ruaumoko: 1983 Mt.Tihia/Tokaanu quakes

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1983 Mt.Tihia/Tokaanu quakes

Between 1974 and 1983 there are no records of events in the area. In 1983 there were only 3 earthquakes, all in the northern area and all in September. Two quakes on the 19th September. one at the base of Mt. Kuharua, and the other near the Waihia River. The other quake , on 26th September was under the northern foothills of Mt. Tihia west of Tokaanu.
Mt. Tihia/Tokaanu quakes 1983

REF, LAT, LONG, TIME, DEPTH, MAG
1564528, -38.95, 175.7, 1983/09/19 10:16:45.0, 12, 3.25
1564530, -38.95, 175.72, 1983/09/19 17:45:01.9, 12, 3.689
1564544, -38.96, 175.75, 1983/09/26 18:17:18.0, 12, 3.344

data by geonet. map by google maps. plots by highace using GPS Visualizer

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Earthquake Swarms

Earthquake swarms are events where a local area experiences sequences of many earthquakes striking in a relatively short period of time. The length of time used to define the swarm itself varies, but the United States Geological Survey points out that an event may be on the order of days, weeks, or months. They are differentiated from earthquakes succeeded by a series of aftershocks by the observation that no single earthquake in the sequence is obviously the main shock. Earthquake swarms are one of the events typically preceding eruptions of volcanoes

Earthquake Aftershocks

An aftershock is an earthquake that occurs after a previous earthquake (the main shock). An aftershock is in the same region of the main shock but is always of smaller magnitude strength. If an aftershock is larger than the main shock, the aftershock is redesignated as the main shock and the original main shock is redesignated as a foreshock. Aftershocks are smaller earthquakes formed as the crust around the displaced fault plane adjusts to the effects of the main shock

Aftershocks are dangerous because they are usually unpredictable, can be of a large magnitude, and can collapse buildings that are damaged from the mainshock. Bigger earthquakes have more and larger aftershocks and the sequences can last for years or even longer especially when a large event occurs in a seismically quiet area; see, for example, the New Madrid Seismic Zone, where events still follow Omori's law from the mainshocks of 1811–1812. An aftershock sequence is deemed to have ended when the rate of seismicity drops back to a background level; i.e., no further decay in the number of events with time can be detected.