Relevant bibliographies by topics / Taupo

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Academic literature on the topic 'Taupo'

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Published: 4 June 2021
Last updated: 28 January 2023

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Journal articles on the topic "Taupo"

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Druitt, Tim. "Turbulent times at Taupo." Nature 381, no. 6582 (June 1996): 476–77. http://dx.doi.org/10.1038/381476a0.

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Wilson, C. J. N. "Emplacement of Taupo ignimbrite." Nature 385, no. 6614 (January 1997): 306–7. http://dx.doi.org/10.1038/385306a0.

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Dade, W. Brian, and Herbert E. Huppert. "Emplacement of Taupo ignimbrite." Nature 385, no. 6614 (January 1997): 307–8. http://dx.doi.org/10.1038/385307a0.

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Stirling, M. W., and C. J. N. Wilson. "Development of a volcanic hazard model for New Zealand." Bulletin of the New Zealand Society for Earthquake Engineering 35, no. 4 (December 31, 2002): 266–77. http://dx.doi.org/10.5459/bnzsee.35.4.266-277.

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We commence development of a volcanic hazard model for New Zealand by applying the well- established methods of probabilistic seismic hazard analysis to volcanoes. As part of this work we use seismologically-based methods to develop eruption volume - frequency distributions for the Okataina and Taupo volcanoes of the central Taupo Volcanic Zone, New Zealand. Our procedure is to use the geologic and historical record of large eruptions (erupted magma volumes ≥ 0.01 cubic km for Taupo and ≥ 0.5 cubic km for Okataina) to construct eruption volume-frequency distributions for the two volcanoes. The two volcanoes show log-log distributions of decreasing frequency as a function of eruption volume, analogous to the shape of earthquake magnitude-frequency distributions constructed from seismicity catalogues. On the basis of these eruption volume-frequency distributions we estimate the maximum eruption volumes that Taupo and Okataina are capable of producing at probability levels of relevance to engineers and planners. We find that a maximum eruption volume of 0.1 cubic km is expected from Taupo with a 10% probability in 50 years, while Okataina may not produce a large eruption at this probability level. However, at the more conservative 2% probability in 50 years, both volcanoes are expected to produce large eruptions (0.5 cubic km for Okataina and 1 cubic km for Taupo). Our study therefore shows significant differences in eruption probabilities for volcanoes in the same physiographic region, and therefore highlights the importance of establishing unique eruption databases for all volcanoes in a hazard analysis.
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Hogg, Alan G. "When was the Taupo eruption?" Quaternary International 279-280 (November 2012): 204. http://dx.doi.org/10.1016/j.quaint.2012.08.381.

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Darby, Desmond J., Kathleen M. Hodgkinson, and Graeme H. Blick. "Geodetic measurement of deformation in the Taupo Volcanic Zone, New Zealand: The north Taupo network revisited." New Zealand Journal of Geology and Geophysics 43, no. 2 (June 2000): 157–70. http://dx.doi.org/10.1080/00288306.2000.9514878.

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Gilmour, Alex E., and Ron A. Heath. "Barotropic and baroclinic waves in Lake Taupo." New Zealand Journal of Marine and Freshwater Research 23, no. 2 (June 1989): 189–94. http://dx.doi.org/10.1080/00288330.1989.9516355.

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Sparks, R. J., W. H. Melhuish, J. W. A. McKee, John Ogden, J. G. Palmer, and B. P. J. Molloy. "14C Calibration in the Southern Hemisphere and the Date of the Last Taupo Eruption: Evidence from Tree-Ring Sequences." Radiocarbon 37, no. 2 (1995): 155–63. http://dx.doi.org/10.1017/s0033822200030599.

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Tree rings from a section of Prumnopitys taxifolia (matai) covering the period ad 1335–1745 have been radiocarbon dated and used to generate a 14C calibration curve for southern hemisphere wood. Comparison of this curve with calibration data for northern hemisphere wood does not show a systematic difference between 14C ages measured in the northern and southern hemispheres. A floating chronology covering 270 yr and terminating at the last Taupo (New Zealand) eruption, derived from a sequence of 10-yr samples of tree rings from Phyllocladus trichomanoides (celery pine, or tanekaha), is also consistent with the absence of a systematic north-south difference, and together with the matai data, fixes the date of the Taupo eruption at ad 232 ± 15.
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Couper, Steve, Jason Ewert, Ted Anderson, and Ian Wallace. "Natural Nutrient Removal Taupo District Land Disposal Scheme." Proceedings of the Water Environment Federation 2009, no. 12 (January 1, 2009): 3837–51. http://dx.doi.org/10.2175/193864709793953728.

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Gilmour, Alex E. "Seiche characteristics in Lake Taupo, New Zealand (Note)." New Zealand Journal of Marine and Freshwater Research 25, no. 2 (June 1991): 163–66. http://dx.doi.org/10.1080/00288330.1991.9516466.

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Dissertations / Theses on the topic "Taupo"

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Karhunen, Ritva Annikki. "The Pokai and Chimp ignimbrites of NW Taupo Volcanic Zone." Thesis, University of Canterbury. Geology, 1993. http://hdl.handle.net/10092/5791.

