispersion Filtered Seismogram 14 s 15 s 16 s 18 s 20 s 22 s 25 s 29s 33 s 40 s 50 s  Phase velocity (C) travels at a different (slower) speed than The Group velocity (U) envelope. Dispersion Curves Group velocities are slower than phase velocities for both Love waves and Rayleigh Waves  Rapid velocity increase at short periods samples crustal velocities  Slower velocity increase at longer periods samples deeper mantle  GLIMPSE Experiment (Gravity Lineations and Intraplate Melting Petrology and Seismic Expedition ) COOK16/Melville VANC04/Melville November, 2001 November, 2002 Brown University Lamont Doherty Observatory Oregon State University Ocean Bottom Seismometer (OBS) Deployment Coauthors: Donald W. Forsyth1, Yingjie Yang1, Spahr Webb2 1. Brown University, 2. Lamont Doherty Observatory Azimuthal Distribution of Earthquakes and Raypaths * Ideal azimuthal distribution * 155 Earthquakes * 4.5 < Ms < 7.8 18s 33s 59s 100s Raypath density varies from 1565 to 132 paths with increasing period. Rayleigh Wave Dispersion and Sensitivity Sensitivity Kernels Depth (km) 40 s 100 s 16 s Filtered Seismogram 14 s 15 s Juan de Fuca event, Ms 5.5 16 s .δC/δβ 18 s 20 s 22 s 25 s 29s 33 s 40 s 50 s * Seismograms filtered at different periods are sensitive to different depths. * The depth of peak sensitivity increases with period. Phase velocity (km/s) Rayleigh Wave Phase Velocities 20 4 M NF ( y GLIMPSE 4 0– M , 8 19 , NF ( y Period (s) * Lowest phase velocities from 22 – 40 s * Velocities increase steadily 40 – 100 s * Resolution of the base of the LVZ ? 9) 8 19 9) Phase Velocity Maps C (km/s) 2 x Std Err (km/s) * Largest velocity variations are observed at short periods. * Low velocity anomalies observed beneath seamount chains to 67 s period. 1D Shear Wave Velocities in the Oceanic Mantle Starting Model (NF, 1998) * High velocity lithosphere extends to 60 km +/ 20 km. * Steep positive velocity gradient identifies the base of the LVZ at ~110 km. Shear Wave Velocity Structure A A ' A A' B B' Vs (km/s) B B' * High velocity lithosphere and LVZ are well resolved. *Low velocities are observed beneath seamount chains. Distance from EPR (km) *Lithospheric thinning beneath Sojourn ridge. Rayleigh Wave Dispersion and Sensitivity ACTIVITY

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