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  • 1
    Monograph available for loan
    Monograph available for loan
    Bergen, Norway : Inst. of Solid Earth Physics, Univ. of Bergen
    Call number: M 15.0171
    Type of Medium: Monograph available for loan
    Pages: v, 245 S. : graph. Darst.
    Edition: Version 8.0 preliminary
    Location: Upper compact magazine
    Branch Library: GFZ Library
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  • 2
    Monograph available for loan
    Monograph available for loan
    Bergen, Norway : Inst. of Solid Earth Physics, Univ. of Bergen
    Call number: M 04.0256
    Type of Medium: Monograph available for loan
    Pages: iv, 255 S.
    Edition: Version 7.2
    Classification:
    Seismology
    Location: Upper compact magazine
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  • 3
    Call number: M 12.0097
    Description / Table of Contents: Contents: 1. Introduction. 1.1. Earthquakes. 1.2. Recording seismic events and picking phases. 1.3. Locating earthquakes. 1.4. Magnitude. 1.5. Fault plane solution. 1.6. Further data analysis. 1.7. Software. 2. Earth structure and seismic phases. 2.1. Earth structure. 2.2. Seismic rays. 2.3. Seismic phases.2. 4. Travel times.2.5. Seismic phases at different distances.2.6. Determination of structure.2.7. Exercises.3. Instruments and waveform data.3.1. Seismic sensors.3.2. Seismic recorders.3.3. Correction for instrument response.3.4. Formats.3.5. Seismic noise.3.6. Exercises.4. Signal processing.4.1. Filtering.4. 2. Spectral analysis and instrument correction. 4.3. Reading seismic phases. 4. 4. Correlation.4.5. Particle motion and component rotation.4.6. Resampling. 4.7. Software.4.8. Exercises.5. Location.5.1. Single station location. 5.2. Multiple station location.5.3. Computer implementation.5.4. Error quantification and statistics. 5.5 Relative lovation methods. 5.6. Practical considerations in earthquake locations. 5.7. Software. 5.8. Exercises. 6. Magnitude. 6.1. Amplitude and period measurements. 6.2. Local magnitude ML . 6.3. Coda magnitude Mc. 6.4. Body wave magnitude mb. 6.5. Broad band body wave magnitude mB. 6.6. Surface wave magnitude Ms. 6.7. Broad band surface wave magnitude MS. 6.8. Lg -- wave magnitude. 6.9. Moment magnitude MW. 6.10. Energy magnitude Me. 6.11. Comparison of magnitude scales. 6.12. Summary. 6.13. Average magnitude and station corrections. 6.14. Adjusting magnitude scales to local or regional conditions. 6.15. Exercises. 7. Focal mechanism and seismogram modeling. 7.1. Fault geometry. 7.2. Source radiation. 7.3. Fault plane solution in practice. 7.4. Obtaining polarity. 7.5. Fault plane solution using local data and polarity. 7.6. Composite fault plane solution. 7.7. Fault plane solution using global data. 7.8. Fault plane solution using amplitudes. 7.9 Moment tensor. 7.10. Moment tensor inversion. 7.11. Seismogram modeling. 7.12. Software. 7.13. Exercises. 8. Spectral analysis. 8.1. Attenuation. 8.2. Seismic source model. 8.3. Geometrical spreading. 8.4. Self similarity and seismic source spectra. 8.5. Determination of Q. 8.6. Soil amplification. 8.7. Exercises. 9. Array processing. 9.1. Basic array parameters. 9.2. Beam forming. 9.3. Frequency -- wavenumber analysis (fk). 9.4. Array response. 9.5. Processing software. 9.6. Using array measurements for identifying phases. 9.7. Exercises. 10. Operation. 10.1. Data and data storage. 10.2. Routine processing. 10.3. Data exchange. 10.4. Earthquake statistics. 10.5. Software. 10.6. Exercises.
    Type of Medium: Monograph available for loan
    Pages: xi, 347 S.