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Taupo Volcanic Zone (TVZ) is the largest active volcanic belt in New Zealand, and has erupted >10.000 km3 of dominantly rhyolitic magma during the last 1.6 m.y. This study concerns the field relations, volcanology and petrology of two post-Whakamaru (330 ka) - pre-Mamaku (140 ka) ignimbrites, informally named as the Pokai and Chimp ignimbrites, occurring in a ca. 360 km2 area SW and W from Rotorua in the north-western TVZ. The Pokai Ignimbrite has a minimum volume of ca. 33 km3 DRE, whereas the older Chimp Ignimbrite has a minimum volume of only ca. 5 km3 DRE. Of the two ignimbrites the younger Pokai Ignimbrite is better preserved and is thus the main emphasis in this thesis. The Chimp Ignimbrite is relatively pumice- and crystal-poor (1-2 vol. % phenocrysts), and the exposed flow units are relatively thin (4-6 m). A short plinian phase preceded the Chimp Ignimbrite, whereas the Pokai Ignimbrite is marked by a number of pre-ignimbrite air-fall pumice and ash layers. The Pokai Ignimbrite represents a multiple flow unit ignimbrite, with single flow units usually ranging from 6-30 m. Thick deposits (>20 m thick) are usually welded in the upper middle part of the deposit. Ground deposits, i.e. layer 1 deposits, are rare. Field evidence suggest that the Pokai Ignimbrite originated from the Kapenga Volcanic Centre, a multiple caldera structure in the northern central TVZ. Two pumice types occur in the Pokai Ignimbrite; a crystal-poor type (2-3 % phenocrysts) and a crystal-rich type (6-12 % phenocrysts). Plagioclase is the dominant phenocryst throughout, with minor amounts of orthopyroxene, Fe-Ti oxides and quartz, which occurs in ca. 30 % of the pumices. Hornblende and clinopyroxene are present occasionally. The Pokai Ignimbrite ranges from mildly to strongly peraluminous, whereas the Chimp Ignimbrite is mildly peraluminous, both coinciding with other TVZ rhyolitic ignimbrites, but clearly differing from the rhyolitic lavas which are usually metaluminous to only mildly peraluminous. Whereas most TVZ rhyolitic eruptives have been regarded as relatively homogeneous, the Pokai Ignimbrite shows significant geochemical variation. The magma chamber was compositionally zoned from crystal-poor, high silica, low Sr (77 % SiO2 , 50 ppm Sr) rhyolitic top to more crystal-rich, low silica, high Sr (70 % SiO2 , 130 ppm Sr) rhyolite at the deeper levels. Prior to the eruption vigorous mixing of magma from different levels occurred, producing different pumice types in the airfall deposits, and multiple phenocryst populations in single pumice clasts. As the eruption progressed successively deeper levels of the magma chamber were tapped, the last eruption products representing the less evolved, crystal-rich magma. Least squares and Rayleigh fractionation models indicate that the Pokai, and the Chimp magmas most probably generated by AFC from TVZ andesitic magmas contaminated by Mesozoic basement sediments.
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Leonard, Graham S. "The evolution of Maroa Volcanic Centre, Taupo Volcanic Zone, New Zealand." Thesis, University of Canterbury. Geology, 2003. http://hdl.handle.net/10092/5437.

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Maroa Volcanic Centre (Maroa) is located within the older Whakamaru caldera, central Taupo Volcanic Zone, New Zealand. Dome lavas make up the majority of Maroa volume, with the large Maroa West and East Complexes (MWC and MEC, respectively) erupted mostly over a short 29 kyr period starting at 251 ± 17 ka. The five mappable Maroa pyroclastics deposits are discussed in detail. The Korotai (283 ± 11 ka), Atiamuri (229 ±12 ka), and Pukeahua (~229 -196 ka) pyroclastics are all s 1 km3 and erupted from (a) northern Maroa, (b) a vent below Mandarin Dome and (c) Pukeahua Dome Complex vents, respectively. The Putauaki (272 ± 10 ka) and Orakonui (256 ± 12 ka) pyroclastics total ~ 4 km3 from a petrologically and geographically very similar central Maroa source. The ~ 220 ka Mokai pyroclastics outcrop partly within Maroa but their source remains unclear, whereas the ~ 240 ka Ohakuri pyroclastics appear to have come from a caldera just north of Maroa. The ages of the Mamaku, Ohakuri and Mokai pyroclastics are equivocaL The Mamaku and Ohakuri pyroclastics appear to be older (~ 240 ka) than the age previously accepted for the Mamaku pyroclastics. Maroa lavas are all plagioclase-orthopyroxene bearing, commonly with lesser quartz. Hornblende +/- biotite are sometimes present and their presence is correlated with geochemical variation. All Maroa deposits are rhyolites (apart from two high-silica dacite analyses) and are peraluminous and calcic. They all have the trace element signatures of arc-related rocks typical of TVZ deposits. Maroa deposits fall geochemically into three magma types based on Rb and Sr content: M (Rb 80-123 ppm, Sr 65-88 ppm), T (Rb 80-113 ppm, Sr 100-175 ppm) and N (Rb 120-150 ppm, Sr 35- 100 ppm). The geochemical distinction of these types is also seen in the concentrations of most other elements. Based on the spatial, chronological and petrological similarities of the MWC/MEC and Pukeahua eastern magma associations (termed (1) and (2)) a further four magma associations are determined ((3) through (6)). These six associations account for almost all Maroa deposits. Two end-member models are proposed for the sources of each of the Maroa magma associations: (a) a single relatively shallow magma source feeding spatially clustered eruptions, and (b) a deeper source feeding multiple shallower offshoots over a wider area. Sources for the Maroa magma associations probably lie on a continuum between these two model end members. The distinction between Maroa and Taupo Volcanic Centres is somewhat arbitrary and is best considered to be the easting directly north of Ben Lomond, north of which most volcanism is older than 100 ka and M and N type, and south of which most volcanism is younger than 100 ka and T type. The remaining boundaries (north to include Ngautuku, west to include Mokauteure and east to include Whakapapa domes) are arbitrary, and include the farthest domes linked closely, spatially and magmatic ally, to the other Maroa domes. From 230 to 64 ka there was a hiatus in caldera-forming ignimbrite eruptions. Maroa and the Western Dome Belt (WDB) constitute the largest concentrated volume of eruptions (as relatively gentle lava extrusion) during this period. The rate of Maroa volcanism has decreased exponentially from a maximum prior to 200 ka. In contrast volcanism at Taupo and Okataina has increased from ~ 64 ka to present. The oldest Maroa dome (305 ± 17 ka) constrains the maximum rate of infilling of Whakamaru caldera as 39-17 km3/kyr. This highlights the extraordinarily fast rate of infilling common at silicic calderas and is in agreement with international case studies, except where post-collapse structural resurgence has continued for more than 100 kyr. The majority of caldera fill, representing voluminous eruption deposits in the first tens of thousands of years post collapse, is buried and only accessible via drilling. The WDB and Maroa are petrologically distinct from one another in terms of some or all of Rb, Sr, Ba and Zr content, despite eruption over a similar period. Magma sources for Maroa and the WDB may have been partly or wholly derived from the Whakamaru caldera magma system(s), but petrological distinctions among all three mean that Maroa and the WDB cannot be considered as simple magmatic resurgence of the Whakamaru caldera. Maroa's distinct Thorpe Rd Fault is in fact a fossil feature which hasn't been active in almost 200 kyr. In addition, the graben across Tuahu Dome was likely created by shallow blind diking. Several recent studies across TVZ show structural features with some associated dike intrusion/eruption. Such volcano tectonic interaction is rarely highlighted in TVZ but may be relatively common and lie on a continuum between dike-induced faulting and dikes following structural features. Although rates of volcanism are now low in Maroa magmatic intrusion appears to remain high. This raises the possibility of a causative link between faulting and volcanism in contrast to traditional views of volcanism controlled by rates of magmatic ascent. Probable future eruptions from Maroa are likely to be of similar scale (<0.1 km3 ) and frequency (every ~ 14,000 years) to most of those over the last 100 ka. Several towns lie in a range of zones of Maroa volcanic hazard from total destruction to possible ash fall. However, the probability of a future eruption is only ~ 0.6 % in an 80 year lifetime.
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Ashwell, Paul. "Controls on rhyolite lava dome eruptions in the Taupo Volcanic Zone." Thesis, University of Canterbury. Geological Sciences, 2014. http://hdl.handle.net/10092/8965.

