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Sacks, IS, Evertson D, Dorman LM.  1971.  Borehole strainmeters. Year Book - Carnegie Institution of Washington. 69:426-430., Washington, DC, United States (USA): Carnegie Institution of Washington, Washington, DCWebsite
Sauter, AM, Dorman LM.  1986.  Instrument Calibration of Ocean Bottom Seismographs. Marine Geophysical Researches. 8:265-275.   10.1007/bf00305486   Website
Sauter, AW, Dorman LM, Schreiner AE.  1986.  A study of sea floor structure using ocean bottom shots and receivers. ( Akal T, Berkson JM, Eds.)., New York, NY, United States (USA): Plenum Press, New York, NYWebsite
Schiffelbein, P, Dorman L.  1986.  Spectral Effects of Time-Depth Nonlinearities in Deep-Sea Sediment Records - a Demodulation Technique for Realigning Time and Depth Scales. Journal of Geophysical Research-Solid Earth and Planets. 91:3821-3835.   10.1029/JB091iB03p03821   Website
Schreiner, AE, Dorman LM.  1990.  Coherence Lengths of Sea-Floor Noise - Effect of Ocean Bottom Structure. Journal of the Acoustical Society of America. 88:1503-1514.   10.1121/1.400307   Website
Schreiner, AE, Dorman LM, Bibee LD.  1991.  Shear wave velocity structure from interface at two deep sites in the Pacific Ocean. Shera waves in marine sediments. ( Hovem JM, Richardson MD, Stoll RD, Eds.).:231-238., Holland: Kluwer academic publishers
Shen, Y, Forsyth DW, Conder J, Dorman LM.  1997.  Investigation of microearthquake activity following an intraplate teleseismic swarm on the west flank of the Southern East Pacific Rise. Journal of Geophysical Research-Solid Earth. 102:459-475.   10.1029/96jb02852   AbstractWebsite

Between February 1991 and May 1992, 33 intraplate earthquakes having body wave magnitudes between 4.3 and 6.0 were located on the west flank of the Southern East Pacific Rise by the International Seismological Center. Seven months after the last teleseismic event we deployed four ocean bottom seismometers at the site of the teleseismic swarm. One hundred and ninety-two microearthquakes were located using P and S travel times of events recorded by three or more instruments during the 16-day deployment. Most of the microearthquakes were in a band about 30 km long and 6 km wide between and parallel to seamount chains. In addition, several events were distributed along a line perpendicular to the main seismicity band and parallel to the ridge axis. The focal depths of the microearthquakes range from 1 to 15 km, and most are between 5 and 12 km, similar to the depth range of the teleseismic events [Hung and Forsyth, 1996]. The composite P wave polarities indicate that the microearthquakes had a variety of focal mechanisms. We developed a new grid-search, inversion technique that utilizes the P wave polarities and the empirically corrected ratios of P and S wave amplitudes to find the focal mechanisms of individual events. Within the acceptable travel time and amplitude misfits, focal solutions are fairly stable. Normal faulting is found in the ridge-parallel seismicity line. The thrust and strike-slip faulting in the main seismicity band is distinctly different from the exclusively normal faulting mechanisms of the teleseismic events. There is no apparent depth dependence of fault types. None of the existing models of the sources of stress (ridge push, thermoelastic stresses; loading by local topographic features, caldera collapse, and north-south extension of the Pacific Plate) provides a satisfactory explanation for both the teleseismic swarm and microearthquakes. We propose a pew tectonic scenario. In this scenario, the lithosphere is prestressed by the cooling of the plate. Magma rising from the deeper mantle induces normal faulting ahead of the dike tips in the lower lithosphere, which is already under extensional, thermal stress, producing the larger, teleseismically detected events. Once the dikes propagate into the lithosphere, the region surrounding the dikes behind the tips is compressed by the overpressure of magma. Depending on the geometry of the dikes, the local orientations of the minimum principal stress, and the local weaknesses in the lithosphere, thrust or strike-slip faulting (the microearthquakes) may occur.

Smith, GP, Wiens DA, Fischer KM, Dorman LM, Webb SC, Hildebrand JA.  2001.  A complex pattern of mantle flow in the Lau backarc. Science. 292:713-716.   10.1126/science.1058763   AbstractWebsite

Shear-wave splitting analysis of Local events recorded on Land and on the ocean floor in the Tonga are acid Lau backarc indicate a complex pattern of azimuthal anisotropy that cannot be explained by mantle flow coupled to the downgoing plate. These observations suggest that the direction of mantle flow rotates from convergence-parallel in the Fiji plateau to north-south beneath the Lau basin and are-parallel beneath the Tonga are. These results correlate with helium isotopes that map mantle flow of the Samoan plume into the Lau basin through an opening tear in the Pacific plate.