| Taupō Fault Belt | |
| Named For: | Taupō |
| Year Def: | 1960 |
| Pushpin Relief: | 1 |
| Country: | New Zealand |
| Region: | Waikato Region |
| Range: | Up to 6.5 Mw[1] |
| Segments: | many |
| Length: | 20km (10miles) |
| Plate: | Indo-Australian |
| Status: | Active |
| Type: | Normal faults |
| Age: | Miocene-Holocene |
| Volcanic Arc/Belt: | Taupō Volcanic Zone |
| Embed: | New Zealand geology database (includes faults) |
The Taupō Fault Belt contains many almost parallel active faults, and is located in the Taupō Rift of the central North Island of New Zealand geographically between Lake Taupō and the lakes of Rotorua, Tarawera, Rotomahana and Rerewhakaaitu.[2] The potential active fault density is very high, with only 0.1kmto1kmkm (00.1milesto01mileskm) separating the north-east to south-west orientated normal fault strands on detailed mapping of part of the belt.[3] The Waikato River bisects the western region of the belt.
The northern Taupō Fault Belt is in the area also referred to as either, the Paeroa Graben or the Kapenga Graben, between the Horohoro Fault[4] and the Paeroa Fault.[5] Aligned with the orientation of the modern Taupō Rift are multiple north-north-east trending normal faults. These include the Ngakuru Fault to the east with the Ngakuru Graben between it and the Whirinaki Fault.[6] Within the 14km (09miles) wide Ngakuru Graben are also to the west the Maleme Fault (Zone), which as a zone also contains the Mangaete/Lakeside Fault and to the east the Hossack Road Fault and the Te Weta Fault.[6] The tectonic activity is driven by the ground subsiding at a rate of 0.3cm/year0.4cm/year since 61,000 years ago with largely orthogonal rifting associated with subduction and the clockwise rotation of the northern North Island allowing the rift to open.[6]
| Fault/ Segment | Surface length | Estimated Risk Mw | Mean Slip rate (mm/year) | Reoccurance (year) | |
|---|---|---|---|---|---|
| → Ngakuru (South West) | 9 | 6.0 | 0.5 | 950 | |
| → Ngakuru (North East) | 18 | 6.5 | 0.5 | 2300 | |
| Maleme | 17 | 6.6 | 3.5 | 300 | |
| Mangatete - Lakeside | 7 | 5.9 | 0.1 | 4500 | |
| Whirinaki | 19.8 | 6.6 | 0.1 (0.75) | 10700 | |
| → Whirinaki West | 10 | 6.1 | 0.2 | 2900 | |
| → Whirinaki East | 12 | 6.2 | 0.2 (1.4) | 5100 | |
| Hossack Road | 4 | 5.5 | 0.1 | 1700 | |
| Te Weta | 35 | 6.3 | 0.4 | 2100 | |
| 27 | 6.7 | 0.8 | 2300 | ||
| → Paeroa North | 9 | 6.1 | 0.8 | 800 | |
| → Paeroa Central | 7 | 6.1 | 0.8 | 600 | |
| → Paeroa South | 10 | 6.2 | 0.8 | 900 | |
| 16 | 6.4 | 0.17 | 4400 | ||
| Horohoro | 20 | 6.5 | 0.17 | 7400 | |
| Ongahoro | ≥13 | 6.3 | 1.7 | <3300 | |
| Rotohouhou | 9.5 | 6.0 | 0.6 | 2900 |
Detailed mapping, supplemented by deep ground trenching, of a portion of the southern Taupō Fault Belt prior to construction of a geothermal power station not only showed how inaccurate the inferred active fault tracings in this area are, with under counting potential active fault strands by a factor of perhaps two, it also caused the relocation of the power station.[3]
There are discontinuities in the definable faults of the modern Taupō Rift imposed by its caldera's, with the Taupō Volcano and the Ōkataina Volcanic Centre at the southern and northern end of the Taupō Fault Belt respectively defining the limits of its predominant tectonic activity. Tectonic activity predominates in the present rift also south of Lake Taupō until the active andesitic volcanoes of the North Island Volcanic Plateau are reached or from the Ōkataina Caldera north through the Whakatāne Graben to the active andesitic volcano of Whakaari / White Island.[9] The recently active vents in the main volcanoes are not aligned with currently active faults in the Taupō Fault Belt but there are interactions and for example there was a complete fault rupture of the Ngapouri-Rotomahana Fault just prior to the 1314±12 CE Kaharoa eruption of Mount Tarawera.[10]
The 2001 Taupō earthquake swarm started within a very constrained area of the Taupō Volcano under the northwestern portion of Lake Taupō within the Oruanui caldera. It spread out horizontally over time with small size predominantly strike-slip faulting constrained to zones associated with the tectonic normal faults. This is consistent with a mafic magma intrusion (rather than one associated with the rhyolytic eruptions of Taupō) causing pressure over predominantly time, rather than place perpendicular to the usual strain on these fault systems and has been seen elsewhere.[7] This is consistent with seismicity rather than volcanic activity poses the main short-term hazard at Taupō Volcano.[7]