|Region:||Hawaii and Pacific Ocean|
|Measurement method(s):||InSAR, GPS - continuous, Levelling, Tiltmeter|
|Duration of observation:||1995-present (GPS), 2000-2010 (InSAR)|
|Inferred cause of deformation:||Magmatic, Faulting/tectonics|
|Characteristics of deformation:|
Segall (2013) studied the 1997 East Rift Zone (Napau) intrusion and eruption on Kilauea volcano, determining the best-fitting dislocation model of the intrusion (including campaign GPS data) aligns well with the eruptive fissures, and the decay in displacement with distance from the dyke constrains the bottom of the dyke to about 2.5 km (Owen et al. 2000).
Volcano-tectonic earthquakes and stronger tectonic earthquakes occur due to interaction between existing fault structures and magmatic and tectonic processes. The most common mode of failure is strike slip faulting. Daily GPS solutions were used by Wauthier et al. (2013) to define three ‘background deformation’ periods – 1. July 2000 to September 2003, 2. October 2006 to March 2007, 3. December 2009 to June 2010.
|Reference:||Owen, S., Segall, P., Lisowski, M., Miklius, A., Murray, M., Bevis, M. & Foster, J. 2000. January 30, 1997 eruptive event on Kilauea volcano, Hawaii, as monitored by continuous GPS. Geophysical Research Letters, 27, 2757–2760.|
|Reference:||Segall, P., 2013. Volcano deformation and eruption forecasting. Geological Society, London, Special Publications, 380(1), pp.85-106.|
|Reference:||Wauthier, C., Roman, D.C., Poland, M.P., Miklius, A., Hooper, A.J., Fukushima, Y. and Cayol, V., 2013, December. Magma-tectonic interactions at Kilauea volcano revealed by the modeling of geodetic and seismic data. In AGU Fall Meeting Abstracts (Vol. 1, p. 02).|
|Reference:||Hawaiian Volcano Observatory: http://hvo.wr.usgs.gov/volcanowatch/archive/2001/01_06_28.html|