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Journal articles on the topic 'Dikes (Geology) New Zealand'

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Author: Grafiati

Published: 10 December 2022

Last updated: 29 January 2023

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1

Grapes, Rodney H., Simon H. Lamb, and Chris J. Adams. "K‐Ar ages of basanitic dikes, Awatere Valley, Marlborough, New Zealand." New Zealand Journal of Geology and Geophysics 35, no. 4 (December 1992): 415–19. http://dx.doi.org/10.1080/00288306.1992.9514536.

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2

Tulloch, A. J. "Petrology of the Sams Creek peralkaline granite dike, Takaka, New Zealand." New Zealand Journal of Geology and Geophysics 35, no. 2 (June 1992): 193–200. http://dx.doi.org/10.1080/00288306.1992.9514513.

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3

Sano, Sakae, Koichi Tazaki, Yoshiyuki Koide, Takashi Nagao, Teruo Watanabe, and Yosuke Kawachi. "Geochemistry of dike rocks in Dun Mountain Ophiolite, Nelson, New Zealand." New Zealand Journal of Geology and Geophysics 40, no. 2 (June 1997): 127–36. http://dx.doi.org/10.1080/00288306.1997.9514747.

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4

Windle, S. J., and D. Craw. "Gold mineralisation in a syntectonic granite dike, Sams Creek, northwest Nelson, New Zealand." New Zealand Journal of Geology and Geophysics 34, no. 4 (December 1991): 429–40. http://dx.doi.org/10.1080/00288306.1991.9514481.

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5

Neef, G. "A clastic dike‐sill assemblage in late Miocene (c. 6 Ma) strata, Annedale, Northern Wairarapa, New Zealand." New Zealand Journal of Geology and Geophysics 34, no. 1 (March 1991): 87–91. http://dx.doi.org/10.1080/00288306.1991.9514442.

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6

Adams, C. J., and Alan F. Cooper. "K‐Ar age of a lamprophyre dike swarm near Lake Wanaka, west Otago, South Island, New Zealand." New Zealand Journal of Geology and Geophysics 39, no. 1 (March 1996): 17–23. http://dx.doi.org/10.1080/00288306.1996.9514691.

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7

Tulloch, A. J., and W. J. Dunlap. "A Carboniferous40Ar/39Ar amphibole emplacement age for the Au‐bearing Sams Creek alkali‐feldspar granite dike, west Nelson, New Zealand." New Zealand Journal of Geology and Geophysics 49, no. 2 (June 2006): 233–40. http://dx.doi.org/10.1080/00288306.2006.9515162.

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8

Gonzales, David. "New Constraints on the Timing and History of Breccia Dikes in the Western San Juan Mountains, Southwestern Colorado." Mountain Geologist 56, no. 4 (October 1, 2019): 397–420. http://dx.doi.org/10.31582/rmag.mg.56.4.397.

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In the western San Juan Mountains, clastic (breccia) dikes crop out in Paleozoic to Cenozoic rocks. The dikes are tabular to bifurcating masses up to several meters thick and are exposed on northwest or northeast trends for up to several kilometers. They are matrix- to clast-supported with angular to rounded pebble- to boulder-sized fragments that in most dikes are dominated by Proterozoic igneous and metamorphic rocks. U-Pb age analyses (n = 3) reveal a range of zircon ages in all samples with several containing high proportions of 1820 to 1390 Ma zircons. The majority of Proterozoic zircons are interpreted as direct contributions from basement rocks during breccia dike formation and emplacement. Field relations and U-Pb zircon analyses reveal that breccia dikes formed in intervals from 65 to 30 Ma (Ouray) and 27 to 12 Ma (Stony Mountain); some dikes are closely allied with mineralization. The dikes formed at depths over 500 meters where Proterozoic basement was fragmented, entrained, and transported to higher structural levels along with pieces of Paleozoic to Cenozoic rocks. A close spatial relationship exists between breccia dikes and latest Mesozoic to Cenozoic plutons. This is best exemplified near Ouray where clastic dikes share similar trends with ~65 Ma granodiorite dikes, and there is a clear transition from intrusive rocks to altered-brecciated plutons, and finally to breccia dikes. The preponderance of evidence supports breccia dike formation via degassing and explosive release of CO2-charged volatiles on deep fractures related to emplacement of 70 to 4 Ma plutons or mantle melts. In addition to breccia dikes, several post-80 Ma events in the region involved explosive release of volatile-charged magmas: 29-27 Ma calderas, ~25 Ma diatremes, and ~24 Ma breccia pipes. Causal factors for production of these gas-charged magmas remain poorly understood, but partial melting or assimilation of altered and metasomatized lithospheric mantle could have played a role.