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The evolution of rhyolitic lava from effusion to cessation of activity is poorly understood. Recent lava dome eruptions at Unzen, Colima, Chaiten and Soufrière Hills have vastly increased our knowledge on the changes in behaviour of active domes. However, in ancient domes, little knowledge of the evolution of individual extrusion events exists. Instead, internal structures and facies variations can be used to assess the mechanisms of eruption. Rhyolitic magma rising in a conduit vesiculates and undergoes shear, such that lava erupting at the surface will be a mix of glass and sheared vesicles that form a permeable network, and with or without phenocryst or microlites. This foam will undergo compression from overburden in the shallow conduit and lava dome, forcing the vesicles to close and affecting the permeable network. High temperature, uniaxial compression experiments on crystal-rich and crystal-poor lavas have quantified the evolution of porosity and permeability in such environments. The deformation mechanisms involved in uniaxial deformation are viscous deformation and cracking. Crack production is controlled by strain rate and crystallinity, as strain is localised in crystals in crystal rich lavas. In crystal poor lavas, high strain rates result in long cracks that drastically increase permeability at low strain. Numerous and small cracks in crystal rich lavas allow the permeable network to remain open (although at a lower permeability than undeformed samples) while the porosity decreases. Flow bands result from shear movement within the conduit. Upon extrusion, these bands will become modified from movement of lava, and can therefore be used to reconstruct styles of eruption. Both Ngongotaha and Ruawahia domes, from Rotorua caldera and Okataina caldera complex (OCC) respectively, show complex flow banding that can be traced to elongated or aligned vents. The northernmost lobe at Ngongotaha exhibits a fan-like distribution of flow bands that are interpreted as resulting from an initial lava flow from a N – S trending fissure. This flow then transitioned into intrusion of obsidian sheets directly above the conduit, bound by wide breccia zones which show vertical movement of the sheets. Progressive intrusions then forced the sheets laterally, forming a sequence of sheets and breccia zones. At Ruawahia, the flow bands show two types of eruption; long flow lobes with ramp structures, and smaller spiny lobes which show vertical movement and possible spine extrusion. The difference is likely due to palaeotopography, as a large pyroclastic cone would have confined the small domes, while the flow lobes were unconfined and able to flow down slope. The vents at Ruawahia are aligned in a NE – SW orientation. Both domes are suggested to have formed from the intrusion of a dyke. The orientations of the alignment or elongation of vents at Ngongotaha and Ruawahia can be attributed to the overall regional structure of the Taupo Volcanic Zone (TVZ). At Ngongotaha, the N – S trending elongated vent is suggested to be controlled by a N – S trending caldera collapse structure at Rotorua caldera. The rest of the lobes at Ngongotaha, as well as other domes at Rotorua caldera, are controlled by the NE – SW trending extensional regional structure or a NW – SE trending basement structure. The collapse of Rotorua caldera, and geometry of the deformation margin, are related to the interplay of these structures. At Ruawahia, the NE – SW trending vent zone is parallel to the regional extension across the OCC, as shown by the orientation of intrusion of the 1886AD dyke through the Tarawera dome complex. The NE – SW trending regional structures observed at both Rotorua caldera and Okataina caldera complex are very similar to each other, but differ from extension within the Taupo rift to the south. Lava domes, such as Ngongotaha, that are controlled by this structure show that the ‘kink’ in the extension across Okataina caldera complex was active across Rotorua caldera during the collapse at 240 ka, and possibly earlier. This study shows the evolution of dyke-fed lava domes during eruption, and the control of regional structures in the location and timing of eruption. These findings improve our knowledge of the evolution of porosity and permeability in a compacting lava dome, as well as of the structures of Rotorua caldera, the longevity of volcanic activity at dormant calderas and the hazard potential of dyke-fed lava domes.
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Mason, Blair Joseph. "The Analysis of Taupo Pumice as an Effective Partial Cement Replacement in Concrete." Thesis, University of Canterbury. Geological Sciences, 2012. http://hdl.handle.net/10092/6825.

