Plate Boundary Observatory Borehole Strainmeter Recordings Of The 29 September 2009 Tsunami
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On 29 September 2009 a M8.3 earthquake on the Australian-Pacific plate boundary generated a tsunami that caused widespread damage in Samoa, American Samoa, and Tonga. Peak to trough wave heights of 314 cm were recorded 250 km from the epicenter at Pago-Pago, American Samoa approximately 20 minutes after the event. NOAA’s West Coast and Alaska Tsunami Warning Center predicted the tsunami would arrive at Tofino, Vancouver Island, British Columbia, at 05:12 UTC, 30 September 2009.Keywords:
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Abstract The damage potential of induced earthquakes associated with fluid injection is a major concern in hydrocarbon resource development. An important source of data for the assessment of damage is macroseismic intensity perceived by people and structures. In the Western Canada Sedimentary Basin (WCSB) where the occurrence of seismicity is mostly related to oil and gas activities, the collection of intensity data is incomplete. In this study, we present a comprehensive dataset gathered by the BC Oil and Gas Commission in the period 2016–2020. We assign intensities to individual felt reports according to the modified Mercalli intensity (MMI) scale and associate each MMI value to an earthquake. The isoseismal map of the largest earthquake in the Septimus region of northeast British Columbia is also provided using the compiled intensity dataset complemented with data from the U.S. Geological Survey and Natural Resources Canada “Did You Feel It?” systems along with the intensities converted from ground-motion amplitudes. We consider an approximate 10 km radius around the mainshock of 30 November 2018 earthquake with moment magnitude of 4.6 to be the meizoseismal area based on maximum intensities of 4–5. We also investigate the distance decay of intensity for shallow induced earthquakes in comparison with deeper natural events with the same magnitudes. Although intensities from shallow earthquakes (depth≤5 km) can be higher than deep events (depth≥10 km) at close distances (10–15 km), they tend to decrease abruptly at greater distances to become lower than deep events. The localization of large intensities from induced earthquakes within the meizoseismal area warrants special attention in future resource developments and call for systematic intensity data collection in the WCSB.
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Moment magnitude scale
Intensity
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In 2018, a large earthquake (Mw7.6) occurred in the Swan Island Fault zone at the northwest boundary of the Caribbean plate. This earthquake generated a small tsunami of 20 cm. However, Puerto Cortes in Honduras is located close to the Swan Island Fault zone. Evaluation of tsunami hazard at Puerto Cortes due to large earthquakes along the fault zone is important. We first estimated the fault parameters of the 2018 Swan Island earthquake using W-phase inversion technique. Then, the moment magnitude of 7.6, the fault length of 134 km, the fault width of 24 km, and the slip amount of 5.1 m were estimated. In addition to those estimates, a small fault dimension of the earthquake, 40 km × 20 km, with a slip amount of 20.8 m was considered. Those two fault models were used to compute tsunami inundation at Puerto Cortes. The tsunami computed from the small fault inundated a large area in Puerto Cortes including the port area. The effect of co-seismic horizontal displacement of ocean floor also enhanced the tsunami inundation at Puerto Cortes. Those results indicate that preparation for future tsunami hazard in Puerto Cortes is important although no significant tsunami was generated historically.
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Tsunami earthquake
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Research Article| June 19, 2019 Ground‐Motion Characteristics of the 30 November 2018 Injection‐Induced Earthquake Sequence in Northeast British Columbia, Canada Alireza Babaie Mahani; Alireza Babaie Mahani Corresponding Author aGeoscience BC, 1101‐750 W. Pender Street, Vancouver, British Columbia, Canada V6C 2T7, ali.mahani@mahangeo.com Search for other works by this author on: GSW Google Scholar Honn Kao; Honn Kao bPacific Geoscience Center, Geological Survey of Canada, 9860 W. Saanich Road, Sidney, British Columbia, Canada V8L 5T5 Search for other works by this author on: GSW Google Scholar Gail M. Atkinson; Gail M. Atkinson cDepartment of Earth Sciences, Western University, 1151 Richmond Street North, London, Ontario, Canada N6A 5B7 Search for other works by this author on: GSW Google Scholar Karen Assatourians; Karen Assatourians cDepartment of Earth Sciences, Western University, 1151 Richmond Street North, London, Ontario, Canada N6A 5B7 Search for other works by this author on: GSW Google Scholar Kofi Addo; Kofi Addo dBC Hydro, 6911 Southpoint Drive, E10, Burnaby, British Columbia, Canada V3N 4X8 Search for other works by this author on: GSW Google Scholar Yajing Liu Yajing Liu eDepartment of Earth and Planetary Sciences, McGill University, 3450 University Street, Montreal, Quebec, Canada H3A 2A7 Search for other works by this author on: GSW Google Scholar Author and Article