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9

Mossman, D. J., D. S. Coombs, Y. Kawachi, and A. Reay. "HIGH-Mg ARC-ANKARAMITIC DIKES, GREENHILLS COMPLEX, SOUTHLAND, NEW ZEALAND." Canadian Mineralogist 38, no. 1 (February 1, 2000): 191–216. http://dx.doi.org/10.2113/gscanmin.38.1.191.

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10

Campbell, Hamish, Alex Malahoff, Greg Browne, Ian Graham, and Rupert Sutherland. "New Zealand Geology." Episodes 35, no. 1 (March 1, 2012): 57–71. http://dx.doi.org/10.18814/epiiugs/2012/v35i1/006.

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11

Lipman, Peter W., and Matthew J. Zimmerer. "Magmato-tectonic links: Ignimbrite calderas, regional dike swarms, and the transition from arc to rift in the Southern Rocky Mountains." Geosphere 15, no. 6 (September 30, 2019): 1893–926. http://dx.doi.org/10.1130/ges02068.1.

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Abstract Radial and linear dike swarms in the eroded roots of volcanoes and along rift zones are sensitive structural indicators of conduit and eruption geometry that can record regional paleostress orientations. Compositionally diverse dikes and larger intrusions that radiate westward from the polycyclic Platoro caldera complex in the Southern Rocky Mountain volcanic field (southwestern United States) merge in structural trend, composition, and age with the enormous but little-studied Dulce swarm of trachybasaltic dikes that continue southwest and south for ∼125 km along the eastern margin of the Colorado Plateau from southern Colorado into northern New Mexico. Some Dulce dikes, though only 1–2 m thick, are traceable for 20 km. More than 200 dikes of the Platoro-Dulce swarm are depicted on regional maps, but only a few compositions and ages have been published previously, and relations to Platoro caldera have not been evaluated. Despite complications from deuteric alteration, bulk compositions of Platoro-Dulce dikes (105 new X-ray fluorescence and inductively coupled plasma mass spectrometry analyses) become more mafic and alkalic with distance from the caldera. Fifty-eight (58) new 40Ar/39Ar ages provide insight into the timing of dike emplacement in relation to evolution of Platoro caldera (source of six regional ignimbrites between 30.3 and 28.8 Ma). The majority of Dulce dikes were emplaced during a brief period (26.5–25.0 Ma) of postcaldera magmatism. Some northeast-trending dikes yield ages as old as 27.5 Ma, and the northernmost north-trending dikes have younger ages (20.1–18.6 Ma). In contrast to high-K lamprophyres farther west on the Colorado Plateau, the Dulce dikes are trachybasalts that contain only anhydrous phenocrysts (clinopyroxene, olivine). Dikes radial to Platoro caldera range from pyroxene- and hornblende-bearing andesite to sanidine dacite, mostly more silicic than trachybasalts of the Dulce swarm. Some distal andesite dikes have ages (31.2–30.4 Ma) similar to those of late precaldera lavas; ages of other proximal dikes (29.2–27.5 Ma) are akin to those of caldera-filling lavas and the oldest Dulce dikes. The largest radial dikes are dacites that have yet younger sanidine 40Ar/39Ar ages (26.5–26.4 Ma), similar to those of the main Dulce swarm. The older andesitic dikes and precaldera lavas record the inception of a long-lived upper-crustal magmatic locus at Platoro. This system peaked in magmatic output during ignimbrite eruptions but remained intermittently active for at least an additional 9 m.y. Platoro magmatism began to decline at ca. 26 Ma, concurrent with initial basaltic volcanism and regional extension along the Rio Grande rift, but no basalt is known to have erupted proximal to Platoro caldera prior to ca. 20 Ma, just as silicic activity terminated at this magmatic locus. The large numbers and lengths of the radial andesitic-dacitic dikes, in comparison to the absence of similar features at other calderas of the San Juan volcanic locus, may reflect location of the Platoro system peripheral to the main upper-crustal San Juan batholith recorded by gravity data, as well as its proximity to the axis of early rifting. Spatial, temporal, and genetic links between Platoro radial dikes and the linear Dulce swarm suggest that they represent an interconnected regional-scale magmatic suite related to prolonged assembly and solidification of an arc-related subcaldera batholith concurrently with a transition to regional extension. Emplacement of such widespread dikes during the late evolution of a subcaldera batholith could generate earthquakes and trigger dispersed small eruptions. Such events would constitute little-appreciated magmato-tectonic hazards near dormant calderas such as Valles, Long Valley, or Yellowstone (western USA).