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Concrete is an integral material in modern infrastructural requirements worldwide. The production of Portland cement is however expensive, energy intensive, and results in globally significant greenhouse gas emissions. Natural pozzolans such as pumice can be used as a partial replacement for Portland cement in concrete, which can reduce production costs and greenhouse gas emissions, and improve concrete performance. A fluvial pumice deposit which may be suited for use as a natural pozzolan has been identified on the floodplains of the Waikato River. A sample was milled in Germany, and returned to New Zealand in two subsamples. These were tested in concrete, with tests divided into four rounds. The first two rounds established baseline concrete strengths at water/binder (w/b) ratios of 0.6 and 0.5, with pumice replacing cement at 5, 10, 15 and 30%. Round Three assessed the use of high pH mix water (pH=12.9), and Round Four assessed the use of a polycarboxylate superplasticiser, both with 10% pumice. Pumice is known to retard early concrete strength, however through optimisation of mix design, improvements in concrete strength and durability can be made. Indeed, all 28 day concrete strengths in this research were below Ultracem, however half of these achieved or exceeded Ultracem strengths at 91 days. The use of superplasticiser achieved the best 28 day concrete strengths, and dosage optimisation is expected to yield further improvements. Concrete durability was tested at w/b=0.5, with 10% and 30% pumice. After prolonged curing (231 days), composite concrete showed substantial improvements in electrical resistivity and resistance to chloride attack, most notably with 30% pumice. Concrete porosity was essentially unaffected. This pumice has shown significant promise as a partial cement replacement. Further mix optimisation is likely to yield greater improvements in concrete strength and durability, and will provide a more economically and environmentally sustainable product for the New Zealand concrete market.
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Harrison, A. J. "Crustal and upper mantle structure of the Taupo Volcanic Zone, New Zealand." Thesis, University of Cambridge, 2004. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.603773.

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The Taupe Volcanic Zone (TVZ) is a major Pliocene-Quaternary NNE-SSW orientated volcano-techonic complex, in central North Island, New Zealand. It is a region characterised by voluminous rhyolitic eruptions, high natural heat flow, intense shallow seismic activity and active NW-SE extension. The central portion of the TVZ is regarded as the most frequently active and productive silicic volcanic system on Earth, yet to date no direct evidence for the source for the magmatisim has been found. In February and December 2001, as part of the NIGHT (North Island GeopHysical Transect) experiment, a total of ten 500 kg land slots were fired into an NW-SE array that ran the width of central North Island, New Zealand. An additional passive array of broad-band and short-period instruments centred on the TVZ recorded local and teleseismic earthquakes for six and a half months. Forward and inverse modelling of this active and shallow (< 10 km) earthquake data shows low-velocity (2.0-3.5 km/s) volcanic sediments reaching a maximum thickness of 3 km beneath the central TVZ. Underlying these sediments to 16 km depth are velocities of 5.0-6.5 km/s, interpreted as quartzo-fieldspathic crust. East and west of the TVZ, these velocities are observed to depths of 30 and 23 km respectively. Beneath the TVZ, material with P-wave velocities of 6.9-7.3 km/s are observed to ~30 km depth and are interpreted as heavily intruded or underplated lower crust. Modelling of deep (> 40 km) earthquake events originating near the top of the subducting Pacific plate, reveals a low-velocity region (LVR) (Vp of 7.4-7.8 km/s) overlying a northwest dipping high-velocity structure that coincides with the Wadati-Benioff zone.
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Spinks, Karl D. "Rift architecture and Caldera volcanism in the Taupo Volcanic Zone, New Zealand." Thesis, University of Canterbury. Geological Sciences, 2005. http://hdl.handle.net/10092/4944.