    ISBN: 9789048186969 , 9789048186976
    Classification:
    Seismology
    Location: Upper compact magazine
    Branch Library: GFZ Library
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  • 4
    Publication Date: 2012-03-01
    Description: INTRODUCTION The Mw = 7.2 El Mayor-Cucapah earthquake occurred on 4 April 2010 in northern Baja California, about 48 km south of the border between Mexico and the United States at shallow depth along the plate boundary between the North American and Pacific plates. This earthquake was felt in the states of Baja California and Sonora, Mexico, and in southern California and Arizona in the United States. The continental plate boundary in northern Baja California consists of a series of strike-slip faults oriented in the NW-SE direction that are separated by pull-apart basins (Figure 1). The Pacific plate has a convergence rate of 4.8 cm/yr with respect to North America (DeMets et al. 1994). Southern California and the northern part of Baja California form a common region affected by a number of regional-scale active faults that are part of a complex lateral system (Goff et al. 1987). The main faults in the epicentral and adjacent areas are the Imperial fault, the Cerro Prieto fault, and the Laguna Salada fault system. The Imperial fault has a length of 75 km and its orientation is N42°W. This fault has generated major earthquakes like the 18 May 1940, El Centro, California earthquake (M = 7.1) and the 15 October 1979, Imperial Valley, Mexico earthquake (M = 6.6). The relative motion of the Imperial fault with respect to North America (NA) is 4.7 cm/yr (Frez and González 1991). The length of the dextral fault of Cerro Prieto is about 80 km with a 5.0 cm/yr relative motion on the fault with respect to NA. Major earthquakes have also taken place on the Cerro Prieto fault in 1852, 1875, and...
    Print ISSN: 0895-0695
    Electronic ISSN: 1938-2057
    Topics: Geosciences
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  • 5
    Publication Date: 2018-04-01
    Description: The Western Hellenic Subduction Zone is characterized by a transition from oceanic to continental subduction. In the southern oceanic portion of the system, abundant seismicity reaches depths of 100 km to 190 km, while the northern continental portion rarely exhibits deep earthquakes. Our study investigates how this oceanic-continental transition affects fluid release and related seismicity along strike. We present results from local earthquake tomography and double-difference relocation in conjunction with published images based on scattered teleseismic waves. Our tomographic images recover both subducting oceanic and continental crusts as low-velocity layers on top of high-velocity mantle. Although the northern and southern trenches are offset along the Kephalonia Transform Fault, continental and oceanic subducting crusts appear to align at depth. This suggests a smooth transition between slab retreat in the south and slab convergence in the north. Relocated hypocenters outline a single-planed Wadati-Benioff Zone with significant along-strike variability in the south. Seismicity terminates abruptly north of the Kephalonia Transform Fault, likely reflecting the transition from oceanic to continental subducted crust. Near 90 km depth, the low-velocity signature of the subducting crust fades out and the Wadati-Benioff Zone thins and steepens, marking the outline of the basalt-eclogite transition. Subarc melting of the mantle is only observed in the southernmost sector of the oceanic subduction, below the volcanic part of the arc. Beneath the nonvolcanic part, the overriding crust appears to have undergone large-scale silica enrichment. This enrichment is observed as an anomalously low Vp/Vs ratio and requires massive transport of dehydration-derived fluids updip through the subducting crust. ©2018. The Authors.
    Print ISSN: 2169-9313
    Electronic ISSN: 2169-9356
    Topics: Geosciences , Physics
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  • 6
  • 7
    Publication Date: 2020-05-27
    Description: Ocean-bottom seismographs (OBSs) are used to obtain seismic recordings offshore and are an increasingly important tool for investigating the globe. However, because OBS data cannot be time stamped using Global Positioning System (GPS) during deployment, correction for drift of the internal clock is required. This time drift is typically derived by synchronizing the clock before and after deployment. Linear correction is then applied using the timing deviation between GPS and the instrument’s internal clock at recovery, that is, the skew measurement. If synchronization measurements are missing, ambient noise cross-correlation functions (CCFs) are commonly used for time correction. When investigating recordings from a small-scale OBS network located on the Mohn’s mid-ocean ridge, we observed a remaining drift on the skew-corrected data. After recalculating the drift of the raw data using CCFs, we found that the skew-based time correction was incorrect. This was also verified with the observation of teleseismic P-wave arrivals. We describe a method to obtain properly time-corrected data and discuss the OBS timing issues in detail. The results shown were obtained using a software package that we developed for this specific purpose and made available as open-source software. Although we cannot explain the technical reason for the failure of skew correction, this study shows that skew corrections should not be trusted alone, and OBS timing should always be verified by either ambient noise correlations or P-wave arrival times.