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12

Afanasiev, V. P., E. I. Nikolenko, N. V. Glushkova, and I. D. Zolnikov. "The new Massadou diamondiferous kimberlite field in Guinea." Геология рудных месторождений 61, no. 4 (August 13, 2019): 92–100. http://dx.doi.org/10.31857/s0016-777061492-100.

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A new kimberlite field, called Massadou, has been discovered in southeastern Guinea near Macenta city. The field consists of numerous ~1 m thick kimberlite dikes with low diamond contents; altogether 16 dikes have been found so far. Mineralization occurs along a 600 m wide zone distinct in satellite images, which is oriented in the same way as the K4 kimberlite reported by Huggerty. The Massadou kimberlite is covered by a thick laterite weathering profile. Main kimberlite indicator minerals found in the area are pyrope, chromite, and ilmenite. The latter occurs as zoned grains with a high-Fe core (hemoilmenite) surrounded by a parallel-columnar aggregate in the rim. The aggregate has a composition of ordinary kimberlitic Mg ilmenite and results from interaction of hemoilmenite with the kimberlite melt. The kimberlite age is estimated as 140—145 Ma by analogy with the surrounding fields. The dikes independent products of kimberlite magmatism in the Guinea-Liberia shield rather than being roots of pipes as interpreted by Skinner (2004). Therefore, the erosion cutout is moderate, and there are no reasons to expect the presence of large and rich diamond placers.

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13

BROWN, L. J., R. D. BEETHAM, B. R. PATERSON, and J. H. WEEBER. "Geology of Christchurch, New Zealand." Environmental & Engineering Geoscience I, no. 4 (December 1, 1995): 427–88. http://dx.doi.org/10.2113/gseegeosci.i.4.427.

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14

Kovaleva, Elizaveta, Dmitry A. Zamyatin, and Gerlinde Habler. "Granular zircon from Vredefort granophyre (South Africa) confirms the deep injection model for impact melt in large impact structures." Geology 47, no. 8 (May 22, 2019): 691–94. http://dx.doi.org/10.1130/g46040.1.