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The Taupo Volcanic Zone (TVZ) is investigated to determine the interaction of regional structure and volcanism. A three-tiered approach is employed involving (i) analysis of rift geometry and segmentation in Modem TVZ(<300 ka) from remote sensing and digital topographic data; (ii) fault kinematic data collected along the length of TVZ; and (iii) combining new and existing volcanological data for TVZ. Modem TVZ is a NNE-SSW trending intra-arc rift zone, subject to dextral transtension, and characterised by a segmented axial rift zone with a number of offset and variably oriented rift segments. These segments are subject to varying degrees of extension, and a general correlation exists between the amount of extension and the volume and style of volcanism in each segment. Segments with the highest degrees of extension correspond to the Okataina and Taupo Caldera Complexes in the central rhyolitic zone of Modem TVZ, while segments with a higher degree of dextral transtension correspond to the volumetrically-subordinate andesitic extremities. The influence of the structural framework on the shape and formation of calderas in Modem TVZ has been inferred from remote sensing and ground-based structural analysis. Detailed analysis of caldera structure and geometry in Modem TVZ indicates that caldera evolution is largely a function of caldera location relative to the axial rift zone. Calderas peripheral to the rift are simple, single-event structures, while those located within the axial rift zone are multiple-event caldera complexes with geometries dictated by their coincidence with rift faulting. These results show that in Modem TVZ the type, volume, and spatial distribution of magmatic activity is strongly influenced by rift structure and kinematics. The inter-relationship between rift geometry and caldera-complex development is particularly clear at the intra-rift Okataina Caldera Complex (OCC). OCC is located at a step-over in the rift where local rotation of the extension direction accompanies the development of a major transfer zone. Three main collapse events are spatially concentrated in a zone of orthogonal extension within the transfer zone. The 28 x 22 km OCC is elongate parallel to the extension direction, with a complicated topographic margin largely controlled by regional faulting. Major embayments occur on each side of OCC where it is intersected by adjacent rift segments. These are contiguous with two intra-caldera dome complexes forming two overlapping linear vent zones, which transect the caldera complex. The development of volcanism at OCC records the progressive interaction between offset rift segments and the propagation of overlapping rift segment axes. As rift propagation proceeded, a diffuse zone of volcanism progressively concentrated in the centre of the transfer zone then divided into two spatially restricted eruptive centres as through-going faults became established. Field investigations at OCC reveal a major revision to the eruptive stratigraphy that has implications for the development of the caldera and for hazard assessment in northern TVZ. Kawerau Ignimbrite is a partially welded pumice-rich ignimbrite that fills Puhipuhi Basin on the eastern side of the caldera complex and forms a thick terrace in and around the Kawerau township area. Within Puhipuhi Basin it is ~100 m thick, exposed on clear-felled knolls and locally forms jointed bluffs in thickest sections where it is valley ponded. Originally mapped as Kaingaroa Ignimbrite, it was subsequently considered distinct and renamed Kawerau Ignimbrite by Beresford & Cole (2000) with an accepted age of 240 ka. In Puhipuhi basin the Kawerau Ignimbrite overlies both the ~280 ka Matahina and ~65 ka Rotoiti ignimbrites and also the older tephras of the 43-31 ka Mangaone Subgroup. Whole-rock and glass geochemistry tie the ignimbrite specifically to the 33 ka Unit I eruptive phase of the subgroup, vastly increasing the eruptive volume of that unit and implying caldera collapse in this recent phase of OCC activity. Two pumice compositions are identified, reflecting eruption of two distinct magma bodies. Vertical variation in the ignimbrite records rapid depletion of a subordinate dacitic magma such that pumices of this composition are rare beyond proximal exposures. Lithic and pumice size distribution data indicate a source within OCC to the west of Puhipuhi basin. The residual volume of the ignimbrite is <15 km3, but estimates of the original volume approach 50 km3 when intra-caldera volumes are considered. Kawerau Ignimbrite thus represents the largest eruption from OCC in the last 65 ka since the Rotoiti event, and is the youngest partially-welded ignimbrite in TVZ.
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Beresford, Stephen Willis. "Volcanology and geochemistry of the Kaingaroa Ignimbrite, Taupo Volcanic Zone, New Zealand." Thesis, University of Canterbury. Geological Sciences, 1997. http://hdl.handle.net/10092/5738.

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The 0.23 Ma Kaingaroa Ignimbrite is a composite multiple flow-unit ignimbrite erupted from Reporoa Caldera, Taupo Volcanic Zone (TVZ), New Zealand. The Kaingaroa Ignimbrite has a complex internal stratigraphy with a complex basal tephra sequence of intercalated fall, surge and flow deposits, and three ignimbrite units, with strikingly proximal to medial facies variation. Proximal facies deposits are dominated by coarse lithic breccias up to 45m thick which are interpreted as co-ignimbrite lag breccias. These lag breccias are-some of the thickest so far documented. Welding and thickness variations in the extensive Old Waiotapu Rd (OWR; kg1) and Webb ignimbrite unit (WIU; kg2) suggests gradual thickening away from source, interpreted to represent ponding in a shallow alluvial lowland or basin. A detailed lithic componentry study indicates changes in lithic diversity and abundance between stratigraphic units which mark changes in vent conditions, increasing depth of lithic provenance and hence inferred fragmentation level. Lithic fragments reveal aspects of the sub-caldera geology, which is dominated by an andesitic volcano with leuco-gabbroic subvolcanic roots, intercalated welded ignimbrites, rare low-grade metasedimentary basement and meta-rhyolites. Gabbros and meta-rhyolites suggest complex metasomatic and fumarolic processes adjacent to the Kaingaroa magma system. The presence of tourmaline-bearing meta-rhyolites and meta-ignimbrites and tourmalinite is the first documented occurrence of tourmaline and tourmalinite in TVZ. Four pumice types are defined on pumice chemistry and mineralogy. These pumices are interpreted to represent samples of a weakly continuously zoned magma chamber (70-75% SiO2), which was progressively tapped during the eruption. Trace element and rare earth element systematics are consistent with an origin of type A magma from a type D parent by minor fractionation of plagioclase, zircon, and trace contents of Fe/Ti oxides and orthopyroxene. An additional hornblende-, 2-pyroxene-phyric dacite pumice/bleb (69% SiO2) was sampled from the Tokiaminga sub-unit, but is mineralogically and compositionally different from Kaingaroa pumices. Post-caldera rhyolites are mineralogically and chemically variable, with broad similarities to Kaingaroa pumices. The Kaingaroa magma components show reverse isotopic zonation i.e. decreasing 87Sr/86Sr and increasing 143Nd/144Nd with differentiation, suggesting syn-eruptive mingling and evisceration of the multiple magma batches occurred during the climactic caldera collapse phase. The Kaingaroa Ignimbrite has been mis-correlated by previous workers with the Matahina, Mamaku, and Rangatira Point ignimbrites, and three new units described in this thesis; Kawerau ignimbrite, Wheao sheet, and the welded ignimbrite of Wairakei drill holes. It is clear that ignimbrite correlation is difficult in TVZ because of the poor exposure and the limited stratigraphic sections that document multiple units. The Kawerau ignimbrite remains an enigma, largely because of the anomalously high Zr, Hf and Zn contents, suggestive of a relationship to 'alkaline' rhyolites, and the presence of unusual magnesium poor manganoan fayalite of vapour-phase origin. Identification of these units and other intermediate size ignimbrite in the stratigraphic interval between Whakamaru-group, and Mamaku ignimbrites requires further careful documentation, but suggests a temporal clustering of ignimbrites sourced from throughout TVZ.
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Ritchie, Alistair B. H. "Volcanic geology and geochemistry of Waiotapu Ignimbrite, Taupo Volcanic Zone, New Zealand." Thesis, University of Canterbury. Geological Sciences, 1996. http://hdl.handle.net/10092/6588.