    Print ISSN: 0895-0695
    Electronic ISSN: 1938-2057
    Topics: Geosciences
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  • 8
    Publication Date: 2020-08-11
    Description: We present a regional short-period Sn magnitude scale mb(Sn) for small earthquakes along the northern Mid-Atlantic Ridge. Surface-wave magnitudes, teleseismic body-wave magnitudes, and seismic moments cannot be reliably determined for small earthquakes along this and other midocean ridges. Local magnitudes that rely on Lg waves are likewise not generally useful due to the substantial oceanic paths for earthquakes along midocean ridges. In contrast, Pn and Sn arrivals for earthquakes along the northern Mid-Atlantic Ridge are generally well recorded by the existing seismographic networks, and, in fact, Sn arrivals are larger than Pn arrivals for about one-third of the ridge events. For this reason, we have developed a new regional Sn magnitude scale that is tied to Mw, so that seismic moments can be readily approximated. In our least-squares fit of peak amplitudes from 120 earthquakes having a published moment magnitude, we solved for the attenuation curve for paths in the oceanic mantle lid, for event magnitude adjustments (EMAs) to account for differences between long-period moment magnitude Mw and short-period Sn magnitude, and for station corrections. We find regional EMAs that are well correlated with the style of faulting: they are positive for normal-faulting earthquakes along spreading ridges and negative for strike-slip earthquakes along transform faults. These source-specific EMAs are approximately +0.11 magnitude units for normal-fault earthquakes and −0.26 magnitude units for strike-slip earthquakes on transform faults, and are consistent with previously reported apparent stresses from these regions. The amplitude distance curve determined for Sn for the northern Atlantic Ocean is similar to that determined for Pn in the northern Atlantic out to a distance of about 500 km, but at larger distances is more similar to the western U.S. Pn curve, likely reflective of the warmer temperatures at greater upper-mantle depths.
    Print ISSN: 0037-1106
    Electronic ISSN: 1943-3573
    Topics: Geosciences , Physics
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  • 9
    Publication Date: 2020-01-21
    Description: The Mw 4.5 southern Viking graben earthquake on 30 June 2017 was one of the largest seismic events in the Norwegian part of the North Sea during the last century. It was well recorded on surrounding broadband seismic stations at regional distances, and it generated high signal-to-noise ratio teleseismic P arrivals at up to 90° with good azimuthal coverage. Here, the teleseismic signals provide a unique opportunity to constrain the event hypocenter. Depth phases are visible globally and indicate a surface reflection in the P-wave coda some 4 s after the initial P arrival, giving a much better depth constraint than regional S-P time differences provide. Moment tensor inversion results in a reverse thrust faulting mechanism. The fit between synthetic and observed surface waves at regional distances is improved by including a sedimentary layer. Synthetic teleseismic waveforms generated based on the moment tensor solution, and a near-source 1D velocity model indicates a depth of 7 km. Correlation detectors using the S-wave coda from the main event were run on almost 30 yr of continuous multichannel seismic data searching for repeating signals. In addition to a magnitude 1.9 aftershock 33 min later, and a few magnitude ∼1 events in the following days, a magnitude 2.5 earthquake on 13 November 2016 was the only event found to match the 30 June 2017 event well. Using double-difference techniques, we find that the two largest events are located within 1 km of the main event. We present a Bayesloc probabilistic multiple event location including the 30 June event and all additional seismic events in the region well recorded on the regional networks. The Bayesloc relocation gave a more consistent seismicity pattern and moved several of the events more toward the west. The results of this study are also discussed within the regional seismotectonic frame of reference.
    Print ISSN: 0037-1106
    Electronic ISSN: 1943-3573
    Topics: Geosciences , Physics
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  • 10
    Publication Date: 2002-04-01
    Print ISSN: 0031-9201
    Electronic ISSN: 1872-7395
    Topics: Geosciences , Physics
    Published by Elsevier
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