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Abstract The Vredefort impact structure, South Africa, is a 2.02 Ga deeply eroded meteorite scar that provides an opportunity to study large impact craters at their lower stratigraphic levels. A series of anomalous granophyre dikes in the core of the structure are believed to be composed of an impact melt, which intruded downwards from the crater floor, exploiting fractures in basement rocks. However, the melt emplacement mechanisms and timing are not constrained. The granophyre dikes contain supracrustal xenoliths captured at higher levels, presently eroded. By studying these clasts and shocked minerals within, we can better understand the nature of dikes, magnitude of impact melt movement, conditions that affected target rocks near the impacted surface, and erosional rates. We report “former reidite in granular neoblastic” (FRIGN) zircon within a granite clast enclosed in the granophyre. High-pressure zircon transformation to reidite (ZrSiO4) and reversion to zircon resulted in zircon grains composed of fine neoblasts (∼0.5–3 µm) with two or three orthogonal orientations. Our finding provides new independent constraints on the emplacement history of Vredefort granophyre dikes. Based on the environment, where other FRIGN zircons are found (impact glasses and melts), the clast was possibly captured near the top of the impact melt sheet and transported to the lowermost levels of the structure, traveling some 8–10 km. Our finding not only provides the highest-pressure shock estimates thus far discovered in the Vredefort structure (≥30 GPa), but also shows that microscopic evidence of high shock pressures can be found within large eroded craters at their lowest stratigraphic levels.

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15

Bastin, Sarah H., Mark C. Quigley, and Kari Bassett. "Paleoliquefaction in Christchurch, New Zealand." Geological Society of America Bulletin 127, no. 9-10 (April 14, 2015): 1348–65. http://dx.doi.org/10.1130/b31174.1.

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16

Schmidt, Alexander R., Uwe Kaulfuss, Jennifer M. Bannister, Viktor Baranov, Christina Beimforde, Natalie Bleile, Art Borkent, et al. "Amber inclusions from New Zealand." Gondwana Research 56 (April 2018): 135–46. http://dx.doi.org/10.1016/j.gr.2017.12.003.

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17

Morriss, Matthew C., Leif Karlstrom, Morgan W. M. Nasholds, and John A. Wolff. "The Chief Joseph dike swarm of the Columbia River flood basalts, and the legacy data set of William H. Taubeneck." Geosphere 16, no. 4 (May 14, 2020): 1082–106. http://dx.doi.org/10.1130/ges02173.1.

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Abstract The Miocene Columbia River Basalt Group (CRBG) is the youngest and best studied continental flood basalt province on Earth. The 210,000 km3 of basaltic lava flows in this province were fed by a series of dike swarms, the largest of which is the Chief Joseph dike swarm (CJDS) exposed in northeastern Oregon and southwestern Washington. We present and augment an extensive data set of field observations, collected by Dr. William H. Taubeneck (1923–2016; Oregon State University, 1955–1983); this data set elucidates the structure of the CJDS in new detail. The large-scale structure of the CJDS, represented by 4279 mapped segments mostly cropping out over an area of 100 × 350 km2, is defined by regions of high dike density, up to ∼5 segments/km−2 with an average width of 8 m and lengths of ∼100–1000 m. The dikes in the CJDS are exposed across a range of paleodepths, from visibly feeding surface flows to ∼2 km in depth at the time of intrusion. Based on extrapolation of outcrops, we estimate the volume of the CJDS dikes to be 2.5 × 102–6 × 104 km3, or between 0.1% and 34% of the known volume of the magma represented by the surface flows fed by these dikes. A dominant NNW dike segment orientation characterizes the swarm. However, prominent sub-trends often crosscut NNW-oriented dikes, suggesting a change in dike orientations that may correspond to magmatically driven stress changes over the duration of swarm emplacement. Near-surface crustal dilation across the swarm is ∼0.5–2.7 km to the E-W and ∼0.2–1.3 km to the N-S across the 100 × 350 km region, resulting in strain across this region of 0.4%–13.0% E-W and 0.04%–0.3% N-S. Host-rock partial melt is rare in the CJDS, suggesting that only a small fraction of dikes were long-lived.

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18

Carter, Lionel, and I. Nicholas McCave. "Eastern New Zealand Drifts, Miocene-Recent." Geological Society, London, Memoirs 22, no. 1 (2002): 385–407. http://dx.doi.org/10.1144/gsl.mem.2002.022.01.27.