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Waiotapu Ignimbrite (0.710 ± 0.06 Ma) is a predominantly densely welded, purple-grey coloured, pumice rich lenticulite, which is exposed on both eastern and western flanks of Taupo Volcanic Zone. The unit is uniform in terms of lithology and mineralogy over its entire extent and has been deposited as a single flow unit. The unit contains abundant pumice clasts which are often highly attenuated (aspect ratios of c.1 :30) and are evenly distributed throughout the deposit. Lithic fragments are rare, never exceeding 1% of total rock volume at an outcrop and no proximal facies, such as lithic lag breccias, have been identified. The deposit is densely welded to the base and only in more distal exposure does the ignimbrite become partially welded at the top of the deposit. Post-depositional devitrification is pervasive throughout the deposit, often destroying original vitroclastic texture in the matrix. Vapour phase alteration is extensive in welded and partially welded facies of the deposit. Pumices within Waiotapu Ignimbrite appear to have been derived from two distinct magma batches, with differing Rb concentrations, that originated along different fractionation trends. Type-A pumices have significantly lower Rb than the subordinate type-B pumices. The presence of the pumices may represent the simultaneous evisceration of two spatially discrete magma chambers or the type-B chamber may have been intruded into type-A body, the magmas subsequently mingling prior to, or during, the eruption. The source of Waiotapu Ignimbrite is poorly constrained, largely owing to the lack of meaningful maximum lithic data, and poor exposure of the unit. The distribution of the ignimbrite suggests that it was erupted from within Kapenga volcanic centre. If so the most proximal exposures of Waiotapu Ignimbrite are approximately 10km from the vent. Intensive and voluminous silicic volcanism, beginning with the eruption of the 0.33 Ma Whakamaru Group Ignimbrite eruptions, and extensive faulting within Kapenga volcanic centre will have obscured any intra-caldera Waiotapu Ignimbrite. The mechanism of eruption suggests that the source may not have been a caldera in the strictest sense, but instead a series of near linear fissures aligned with the trend of regional faulting. Waiotapu Ignimbrite was generated in one sustained eruption and produced an energetic and high temperature pyroclastic flow. The lack of any recognised preceding plinian deposit, coupled with the energetic nature and paucity of lithics suggests eruption by an unusual mechanism. The eruption most likely resulted from the large scale collapse of a caldera block into the underlying chamber resulting in high discharge rates, which were no conducive to the development of a convecting column, and minimal vent erosion, resulting in negligible entrainment of lithics. The density of welding and recrystallisation textures suggest that the flow retained heat to considerable distances which allowed the ignimbrite to weld densely to the base. The deposit was most likely progressively aggraded from the base, with material being supplied from an overriding particulate flow.
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Rogan, William. "New insights on magmatic processes from trace element zonation in phenocrysts." Thesis, Open University, 1996. http://ethos.bl.uk/OrderDetails.do?uin=uk.bl.ethos.363965.

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Christenson, Bruce William. "Fluid-mineral equilibria in the Kawerau hydrothermal system, Taupo Volcanic Zone, New Zealand." Thesis, University of Auckland, 1987. http://wwwlib.umi.com/dissertations/fullcit/8904865.

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The Kawerau hydrothermal system lies at the northern end of the Taupo Volcanic Zone, on the some 20 km south of the Bay of Plenty. The system, which is thought to have been active for at least 200,000 years, is situated over an area which has been volcanically active through time. Relatively recent local magmatism is found in the 800 m high, 3000-10,000 year old Mt. Edgecumbe dacite massif and the 200 m high Onepu Dome complex which lie adjacent to and within, respectively, the present day resistivity anomaly. Shallow reservoir fluids show evidence of steam heating as expressed by elevated bicarbonate and/or sulphate contents and mildly to strongly acidic pH, whereas the deep fluids are dominantly alkaline at their respective temperatures. The calculated base fluid composition is comprised of 2.5 wt% CO$/sb2$ and ca. 890 mg/kg Cl at 310$/sp/circ$C. Fluid inclusion studies show a largely stable, boiling point thermal regime through time, whereas oxygen stable isotope studies on hydrothermal carbonates prove the existence of one or more pulses of isotopically heavy fluids into the reservoir at some time(s) in the past. Hydrothermal alteration associated with these isotopic anomalies indicate strongly oxidising conditions relative to both alteration elsewhere in the reservoir and the present day reservoir redox conditions. Collectively, the data suggest a magmatic source for these transient, isotopically heavy fluids. The present day system is ore forming, as evident from both metal rich scales formed in the production silencers of the geothermal wells and open fracture reservoir mineralogy. Stockwork environments in the deep reservoir are host to both base and precious metals, and evidence indicates that boiling is the main depositional mechanism for these ore phases.
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Books on the topic "Taupo"

1

Fletcher, H. M. Tales of early Taupo. 2nd ed. Christchurch [N.Z.]: Cadsonbury Publications, 2009.

