Banks Peninsula Volcano

The Banks Peninsula Volcano is an extinct volcanic complex to the east of Christchurch on New Zealand's South Island.[2] While the volcano is highly eroded it still forms the majority of Banks Peninsula with a highest point of 919 m (3,015 ft).[3] It is a composite of two main eruptive centres one originating at Lyttelton Harbour, the other at Akaroa Harbour. The eruptions were predominantly basaltic, with associated andesite and trachytes, with minor rhyolite. The volcanic activity occurred in the Late Miocene and possibly extended into the Early Pliocene. There are four volcanic groups, all of which are within the Māui Supergroup.[4] The Christchurch earthquakes led to rumors of a possible eruption, however, there is no known magma chamber beneath the volcano and there has not been any sign of volcanic activity in the last 5 million years.[5]

Banks Peninsula Volcano
Stratigraphic range:
Banks Peninsula with Akaroa Harbour (West, Lower) and Lyttelton Harbour (East, Upper)
TypeVolcanic Complex
Sub-unitsDiamond Harbour Volcanic Group, Mount Herbert Volcanic Group, Akaroa Volcanic Group, Lyttelton Volcanic Group
OverliesTorlesse Composite Terrane and Mount Somers Volcanics
ThicknessOriginally c.1500m
Lithology
PrimaryBasalt
OtherAndesite, trachytes and rhyolite
Location
Coordinates43°44′58″S 172°52′10″E

Origin and relationship to other volcanoes

New Zealand's South Island has many extinct volcanic centres with no obvious tectonic mechanism of formation.[6][1] Because of this the cause of these intraplate volcanoes is debated. They extend in age from the Cretaceous to the Pliocene and outcrop throughout Otago, Canterbury and on the Chatham Islands.[1] The largest of these is the Banks Peninsula Volcano followed by the Dunedin Volcano which is half its size, but part of a much larger volcanic area, the Dunedin Volcanic Group.[7] Also the Cretaceous Mount Somers Volcanics occur throughout Canterbury including Banks Peninsula resulting in adjacent volcanics say near McQueens Valley having very different ages being rhyolites at 98.0 ± 1.2 million years ago[1] and basaltic and trachytic lava flows at 11.59 ± 0.08 million years ago.[8]

These volcanic centres can be dormant for tens of millions of years between eruptions. This implies that the mechanism of formation is connected to the lithosphere unlike some other intraplate volcanoes such as the Hawaii island chain, which are rooted in the asthenosphere. One mechanism for the creation of these volcanoes is the flaking off of the base of Zealandia's lower lithosphere into the asthenosphere. Zealandia has a thin lithosphere as it has been extended while rafting away from Australia. If large sections of this already thin lithosphere sank into the asthenosphere, it would be replaced with hotter rock leading to decompression melting. This theoretically could cause volcanic activity that is locked to the moving lithosphere over many millions of years.[1]

Geomorphology and structure

The shape of the volcano was controlled by a north-west south-east fault system that controlled magma flow.[9] Local extension formed the Lyttelton Volcanic Complex. Erosion has formed streams radially around the volcanic cones and more significant valleys have formed where these radial patterns meet.[10] The erosion and destruction of one wall of these cones has led to an increase in catchment size and associated erosion. Therefore, forming the significant natural harbours of Banks Peninsula. By this mechanism Lyttelton Harbour had started to form by 8.1 Ma.[10] The large mass of resistant volcanic rock that now makes up Banks Peninsula has significantly controlled the shape of the Canterbury Plains.[11]

Volcanic subunits

Volcanic activity started at Lyttelton Harbour (c.11 Ma)[12] then extended through the Mount Herbert Volcanic Group to Akaroa Harbour (c.9 Ma).[12] During the latter phase of the volcano it was simultaneous active from both its major magma chambers, at Akaroa and Lyttelton. The complex geochemically evolved over time and has cyclic eruptive phases. Each progressive cycle has an increase feldspar with time, which created more blocky lava flows due to increased viscosity.[10]

Lyttelton Volcanic Group
A sample of rhyolite from the Allandale Rhyolite, Lyttelton, New Zealand

The oldest eruptions of the Banks Peninsula occurred between 11–9.7 Ma around the modern town of Lyttelton. These volcanic rocks rest unconformably on Mount Somers Volcanic Group and Rakaia Terrane. The Lyttelton Volcanic Group is primarily basalt and it has been constructed by the formation of five overlapping volcanic cones.[12][2]

The Allandale Rhyolite is composed of rhyolite and dacite banded flows with rare tuffs and obsidian (10.8 Ma). it is conformably overlain by Governors Bay Andesites in the Lyttelton Harbour area.[12]

Mount Herbert Volcanic Group

The Mount Herbert Volcanic Group (9.7–8 Ma) represents the movement of volcanic activity towards the east.[12][2][10]

Akaroa Volcanic Group

The Akaroa Volcanic Group (9–8Ma) are basaltic to trachytic lava flows centred on Akaroa Harbour.[12][2]

Diamond Harbour Volcanic Group
The Monument on Banks Peninsula near Diamond Harbour, with some fresh rockfall from the 2011 Christchurch earthquake.

The Diamond Harbour Volcanic Group represents a return of volcanic activity to the western side of the peninsula (7–5.8Ma). The group is mostly made up of basalt, with rare interbedded carbonaceous mud.[12][2]

See also

References
  1. Hoernle 2006 et al.
  2. Sewell 1986
  3. "Banks Peninsula tramping tracks". Department of Conservation. Archived from the original on 18 June 2017. Retrieved 19 June 2017.
  4. Mortimer et al. 2014
  5. "Lyttelton eruption 'not possible'". Stuff. 23 June 2011. Archived from the original on 26 February 2019. Retrieved 21 February 2019.
  6. Timm 2009
  7. Scott, James M.; Pontesilli, Alessio; Brenna, Marco; White, James D. L.; Giacalone, Emanuele; Palin, J. Michael; le Roux, Petrus J. (2020). "The Dunedin Volcanic Group and a revised model for Zealandia's alkaline intraplate volcanism". New Zealand Journal of Geology and Geophysics. 63 (4): 510–529. doi:10.1080/00288306.2019.1707695. S2CID 212937447. Archived from the original on 19 February 2023. Retrieved 19 February 2023.
  8. Barley, ME; Weaver, SD; De Laeter, JR (1988). "Strontium isotope composition and geochronology of intermediate—silicic volcanics, Mt Somers and Banks Peninsula, New Zealand". New Zealand Journal of Geology and Geophysics. 31 (2): 197–206. doi:10.1080/00288306.1988.10417769. Archived from the original on 12 February 2023. Retrieved 12 February 2023.
  9. Ring 2012
  10. Hampton 2010
  11. Ballance 2009 p.252
  12. Forsyth 2008 p.29

Bibliography
This article is issued from Wikipedia. The text is licensed under Creative Commons - Attribution - Sharealike. Additional terms may apply for the media files.