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19

Lingen, G. J. "2. New Zealand Petroleum Conference: Rotorua, New Zealand." Journal of Petroleum Geology 17, no. 4 (October 1994): 483–84. http://dx.doi.org/10.1111/j.1747-5457.1994.tb00154.x.

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20

Fitzsimons, Sean, Michael Pollington, and Eric Colhoun. "Palaeomagnetism of New Zealand glacigenic deposits." Exploration Geophysics 24, no. 2 (June 1993): 303–4. http://dx.doi.org/10.1071/eg993303.

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21

de Lange, W. P., and V. G. Moon. "Tsunami washover deposits, Tawharanui, New Zealand." Sedimentary Geology 200, no. 3-4 (August 2007): 232–47. http://dx.doi.org/10.1016/j.sedgeo.2007.01.006.

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22

Corral, Isaac, David Gómez-Gras, Albert Griera, Mercè Corbella, and Esteve Cardellach. "Sedimentation and volcanism in the Panamanian Cretaceous intra-oceanic arc and fore-arc: New insights from the Azuero peninsula (SW Panama)." Bulletin de la Société Géologique de France 184, no. 1-2 (January 1, 2013): 35–45. http://dx.doi.org/10.2113/gssgfbull.184.1-2.35.

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Abstract The Azuero Peninsula, located in SW Panama, is a region characterized by a long-lived intra-oceanic subduction zone. Volcanism began in Late Cretaceous time, as the result of subduction of the Farallon plate beneath the Caribbean plate. Usually, ancient volcanic arcs related to intra-oceanic subduction zones are not preserved, because they are in areas with difficult access or covered by modern volcanic arc material. However, on the Azuero peninsula, a complete section of the volcanic arc together with arc basement rocks provides the opportunity to study the sedimentation and volcanism in the initial stages of volcanic arc development. The lithostratigraphic unit which records fore-arc evolution is the “Río Quema” Formation (RQF), a volcanic apron composed of volcanic and volcaniclastic sedimentary rocks interbedded with hemipelagic limestones, submarine dacite lava domes, and intruded by basaltic-andesitic dikes. The “Río Quema” Formation, interpreted as a fore-arc basin infilling sequence, lies discordantly on top of arc basement rocks. The exceptionally well exposed arc basement, fore-arc basin, volcanic arc rocks and arc-related intrusive rocks provide an unusual opportunity to study the relationship between volcanism, sedimentation and magmatism during the arc development, with the objective to reconstruct its evolution. The “Río Quema” Formation can be divided into three groups: 1) proximal apron, a sequence dominated by lava flows, interbedded with breccias, mass flows and channel fill, all intruded by basaltic dikes. The rocks represent the nearest materials to the volcanic source, reflecting a coarse sediment supply. This depositional environment is similar to gravel-rich fan deltas and submarine ramps; 2) medial apron, characterized by a volcanosedimentary succession dominated by andesitic lava flows, polymictic volcanic conglomerates and crystal-rich sandstones with minor pelagic sediments and turbidites. These rocks were deposited from high-density turbidity currents and debris flows, directly derived from erupted material and gravitational collapse of an unstable volcanic edifice or volcaniclastic apron; 3) distal apron, a thick succession of sandy to muddy volcaniclastic rocks, interbedded with pelagic limestones and minor andesitic lavas, intruded by dacite domes and by basaltic to andesitic dikes. Bedforms and fossils suggest a quiet, relatively deep-water environment characterized by settling of clay and silt (claystone, siltstone) and by dilute turbidity currents of reworked volcaniclastic detritus. The timing of the initial stages of the volcanic arc has been constrained through a biostratigraphic study, using planktonic foraminifera and radiolarian species. The fossil assemblage indicates that the age of the “Río Quema” Formation ranges from Late Campanian to Maastrichtian, providing a good constraint for the development of the volcanic arc and volcaniclastic apron, during the initial stages of an intra-oceanic subduction zone.