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Macgregor, Miriam. The house at Lake Taupo. Leicester: Ulverscroft, 1987.

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Wilson, C. J. N. The Taupo eruption, New Zealand. London: Royal Society of London, 1985.

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Taylor, Amy. Lake Taupo Cycle Challenge guide. Wellington, N.Z: Awa Press, 2008.

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Taylor, Amy. Lake Taupo Cycle Challenge guide. Wellington, N.Z: Awa Press, 2008.

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McElwee, Christine. Tribute to Western Bay, Lake Taupo. Taupo, New Zealand: Acacia Bay Books, 2013.

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Ann, Williams. Early landuse patterns in the Lake Taupo area. Wellington, N.Z: Department of Conservation, 2003.

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Grace, John Te H. Tuwharetoa: The history of the Maori people of the Taupo district. Auckland: Reed, 1992.

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New Zealand. Parliament. Regulations Review Committee. Complaint regarding Differential Airport Charges Notice 1997 (Taupo Airport): Report of the Regulations Review Committee. [Wellington, N.Z.]: House of Representatives, 2006.

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C-VET (NZ) 1996 Summer Symposium on Respiratory Medicine (1996 Christchurch and Taupo). Proceedings from C-VET (NZ) 1996 Summer Symposium on Respiratory Medicine, Christchurch 23rd February and Taupo 1st March. Palmerston North (New Zealand): Massey University, 1996.

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Book chapters on the topic "Taupo"

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Hurst, A. W., S. Sherburn, and V. M. Stagpoole. "The Taupo Seismic System." In IAVCEI Proceedings in Volcanology, 513–19. Berlin, Heidelberg: Springer Berlin Heidelberg, 1989. http://dx.doi.org/10.1007/978-3-642-73759-6_29.

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Wilson, C. J. N., A. M. Rogan, I. M. E. Smith, D. J. Northey, I. A. Nairn, and B. F. Houghton. "Caldera Volcanoes of the Taupo Volcanic Zone, New Zealand." In Collected Reprint Series, 8463–84. Washington, DC: American Geophysical Union., 2014. http://dx.doi.org/10.1002/9781118782095.ch18.

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Healy, J. "Structure and Volcanism in the Taupo Volcanic Zone, New Zealand." In Geophysical Monograph Series, 151–57. Washington, D. C.: American Geophysical Union, 2013. http://dx.doi.org/10.1029/gm006p0151.

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Otway, P. M. "Vertical Deformation Monitoring by Periodic Water Level Observations, Lake Taupo, New Zealand." In IAVCEI Proceedings in Volcanology, 561–74. Berlin, Heidelberg: Springer Berlin Heidelberg, 1989. http://dx.doi.org/10.1007/978-3-642-73759-6_33.

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Cole, J. W., D. J. Darby, and T. A. Stern. "Taupo Volcanic Zone and Central Volcanic Region Backarc Structures of North Island, New Zealand." In Backarc Basins, 1–28. Boston, MA: Springer US, 1995. http://dx.doi.org/10.1007/978-1-4615-1843-3_1.

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Manville, V., and K. A. Hodgson. "Paleohydrology of Volcanogenic Lake Break-Out Floods in the Taupo Volcanic Zone, New Zealand." In Natural and Artificial Rockslide Dams, 519–41. Berlin, Heidelberg: Springer Berlin Heidelberg, 2010. http://dx.doi.org/10.1007/978-3-642-04764-0_21.

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Houghton, B. F., B. J. Hobden, K. V. Cashman, C. J. N. Wilson, and R. T. Smith. "Large-scale interaction of lake water and rhyolitic magma during the 1.8 ka Taupo eruption, New Zealand." In Explosive Subaqueous Volcanism, 97–109. Washington, D. C.: American Geophysical Union, 2003. http://dx.doi.org/10.1029/140gm06.

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Dedual, M. "Vertical distribution and movements of brown bullhead (Ameiurus nebulosus Lesueur 1819) in Motuoapa Bay, southern Lake Taupo, New Zealand." In Aquatic Telemetry, 129–35. Dordrecht: Springer Netherlands, 2002. http://dx.doi.org/10.1007/978-94-017-0771-8_15.

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Giggenbach, W. F. "Composition of fluids in geothermal systems of the Taupo Volcanic Zone, New Zealand, as a function of source magma." In Water-Rock Interaction, 9–12. London: Routledge, 2021. http://dx.doi.org/10.1201/9780203734049-3.

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Pauly, Michael. "TAURO — Teilautonomer Serviceroboter für Überwachungsaufgaben." In Informatik aktuell, 30–39. Berlin, Heidelberg: Springer Berlin Heidelberg, 1995. http://dx.doi.org/10.1007/978-3-642-80064-1_4.

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Conference papers on the topic "Taupo"

1

Pamukcu, Ayla S., Kylie A. Wright, Guilherme A. R. Gualda, and Darren M. Gravley. "Magma Residence and Eruption at the Taupo Volcanic Center (Taupo Volcanic Zone, New Zealand)." In Goldschmidt2020. Geochemical Society, 2020. http://dx.doi.org/10.46427/gold2020.2019.

