| Mangakino Caldera | |
| Map: | North Island |
| Location: | North Island, New Zealand |
| Coordinates: | -38.3833°N 222°W |
| Type: | Caldera |
| Length: | 30km (20miles) |
| Width: | 15km (09miles) |
| Volcanic Arc/Belt: | Taupo Volcanic Zone |
| Last Eruption: | 900,000 years ago |
The Mangakino caldera complex (other names are Mangakino volcanic center, Mangakino Caldera) is the westernmost and one of oldest extinct rhyolitic caldera volcanoes in the Taupō Volcanic Zone of New Zealand's North Island.[1] It produced about a million years ago (1 Ma) in the Kidnappers eruption of 1200km3, the most widespread ignimbrite deposits on Earth being over 45000km2 and was closely followed in time by the smaller 200km3 Rocky Hill eruption.[2] The Kidnappers eruption had a estimated VEI of 8 and has been assigned a total eruption volume (not just tephra) of 2760km3.
However this was only in its most recent caldera forming phase from 1.21 to 0.91 million years ago as it had its earliest caldera generating phase from 1.62 to 1.51 million years ago. There are at least 11 major historic eruptions assigned to this complex.[3] At least 5 of these contributed significant welded ignimbrite deposits that represent major pyroclastic events in the central North Island.[4] Ongatiti Ignimbrite (Hinuera Stone) from a 7 VEI event, about 1.3 million years ago, has now been found over a wider area and several meter thick tephra deposits from the eruption exist on drill samples from both Auckland and Wellington.
The earliest characterised eruptives from the complex are andesitic and the mechanism of transition from this to the more explosive later rhyolitic eruptions is related to increased heat flow from the magma sources.
Later many of these deposits were covered over by deposits from other eruptive centres such as those of the Oruanui eruption.
The caldera can be defined by gravitational measurements as 30km (20miles) by 15km (09miles) and its "basement" floor is at least 4km (02miles) below the present ground surface.
| Formations | Layer names | Age range estimate by various methods (if only one method ± error) | Eruptive volume | |
|---|---|---|---|---|
| Marshall | Unit I (Marshall A and B) Ignimbrite Unit H (Kaahu) Ignimbrite Unit G | 0.95 ± 0.03 Ma | ||
| Whakaahu | Rhyolite dome | 1.02 ± 0.02 Ma | ||
| Raepahu (Potaka Tephra) | Rocky Hill Ignimbrite Kidnappers Unit E Ignimbrite and fall deposit | 0.95 to 1.15 Ma 0.93 to 1.07 Ma | > | |
| Mangaokewa | Ahuroa Ignimbrite Unit D Ignimbrite and fall deposit | 1.16 to 1.33 Ma 1.20 ± 0.04 Ma | ||
| Ongatiti | Ongatiti Ignimbrite (Oparau tephra, K12a Kauroa Ash Formation, K12) Tumai Rd dome | 1.37 ± 0.04 Ma (1.31 ± 0.09 Ma, 1.38 ± 0.06 Ma, 1.38 ± 0.05 Ma) 1.16 to 1.34 Ma 1.27 ± 0.05 Ma | > DRE | |
| Pouakani | Unit C Ignimbrite | 1.68 ± 0.07 Ma (This age inconsistent with position) | ||
| Tolley | Unit B Ignimbrite | 1.53 ± 0.04 Ma | ||
| Ngaroma | Ngaroma (Unit A) Ignimbrite | 1.31 to 1.6 Ma | ||
| Link (source unknown) | Unit F Ignimbrite | 1.60 ± 0.09 Ma |
That there was a separate Mangakino volcanic complex was first understood in 1965, and a caldera structure by gravity studies in 1982. The recognition was impaired mainly because of erosion produced discontinuities, burying by later volcanic deposits or overburden displacement in later caldera formation. The extent of eastern ignimbrite deposits from the early Ongatiti event is still unknown and even the eastern caldera boundary is ill defined due to the very disruptive margins of the new Taupō Rift to the east of the complex. At Tokoroa to the complexes north, Ongatiti ignimibrite is for example found at a depth of between 392m to 457mm (1,286feet to 1,499feetm).[5]
What are now termed ignimbrites and manifest as prominent surface deposits, far from the complex, were recognised by Ferdinand von Hochstetter in his 1859 maps. From the early 1960s the various ignimbrites from the complex were assigned names and studied in more detail. Colin Wilson first defined the Mangakino caldera complex in 1964 and went on to improve the understanding of its ignimbrite distribution and stratigraphy. Reliable age data became available from the 1990s. It was in the late 1990s that it first became recognised that the size of the eruptions had been underestimated, but not until 2016–17 that proof of super eruptions was presented.
The Mangakino caldera eruptives are definitely assignable to the Taupō Volcanic Zone but are to the west of the currently most active portion of the Taupō Rift. To its north the transition between the north-western Taupō Rift and the Coromandel Volcanic Zone via the Tauranga Volcanic Centre and its 2.1 million year old Waiteariki Formation are subject to on going study.[6]