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23

Moghadam, Hadi Shafaii, R. J. Stern, W. L. Griffin, M. Z. Khedr, M. Kirchenbaur, C. J. Ottley, S. A. Whattam, et al. "Subduction initiation and back-arc opening north of Neo-Tethys: Evidence from the Late Cretaceous Torbat-e-Heydarieh ophiolite of NE Iran." GSA Bulletin 132, no. 5-6 (October 15, 2019): 1083–105. http://dx.doi.org/10.1130/b35065.1.

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Abstract How new subduction zones form is an ongoing scientific question with key implications for our understanding of how this process influences the behavior of the overriding plate. Here we focus on the effects of a Late Cretaceous subduction-initiation (SI) event in Iran and show how SI caused enough extension to open a back-arc basin in NE Iran. The Late Cretaceous Torbat-e-Heydarieh ophiolite (THO) is well exposed as part of the Sabzevar-Torbat-e-Heydarieh ophiolite belt. It is dominated by mantle peridotite, with a thin crustal sequence. The THO mantle sequence consists of harzburgite, clinopyroxene-harzburgite, plagioclase lherzolite, impregnated lherzolite, and dunite. Spinel in THO mantle peridotites show variable Cr# (10–63), similar to both abyssal and fore-arc peridotites. The igneous rocks (gabbros and dikes intruding mantle peridotite, pillowed and massive lavas, amphibole gabbros, plagiogranites and associated diorites, and diabase dikes) display rare earth element patterns similar to MORB, arc tholeiite and back-arc basin basalt. Zircons from six samples, including plagiogranites and dikes within mantle peridotite, yield U-Pb ages of ca. 99–92 Ma, indicating that the THO formed during the Late Cretaceous and was magmatically active for ∼7 m.y. THO igneous rocks have variable εNd(t) of +5.7 to +8.2 and εHf(t) ranging from +14.9 to +21.5; zircons have εHf(t) of +8.1 to +18.5. These isotopic compositions indicate that the THO rocks were derived from an isotopically depleted mantle source similar to that of the Indian Ocean, which was slightly affected by the recycling of subducted sediments. We conclude that the THO and other Sabzevar-Torbat-e-Heydarieh ophiolites formed in a back-arc basin well to the north of the Late Cretaceous fore-arc, now represented by the Zagros ophiolites, testifying that a broad region of Iran was affected by upper-plate extension accompanying Late Cretaceous subduction initiation.

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24

King, P. R., and P. H. Robinson. "An Overview of Taranaki Region Geology, New Zealand." Energy Exploration & Exploitation 6, no. 3 (June 1988): 213–32. http://dx.doi.org/10.1177/014459878800600304.

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Recent revisions to the paleontologic dating and lithologic correlation of the late Cretaceous and Cenozoic sediments in many wells have improved the chronostratigraphic framework for the Taranaki Basin. When combined with detailed seismic mapping and results of a study of basement trends, refinements to the timing of major structural and sedimentary events in the basin's history can be made. A resultant series of paleogeographic maps is presented. The Taranaki Basin has developed primarily within an extensional tectonic regime, with a compressional overprint occurring variously in places from early Miocene to Pliocene. An overall transgressive sedimentary cycle existed from the late Cretaceous to early Miocene. Thereafter a generally regressive trend has continued to the present day. Subsidence patterns were broadly similar across the basin until the late Miocene, whereupon tectonic controls on basin morphology and sedimentation became more diverse.

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25

Bell, D. H., and J. R. Pettinga. "Engineering geology and subdivision planning in New Zealand." Engineering Geology 22, no. 1 (September 1985): 45–59. http://dx.doi.org/10.1016/0013-7952(85)90037-7.

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26

SEPPÄLÄ, MATTI. "A brief geology and palaeontology of New Zealand." Boreas 10, no. 4 (January 16, 2008): 368. http://dx.doi.org/10.1111/j.1502-3885.1981.tb00497.x.