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Rocco, Nicole, Adam J. R. Kent, Kari M. Cooper, Chad D. Deering, and Darren Gravley. "GEOCHEMICAL EVOLUTION THROUGH A FULL CALDERA CYCLE: TAUPO VOLCANIC ZONE, NZ." In 115th Annual GSA Cordilleran Section Meeting - 2019. Geological Society of America, 2019. http://dx.doi.org/10.1130/abs/2019cd-329060.

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Ebinger, Cynthia, Sophie Aber, Andrew Gase, Samia Sabir, Finnigan Illsley-Kemp, Martha Savage, Jennifer Eccles, and John Ristau. "CASCADING EARTHQUAKE SWARMS IN THE NORTHERN TAUPO VOLCANIC ZONE, NEW ZEALAND." In GSA Connects 2022 meeting in Denver, Colorado. Geological Society of America, 2022. http://dx.doi.org/10.1130/abs/2022am-382271.

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Hadfield, J. C., U. Morgenstern, and J. J. Piper. "Delayed impacts of land-use via groundwater on Lake Taupo, New Zealand." In WATER RESOURCES MANAGEMENT IV. Southampton, UK: WIT Press, 2007. http://dx.doi.org/10.2495/wrm070281.

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Zaliotovaitė, Viktorija, and Kamilė Taujanskaitė. "LIETUVOS NAMŲ ŪKIŲ TAUPYMO IR INVESTAVIMO PROCESŲ PALYGINAMOJI ANALIZĖ 2006–2016 m." In Conference for Junior Researchers „Science – Future of Lithuania“. VGTU Technika, 2017. http://dx.doi.org/10.3846/vvf.2017.022.

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Straipsnyje nagrinėjami įvairių autorių požiūriai charakterizuojant investicijas ir jų sampratą. Analizuojami svarbiausi asmeninių finansų aspektai, didžiausią dėmesį skiriant asmeninių investicijų ir taupymo sritims. Siekiama atskleisti investavimo galimybes, apibūdinant investicinių priemonių teorinius ypatumus bei išskiriant jų privalumus ir trūkumus. Remiantis investicijų grąžos rodikliais ir namų ūkių finansinės elgsenos apžvalga, įvertinamas taupymo ir investavimo aktyvumas bei tendencijos Lietuvos finansų rinkoje. Apibendrinant teorinius ir praktinius duomenų rezultatus, pateikiamos išvados. Atlikta analizė parodė, kad Lietuvos namų ūkių finansinė elgsena pasižymi konservatyvumu – didžioji dauguma laisvas lėšas taupo grynųjų pinigų pavidalu arba sąskaitose finansinėse įstaigose, o kitų alternatyvų, tokių kaip investavimas, pasirinkimo aktyvumas yra mažas.
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Wigger, Natalie E., James E. Faulds, Samuel J. Hampton, Josh W. Borella, and Isabelle Chambefort. "FAVORABLE STRUCTURAL SETTINGS FOR POTENTIAL GEOTHERMAL UPWELLINGS IN THE CENTRAL TAUPO VOLCANIC ZONE, NEW ZEALAND." In GSA Annual Meeting in Indianapolis, Indiana, USA - 2018. Geological Society of America, 2018. http://dx.doi.org/10.1130/abs/2018am-324134.

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Mitchell, Samuel J., Sebastien Biass, Bruce F. Houghton, Brett H. Walker, Alyssa Anderson, Estelle Bonny, Bianca G. Mintz, Nicolas Turner, and David Frank. "THE INTERPLAY OF CLAST SIZE, VESICULARITY AND SECONDARY FRAGMENTATION: AN EXAMPLE FROM THE 1.8KA TAUPO ERUPTION." In 113th Annual GSA Cordilleran Section Meeting - 2017. Geological Society of America, 2017. http://dx.doi.org/10.1130/abs/2017cd-292666.

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Harvey, Mark C., and Julie V. Rowland. "CO2 FLUX INVESTIGATION AT WAIRAKEI, A LOW-CO2 GEOTHERMAL SYSTEM IN THE TAUPO VOLCANIC ZONE, NEW ZEALAND." In 113th Annual GSA Cordilleran Section Meeting - 2017. Geological Society of America, 2017. http://dx.doi.org/10.1130/abs/2017cd-292857.

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Corella Santa Cruz, Carlos, Georg Zellmer, Claudine Stirling, Susanne M. Straub, Marco Brenna, Karoly Nemeth, Malcolm Reid, and David Barr. "Origin of compositional variations of Taupo Volcanic Zone (TVZ) eruption products: crustal differentiation or subduction mélange diapirism?" In Goldschmidt2022. France: European Association of Geochemistry, 2022. http://dx.doi.org/10.46427/gold2022.10747.

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Farsky, David, Michael Rowe, Isabelle Chambefort, David Graham, Shane Rooyakkers, Kevin Faure, and Simon Barker. "Understanding Sources and Modification of Primary Magmatic Volatiles in the Taupo Volcanic Zone: Evidence from Helium and Oxygen Isotopes." In Goldschmidt2022. France: European Association of Geochemistry, 2022. http://dx.doi.org/10.46427/gold2022.11854.

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Reports on the topic "Taupo"

1

Hochstein, M. P., S. Sherburn, and J. Tikku. Earthquake Swarm Activity Beneath the Tokaanu-Waihi Geothermal System, Lake Taupo, New Zealand. Office of Scientific and Technical Information (OSTI), January 1995. http://dx.doi.org/10.2172/895933.

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Surface Fractures Formed in the Potrero Canyon, Tapo Canyon, and McBean Parkway Areas in Association with the 1994 Northridge, California Earthquake. US Geological Survey, 2001. http://dx.doi.org/10.3133/mf2360.

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