Information Alireza Babaie Mahani Corresponding Author aGeoscience BC, 1101‐750 W. Pender Street, Vancouver, British Columbia, Canada V6C 2T7, ali.mahani@mahangeo.com Honn Kao bPacific Geoscience Center, Geological Survey of Canada, 9860 W. Saanich Road, Sidney, British Columbia, Canada V8L 5T5 Gail M. Atkinson cDepartment of Earth Sciences, Western University, 1151 Richmond Street North, London, Ontario, Canada N6A 5B7 Karen Assatourians cDepartment of Earth Sciences, Western University, 1151 Richmond Street North, London, Ontario, Canada N6A 5B7 Kofi Addo dBC Hydro, 6911 Southpoint Drive, E10, Burnaby, British Columbia, Canada V3N 4X8 Yajing Liu eDepartment of Earth and Planetary Sciences, McGill University, 3450 University Street, Montreal, Quebec, Canada H3A 2A7 Publisher: Seismological Society of America First Online: 19 Jun 2019 Online Issn: 1938-2057 Print Issn: 0895-0695 © Seismological Society of America Seismological Research Letters (2019) 90 (4): 1457–1467. https://doi.org/10.1785/0220190040 Article history First Online: 19 Jun 2019 Cite View This Citation Add to Citation Manager Share Icon Share Facebook Twitter LinkedIn MailTo Tools Icon Tools Get Permissions Search Site Citation Alireza Babaie Mahani, Honn Kao, Gail M. Atkinson, Karen Assatourians, Kofi Addo, Yajing Liu; Ground‐Motion Characteristics of the 30 November 2018 Injection‐Induced Earthquake Sequence in Northeast British Columbia, Canada. Seismological Research Letters 2019;; 90 (4): 1457–1467. doi: https://doi.org/10.1785/0220190040 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietySeismological Research Letters Search Advanced Search ABSTRACT On 30 November 2018, three felt earthquakes occurred in the Septimus region of northeast British Columbia in an area where hydraulic fracturing was in progress. The proximity of oil and gas activities to populated areas and to critical infrastructure including major dams raises significant concern regarding the seismic hazard posed by moderate induced events and motivates study of their ground motions. Here, we analyze the ground‐motion amplitudes from these events recorded between 3 and 400 km. We use three‐component waveforms from 45 seismometer and accelerometer sensors to analyze the observed ground motions. The moment magnitude (Mw) of the first event is estimated as 4.6 using the vertical pseudoresponse spectral acceleration (PSA) based on the relations provided by Novakovic et al. (2018). The Mw for the two smaller earthquakes are 3.5 and 4.0. The intensity of shaking from the Mw 4.6 and 4.0 events generally exceeded modified Mercalli intensity (MMI) VI at distances <6 km. The maximum duration above the MMI VI threshold at the closest station (3.5 km distance) from the mainshock is 1.6 s. The observed ground motions agree with the ground‐motion prediction equation (GMPE) of Novakovic et al. (2018) for induced events in Oklahoma, with attenuation modified to match that for the study region, assuming typical regional site amplification. The inferred value of stress drop for the mainshock and the largest aftershock is approximately 50 bars based on the agreement of observed PSA values with the Novakovic et al. (2018) GMPE. You do not have access to this content, please speak to your institutional administrator if you feel you should have access.
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The magnitude 9.0 earthquake centered off the west coast of northern Sumatra (3.307°N, 95.947°E) on December 26, 2004 at 00:59 UTC (United States Geological Survey (USGS) (2005), USGS Earthquake Hazards Program‐Latest Earthquakes, Earthquake Hazards Program, http://earthquake.usgs.gov/eqinthenews/2004/usslav/ , 2005) generated a series of tsunami waves that devastated coastal areas throughout the Indian Ocean. Tide gauges operated on behalf of national and international organizations recorded the wave form at a number of island and continental locations. This report summarizes the tide gauge observations of the tsunami in the Indian Ocean (available as of January 2005) and provides a recommendation for the use of the basin‐wide tide gauge network for future warnings.
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Geological survey
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Thrust fault
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We modeled a tsunami from the West Papua, Indonesia earthquakes on January 3, 2009 (M w = 7.7). After the first earthquake, tsunami alerts were issued in Indonesia and Japan. The tsunami was recorded at many stations located in and around the Pacific Ocean. In particular, at Kushimoto on Kii Peninsula, the maximum amplitude was 43 cm, larger than that at Manokwari on New Guinea Island, near the epicenter. The tsunami was recorded on near-shore wave gauges, offshore GPS sensors and deep-sea bottom pressure sensors. We have collected more than 150 records and used 72 stations' data with clear tsunami signals for the tsunami source modeling. We assumed two fault models (single fault and five subfaults) which are located to cover the aftershock area. The estimated average slip on the single fault model (80 × 40 km) is 0.64 m, which yields a seismic moment of 1.02 × 1020 Nm (M w = 7.3). The observed tsunami waveforms at most stations are well explained by this model.
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