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27

Ezzeldin, Riham Mohsen. "Numerical and experimental investigation for the effect of permeability of spur dikes on local scour." Journal of Hydroinformatics 21, no. 2 (February 1, 2019): 335–42. http://dx.doi.org/10.2166/hydro.2019.114.

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Abstract The effect of using permeable spur dikes on the produced maximum scour depth compared to that of solid spur dikes is numerically investigated. The numerical model used for such purpose is the Nays-2DH model of the International River Interface Cooperative (iRIC) software package for bed and bank erosion. The model results are verified using the experimental data collected in this study by conducting experiments on five different models of spur dikes having different opening ratios. Using the statistical performance indices, the root mean square error and the coefficient of determination, the results showed an acceptable agreement between the numerical model results for the relative maximum scour depth defined by the ratio of the maximum scour depth to the flow depth and their corresponding observed values. A new empirical equation using nonlinear regression is developed using the experimental data collected in this study and tested with another existing empirical equation available in the literature for their accuracy in determining the relative maximum scour depth.

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28

Wilson, C. J. N., V. R. Switsur, and A. P. Ward. "A new 14C age for the Oruanui (Wairakei) eruption, New Zealand." Geological Magazine 125, no. 3 (May 1988): 297–300. http://dx.doi.org/10.1017/s0016756800010232.

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AbstractThe Oruanui eruption was the largest known outburst of Taupo volcano, New Zealand, and is among the larger Quaternary eruptions documented. The eruption deposits are variously known as the Oruanui, Wairakei, Kawakawa Tephra, or Aokautere Ash formations, and represent a bulk volume probably exceeding 500 km3. Four new 14C age determinations on carbonized vegetation in the non-welded Oruanui ignimbrite are combined to give a conventional age of 22590±230 yr b.p. Compared with the previously accepted figure of 20000 yr b.p., this new age resolves the anomaly of apparently older 14C ages being obtained from a demonstrably younger New Zealand deposit, and strengthens correlation of this eruption with an Antarctic ice-core acid anomaly. The trace of this eruption has great potential as a time-plane marker in the Antarctic just prior to the last glacial maximum. The close similarity in ages between the Oruanui and a comparable sized eruption (Ito/Aira-Tn) in Japan suggests that this period of activity may represent the best chance of resolving any linkages between large-scale explosive silicic volcanism and climate changes.

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29

Garnish, John. "11th New Zealand geothermal workshop." Geothermics 18, no. 5-6 (January 1989): 789–95. http://dx.doi.org/10.1016/0375-6505(89)90108-9.

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30

Grapes, Rodney. "Geomorphology of faulting: The Wairarapa Fault, New Zealand." Zeitschrift für Geomorphologie Supplement Volumes 115 (July 1, 1999): 191–217. http://dx.doi.org/10.1127/zfgsuppl/115/1999/191.

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31

Dickson, Mark E., and Wayne J. Stephenson. "Chapter 13 The rock coast of New Zealand." Geological Society, London, Memoirs 40, no. 1 (2014): 225–34. http://dx.doi.org/10.1144/m40.13.

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32

Wadsworth, W. J. "Intraplate volcanism in Eastern Australia and New Zealand." Journal of Structural Geology 14, no. 3 (March 1992): 379–80. http://dx.doi.org/10.1016/0191-8141(92)90097-g.

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33

Ingham, M. R. "Geomagnetic induction studies in central New Zealand." Exploration Geophysics 17, no. 1 (March 1986): 35–36. http://dx.doi.org/10.1071/eg986035.

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34

McKnight, J. O., and F. H. Chamalaun. "A Magnetometer Array Experiment In New Zealand." Exploration Geophysics 24, no. 2 (June 1993): 191–94. http://dx.doi.org/10.1071/eg993191.

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McFadgen, B. G., and J. R. Goff. "Tsunamis in the New Zealand archaeological record." Sedimentary Geology 200, no. 3-4 (August 2007): 263–74. http://dx.doi.org/10.1016/j.sedgeo.2007.01.007.

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Wang, Ming, Cai Li, Xiao-Wen Zeng, Hang Li, Jian-Jun Fan, Chao-Ming Xie, and Yu-Jie Hao. "Petrogenesis of the southern Qiangtang mafic dykes, Tibet: Link to a late Paleozoic mantle plume on the northern margin of Gondwana?" GSA Bulletin 131, no. 11-12 (April 16, 2019): 1907–19. http://dx.doi.org/10.1130/b35110.1.

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AbstractThis study presents 13 new U-Pb zircon ages obtained by laser ablation–inductively coupled plasma–mass spectrometry (LA-ICP-MS) together with whole-rock geochemical, Sr-Nd isotopic and zircon Hf isotopic data for a mafic dike swarm in the southern Qiangtang area of Tibet. These data provide the basis for a new model of the late Paleozoic evolution of the Tethys. Combined with the results of previous zircon U-Pb dating, the magmatic zircon grains extracted from mafic dikes yield latest Carboniferous to Early Permian ages (317–279 Ma). The geochemistry of the southern Qiangtang mafic rocks indicates the presence of low-Ti (QLT) and high-Ti (QHT) suites. The magmas that formed the QLT suite underwent higher degrees of partial melting (>5%) and display evidence of crustal contamination, whereas the QHT suite was derived from magmas generated by low-degree (1%–5%) partial melting of a garnet-bearing mantle source, with a greater extent of fractional crystallization than the QLT suite, and no evidence of crustal contamination. We propose that the QHT and QLT suites may have been derived from magmas from different parts of a single mantle plume. The formation of the southern Qiangtang mafic dikes (latest Carboniferous to Early Permian; 317–279 Ma) may have been related to the northward drift of the Cimmerian continent from the northern Gondwana margin, which resulted in the opening of the Meso-Tethys Ocean.

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Goldsmith, P. R., and E. H. Smith. "Tunnelling soils in South Auckland, New Zealand." Engineering Geology 22, no. 1 (September 1985): 1–11. http://dx.doi.org/10.1016/0013-7952(85)90033-x.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 30, no. 4 (December 31, 1997): 371–72. http://dx.doi.org/10.5459/bnzsee.30.4.371-372.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 31, no. 1 (March 31, 1998): 69–70. http://dx.doi.org/10.5459/bnzsee.31.1.69-70.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 31, no. 3 (September 30, 1998): 213. http://dx.doi.org/10.5459/bnzsee.31.3.213.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 31, no. 4 (December 31, 1998): 298. http://dx.doi.org/10.5459/bnzsee.31.4.298.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 32, no. 1 (March 31, 1999): 41. http://dx.doi.org/10.5459/bnzsee.32.1.41.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 32, no. 2 (June 30, 1999): 123. http://dx.doi.org/10.5459/bnzsee.32.2.123.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 32, no. 3 (September 30, 1999): 190–91. http://dx.doi.org/10.5459/bnzsee.32.3.190-191.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 32, no. 4 (December 31, 1999): 263–64. http://dx.doi.org/10.5459/bnzsee.32.4.263-264.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 33, no. 1 (March 31, 2000): 60–61. http://dx.doi.org/10.5459/bnzsee.33.1.60-61.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 33, no. 2 (June 30, 2000): 173–74. http://dx.doi.org/10.5459/bnzsee.33.2.173-174.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 33, no. 4 (December 31, 2000): 498–500. http://dx.doi.org/10.5459/bnzsee.33.4.498-500.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 34, no. 1 (March 31, 2001): 87–89. http://dx.doi.org/10.5459/bnzsee.34.1.87-89.

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Editor. "Significant New Zealand earthquakes." Bulletin of the New Zealand Society for Earthquake Engineering 34, no. 2 (June 30, 2001): 167. http://dx.doi.org/10.5459/bnzsee.34.2.167.

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